The first discovery in North America of a succession of graptolite faunas across the Ordovician–Silurian boundary has been made on Esquibel Island, in south-eastern Alaska, where five graptolite zones are represented in an 18 m interval of shale in the Descon Formation. Despite the thinness of the graptolite zones, no stratigraphical breaks can be inferred from more complete graptolite successions known elsewhere. The Alaskan faunas can be closely correlated with those of the standard British zones—the Dicellograptus anceps Zone (uppermost Ordovician), the Glyptograptus persculptus Zone (lowermost Silurian) and the immediately overlying Akidograptus acuminatus, Orthograptus vesiculosus and Monograptus cyphus Zones of the Lower Silurian. They thus give evidence of the cosmopolitan distribution of graptolite faunas during latest Ordovician and earliest Silurian time.
The geochronology of Tertiary igneous events at the Nevada Test Site and adjacent area is outlined by 36 recently determined K-Ar ages, together with other published K-Ar ages. The first evidence of Tertiary igneous activity is the ash-fall bedded tuffs in the Horse Spring Formation. One such tuff has been dated as 29 m.y. old (late Oligocene). Other ash-flow tuffs and lavas formed during the Miocene and Pliocene, according to radiometric age determinations. The youngest ash-flow tuff in this area is about 6 m.y. old.
Great volumes of ash and lava were spewed forth 13 to 11 m.y. ago to form the Paintbrush and Timber Mountain Tuffs. Sixteen replicate age determinations on minerals from four densely welded ash-flow tuffs from these formations gave a pooled standard deviation of about ± 2 percent error, provided anomalous ages were rejected on the basis of rock alteration or analytical difficulties.
In the Air Force Gunnery Range, just north of the test site, K-Ar ages suggest that the oldest ash flows, the Monotony Tuff, were emplaced 27.6 m.y. ago (late Oligocene) and were followed by outpourings of lava and ash throughout most of the Miocene. Youngest dated lava is about 13 m.y. old.
In the southern Egan and northern Seaman Ranges of central Nevada, the Needles Range (?) Formation has an averaged K-Ar age of about 30 m.y., which compares closely with 29.2 m.y., the average of four earlier K-Ar ages determined by other investigators on known Needles Range Formation in eastern Nevada and western Utah.
K-Ar ages given by micas from two exposed plutons in the Nevada Test Site suggest emplacement of these plutons at about 93 m.y. ago (early Late Cretaceous), although earlier emplacement in the Mesozoic would be more consistent with Pb-α ages
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1970)81[2657:RAASSO]2.0.CO;2","usgsCitation":"Marvin, R.F., Byers, F., Mehnert, H.H., Orkild, P.P., and Stern, T.W., 1970, Radiometric ages and stratigraphic sequence of volcanic and plutonic rocks, southern Nye and western Lincoln Counties, Nevada: Bulletin of the Geological Society of America, v. 81, no. 9, p. 2657-2676, https://doi.org/10.1130/0016-7606(1970)81[2657:RAASSO]2.0.CO;2.","productDescription":"20 p.","startPage":"2657","endPage":"2676","costCenters":[],"links":[{"id":392053,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nevada","county":"Lincoln County, Nye County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.0098876953125,\n 36.42791246440695\n ],\n [\n -114.027099609375,\n 36.42791246440695\n ],\n [\n -114.027099609375,\n 38.50948995925553\n ],\n [\n -117.0098876953125,\n 38.50948995925553\n ],\n [\n -117.0098876953125,\n 36.42791246440695\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"81","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Marvin, Richard F.","contributorId":23125,"corporation":false,"usgs":true,"family":"Marvin","given":"Richard","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":827307,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Byers, F.M. Jr.","contributorId":78338,"corporation":false,"usgs":true,"family":"Byers","given":"F.M.","suffix":"Jr.","affiliations":[],"preferred":false,"id":827308,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Mehnert, Harald H.","contributorId":56221,"corporation":false,"usgs":true,"family":"Mehnert","given":"Harald","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":827309,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Orkild, Paul P.","contributorId":14441,"corporation":false,"usgs":true,"family":"Orkild","given":"Paul","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":827310,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Stern, T. W.","contributorId":36122,"corporation":false,"usgs":true,"family":"Stern","given":"T.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":827311,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":70226484,"text":"70226484 - 1970 - A re-evaluation of basalt-obsidian relations at East Lake Fissure, Newberry Caldera, Oregon","interactions":[],"lastModifiedDate":"2021-11-19T16:24:37.732118","indexId":"70226484","displayToPublicDate":"1970-09-01T10:15:58","publicationYear":"1970","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":"A re-evaluation of basalt-obsidian relations at East Lake Fissure, Newberry Caldera, Oregon","docAbstract":"Andesite scoria, agglutinate, and small flows formed by thin lava gushes that erupted from East Lake Fissure on the north wall of Newberry Caldera carry numerous inclusions of platy rhyolite, partly melted platy rhyolite, and frothy obsidian. This association of obsidian and “basalt” has been interpreted as the result of intermingling of mafic and siliceous magmas. The locality has been repeatedly cited as an example of a mixed intrusion of the “basalt-rhyolite association.” Field, petrographic, chemical, and experimental evidence suggest, however, that the inclusions of frothy and massive obsidian are melted fragments of platy rhyolite which were ripped from a rhyolite unit forming part of the caldera wall by uncontaminated andesite magma which rose and fountained from the fissure.
Potassium-argon dating of Tertiary igneous rocks in Lander County, central Nevada, indicates that igneous activity was episodic and can be separated into three periods. Igneous activity started abruptly about 37 m.y. ago with local extrusion of andesitic to quartz-latitic lava flows and intrusion of hypabyssal rocks of similar composition. This activity ceased about 33 m.y. ago and was followed by extrusion of rhyolite ash-flow sheets that blanketed large parts of the region. These ash-flow sheets range from about 34 to 22 m.y. in age. The final phase, represented by basalt and basaltic-andesite flows and intrusive rhyolite flow-dome complexes, took place about 16 to 10 m.y. ago.
Andesitic to dacitic lava and hypabyssal rocks about 35 m.y. old are widespread east of Lander County and rhyolitic ash-flow tuffs 34 to 20 m.y. old are found south and east of Lander County. The younger (16 to 10 m.y.) basalt and basaltic-andesite flows are related to volcanism of the Snake River plain province to the north.
The precision of the ages was evaluated by means of: (1) repeat analyses of the same mineral separate, (2) age determination of mineral pairs from the same hand specimen, and (3) age determinations on widely spaced samples from the same geologic body or formation. The last method seems most meaningful from a geologic point of view.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1970)81[2317:GOTIRI]2.0.CO;2","usgsCitation":"McKee, E.H., and Silberman, M.L., 1970, Geochronology of Tertiary igneous rocks in central Nevada: Bulletin of the Geological Society of America, v. 81, no. 8, p. 2317-2327, https://doi.org/10.1130/0016-7606(1970)81[2317:GOTIRI]2.0.CO;2.","productDescription":"11 p.","startPage":"2317","endPage":"2327","costCenters":[],"links":[{"id":391994,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nevada","county":"Lander 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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":827170,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Silberman, Miles L.","contributorId":92536,"corporation":false,"usgs":true,"family":"Silberman","given":"Miles","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":827171,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010268,"text":"70010268 - 1970 - Deuterium content of snow cores from Sierra Nevada area","interactions":[],"lastModifiedDate":"2026-01-29T17:24:31.49247","indexId":"70010268","displayToPublicDate":"1970-07-31T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Deuterium content of snow cores from Sierra Nevada area","docAbstract":"The relative deuterium content was measured on 37 snow cores collected in April 1969 in the Sierra Nevada. The deuterium content varies inversely with altitude of collection (approximately 40 per mil per 1000 meters) but is unrelated to latitude. The altitude relationship is particularly well defined west of the crest of the range but is not well defined east of the crest. However, samples from east of the crest tend to be depleted by about 10 to 15 per mil relative to samples collected at the same elevation west of the crest. We propose that the deuterium content of snow cores, collected so as to include the total winter's precipitation, can be used as a climatic indicator to compare the climate of one winter with that of another.","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.169.3944.467","issn":"00368075","usgsCitation":"Friedman, I., and Smith, G., 1970, Deuterium content of snow cores from Sierra Nevada area: Science, v. 169, no. 3944, p. 467-470, https://doi.org/10.1126/science.169.3944.467.","productDescription":"4 p.","startPage":"467","endPage":"470","costCenters":[],"links":[{"id":218786,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California, Nevada","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -121.01606059384827,\n 39.24050139709556\n ],\n [\n -121.01606059384827,\n 38.20977649215865\n ],\n [\n -119.38801271817681,\n 38.20977649215865\n ],\n [\n -119.38801271817681,\n 39.24050139709556\n ],\n [\n -121.01606059384827,\n 39.24050139709556\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"169","issue":"3944","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0003e4b0c8380cd4f531","contributors":{"authors":[{"text":"Friedman, I.","contributorId":95596,"corporation":false,"usgs":true,"family":"Friedman","given":"I.","email":"","affiliations":[],"preferred":false,"id":358485,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Smith, G.I.","contributorId":103694,"corporation":false,"usgs":true,"family":"Smith","given":"G.I.","email":"","affiliations":[],"preferred":false,"id":358486,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70170770,"text":"70170770 - 1970 - 4 Earthquake: Major offshore earthquakes recall the Aztec myth","interactions":[],"lastModifiedDate":"2016-05-02T14:14:17","indexId":"70170770","displayToPublicDate":"1970-07-01T15:15:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1435,"text":"Earthquake Information Bulletin (USGS)","active":true,"publicationSubtype":{"id":10}},"title":"4 Earthquake: Major offshore earthquakes recall the Aztec myth","docAbstract":"Long before the sun clears the eastern mountains of April 29, 1970, the savanna highlands of Chiapas tremble from a magnitude 6.7 earthquake centered off the Pacific coast near Mexico’s southern border. Then, for a few hours, he Isthmus of Tehuantepec is quiet.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","usgsCitation":"United States Department of Commerce, 1970, 4 Earthquake: Major offshore earthquakes recall the Aztec myth: Earthquake Information Bulletin (USGS), v. 2, no. 4, p. 4-7.","productDescription":"4 p.","startPage":"4","endPage":"7","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":320828,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Mexico","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.158203125,\n 32.58384932565662\n ],\n [\n -114.78515624999999,\n 32.731840896865684\n ],\n [\n -114.697265625,\n 32.58384932565662\n ],\n [\n -110.830078125,\n 31.39115752282472\n ],\n [\n -108.28125,\n 31.39115752282472\n ],\n [\n 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]\n}","volume":"2","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57287a2be4b0b13d391865ad","contributors":{"authors":[{"text":"United States Department of Commerce","contributorId":169080,"corporation":true,"usgs":false,"organization":"United States Department of Commerce","id":628351,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70139928,"text":"70139928 - 1970 - Saline ground-water resources of the Tularosa Basin, New Mexico","interactions":[],"lastModifiedDate":"2016-02-03T10:09:14","indexId":"70139928","displayToPublicDate":"1970-07-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":1,"text":"Federal Government Series"},"seriesTitle":{"id":3864,"text":"Research and Development Progress Report","active":true,"publicationSubtype":{"id":10}},"seriesNumber":"561","title":"Saline ground-water resources of the Tularosa Basin, New Mexico","docAbstract":"This report describes the location, extent, and quality of saline ground water in the Tularosa Basin, a north-trending elongated, intermontane, desert basin in south-central New Mexico. There are no through-flowing streams; runoff from the bordering mountains flows to ephemeral lakes in the center of the basin.
