Five nodules of eclogite, one nodule of garnet peridotite and one sample of kimberlite from the Roberts Victor mine were analyzed for concentrations of U, Th, Pb, Rb and Sr and isotopic compositions of Pb and Sr. In the eclogites, U content ranges from 0.09 to 0.26 ppm, Th from 0.35 to 1.1 ppm, Pb from 0.79 to 5.5 ppm, Rb from 2.1 to 28 ppm and Sr from 133 to 346 ppm;206Pb/204Pb ratios range from 14.8 to 18.5,207Pb/204Pb from 14.9 to 15.7,208Pb/204Pb from 35.2 to 38.5. The garnet peridotite contains 0.22 ppm U, 0.97 ppm Th, 1.05 ppm Pb, 6.9 ppm Rb and 108 ppm Sr and the kimberlite contains 2.5 ppm U, 30 ppm Th, 37 ppm Pb, 113 ppm Rb and 2040 ppm Sr. The lead in the eclogites has two components, a lead pyroextractable at 1100–1200° and a non-pyroextractable residual lead. In three of the eclogites, which are to some extent altered, a proportion of the pyroextractable lead may be contaminating lead from the kimberlite, but an altered kyanite eclogite does not appear to be contaminated by this same kimberlite. The pyroextractable lead from a less altered eclogite contains a much larger proportion of206Pb. Compositions calculated for the residual leads vary greatly. In many of the pyroextraction runs the primary eclogitic phases disappeared and the new phases plagioclase, clinopyroxene and a magnetic iron compound were formed. Why part of the lead should have been retained by these new phases is not understood.
Quartz crystals from calcite veins of unknown age in Precambrian metasedimentary rocks at Geiaus No. 6 and Aukam farms in South-West Africa contain both primary and secondary inclusions filled with one or a variable combination of: organic liquid, moderately saline aqueous liquid, dark-colored solid, and vapor. Analysis of these materials by microscopy and by gas chromatography and mass spectrometry shows the presence of constituents of both low and high molecular weights. The former include CH4, C2H6, C3H8 and possibly C4H10 as well as CO, CO2, H2O, N2 and H2. High molecular weight components are dominantly n-alkanes and isoprenoid hydrocarbons. The n-alkanes range from at least n-C10 to n-C33. Concentrations of n-alkanes larger than n-C17 decrease regularly with increasing carbon number. An homologous series of isoprenoid hydrocarbons ranging from at least C14 to C20 is present in unusually high concentrations. Pristane (C19) is most abundant, and C17 isoprenoid is least abundant. The molecular composition and distribution of hydrocarbons suggest biological precursors for these components.
Consideration of data provided by freezing, crushing and heating experiments suggests that the pressures at the time these in part supercritical fluids were trapped probably exceeded 30–40 atm, and the minimum trapping temperature was about 120–160°C. Both primary and secondary inclusions apparently containing only organic materials were trapped by the growth of the host quartz from aqueous solution. The data obtained neither prove nor preclude Precambrian, Paleozoic or younger sources for the organic materials.
Acidic industrial wastes have been injected into deep wells in a limestone aquifer near Pensacola, Florida, since 1963. Prior geohydrologic studies in the area had indicated that the limestone aquifer contained nonpotable water and was overlain by an extensive clay confining layer.
Two injection wells are presently being used to inject the waste at a rate of approximately 2,000 gallons per minute. The injection pressures are about 200 pounds per square inch. Over 3 billion gallons have been injected. Data from a current study indicate that the waste may extend outward about 1 mile from the injection wells, and pressure effects may extend outward more than 25 miles. Monitor wells show that pressure changes are following a predictable pattern. No wastes have been detected in a monitor well open to the Floridan aquifer immediately above the Bucatunna Clay Member of the Byram Formation and 100 feet from one of the injection wells.
A monitor well open to the receiving formation was constructed about 1,300 feet south of the injection wells. Geochemical effects of the wastes were detected at this well about 10 months after injection began. In early 1968, the pH of the waste was lowered to about 3. Effects of this waste, which included a large increase in calcium, were detected at the monitor well about 5 months later.