\nFresh-water supplies in the Tularosa Basin are limited; however, large volumes of saline ground-water underlie most of the basin.
\nConsolidated rocks ranging from Precambrian through Cretaceous in age form \"bedrock\" aquifers in the basin. Where these rocks are exposed in the mountains bordering the basin, and in the north part of the basin, they may yield up to 150 gallons per minute, although yields are usually less than 20 gpm. Water at shallow depths in these rocks usually contain 1-3 g/l. Water quality deteriorates with depth, and more than 35 g/l water is present in some rock units. Few wells have penetrated these rocks beneath the alluvial deposits in the central part of the basin, where well yields and water quality are generally unknown.
\nThe most widely developed aquifer in the basin is the alluvial fill of Tertiary to Holocene age which exceeds 6,000 feet in thickness in the southern part of the basin. Well yields of as much as 1,400 gallons per minute have been measured. Fresh water lenses occur in the alluvial fill adjacent to the mountains on the east and west sides of the southern part of the basin. The water below the fresh-water lenses in the alluvial fill increases in salinity with depth. Salinity also increases toward the center of the basin.
\nThe altitude of isosaline surfaces and thickness of the saline-water zones are shown on maps of the entire basin and of the following detailed areas within the basin: Alamogordo, Tularosa, Carrizozo, and the western margin of the basin.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","usgsCitation":"McLean, J.S., 1970, Saline ground-water resources of the Tularosa Basin, New Mexico: Research and Development Progress Report 561, ix, 128 p.","productDescription":"ix, 128 p.","numberOfPages":"162","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":298745,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70139928.jpg"},{"id":316473,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70139928/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"New Mexico","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -106.787109375,\n 32.00341778396365\n ],\n [\n -106.787109375,\n 34.14363482031264\n ],\n [\n -106.19384765625,\n 34.14363482031264\n ],\n [\n -106.19384765625,\n 32.00341778396365\n ],\n [\n -106.787109375,\n 32.00341778396365\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"550bf335e4b02e76d759cdfa","contributors":{"authors":[{"text":"McLean, J. S.","contributorId":116657,"corporation":false,"usgs":true,"family":"McLean","given":"J.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":539697,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70226464,"text":"70226464 - 1970 - Aspects of oil and gas operations on federal and Indian lands of interest to engineers","interactions":[],"lastModifiedDate":"2021-11-18T15:20:47.13393","indexId":"70226464","displayToPublicDate":"1970-06-08T08:58:43","publicationYear":"1970","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Aspects of oil and gas operations on federal and Indian lands of interest to engineers","docAbstract":"It is always enjoyable to attend any meeting of the Society of Petroleum Engineers. I am happy to have this opportunity to speak to you because I believe that petroleum engineers can benefit from a better understanding of the Mineral Leasing Act and the regulations that implement the act insofar as these affect or influence your work. The regulations that implement the leasing act are commonly known as the Oil and Gas Operating Regulations. These regulations are officially described as Part 221 of Title 30 of the Code of Federal Regulations. They are printed in a small green booklet which most printed in a small green booklet which most of you have probably seen at one time or other. The requirements of the operating regulations, as specifically set forth in the booklet, or as determined by policy judgments in our various offices, can affect some aspects of your work.
I think it would be appropriate first to discuss the two types of lands, Federal lands and Indian lands, which are subject to the Oil and Gas Operating Regulations. Federal lands generally are classified in two categories, acquired land and public domain lands. Acquired lands are lands to which the Federal Government obtained title by purchase, exchange, condemnation, or private gift. These lands are scattered private gift. These lands are scattered throughout the United States and total about 54 million acres, or about 7.5 percent of the area classified as public percent of the area classified as public lands.
The public domain lands are lands to which the United States has held title since their original acquisition. There are public lands in 30 states, but the large bulk of the lands are located in Alaska and the Western States. You may recall from your history courses some of the purchases and treaties by which the United States obtained most of the lands now described as public domain lands. The Louisiana Purchase in 1803 included among the Western States most of Montana, eastern and central Wyoming, northeast Colorado, and the northern part of Texas. This treaty also included a large part of the area now generally referred to as The \"Midwest\". The annexation of Texas occurred in 1845 and it is somewhat surprising to realize that this included, among other lands, a strip of land through western Colorado and a rectangular shaped piece of land in Wyoming, south of Rawlins piece of land in Wyoming, south of Rawlins The acquisition of the Oregon Territory in 1846 brought into the Union parts of western Wyoming and Montana as well as what is now Idaho, Oregon, and Washington.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"SPE Rocky Mountain regional meeting","largerWorkSubtype":{"id":12,"text":"Conference publication"},"conferenceTitle":"SPE Rocky Mountain Regional Meeting","conferenceDate":"June 8-9, 1970","conferenceLocation":"Casper, WY","language":"English","publisher":"American Institute of Mining, Metallurgical, and Petroleum Engineers, Inc.","doi":"10.2118/2899-MS","usgsCitation":"Curtis, C.J., 1970, Aspects of oil and gas operations on federal and Indian lands of interest to engineers, in SPE Rocky Mountain regional meeting, Casper, WY, June 8-9, 1970, p. 1-6, https://doi.org/10.2118/2899-MS.","productDescription":"SPE-2899-MS, 8 p.","startPage":"1","endPage":"6","costCenters":[],"links":[{"id":391865,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado, Idaho, Montana, North Dakota, South Dakota, Utah, Wyoming","otherGeospatial":"Rocky Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.1142578125,\n 42.06560675405716\n ],\n [\n -114.12597656249999,\n 41.96765920367816\n ],\n [\n -114.12597656249999,\n 36.96744946416934\n ],\n [\n -110.85205078124999,\n 37.00255267215955\n ],\n [\n -109.86328125,\n 38.06539235133249\n ],\n [\n -109.05029296875,\n 38.09998264736481\n ],\n [\n -109.05029296875,\n 38.324420427006544\n ],\n [\n -106.76513671875,\n 38.35888785866677\n ],\n [\n -106.76513671875,\n 37.00255267215955\n ],\n [\n -102.01904296874999,\n 37.020098201368114\n ],\n [\n -102.01904296874999,\n 41.04621681452063\n ],\n [\n -107.95166015624999,\n 41.02964338716638\n ],\n [\n -107.99560546875,\n 42.71473218539458\n ],\n [\n -108.83056640625,\n 42.69858589169842\n ],\n [\n -109.51171875,\n 43.35713822211053\n ],\n [\n -108.03955078125,\n 43.35713822211053\n ],\n [\n -108.06152343749999,\n 44.59046718130883\n ],\n [\n -108.34716796875,\n 45.01141864227728\n ],\n [\n -106.28173828125,\n 44.98034238084973\n ],\n [\n -106.2158203125,\n 43.32517767999296\n ],\n [\n -104.96337890625,\n 43.32517767999296\n ],\n [\n -104.94140625,\n 42.53689200787315\n ],\n [\n -104.0625,\n 42.56926437219384\n ],\n [\n -104.04052734375,\n 42.98857645832184\n ],\n [\n -98.63525390624999,\n 42.98857645832184\n ],\n [\n -98.0859375,\n 42.71473218539458\n ],\n [\n -97.84423828125,\n 42.779275360241904\n ],\n [\n -97.31689453125,\n 42.779275360241904\n ],\n [\n -96.328125,\n 42.4234565179383\n ],\n [\n -96.5478515625,\n 42.71473218539458\n ],\n [\n -96.39404296875,\n 43.052833917627936\n ],\n [\n -96.43798828125,\n 43.26120612479979\n ],\n [\n -96.45996093749999,\n 43.51668853502906\n ],\n [\n -96.39404296875,\n 45.38301927899065\n ],\n [\n -96.74560546875,\n 45.644768217751924\n ],\n [\n -96.50390625,\n 45.93587062119052\n ],\n [\n -96.48193359375,\n 46.31658418182218\n ],\n [\n -96.74560546875,\n 46.649436163350245\n ],\n [\n -96.74560546875,\n 46.86019101567027\n ],\n [\n -96.8115234375,\n 47.635783590864854\n ],\n [\n -97.14111328125,\n 48.07807894349862\n ],\n [\n -97.03125,\n 48.66194284607006\n ],\n [\n -97.18505859374999,\n 49.03786794532644\n ],\n [\n -117.1142578125,\n 49.023461463214126\n ],\n [\n -117.1142578125,\n 46.31658418182218\n ],\n [\n -117.04833984375001,\n 45.99696161820381\n ],\n [\n -116.76269531249999,\n 45.66012730272194\n ],\n [\n -117.42187500000001,\n 44.308126684886126\n ],\n [\n -117.00439453125,\n 44.10336537791152\n ],\n [\n -117.13623046874999,\n 43.88205730390537\n ],\n [\n -117.1142578125,\n 42.06560675405716\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationDate":"1970-06-08","publicationStatus":"PW","contributors":{"authors":[{"text":"Curtis, Charles J.","contributorId":269397,"corporation":false,"usgs":false,"family":"Curtis","given":"Charles","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":827006,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70226541,"text":"70226541 - 1970 - Geophysical studies of the Cripple Creek mining district, Colorado","interactions":[],"lastModifiedDate":"2021-11-23T15:03:17.217595","indexId":"70226541","displayToPublicDate":"1970-06-01T08:56:13","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1808,"text":"Geophysics","active":true,"publicationSubtype":{"id":10}},"title":"Geophysical studies of the Cripple Creek mining district, Colorado","docAbstract":"Integrated geophysical, geochemical, and geological interpretations expand the knowledge about the localization of the ore deposits in the Cripple Creek district, Colorado. The principal gold deposits occur in a Tertiary volcanic subsidence basin within Precambrian granite, gneiss, and schist. The basin is filled with volcanic breccia and is intruded by dikes and irregular masses of phonolite, latite-phonolite, syenite, trachydolerite, and basalt. The volcanic complex gives rise to a broad 10 mgal gravity minimum anomaly upon which are superimposed local minima believed to be related to deep mineralized fissure zones. A negative magnetic anomaly over the volcanic subsidence basin probably reflects the degree of alteration of rocks in the subsurface. Two local closed magnetic lows may represent highly altered volcanic centers in the bottom of the basin. The gravity and magnetic anomalies of the basin correlate geographically with positive geochemical anomalies for gold, silver, and tellurium. Just east of the volcanic basin, a prominent negative magnetic anomaly and a corresponding gravity low may represent an altered zone in the granite subsurface.
The northern part of the disturbed belt in Montana is a northwesterly trending zone of closely spaced westerly dipping thrust faults, many folds, and some longitudinal normal faults and transverse faults. The theory of vertical uplift that results in gravitational gliding is a reasonable explanation of the origin of the disturbed belt of northwestern Montana.
The outcropping sedimentary rocks range in age from Precambrian (Belt Supergroup) to Tertiary. All Precambrian, Paleozoic, and Mesozoic stratigraphic rock units thin markedly to the east. Westernmost Montana was a slowly subsiding geosynclme during Precambrian (Belt) sedimentation and a miogeosyncline during much of Paleozoic sedimentation. The miogeosynclinal area was uplifted into a highland during the Jurassic and Cretaceous, and sediment from the highland was deposited in a basin to the east. Periodic uplift and erosion continued through Cretaceous and very early Tertiary. I believe that a décollement was established, in the easterly tilted sediments, and the mass moved eastward under the influence of gravity across the small Mesozoic basin. The décollement migrated upsection to the east. East of the slide mass the rocks were folded, marking the east edge of the northern part of the disturbed belt in Montana. This edge was probably controlled by the erosional edge of the Precambrian (Belt) rocks and the west side of the craton. Additional uplift continued to produce sliding that piled one fault block upon another. The minimum amount of shortening of this upper part of the crust by thrust faulting and folding computed along one line of section is more than 29 miles. The amount of uplift to the west very likely exceeded 45,000 ft during the period from very Late Cretaceous to late Eocene. The main décollement was under an overburden of as much as 25,000 ft of strata—a thickness that would probably permit abnormal fluid pressures to develop in mudstone. The slope of the strata and glide surface by the end of uplift may have been as much as 8.5°.
Large Basin-and-Range-type normal faults developed, after thrusting, between the area of maximum uplift and the thrust fault belt. The westernmost of these faults formed the graben and horsts in the Rocky Mountain trench. The total amount of displacement of the normal faults along one line of section is about 43,000 ft. The total thickness of strata eroded from the area of maximum uplift is about 45,000 ft.
The theory of vertical uplift and gravitational sliding may also be applicable to the disturbed belt in Alberta and British Columbia. The disturbed belt, Rocky Mountain trench, and areas of uplift are continuous from northwestern Montana to northern British Columbia. Much of the geologic history of western Alberta and eastern British Columbia is like that of northwestern Montana.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1970)81[377:OOTDBI]2.0.CO;2","usgsCitation":"Mudge, M., 1970, Origin of the disturbed belt in northwestern Montana, v. 81, no. 2, p. 377-392, https://doi.org/10.1130/0016-7606(1970)81[377:OOTDBI]2.0.CO;2.","productDescription":"17 p.","startPage":"377","endPage":"392","costCenters":[],"links":[{"id":392188,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Montana","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -116.103515625,\n 49.009050809382046\n ],\n [\n -116.12548828124999,\n 47.945786463687185\n ],\n [\n -115.68603515624999,\n 47.57652571374621\n ],\n [\n -115.90576171874999,\n 47.338822694822\n ],\n [\n -114.67529296874999,\n 46.51351558059737\n ],\n [\n -114.3896484375,\n 46.5739667965278\n ],\n [\n -111.37939453125,\n 46.543749602738565\n ],\n [\n -113.35693359375,\n 49.03786794532644\n ],\n [\n -116.103515625,\n 49.009050809382046\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"81","issue":"2","tableOfContents":"https://doi.org/10.1130/0016-7606(1970)81[377:OOTDBI]2.0.CO;2
","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Mudge, Melville R.","contributorId":72370,"corporation":false,"usgs":true,"family":"Mudge","given":"Melville R.","affiliations":[],"preferred":false,"id":827394,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70226767,"text":"70226767 - 1970 - Variations of major chemical constituents across the central Sierra Nevada batholith","interactions":[],"lastModifiedDate":"2021-12-10T14:42:25.323858","indexId":"70226767","displayToPublicDate":"1970-02-01T08:34:40","publicationYear":"1970","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":"Variations of major chemical constituents across the central Sierra Nevada batholith","docAbstract":"A study of 193 chemical analyses of plutonic rocks from 132 localities in the central Sierra Nevada shows convincingly that K2O decreases systematically westward and suggests that Fe2O3 and TiO2 may also decrease westward and that FeO, MgO, and CaO may increase. The ratio K2O/SiO2 obviously decreases westward across six of eight provisionally established sequences of granitic rocks. Plots of analyses of rocks from each sequence form discrete fields that are strongly elongate toward zero K2O at 40 to 45 percent SiO2. The boundaries between fields on these plots and between fields on plots of normative minerals on triangular diagrams are sharp. Compositional trends within sequences are different than the compositional changes that take place across the batholith—rocks in the western Sierra Nevada probably are not compositionally identical with rocks that are present at depth beneath the eastern Sierra Nevada.
Progressive decrease of K2O in the Paleozoic and Mesozoic country rocks westward across the batholith is consistent with the anatectic model for its origin. However, it also is consistent with the hypothesis developed to explain chemical patterns in volcanic island arcs—that K2O increases toward continental land masses because of increasing depth of magma generation along landward-dipping seismic (Benioff) zones. The seismic-zone hypothesis encounters several difficulties, but it cannot be ruled out.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1970)81[409:VOMCCA]2.0.CO;2","usgsCitation":"Bateman, P.C., and Dodge, F.C., 1970, Variations of major chemical constituents across the central Sierra Nevada batholith: Bulletin of the Geological Society of America, v. 81, no. 2, p. 409-420, https://doi.org/10.1130/0016-7606(1970)81[409:VOMCCA]2.0.CO;2.","productDescription":"12 p.","startPage":"409","endPage":"420","costCenters":[],"links":[{"id":392724,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Sierra Nevada","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -119.92675781249999,\n 36.677230602346214\n ],\n [\n -117.674560546875,\n 36.677230602346214\n ],\n [\n -117.674560546875,\n 37.95286091815649\n ],\n [\n -119.92675781249999,\n 37.95286091815649\n ],\n [\n -119.92675781249999,\n 36.677230602346214\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"81","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Bateman, P. C.","contributorId":27851,"corporation":false,"usgs":true,"family":"Bateman","given":"P.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":828193,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dodge, F. C. W.","contributorId":18755,"corporation":false,"usgs":true,"family":"Dodge","given":"F.","email":"","middleInitial":"C. W.","affiliations":[],"preferred":false,"id":828194,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70168632,"text":"70168632 - 1970 - Geology and ground-water resources of Linn County, Iowa","interactions":[],"lastModifiedDate":"2021-02-22T17:06:26.745895","indexId":"70168632","displayToPublicDate":"1970-01-01T13:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":148,"text":"Water Supply Bulletin","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"10","title":"Geology and ground-water resources of Linn County, Iowa","docAbstract":"Linn County, in east-central Iowa, covers about 713 square miles and lies in the Western Young Drift section of the Central Lowlands physiographic province. The normal annual rainfall in the county is about 88 inches and the annual mean temperature is about 48°F. The population in 1960 was 136,899, of which 75 percent was urban.
Ground water is a vital natural resource in Linn County-all municipal, farm-domestic, livestock, and most industrial supplies are obtained from this source. An estimated 24 mgd (million gallons per day) of ground water was used in the county in 1964.
The principal aquifers are alluvium, buried channel deposits, Silurian-Devonian limestones and dolomites, and the Jordan Sandstone. All yield fair-to-good quality water, although the water is hard and locally contains high concentrations of iron. All are capable of yielding as much as 500 gallons or more per minute to wells.
Alluvium has been developed for water supplies only at Cedar Rapids, where withdrawals in 1964 averaged 12 mgd for municipal supplies and 2.7 mgd for industrial supplies. The alluvial aquifer yields up to 2,000 gpm (gallons per minute) to wells in the Cedar Rapids well field. Similar yields from alluvium may be available along several reaches of the Cedar and Wapsipinicon Rivers. Smaller quantities are available from the alluvium of Prairie Creek. Alluvial aquifers are readily recharged by precipitation and induced infiltration.
Buried channel deposits occur in preglacial or interglacial valleys that were carved into the bedrock. These old valleys, whose trends roughly parallel the present Cedar River and Prairie Creek, contain water-bearing alluvial deposits that are covered by glacial drift. Data from a few wells tapping these deposits indicate that yields of up to 500 gpm of good-quality water are available from this source. The most favorable areas for development of water supplies are those areas where the channel deposits underlie and receive recharge from the alluvium of the Cedar River and Prairie Creek.
The Silurian-Devonian aquifer's county-wide occurrence, near-surface position, and ability to yield as much as several hundred gallons per minute of good-quality water makes it the most widely used aquifer in Linn County. During 1960-64, withdrawals averaged about 1.5 mgd for domestic-livestock use, about 0.6 mgd for small community use, and about 4 mgd for industrial-commercial use. Withdrawals are concentrated in the Cedar Rapids area, where 65 percent of the withdrawals from the aquifer occur. This concentrated pumpage has caused a progressive lowering of the aquifer's piezometric surface in downtown Cedar Rapids. During the past 70 years, water levels in wells in this locality have declined about 105 feet in the center of the cone of depression and about 26 feet about one mile from the cone's center. Water level in the center of the cone presently is declining at an average rate of 1 foot per year. Because the rate of decline in the same area was determined to have been 2 to 3 feet per year during the 1940's and 50's, the cone is believed to be stabilizing or pumpage is being reduced. The aquifer probably could withstand an additional 150 to 200 feet of piezometric lowering in the Cedar Rapids area, but individual wells would be adversely affected.
The Jordan aquifer, which underlies the entire county, is considered to be the most isotropic and homogeneous aquifer in Linn County. Yields of 1,000 gpm or more of fair-to-good quality water from this source are believed to be available anywhere in the county. The aquifer is not yet developed extensively; an average of about 2.4 mgd was pumped during 1964 for industrial and municipal use in the Cedar Rapids-Marion area.
The shallow bedrock and glacial drift aquifers yield only small quantities of good quality water. Their widespread extent and shallow depth, however, make them suitable for the development of small supplies for domestic and livestock use.