","language":"English","publisher":"Wiley","doi":"10.1111/j.1745-6584.1971.tb03526.x","usgsCitation":"Goolsby, D.A., 1971, Hydrogeochemical effects of injecting wastes into a limestone aquifer near Pensacola, Florida: Groundwater, v. 9, no. 1, p. 13-19, https://doi.org/10.1111/j.1745-6584.1971.tb03526.x.","productDescription":"7 p. ","startPage":"13","endPage":"19","costCenters":[{"id":589,"text":"Toxic Substances Hydrology Program","active":true,"usgs":true}],"links":[{"id":338340,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Florida","city":"Pensacola ","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -87.2314453125,\n 30.334953881988564\n ],\n [\n -86.98974609375,\n 30.334953881988564\n ],\n [\n -86.98974609375,\n 30.619004797647808\n ],\n [\n -87.2314453125,\n 30.619004797647808\n ],\n [\n -87.2314453125,\n 30.334953881988564\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"9","issue":"1","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","scienceBaseUri":"58d63043e4b05ec799131137","contributors":{"authors":[{"text":"Goolsby, Donald A.","contributorId":46083,"corporation":false,"usgs":true,"family":"Goolsby","given":"Donald","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":686180,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010334,"text":"70010334 - 1971 - Genetic implications of the shapes of martian and lunar craters","interactions":[],"lastModifiedDate":"2020-12-19T00:05:51.268039","indexId":"70010334","displayToPublicDate":"1971-01-01T00:00:00","publicationYear":"1971","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1963,"text":"Icarus","active":true,"publicationSubtype":{"id":10}},"title":"Genetic implications of the shapes of martian and lunar craters","docAbstract":"Craters on Mars and the Moon are alike in that larger craters differ in shape from smaller ones, and older craters differ in shape from younger ones. Smoothed depth-diameter curves for 41 large martian craters photographed by Mariner IV inflect at a crater diameter of 10–20km in a manner similar to curves for lunar craters. Below 10–20km, both depth-diameter curves are linear with a slope of roughly 1.0; above this threshold range, the curves assume a much lower slope. Diminution of lunar crater depth-diameter ratios with age indicates that the shapes of lunar and, by inference, martian craters have changed systematically since formation. Martian craters sampled here are shallower than most pre-Imbrian lunar craters. By analogy with the Moon, martian craters seem both to vary in initial shape according to the energy of the impact that formed them and to have been modified subsequently by endogenic and surface processes. A proposed model for the geologic development of large martian and lunar craters outlines a time- dependent sequence of events. Craters which have undergone rapid isostatic adjustment on the Moon have distinctive morphologies and occur preferentially along mare basin-upland margins.
Systematic geologic mapping of the near side of the Moon has provided the basis for defining and delineating the major geological provinces of the near side. From the nature of the provinces and their distribution patterns a general historical sequence evolves. Five main surface-shaping periods are recognized: (1) one of intense early impact cratering; (2) another, probably overlapping the first, during which the impact basins were formed; (3) a prolonged period of varied terra volcanism; (4) a short period of mare volcanism that resulted in filling of the multiring basins; and (5) a period of diminishing volcanic activity continuing up to the time of formation of the last ray craters.
New data show that the Olduvai normal geomagnetic polarity event is represented in Olduvai Gorge, Tanzania, by rocks covering a time span of roughly from 0.1 to 0.2 my and is no older than 2.0 my. Hence the long normal polarity event of this age that is seen in deep-sea sediment cores and in magnetic profiles over oceanic ridges should be called the Olduvai event. The lava from which the Gilsàevent was defined may have been erupted during the Olduvai event and, if so, the term Gilsàshould now be abandoned. Many dated lavas that were originally assigned to the Olduvai event represent one or two much shorter normal polarity events that preceded the Olduvai event; these are herein named the Réunion normal polarity events. This revision brings the geomagnetic reversal time scale into conformity with the one implied by assumptions of uniform sedimentation rates on the ocean floor and uniform rates of sea-floor spreading.
Ficken and Ficken (Auk, 85: 136, 1968) suggest that the \"Head-scratching method may prove a valuable addition to the set of complex characters that can be used in defining genera,\" and that field observers should continue to fill gaps in our knowledge of this behavior. In the course of a series of observations of Swainson's Warblers (Limnothlypis swainsonii) in the Dismal Swamp, Virginia, I saw head-scratching in three individuals, four times in one, three in another, and once in the third. All three birds used the direct method, bringing the foot forward and under the wing.
","language":"English","publisher":"American Ornithological Society","doi":"10.2307/4083673","usgsCitation":"Meanley, B., 1970, Head-scratching method of the Swainson's warbler: The Auk, v. 87, no. 1, p. 163-163, https://doi.org/10.2307/4083673.","productDescription":"1 p.","startPage":"163","endPage":"163","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":194089,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"87","issue":"1","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a6be4b07f02db63d347","contributors":{"authors":[{"text":"Meanley, Brooke","contributorId":79938,"corporation":false,"usgs":true,"family":"Meanley","given":"Brooke","email":"","affiliations":[],"preferred":false,"id":331771,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":5220531,"text":"5220531 - 1970 - Passive immunization of pigeons against trichomoniasis","interactions":[],"lastModifiedDate":"2025-05-09T15:45:50.520244","indexId":"5220531","displayToPublicDate":"2010-06-16T12:18:01","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2434,"text":"Journal of Protozoology","active":true,"publicationSubtype":{"id":10}},"title":"Passive immunization of pigeons against trichomoniasis","docAbstract":"Nonimmune homing pigeons Columba livia were infected with the Jones' Barn strain of Trichomonas gallinae and subsequently transfused with plasma from acute or chronically infected pigeons harboring one of 3 different strains of T. gallinae. The transfusions were either a single 2 ml dose given one day after inoculation or three 1 ml doses given 0, 5, and 10 days after inoculation. Plasma from pigeons harboring any of the 3 strains was capable of passively immunizing nonimmune birds. All birds which were immunized with plasma from infected pigeons survived until killed at the end of the test period and no visceral lesions were found on necropsy but trichomonads were present in the oropharynx. All controls (untreated or transfused with normal plasma) died of visceral trichomoniasis.