","language":"English","publisher":"State of Iowa","publisherLocation":"Des Moines, IA","usgsCitation":"Hansen, R.E., 1970, Geology and ground-water resources of Linn County, Iowa: Water Supply Bulletin 10, 66 p.","productDescription":"66 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":351,"text":"Iowa Water Science Center","active":true,"usgs":true}],"links":[{"id":318268,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70168632.JPG"},{"id":318267,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://www.iihr.uiowa.edu/igs/publications/uploads/WSB-10.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Iowa","county":"Linn","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-91.3649,42.2964],[-91.3651,42.2082],[-91.3653,42.1215],[-91.3661,42.0343],[-91.3669,41.948],[-91.3677,41.8603],[-91.4836,41.8608],[-91.5989,41.8612],[-91.716,41.862],[-91.8318,41.8617],[-91.8329,41.9485],[-91.8338,42.0366],[-91.8342,42.1242],[-91.8328,42.2087],[-91.8319,42.2987],[-91.7153,42.2971],[-91.5969,42.2959],[-91.4809,42.296],[-91.3649,42.2964]]]},\"properties\":{\"name\":\"Linn\",\"state\":\"IA\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"56cc3fdce4b059daa47e45ab","contributors":{"authors":[{"text":"Hansen, Robert E.","contributorId":167112,"corporation":false,"usgs":false,"family":"Hansen","given":"Robert","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":621075,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70226515,"text":"70226515 - 1970 - Tertiary tectonics of the White Pine-Grant Range region, east-central Nevada, and some regional implications: Discussion","interactions":[],"lastModifiedDate":"2021-11-22T18:46:38.983742","indexId":"70226515","displayToPublicDate":"1970-01-01T12:29:54","publicationYear":"1970","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":"Tertiary tectonics of the White Pine-Grant Range region, east-central Nevada, and some regional implications: Discussion","docAbstract":"No abstract available.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1970)81[319:TTOTWP]2.0.CO;2","usgsCitation":"Drewes, H., 1970, Tertiary tectonics of the White Pine-Grant Range region, east-central Nevada, and some regional implications: Discussion: Bulletin of the Geological Society of America, v. 81, no. 1, p. 319-321, https://doi.org/10.1130/0016-7606(1970)81[319:TTOTWP]2.0.CO;2.","productDescription":"3 p.","startPage":"319","endPage":"321","costCenters":[],"links":[{"id":391992,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"White Pine-Grant Range","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -115.60638427734375,\n 38.807610542357594\n ],\n [\n -115.19027709960936,\n 38.807610542357594\n ],\n [\n -115.19027709960936,\n 39.299236474818194\n ],\n [\n -115.60638427734375,\n 39.299236474818194\n ],\n [\n -115.60638427734375,\n 38.807610542357594\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"81","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Drewes, Harald","contributorId":52567,"corporation":false,"usgs":true,"family":"Drewes","given":"Harald","affiliations":[],"preferred":false,"id":827169,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70139638,"text":"70139638 - 1970 - Taunton River basin","interactions":[],"lastModifiedDate":"2015-02-09T09:55:14","indexId":"70139638","displayToPublicDate":"1970-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":367,"text":"Massachusetts Hydrologic - Data Report","active":false,"publicationSubtype":{"id":6}},"seriesNumber":"12","title":"Taunton River basin","docAbstract":"The Taunton River, emptying into an arm of Narragansett Bay at Fall River, drains 528 square miles of interior southeastern Massachusetts. The Taunton River basin is separated from the basins of short streams draining to the coast by low divides on the east, south, and southwest. On the west and north, the basin is bordered by the Ten Mile, Charles, Neponset, and Weymouth River basins. Principal tributaries of the lower Taunton River are Segreganset, Threemile, Mill, Assonet, Nemasket, and Winnetuxet Rivers. The upper part of the basin is drained by the Canoe, Wading, and Rumford Rivers which empty into Mill and Threemile Rivers and by the Matfield and Town Rivers which unite to form the Taunton River.
\nThis report presents in tabular form selected records of wells, test wells, and borings collected during a study of the basin from 1966 to 1968 in cooperation with the Massachusetts Water Resources Commission, and during earlier studies. This report is released in order to make available to the public and to local, state, and federal agencies basic ground-water information that may aid in planning water-resources development. Basic records contained in this report will complement an interpretative report on the Taunton River basin to be released at a later date.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Boston, MA","doi":"10.3133/70139638","collaboration":"Prepared in cooperation with the Commonwealth of Massachusetts, Water Resources Commission","usgsCitation":"Williams, J.R., and Willey, R.E., 1970, Taunton River basin: U.S. Geological Survey Massachusetts Hydrologic - Data Report 12, Report: 102 p.; 2 Plates, https://doi.org/10.3133/70139638.","productDescription":"Report: 102 p.; 2 Plates","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":297614,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"scale":"48000","country":"United States","state":"Massachusetts","otherGeospatial":"Taunton River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -71.39465332031249,\n 41.65034063112266\n ],\n [\n -71.39465332031249,\n 42.132858175814626\n ],\n [\n -70.78216552734375,\n 42.132858175814626\n ],\n [\n -70.78216552734375,\n 41.65034063112266\n ],\n [\n -71.39465332031249,\n 41.65034063112266\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"54dd2c67e4b08de9379b379f","contributors":{"authors":[{"text":"Williams, John R.","contributorId":107260,"corporation":false,"usgs":true,"family":"Williams","given":"John","email":"","middleInitial":"R.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":539473,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Willey, Richard E.","contributorId":30972,"corporation":false,"usgs":true,"family":"Willey","given":"Richard","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":539474,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70043189,"text":"70043189 - 1970 - Foraminiferal zonation and carbonate facies of Carboniferous (Mississippian and Pennsylvanian) Lisburne group, central and eastern Brooks range, Arctic Alaska","interactions":[{"subject":{"id":12478,"text":"ofr6912 - 1970 - Availability of petrographic thin-sections of the Lisburne Group from northeastern Brooks Range, Alaska","indexId":"ofr6912","publicationYear":"1970","noYear":false,"title":"Availability of petrographic thin-sections of the Lisburne Group from northeastern Brooks Range, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":70043189,"text":"70043189 - 1970 - Foraminiferal zonation and carbonate facies of Carboniferous (Mississippian and Pennsylvanian) Lisburne group, central and eastern Brooks range, Arctic Alaska","indexId":"70043189","publicationYear":"1970","noYear":false,"title":"Foraminiferal zonation and carbonate facies of Carboniferous (Mississippian and Pennsylvanian) Lisburne group, central and eastern Brooks range, Arctic Alaska"},"id":1},{"subject":{"id":12479,"text":"ofr6914 - 1969 - Foraminiferal zonation and carbonate facies of the Mississippian and Pennsylvanian Lisburne Group, central and eastern Brooks Range, Arctic Alaska","indexId":"ofr6914","publicationYear":"1969","noYear":false,"title":"Foraminiferal zonation and carbonate facies of the Mississippian and Pennsylvanian Lisburne Group, central and eastern Brooks Range, Arctic Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":70043189,"text":"70043189 - 1970 - Foraminiferal zonation and carbonate facies of Carboniferous (Mississippian and Pennsylvanian) Lisburne group, central and eastern Brooks range, Arctic Alaska","indexId":"70043189","publicationYear":"1970","noYear":false,"title":"Foraminiferal zonation and carbonate facies of Carboniferous (Mississippian and Pennsylvanian) Lisburne group, central and eastern Brooks range, Arctic Alaska"},"id":2}],"lastModifiedDate":"2023-01-31T17:51:44.79545","indexId":"70043189","displayToPublicDate":"1970-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":701,"text":"American Association of Petroleum Geologists Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Foraminiferal zonation and carbonate facies of Carboniferous (Mississippian and Pennsylvanian) Lisburne group, central and eastern Brooks range, Arctic Alaska","docAbstract":"The Lisburne Group carbonate rocks of the central and eastern Brooks Range contain foraminiferal assemblages assigned to zones of late Tournaisian (Osage) to early Moscovian (Atoka) age. Representatives of both Eurasiatic and American cratonic microfaunas permit correlation with the original Carboniferous type sections in western Europe as well as with the standard Mississippian and Pennsylvanian sequences in the Mid-Continent region of North America. Correlation anomalies in the lower part of the sequence are discussed.","language":"English","publisher":"American Association of Petroleum Geologists","publisherLocation":"Tulsa, OK","doi":"10.1306/5D25CA2F-16C1-11D7-8645000102C1865D","usgsCitation":"Armstrong, A.K., Mamet, B.L., and Dutro, J.T., 1970, Foraminiferal zonation and carbonate facies of Carboniferous (Mississippian and Pennsylvanian) Lisburne group, central and eastern Brooks range, Arctic Alaska: American Association of Petroleum Geologists Bulletin, v. 54, no. 5, p. 687-698, https://doi.org/10.1306/5D25CA2F-16C1-11D7-8645000102C1865D.","productDescription":"12 p.","startPage":"687","endPage":"698","costCenters":[{"id":255,"text":"Energy Resources Program","active":true,"usgs":true}],"links":[{"id":267106,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Brooks Range","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -153.4103906372097,\n 70\n ],\n [\n -153.4103906372097,\n 67.54650489763466\n ],\n [\n -142.48531896350084,\n 67.54650489763466\n ],\n [\n -142.48531896350084,\n 70\n ],\n [\n -153.4103906372097,\n 70\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"54","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5114db04e4b0ca7af0743b22","contributors":{"authors":[{"text":"Armstrong, Augustus K.","contributorId":68282,"corporation":false,"usgs":true,"family":"Armstrong","given":"Augustus","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":473129,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Mamet, Bernard L.","contributorId":32524,"corporation":false,"usgs":true,"family":"Mamet","given":"Bernard","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":473127,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Dutro, J. Thomas","contributorId":54204,"corporation":false,"usgs":true,"family":"Dutro","given":"J.","email":"","middleInitial":"Thomas","affiliations":[],"preferred":false,"id":473128,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70231277,"text":"70231277 - 1969 - Structural control of wind gaps and water gaps and of stream capture in the Stroudsburg area","interactions":[],"lastModifiedDate":"2022-05-04T16:46:28.079197","indexId":"70231277","displayToPublicDate":"2022-05-04T11:43:21","publicationYear":"1969","noYear":false,"publicationType":{"id":24,"text":"Conference Paper"},"publicationSubtype":{"id":19,"text":"Conference Paper"},"title":"Structural control of wind gaps and water gaps and of stream capture in the Stroudsburg area","docAbstract":"No abstract available.
","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Geology of selected areas in New Jersey and eastern Pennsylvania and guidebook","largerWorkSubtype":{"id":12,"text":"Conference publication"},"language":"English","publisher":"Geological Society of America","usgsCitation":"Epstein, J.B., 1969, Structural control of wind gaps and water gaps and of stream capture in the Stroudsburg area, in Geology of selected areas in New Jersey and eastern Pennsylvania and guidebook, p. 206-213.","productDescription":"8 p.","startPage":"206","endPage":"213","costCenters":[{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"links":[{"id":400162,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"New Jersey, Pennsylvania","city":"Stroudsburg","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -75.23849487304686,\n 40.914550362677204\n ],\n [\n -75.06546020507812,\n 40.914550362677204\n ],\n [\n -75.06546020507812,\n 41.03896645352545\n ],\n [\n -75.23849487304686,\n 41.03896645352545\n ],\n [\n -75.23849487304686,\n 40.914550362677204\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Epstein, Jack B. jepstein@usgs.gov","contributorId":1412,"corporation":false,"usgs":true,"family":"Epstein","given":"Jack","email":"jepstein@usgs.gov","middleInitial":"B.","affiliations":[{"id":40020,"text":"Florence Bascom Geoscience Center","active":true,"usgs":true},{"id":243,"text":"Eastern Geology and Paleoclimate Science Center","active":true,"usgs":true}],"preferred":true,"id":842188,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":13004,"text":"ofr1305MP - 1969 - Petroleum potential of the Kandik basin, east-central Alaska","interactions":[],"lastModifiedDate":"2018-06-14T13:51:28","indexId":"ofr1305MP","displayToPublicDate":"2013-07-30T10:21:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"1305 MP","title":"Petroleum potential of the Kandik basin, east-central Alaska","docAbstract":"No abstract available.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/ofr1305MP","usgsCitation":"Churkin, M., and Brabb, E.E., 1969, Petroleum potential of the Kandik basin, east-central Alaska: U.S. Geological Survey Open-File Report 1305 MP, iii, 11 p., https://doi.org/10.3133/ofr1305MP.","productDescription":"iii, 11 p.","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":291385,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"country":"United States","state":"Alaska","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -142.52,65.37 ], [ -142.52,65.84 ], [ -141.0,65.84 ], [ -141.0,65.37 ], [ -142.52,65.37 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57ffc827e4b0824b2d17454c","contributors":{"authors":[{"text":"Churkin, Michael","contributorId":66677,"corporation":false,"usgs":true,"family":"Churkin","given":"Michael","affiliations":[],"preferred":false,"id":167121,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brabb, Earl E.","contributorId":48939,"corporation":false,"usgs":true,"family":"Brabb","given":"Earl","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":167120,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70038241,"text":"70038241 - 1969 - Hydrogeologic data for the southwestern coastal river basins, Connecticut","interactions":[],"lastModifiedDate":"2014-05-09T07:59:18","indexId":"70038241","displayToPublicDate":"2012-04-22T14:06:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":108,"text":"Connecticut Water Resources Bulletin","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"18","title":"Hydrogeologic data for the southwestern coastal river basins, Connecticut","docAbstract":"This report presents hydrologic and geologic data collected by the U.S.\nGeological Survey during an investigation of water resources in the southwestern\ncoastal river basins of Connecticut in cooperation with the Connecticut Water\nResources Commission. These basins occupy about 394 square miles in Connecticut\nand 46 square miles in New York, including the towns of Greenwich, Stamford,\nDarien, New Canaan, Norwalk, Wilton, Westport, Weston, Fairfield, Easton, and\nBridgeport and parts of Danbury, Ridgefield, Redding, Bethel, Newtown, Trumbull,\nMonroe, Shelton, and Stratford. A companion interpretive report evaluating the\nwater resources of the basins will be published as Connecticut Water Resources\nBulletin No. 17. The data on the following pages serve to document and supplement\nthat report and should be especially useful in planning the development of water\nresources at specific localities.\nData were collected as part of this investigation during the period July 1963\nthrough November 1966. Streamflow records from continuous-record gaging stations\nin the basins have been published annually along with data from other parts of\nthe State in a series of U.S. Geological Survey reports entitled \"Surface Water\nRecords of Connecticut.\" Water-level measurements in wells throughout the State\nfrom 1960 through 1966, including most of those made as part of this investigation,\nare published in Connecticut Water Resources Bulletins No. 7 and No. 13. Most\nother data collected during this investigation are tabulated on the following pages.\nIncluded are some well records and chemical analyses of water samples collected\nprior to July 1963 and not previously published.\nThe locations of sites at which data were collected are shown on plate A\nin the pocket at the back of the report. Data presented, unless otherwise noted,\nwere collected by U.S. Geological Survey personnel.","language":"English","publisher":"Connecticut Water Resources Commission","collaboration":"Prepared by the U.S. Geological Survey in cooperation with the Connecticut Water Resources Commission","usgsCitation":"Thomas, M.P., Ryder, R.B., and Thomas, C.E., 1969, Hydrogeologic data for the southwestern coastal river basins, Connecticut: Connecticut Water Resources Bulletin 18, Report: 45 p.; 1 Plate: 23.67 x 22.80 inches.","productDescription":"Report: 45 p.; 1 Plate: 23.67 x 22.80 inches","numberOfPages":"49","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":258803,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ctwrb/0018/plate-a.pdf","size":"3986","linkFileType":{"id":1,"text":"pdf"}},{"id":258804,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/ctwrb/0018/report-thumb.jpg"},{"id":287014,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70038241/report.pdf"}],"scale":"48000","country":"United States","state":"Connecticut","otherGeospatial":"Coastal River Basins","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -73.75,40.933333 ], [ -73.75,41.383333 ], [ -73.116667,41.383333 ], [ -73.116667,40.933333 ], [ -73.75,40.933333 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a33b8e4b0c8380cd5f1ec","contributors":{"authors":[{"text":"Thomas, Mendall P.","contributorId":104314,"corporation":false,"usgs":true,"family":"Thomas","given":"Mendall","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":463725,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ryder, Robert B. rryder@usgs.gov","contributorId":68294,"corporation":false,"usgs":true,"family":"Ryder","given":"Robert","email":"rryder@usgs.gov","middleInitial":"B.","affiliations":[],"preferred":false,"id":463724,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Thomas, Chester E. Jr.","contributorId":37182,"corporation":false,"usgs":true,"family":"Thomas","given":"Chester","suffix":"Jr.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":463723,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70001751,"text":"70001751 - 1969 - Primitive and contaminated basalts from the Southern Rocky Mountains, U.S.A","interactions":[],"lastModifiedDate":"2020-11-29T17:39:58.795047","indexId":"70001751","displayToPublicDate":"2010-09-28T23:09:23","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1336,"text":"Contributions to Mineralogy and Petrology","active":true,"publicationSubtype":{"id":10}},"title":"Primitive and contaminated basalts from the Southern Rocky Mountains, U.S.A","docAbstract":"Basalts in the Southern Rocky Mountains province have been analyzed to determine if any of them are primitive. Alkali plagioclase xenocrysts armored with calcic plagioclase seem to be the best petrographic indicator of contamination. The next best indicator of contamination is quartz xenocrysts armored with clinopyroxene. On the rocks and the region studied, K2O apparently is the only major element with promise of separating primitive basalt from contaminated basalt inasmuch as it constitutes more than 1 % in all the obviously contaminated basalts. K2O: lead (> 4 ppm) and thorium (> 2 ppm) contents and Rb/Sr (> 0.035) are the most indicative of the trace elements studied. Using these criteria, three basalt samples are primitive (although one contains 1.7% K2O) and are similar in traceelement contents to Hawaiian and Eastern Honshu, Japan, primitive basalts.
Contamination causes lead isotope ratios, 206Pb/204Pb and 208Pb/204Pb, to become less radiogenic, but it has little or no effect on 87Sr/86Sr. We interpret the effect on lead isotopes to be due to assimilation either of lower crustal granitic rocks, which contain 5–10 times as much lead as basalt and which have been low in U/Pb and Th/Pb since Precambrian times, or of upper crustal Precambrian or Paleozoic rocks, which have lost much of their radiogenic lead because of heating prior to assimilation. The lack of definite effects on strontium isotopes may be due to the lesser strontium contents of granitic crustal rocks relative to basaltic rocks coupled with lack of a large radiogenic enrichment in the crustal rocks.
Lead isotope ratios were found to be less radiogenic in plagioclase separates from an obviously contaminated basalt than in the primitive basalts. The feldspar separate that is rich in sodic plagioclase xenocrysts was found to be similar to the whole-rock composition for 206Pb/204Pb and 208Pb/204Pb whereas a more dense fraction probably enriched in more calcic plagioclase phenocrysts is more similar to the primitive basalts in lead isotope ratios.
The primitive basalts have: 206Pb/204Pb ∼ 18.09–18.34, 207Pb/204Pb ∼ 15.5, 208Pb/204Pb ∼ 37.6–37.9, 87Sr/86Sr ∼ 0.704–0.705. In the primitive basalts from the Southern Rocky Mountains the values of 206Pb/204Pb are similar to values reported by others for Hawaiian and eastern Honshu basalts and abyssal basalts, whereas 208Pb/204Pb tends to be equal to or a little less radiogenic than those from the oceanic localities. 87Sr/86Sr appears to be equal to or a little greater than those of the oceanic localities. These 206Pb/204Pb and 208Pb/204Pb ratios are distinctly less radiogenic and 87Sr/86Sr values are about equal to those reported by others for volcanic islands on oceanic ridges and rises.
","language":"English","publisher":"Springer","doi":"10.1007/BF00403342","issn":"00107999","usgsCitation":"Doe, B.R., Lipman, P.W., Hedge, C., and Kurasawa, H., 1969, Primitive and contaminated basalts from the Southern Rocky Mountains, U.S.A: Contributions to Mineralogy and Petrology, v. 21, no. 2, p. 142-156, https://doi.org/10.1007/BF00403342.","productDescription":"15 p.","startPage":"142","endPage":"156","costCenters":[],"links":[{"id":203299,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado","otherGeospatial":"Southern Rocky Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -109.05029296875,\n 36.94111143010769\n ],\n [\n -104.359130859375,\n 36.94111143010769\n ],\n [\n -104.359130859375,\n 40.93841495689795\n ],\n [\n -109.05029296875,\n 40.93841495689795\n ],\n [\n -109.05029296875,\n 36.94111143010769\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"21","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67be3d","contributors":{"authors":[{"text":"Doe, B. R.","contributorId":52173,"corporation":false,"usgs":true,"family":"Doe","given":"B.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":346828,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lipman, P. W.","contributorId":93470,"corporation":false,"usgs":true,"family":"Lipman","given":"P.","middleInitial":"W.","affiliations":[],"preferred":false,"id":346830,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hedge, C. E.","contributorId":73611,"corporation":false,"usgs":true,"family":"Hedge","given":"C. E.","affiliations":[],"preferred":false,"id":346829,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Kurasawa, H.","contributorId":41565,"corporation":false,"usgs":true,"family":"Kurasawa","given":"H.","email":"","affiliations":[],"preferred":false,"id":346827,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":6309,"text":"pp542G - 1969 - Effects of the earthquake of March 27, 1964, on various communities","interactions":[{"subject":{"id":6309,"text":"pp542G - 1969 - Effects of the earthquake of March 27, 1964, on various communities","indexId":"pp542G","publicationYear":"1969","noYear":false,"chapter":"G","title":"Effects of the earthquake of March 27, 1964, on various communities"},"predicate":"IS_PART_OF","object":{"id":70048211,"text":"pp542 - 1969 - The Alaska earthquake, March 27, 1964: Effects on communities","indexId":"pp542","publicationYear":"1969","noYear":false,"title":"The Alaska earthquake, March 27, 1964: Effects on communities"},"id":1}],"isPartOf":{"id":70048211,"text":"pp542 - 1969 - The Alaska earthquake, March 27, 1964: Effects on communities","indexId":"pp542","publicationYear":"1969","noYear":false,"title":"The Alaska earthquake, March 27, 1964: Effects on communities"},"lastModifiedDate":"2022-04-28T19:46:13.571561","indexId":"pp542G","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"542","chapter":"G","title":"Effects of the earthquake of March 27, 1964, on various communities","docAbstract":"The 1964 earthquake caused wide-spread damage to inhabited places throughout more than 60,000 square miles of south-central Alaska. This report describes damage to all communities in the area except Anchorage, Whittier, Homer, Valdez, Seward, the communities of the Kodiak group of islands, and communities in the Copper River Basin; these were discussed in previous chapters of the Geological Survey's series of reports on the earthquake. At the communities discussed herein, damage resulted primarily from sea waves of diverse origins, displacements of the land relative to sea level, and seismic shaking. Waves took all of the 31 lives lost at those communities; physical damage was primarily from the waves and vertical displacements of the land relative to sea level.
\n\nDestructive waves of local origin struck during or immediately after the earthquake throughout much of Prince William Sound, the southern Kenai Peninsula, and the shores of Kenai Lake. In Prince William Sound, waves demolished all but one home at the native village of Chenega, destroyed homesites at Point Nowell and Anderson Bay, and caused varying amounts of damage to waterfront facilities at Sawmill Bay, Latouche, Port Oceanic, Port Nellie Juan, Perry Island, and western Port Valdez. The local waves, which ran up as high as 70 feet above tide level at Chenega and more than 170 feet in several uninhabited parts of the Sound, took nearly all of the lives lost by drowning at these communities. Destructive local waves that devastated shores of Anderson Bay and adjacent parts of western Port Valdez probably were generated primarily by massive submarine slides of glacial and fluvioglacial deposits ; the origin of the waves that caused damage at most of the other communities and at extensive uninhabited segments of shoreline is not known. At these places the most probable generative mechanisms are: unidentified submarine slides of unconsolidated deposits, and (or) the horizontal tectonic displacements, of 20 to more than 60 feet, that occurred in the Prince William Sound region during the earthquake.
\n\nA train of long-period seismic sea waves that began about 20 minutes after the start of the earthquake inundated shores along the Gulf of Alaska coast to a maximum height of 35 feet above tide level. At the communities described, they virtually destroyed two logging camps at Whidbey Bay and Puget Bay on the south coast of the Kenai Peninsula, caused moderate damage to boat harbors and docks at Seldovia and Cordova, floated away some beach cabins in the Cordova area, and drowned two people, one at Point Whitshed near Cordora and one at the Cape Saint Elias Light Station. The seismic sea waves were generated by regional tectonic uplift of the sea floor on the Continental Shelf.
\n\nVertical tectonic displacements of the land relative to sea level that accompanied the earthquake affected virtually all the coastal communities. Tectonic subsidence of 5 to 6 feet, augmented locally by surficial subsidence of unconsolidated deposits required either the relocation or raising of structures at Portage, Girdwood, and Hope on Turnagain Arm. Shoreline submergence resulting from about 3½ feet of tectonic subsidence at Seldovia necessitated raising all waterfront facilities and the airstrip above the level of high tides. On the other hand, tectonic uplift of the land in the Prince Williams Sound region required deepening of the small-boat harbors at Cordora and Tatitlek, dredging of the waterways in the Cordova area, and lengthening of some docks or piers at Cordova, the Cape Hinchinbrook Light Station, and in Sawmill Bay.
\n\nSignificant structural damage from direct seismic shaking was largely confined to fluid containers and a pier facility near Kenai. Indirect damage from fissuring and differential settling of foundation mterials in the vicinity of the Cordova airfield mused damage to a building, underground utilities, an airfield fill, and the highway. Minor amounts of direct and indirect damage from seismic vibrations were sustained by most of the communities situated on unconsolidated deposits as far east as Yakutat, north to Fairbanks, and west to King Salmon. Except for a few cracked or toppled chimney, all the damage from shaking was confined to areas of thick, unconsolidated deposits. Foundation damage was almost entirely restricted to water-saturated unconsolidated deposits which, when liquefied by seismic shaking, could spread laterally toward free faces and (or) settle differentially through compaction.
","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"The Alaska earthquake, March 27, 1964: Effects on communities (Professional Paper 542)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, DC","doi":"10.3133/pp542G","usgsCitation":"Plafker, G., Kachadoorian, R., Eckel, E.B., and Mayo, L.R., 1969, Effects of the earthquake of March 27, 1964, on various communities: U.S. Geological Survey Professional Paper 542, Report: vi, 50 p.; 2 Plates: 47 x 35 inches and 41.96 x 37 inches, https://doi.org/10.3133/pp542G.","productDescription":"Report: vi, 50 p.; 2 Plates: 47 x 35 inches and 41.96 x 37 inches","numberOfPages":"61","additionalOnlineFiles":"Y","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":399843,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4589.htm"},{"id":33598,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0542g/pp542g_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33597,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542g/pp542g_plate2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":33596,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542g/pp542g_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":117253,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0542g/report-thumb.jpg"},{"id":104505,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0542g/index.html","linkFileType":{"id":5,"text":"html"},"description":"4589"}],"scale":"2500000","datum":"Mean Sea Level","country":"United States","state":"Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -168,\n 52\n ],\n [\n -130,\n 52\n ],\n [\n -130,\n 66.5\n ],\n [\n -168,\n 66.5\n ],\n [\n -168,\n 52\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c82f","contributors":{"authors":[{"text":"Plafker, George","contributorId":3920,"corporation":false,"usgs":false,"family":"Plafker","given":"George","email":"","affiliations":[],"preferred":false,"id":152485,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Kachadoorian, Reuben","contributorId":24336,"corporation":false,"usgs":true,"family":"Kachadoorian","given":"Reuben","email":"","affiliations":[],"preferred":false,"id":152486,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Eckel, Edwin B.","contributorId":26680,"corporation":false,"usgs":true,"family":"Eckel","given":"Edwin","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":152487,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Mayo, Lawrence R.","contributorId":98344,"corporation":false,"usgs":true,"family":"Mayo","given":"Lawrence","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":152488,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":68445,"text":"ha311 - 1969 - Hydrology of a part of the Big Sioux drainage basin, eastern South Dakota","interactions":[],"lastModifiedDate":"2022-02-03T21:34:22.779976","indexId":"ha311","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":318,"text":"Hydrologic Atlas","code":"HA","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"311","title":"Hydrology of a part of the Big Sioux drainage basin, eastern South Dakota","docAbstract":"In 1960 the U.S. Geological Survey, in cooperation with the South Dakota State Water Resources Commission and the South Dakota State Geological Survey, started a program for the hydrogeologic investigation of glacial drift in selected drainage basins in eastern South Dakota. This program was designed to delineate water-bearing deposits of glacial-outwash sand and gravel, and to determine their water-yielding characteristics, particularly with regard to irrigation and industrial use. Investigations of this type will aid in planning the use and conservation of ground water for future agricultural and industrial growth in South Dakota.
\nThis report describes the part of the Big Sioux River drainage basin from Sioux Falls north to a U.S. Geological Survey gaging station 9M miles southeast of Brookings (see fig. 1).
\nThe drainage area, about 675 square miles, is in the southwestern part of the Coteau des Prairies section of the Central Lowland physiographic province, as defined by Flint (1955, p. 5). It includes the Big Sioux River valley in Moody and north-central Minnehaha Counties, and the uplands that drain into the valley, from Brookings, Lake, Moody, and Minnehaha Counties, South Dakota, and Pipestone and Lincoln Counties, Minnesota.
\nThis report is based on data from field and laboratory studies and from published and unpublished records of State and Federal agencies. The investigations included: (1) Delineating area of water-bearing glacial outwash deposits; (2) inventorying wells to locate areas of greatest ground-water potential; (3) examining samples from auger holes to define thickness, extent, and character of water-bearing deposits; (4) determining the altitudes of selected test holes and wells for use in preparing cross sections and watertable maps; (5) collecting and analyzing water samples to determine the chemical character of water; and (6) testing aquifers to determine the hydrologic properties of the water-bearing deposits.
\nData consisting of logs of wells and test holes, waterlevel measurements, chemical analyses of water, stream-runoff measurements, and determinations of the hydrologic properties of aquifers are contained in a separate report by Ellis and Adolphson (1968).
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ha311","usgsCitation":"Ellis, M.J., Adolphson, D.G., and West, R.E., 1969, Hydrology of a part of the Big Sioux drainage basin, eastern South Dakota: U.S. Geological Survey Hydrologic Atlas 311, Report: 5 p.; 1 Plate: 41.0 x 51.0 inches, https://doi.org/10.3133/ha311.","productDescription":"Report: 5 p.; 1 Plate: 41.0 x 51.0 inches","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":562,"text":"South Dakota Water Science Center","active":true,"usgs":true},{"id":34685,"text":"Dakota Water Science Center","active":true,"usgs":true}],"links":[{"id":89976,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/ha/311/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":89977,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/ha/311/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":395411,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_15684.htm"},{"id":186197,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/ha/311/report-thumb.jpg"}],"scale":"125000","country":"United States","state":"South Dakota","otherGeospatial":"Big Sioux drainage basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -97.37182617187499,\n 43.50872101129684\n ],\n [\n -97.37182617187499,\n 44.3002644115815\n ],\n [\n -95.833740234375,\n 44.3002644115815\n ],\n [\n -95.833740234375,\n 43.50872101129684\n ],\n [\n -97.37182617187499,\n 43.50872101129684\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a17e4b07f02db604747","contributors":{"authors":[{"text":"Ellis, Michael J.","contributorId":40360,"corporation":false,"usgs":true,"family":"Ellis","given":"Michael","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":278232,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Adolphson, Donald G.","contributorId":53872,"corporation":false,"usgs":true,"family":"Adolphson","given":"Donald","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":278233,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"West, Robert E.","contributorId":10101,"corporation":false,"usgs":true,"family":"West","given":"Robert","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":278231,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":38817,"text":"pp543I - 1969 - Tectonics of the March 27, 1964, Alaska earthquake","interactions":[{"subject":{"id":38817,"text":"pp543I - 1969 - Tectonics of the March 27, 1964, Alaska earthquake","indexId":"pp543I","publicationYear":"1969","noYear":false,"chapter":"I","title":"Tectonics of the March 27, 1964, Alaska earthquake"},"predicate":"IS_PART_OF","object":{"id":70048225,"text":"pp543 - 1966 - The Alaska earthquake, March 27, 1964: regional effects","indexId":"pp543","publicationYear":"1966","noYear":false,"title":"The Alaska earthquake, March 27, 1964: regional effects"},"id":1}],"isPartOf":{"id":70048225,"text":"pp543 - 1966 - The Alaska earthquake, March 27, 1964: regional effects","indexId":"pp543","publicationYear":"1966","noYear":false,"title":"The Alaska earthquake, March 27, 1964: regional effects"},"lastModifiedDate":"2022-06-28T18:18:07.763935","indexId":"pp543I","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":331,"text":"Professional Paper","code":"PP","onlineIssn":"2330-7102","printIssn":"1044-9612","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"543","chapter":"I","title":"Tectonics of the March 27, 1964, Alaska earthquake","docAbstract":"The March 27, 1964, earthquake was accomp anied by crustal deformation-including warping, horizontal distortion, and faulting-over probably more than 110,000 square miles of land and sea bottom in south-central Alaska. Regional uplift and subsidence occurred mainly in two nearly parallel elongate zones, together about 600 miles long and as much as 250 miles wide, that lie along the continental margin. From the earthquake epicenter in northern Prince William Sound, the deformation extends eastward 190 miles almost to long 142° and southwestward slightly more than 400 miles to about long 155°. It extends across the two zones from the chain of active volcanoes in the Aleutian Range and Wrangell Mountains probably to the Aleutian Trench axis.\n\nUplift that averages 6 feet over broad areas occurred mainly along the coast of the Gulf of Alaska, on the adjacent Continental Shelf, and probably on the continental slope. This uplift attained a measured maximum on land of 38 feet in a northwest-trending narrow belt less than 10 miles wide that is exposed on Montague Island in southwestern Prince William Sound. Two earthquake faults exposed on Montague Island are subsidiary northwest-dipping reverse faults along which the northwest blocks were relatively displaced a maximum of 26 feet, and both blocks were upthrown relative to sea level. From Montague Island, the faults and related belt of maximum uplift may extend southwestward on the Continental Shelf to the vicinity of the Kodiak group of islands. To the north and northwest of the zone of uplift, subsidence forms a broad asymmetrical downwarp centered over the Kodiak-Kenai-Chugach Mountains that averages 2½ feet and attains a measured maximum of 7½ feet along the southwest coast of the Kenai Peninsula. Maximum indicated uplift in the Alaska and Aleutian Ranges to the north of the zone of subsidence was l½ feet. Retriangulation over roughly 25,000 square miles of the deformed region in and around Prince William Sound shows that vertical movements there were accompanied by horizontal distortion, involving systematic shifts of about 64 feet in a relative seaward direction. Comparable horizontal movements are presumed to have affected those parts of the major zones of uplift and subsidence for which retriangulation data are unavailable.\n\nRegional vertical deformation generated a train of destructive long-period seismic sea waves in the Gulf of Alaska as well as unique atmospheric and ionospheric disturbances that were recorded at points far distant from Alaska. Warping resulted in permanent tilt of larger lake basins and temporary reductions in discharge of some major rivers. Uplift and subsidence relative to sea level caused profound modifications in shoreline morphology with attendant catastrophic effects on the nearshore biota and costly damage to coasta1 installations. Systematic horizontal movements of the land relative to bodies of confined or semiconfined water may have caused unexplained short-period waves—some of which were highly destructive—observed during or immediately after the earthquake at certain coastal localities and in Kenai Lake. Porosity increases, probably related to horizontal displacements in the zone of subsidence, were reflected in lowered well-water levels and in losses of surface water.\n\nThe primary fault, or zone of faults, along which the earthquake occurred is not exposed at the surface on land. Focal-mechanism studies, when considered in conjunction with the pattern of deformation and seismicity, suggest that it was a complex thrust fault (megathrust) dipping at a gentle angle beneath the continental margin from the vicinity of the Aleutian Trench. Movement on the megathrust was accompanied by subsidiary reverse faulting, and perhaps wrench faulting, within the upper plate. Aftershock distribution suggests movement on a segment of the megathrust, some 550–600 miles long and 110–180 miles wide, that underlies most of the major zone of uplift and the seaward part of the major zone of subsidence.\n\nAccording to the postulated model, the observed and inferred tectonic displacements that accompanied the earthquake resulted primarily from (1) relative seaward displacement and uplift of the seaward part of the block by movement along the dipping megathrust and subsidiary faults that break through the upper plate to the surface, and (2) simultaneous elastic horizontal extension and vertical attenuation (subsidence) of the crustal slab behind the upper plate. Slight uplift inland from the major zones of deformation presumably was related to elastic strain changes resulting from the overthrusting; however, the data are insufficient to permit conclusions regarding its cause.\n\nThe belt of seismic activity and major zones of tectonic deformation associated with the 1964 earthquake, to a large extent, lie between and parallel to the Aleutian Volcanic Arc and the Aleutian Trench, and are probably genetically related to the arc. Geologic data indicate that the earthquake-related tectonic movements were but the most recent pulse in an episode of deformation that probably began in late Pleistocene time and has continued intermittently to the present. Evidence for progressive coastal submergence in the deformed region for several centuries preceding the earthquake, in combin1ation with transverse horizontal shortening indicated by the retriangulation data, suggests pre-earthquake strain directed at a gentle angle downward beneath the arc. The duration of strain accumulation in the epicentral region, as interpreted from the time interval during which the coastal submergence occurred, probably is 930–1,360 years.","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"The Alaska earthquake, March 27, 1964: Regional effects (Professional Paper 543)","largerWorkSubtype":{"id":5,"text":"USGS Numbered Series"},"language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp543I","usgsCitation":"Plafker, G., 1969, Tectonics of the March 27, 1964, Alaska earthquake: U.S. Geological Survey Professional Paper 543, Report: viii, 74 p.; 2 Plates: 27.08 x 21.87 inches and 16.09 x 20.66 inches, https://doi.org/10.3133/pp543I.","productDescription":"Report: viii, 74 p.; 2 Plates: 27.08 x 21.87 inches and 16.09 x 20.66 inches","numberOfPages":"88","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":402614,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4593.htm","linkFileType":{"id":5,"text":"html"}},{"id":277849,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0543i/index.html"},{"id":65741,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0543i/pp543i_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":264156,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0543i/pp543i_plate2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":264155,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0543i/pp543i_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":122539,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0543i/report-thumb.jpg"}],"country":"United States","state":"Alaska","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -141.2,51.8 ], [ -141.2,64.0 ], [ -174.1,64.0 ], [ -174.1,51.8 ], [ -141.2,51.8 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adae4b07f02db6858cd","contributors":{"authors":[{"text":"Plafker, George","contributorId":3920,"corporation":false,"usgs":false,"family":"Plafker","given":"George","email":"","affiliations":[],"preferred":false,"id":220493,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2202,"text":"wsp1868 - 1969 - Sediment transport by streams in the Walla Walla River basin, Washington and Oregon, July 1962 - June 1965","interactions":[],"lastModifiedDate":"2021-12-06T21:19:26.174161","indexId":"wsp1868","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1868","title":"Sediment transport by streams in the Walla Walla River basin, Washington and Oregon, July 1962 - June 1965","docAbstract":"The Walla Walla River basin covers about 1,760 square miles in southeastern Washington and northeastern Oregon. From the 6,000-foot crest of the Blue Mountains on the east to the 340-foot altitude of Lake Wallula (Columbia River) on the west, the basin is drained by the Touchet River and Dry Creek, entirely within Washington, and by Mill Creek, North and South Forks Walla Walla River, and Pine Creek-Dry Creek, which all head in Oregon. The central lowland of the basin is bordered on the north by Eureka Flat, Touchet slope, and Skyrocket Hills, on the east by the Blue Mountains, and on the south by the Horse Heaven Hills. \r\n\r\nThe basin is underlain by basalt of the Columbia River Group, which .is the only consolidated rock to crop out in the region. Various unconsolidated fluviatile, lacustrine, and eolian sediments cover the basalt. In the western part of the basin the basalt is overlain by lacustrine deposits of silt and sand which in places are mantled by varying thicknesses of loessal deposits. In the northern and central parts of the basin the loess is at least 100 feet thick. The mountainous eastern part of the basin is underlain at shallow depth by basalt which has a residual soil mantle weathered from the rock. The slopes of the mountains are characterized by alluvial fans and deeply cut stream valleys ,filled with alluvium of sand, gravel, and cobbles. \r\n\r\nAverage annual precipitation in the basin ranges from less than 10 inches in the desert-like areas of the west to more than 45 inches in the timbered mountains of the east; 65 percent of the precipitation occurs from October through March. The average runoff from the basin is about 4.8 inches per year. Most of the runoff occurs during late winter and early spring. Exceptionally high runoff generally results from rainfall and rapid melting of snow on partially frozen ground. \r\n\r\nDuring the study period, July 1964-June 1965, average annual sediment yields in the basin ranged from 420 tons per square mile in the mountainous area to more than 4,000 tons per square mile in the extensively cultivated northern and central parts of the basin, which are drained by the Touchet River and Dry Creek. The Touchet River and Dry Creek transported approximately 80 percent of the total sediment load discharged from the Walla Walla River basin. The highest concentrations were contributed by the loessal deposits in the Dry Creek drainage. Two runoff events resulting from rain and snowmelt on partially frozen ground produced 76 percent of the suspended sediment discharged from the basin during the study period. The maximum concentration measured, 316,000 milligrams per liter, was recorded for Dry Creek at Lowden on December 23. 1964. \r\n\r\nDaily suspended-sediment concentrations for the Walla Walla River near Touchet exceeded 700 milligrams per liter about 10 percent of the time, and 14,000 milligrams per liter about 1 percent of the time. The discharge-weighted mean concentration for the 3-year period of study was 7,000 milligrams per liter. Silt predominates in the suspended sediment transported by all streams in the basin. On the average, sediment from streams draining the Blue Mountains was composed of 20 percent sand, 60 percent silt, and 20 percent clay ; for streams draining the Blue Mountains slope-Horse Heaven Hills area, the percentages are 9, 65, and 26, respectively ; and for those draining the Skyrocket Hills-Touchet slope, the percentages are 5, 75, and 20, respectively. \r\n\r\nThe bedload in the mountain and upland streams was estimated to be about 5-12 percent as much as the suspended load. For the Walla Walla River and its tributaries in the lower basin area, the bedload was estimated to be only about 2-8 percent as much as the suspended load.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wsp1868","usgsCitation":"Mapes, B.E., 1969, Sediment transport by streams in the Walla Walla River basin, Washington and Oregon, July 1962 - June 1965: U.S. Geological Survey Water Supply Paper 1868, Report: iv, 32 p.; 1 Plate: 19.00 × 16.92 inches, https://doi.org/10.3133/wsp1868.","productDescription":"Report: iv, 32 p.; 1 Plate: 19.00 × 16.92 inches","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":392519,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_25089.htm"},{"id":27864,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1868/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":27863,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1868/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":138140,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1868/report-thumb.jpg"}],"country":"United States","state":"Oregon, Washington","otherGeospatial":"Walla Walla River basin","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.75,\n 45.775\n ],\n [\n -118.912,\n 45.775\n ],\n [\n -118.912,\n 46.479\n ],\n [\n -117.75,\n 46.479\n ],\n [\n -117.75,\n 45.775\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e0e4b07f02db5e3fe5","contributors":{"authors":[{"text":"Mapes, B. E.","contributorId":26286,"corporation":false,"usgs":true,"family":"Mapes","given":"B.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":144818,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":53421,"text":"ofr69328 - 1969 - Geology, hydrology, and water quality in the Fresno area, California","interactions":[],"lastModifiedDate":"2024-08-01T13:34:45.292576","indexId":"ofr69328","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"69-328","title":"Geology, hydrology, and water quality in the Fresno area, California","docAbstract":"The Fresno area comprises about 1.400 square miles lying west of the foothills of the Sierra Nevada and east of the trough of the San Joaquin Valley. The rainfall averages less than 10 inches per year causing agricultural development to depend mainly on surface-water deliveries and ground-water pumpage. Surface-water deliveries and ground-water pumpage, however, vary considerably from year to year. For example, in agricultural year 1958 (April 1, 1958-March 31, 1959) surface-water deliveries were about 1,340,000 acre-feet and agricultural ground-water pumpage was about 1,740,000 acre-feet, but in agricultural year 1960 deliveries were only about 560,000 acre-feet and pumpage was about 2,520,000 acre-feet.
Alluvial fans are the dominant geomorphic features in the area. Small alluvial fans have been formed near the foothills by the deposits from the numerous intermittent streams that lie both north and south of the Kings River. Thicker and much more extensive alluvial fans have been formed under most of the area by deposits from the San Joaquin and Kings Rivers.
Geologic units in the area consist of consolidated rocks and unconsolidated deposits. In turn, consolidated rocks consist of basement complex of pre-Tertiary age and marine and continental sedimentary rocks of Cretaceous and Tertiary age. Unconsolidated deposits are of both Tertiary and Quaternary age. Most of the geologic units dip gently southwestward approximately paralleling the back slope of the Sierra Nevada. Although some of these geologic units are faulted, especially in the deep subsurface, faulting has not affected the occurrence and movement of fresh ground water.
The basement complex crops out along the eastern border of the area and yields only small amounts of water to wells; the marine and continental sedimentary rocks do not crop out in the area and do not yield any water to wells.
The unconsolidated deposits are divided into an older series of Tertiary and Quaternary age, and a younger series of Quaternary age. The continental deposits of Tertiary and Quaternary age crop out beneath the extreme southeastern part of the area and yield small amounts of water to wells, and the deposits of Quaternary age crop out over most of the area and yield more than 90 percent of the water pumped from wells.
The deposits of Quaternary age in turn are divided into older alluvium, lacustrine and marsh deposits, younger alluvium, flood-basin deposits. and sand dunes.
The older alluvium is by far the most important aquifer in the Fresno area. It consists of intercalated lenses of clay, silt, silty and sandy clay, clayey and silty sand, sand, gravel, cobbles, and boulders, and in general it is fine grained near the trough of the valley and beneath the alluvial fans of intermittent streams.
In the older alluvium, yields to wells range from less than 20 gpm (gallons per minute) to more than 3,000 gpm.
The lacustrine and marsh deposits occur only in the subsurface in the western part of the area. Consisting mostly of silt and clay, they are virtually impermeable and thus restrict the vertical movement of water. These deposits from oldest to youngest are designated the E-clay, the C-clay, and the A-clay. The E-clay is the thickest and most extensive of all the lacustrine and marsh deposits.
Because the clays tend to confine ground water in the Fresno area, five water bodies are recognized. These are the unconfined water body, the shallow water body, the confined water body below the A-clay, the confined water body below the C-clay, and the confined water body below the E-clay. The unconfined water body underlies most of the Fresno area. The shallow and confined water bodies underlie parts of the extreme western part of the area. There, heads in successively underlying water bodies are less than those in overlying water bodies, indicating that some ground water moves slowly downward through the clays.
From agricultural years 1957 to 1962, outflow in the area exceeded inflow. As a result, for this period, the Fresno area had a net deficit of about 2,890,000 acre-feet. This deficit was made up for mostly by a decline in ground water stored.
Water levels in all water bodies have been declining over the years, yet when streamflow and canal deliveries are large they show a general rise.
The general movement of ground water in the Fresno area is toward the southwest, although pumping depressions near Fresno and near the western part of the area, cause ground water to move northward, southward, and westward toward them.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr69328","collaboration":"Prepared in cooperation with the California Department of Water Resources","usgsCitation":"Page, R.W., and LeBlanc, R., 1969, Geology, hydrology, and water quality in the Fresno area, California: U.S. Geological Survey Open-File Report 69-328, Report: vii, 70 p.; 21 Plates; 35.12 x 22.4 inches or smaller, https://doi.org/10.3133/ofr69328.","productDescription":"Report: vii, 70 p.; 21 Plates; 35.12 x 22.4 inches or smaller","costCenters":[],"links":[{"id":432023,"rank":24,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_53766.htm","linkFileType":{"id":5,"text":"html"}},{"id":100353,"rank":22,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-20.pdf","text":"Plate 20","linkFileType":{"id":1,"text":"pdf"}},{"id":100352,"rank":21,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-19.pdf","text":"Plate 19","linkFileType":{"id":1,"text":"pdf"}},{"id":100351,"rank":20,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-18.pdf","text":"Plate 18","linkFileType":{"id":1,"text":"pdf"}},{"id":100350,"rank":19,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-17.pdf","text":"Plate 17","linkFileType":{"id":1,"text":"pdf"}},{"id":100349,"rank":18,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-16.pdf","text":"Plate 16","linkFileType":{"id":1,"text":"pdf"}},{"id":100348,"rank":17,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-15.pdf","text":"Plate 15","linkFileType":{"id":1,"text":"pdf"}},{"id":100347,"rank":16,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-14.pdf","text":"Plate 14","linkFileType":{"id":1,"text":"pdf"}},{"id":100342,"rank":11,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-09.pdf","text":"Plate 9","linkFileType":{"id":1,"text":"pdf"}},{"id":100341,"rank":10,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-08.pdf","text":"Plate 8","linkFileType":{"id":1,"text":"pdf"}},{"id":100336,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-03.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"}},{"id":100335,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-02.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"}},{"id":100334,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-01.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"}},{"id":87390,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0328/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":181213,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0328/report-thumb.jpg"},{"id":100354,"rank":23,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-21.pdf","text":"Plate 21","linkFileType":{"id":1,"text":"pdf"}},{"id":100337,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-04.pdf","text":"Plate 4","linkFileType":{"id":1,"text":"pdf"}},{"id":100338,"rank":7,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-05.pdf","text":"Plate 5","linkFileType":{"id":1,"text":"pdf"}},{"id":100339,"rank":8,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-06.pdf","text":"Plate 6","linkFileType":{"id":1,"text":"pdf"}},{"id":100340,"rank":9,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-07.pdf","text":"Plate 7","linkFileType":{"id":1,"text":"pdf"}},{"id":100343,"rank":12,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-10.pdf","text":"Plate 10","linkFileType":{"id":1,"text":"pdf"}},{"id":100344,"rank":13,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-11.pdf","text":"Plate 11","linkFileType":{"id":1,"text":"pdf"}},{"id":100345,"rank":14,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-12.pdf","text":"Plate 12","linkFileType":{"id":1,"text":"pdf"}},{"id":100346,"rank":15,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0328/plate-13.pdf","text":"Plate 13","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"California","city":"Fresno","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -120.02988891671723,\n 36.89960479988267\n ],\n [\n -120.02988891671723,\n 36.64450581438264\n ],\n [\n -119.54120698550426,\n 36.64450581438264\n ],\n [\n -119.54120698550426,\n 36.89960479988267\n ],\n [\n -120.02988891671723,\n 36.89960479988267\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c682","contributors":{"authors":[{"text":"Page, Roland Westland","contributorId":51378,"corporation":false,"usgs":true,"family":"Page","given":"Roland","email":"","middleInitial":"Westland","affiliations":[],"preferred":false,"id":247558,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"LeBlanc, R.A.","contributorId":69223,"corporation":false,"usgs":true,"family":"LeBlanc","given":"R.A.","email":"","affiliations":[],"preferred":false,"id":247559,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":16403,"text":"ofr69309 - 1969 - An analysis of gravity data in Area 12, Nevada Test Site","interactions":[],"lastModifiedDate":"2025-07-28T20:08:52.024588","indexId":"ofr69309","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"69-309","title":"An analysis of gravity data in Area 12, Nevada Test Site","docAbstract":"The gravity data available from Healey and Miller (1963a) were augmented by new observations along three profiles through two new drill holes in Area 12; UEI2t #1 and UEI2p #1. The data were interpreted to allow evaluation of the geologic structure prior to the planning and excavation of two proposed tunnel complexes, Ul2t and Ul2p.\r\n\r\nDensity values for each of six rock units were determined to allow a two-dimensional analysis of the gravity data along the above-mentioned profiles. The surficial rocks of Quaternary and Tertiary age and the Tertiary volcanic rocks have a weighted average density of 1.86 gm/cc. The density of the caprock at Rainier and Aqueduct Mesas ranges from 2.17 gm/cc at UEI2p #1 to 2.27 gm/cc at UEI2t #1. The Gold Meadows stock and the associated Precambrian quartzite have an arithmetic average density of 2.60 gm/cc for all samples measured. The middle Paleozoic dolomite in Area 12 has an arithmetic average density of 2.75 gm/cc. The clastic rocks of Paleozoic age have an arithmetic average density of 2.60 gm/cc. \r\n\r\nInterpretation of the residual gravity data indicates a maximum thickness of about 2,800 feet for all Tertiary volcanic rocks. A normal fault striking N. 30 ? E. disrupts the pre-Cenozoic surface at UEI2p #1 and 0.4 mile east of UEI2t #1. The throw within rock of Paleozoic age is about 400-500 feet. Another normal fault that strikes about N. 20 ? E. is located about 1.5 miles east of UEI2p #1. The throw of this fault is at least 1,100 feet in rocks of pre-Cenozoic age.\r\n\r\nElevation contours representing the pre-Cenozoic surface in Area 12 show a maximum relief of about 2,000 feet.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr69309","usgsCitation":"Wahl, R.R., 1969, An analysis of gravity data in Area 12, Nevada Test Site: U.S. Geological Survey Open-File Report 69-309, Report: iii, 23 p.; 3 Plates: 42.76 x 29.41 inches or smaller, https://doi.org/10.3133/ofr69309.","productDescription":"Report: iii, 23 p.; 3 Plates: 42.76 x 29.41 inches or smaller","costCenters":[],"links":[{"id":493049,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_8426.htm","linkFileType":{"id":5,"text":"html"}},{"id":45377,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1969/0309/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":45376,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0309/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":45375,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0309/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":45374,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1969/0309/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":147470,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1969/0309/report-thumb.jpg"}],"country":"United States","state":"Nevada","otherGeospatial":"Area 12, Nevada Test Site","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -116.25,\n 37.265\n ],\n [\n -116.25,\n 37.164\n ],\n [\n -116.083,\n 37.164\n ],\n [\n -116.083,\n 37.265\n ],\n [\n -116.25,\n 37.265\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4adbe4b07f02db685a2a","contributors":{"authors":[{"text":"Wahl, R. R.","contributorId":27462,"corporation":false,"usgs":true,"family":"Wahl","given":"R.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":172787,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}