Immune plasma produced some lysis of trichomonads in vitro, and inhibition of motility and vacuolization occurred in some of the non-lysed organisms. The overall lytic activity in vitro affected less than 10% of the suspended trichomonads.
","language":"English","publisher":"Wiley","doi":"10.1111/j.1550-7408.1970.tb04726.x","usgsCitation":"Kocan, R.M., 1970, Passive immunization of pigeons against trichomoniasis: Journal of Protozoology, v. 17, no. 4, p. 551-553, https://doi.org/10.1111/j.1550-7408.1970.tb04726.x.","productDescription":"3 p.","startPage":"551","endPage":"553","numberOfPages":"3","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":197980,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"17","issue":"4","noUsgsAuthors":false,"publicationDate":"2007-04-30","publicationStatus":"PW","scienceBaseUri":"4f4e4ae2e4b07f02db688c33","contributors":{"authors":[{"text":"Kocan, R. M.","contributorId":41783,"corporation":false,"usgs":true,"family":"Kocan","given":"R.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":331966,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":5221251,"text":"5221251 - 1970 - Toxicity of DDT to Japanese quail as influenced by body weight, breeding condition, and sex","interactions":[],"lastModifiedDate":"2026-03-12T14:47:37.711735","indexId":"5221251","displayToPublicDate":"2010-06-16T12:18:01","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3612,"text":"Toxicology and Applied Pharmacology","active":true,"publicationSubtype":{"id":10}},"title":"Toxicity of DDT to Japanese quail as influenced by body weight, breeding condition, and sex","docAbstract":"Controlled experiments were utilized to simulate the stresses on wild birds of breeding condition and of weight loss due to migration. Light conditions in the laboratory were manipulated to produce Japanese quail (Coturnix coturnix japonica) in breeding condition and not in breeding condition. Within each of these groups, some birds were partially starved before dosage and some were fully fed. Birds were then fed dietary levels of 0, 700, 922, 1214, or 1600 ppm dry weight of p,p′-DDT for a period of 20 days or until death.
Birds partially starved before dosage were more susceptible to DDT intoxication than nonstarved ones, and birds not in breeding condition were slightly more so than birds in breeding condition. Similarly, males died earlier than females, and the birds of the lighter weight strain used in the second half of the study died earlier than the birds of the heavier strain used in the first half. The heavier birds of each sex not only survived longer than lighter individuals receiving the same treatments, but they also lost a greater proportion of their weight before death.
During the early portion of the dosage period, females in breeding condition were less sensitive to DDT than were females not in breeding condition and males. After 10 days on dosage, however, the cumulative mortality of females in breeding condition rapidly approached that of males and of females not in breeding condition. Food restriction prior to dosage, strains of quail, breeding conditions, and sexes resulted in weight differences and a corresponding accentuation or delay of the effects of the different levels of DDT.
","language":"English","publisher":"Elsevier","doi":"10.1016/0041-008X(70)90049-9","usgsCitation":"Gish, C., and Chura, N., 1970, Toxicity of DDT to Japanese quail as influenced by body weight, breeding condition, and sex: Toxicology and Applied Pharmacology, v. 17, no. 3, p. 740-751, https://doi.org/10.1016/0041-008X(70)90049-9.","productDescription":"12 p.","startPage":"740","endPage":"751","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":194117,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"17","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e499ee4b07f02db5bcc2d","contributors":{"authors":[{"text":"Gish, C.D.","contributorId":21651,"corporation":false,"usgs":true,"family":"Gish","given":"C.D.","email":"","affiliations":[],"preferred":false,"id":333407,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Chura, N.J.","contributorId":8571,"corporation":false,"usgs":true,"family":"Chura","given":"N.J.","email":"","affiliations":[],"preferred":false,"id":333406,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010274,"text":"70010274 - 1970 - Rapid changes in the head of the Rio Balsas Submarine Canyon system, Mexico","interactions":[],"lastModifiedDate":"2025-04-16T15:18:10.725351","indexId":"70010274","displayToPublicDate":"2003-04-02T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2667,"text":"Marine Geology","active":true,"publicationSubtype":{"id":10}},"title":"Rapid changes in the head of the Rio Balsas Submarine Canyon system, Mexico","docAbstract":"The investigation of a river delta and the heads of several nearby submarine canyons in western Mexico produced evidence for rapid changes in the configuration and depth of the nearshore portions of canyon tributaries. General scarcity of data on the rates of submarine canyon formation and the relationship to river discharge should make these results of special interest.
The Rio Balsas, one of Mexico's largest rivers, empties into the ocean near the heads of a large submarine canyon that terminates in the Middle America Trench. One of the distributaries of the Rio Balsas presently is discharging at the head of Cañón de la Necesidad, which is being eroded actively. Two inactive canyons are related to former discharge channels of the river. Their heads lie at some distance from shore and are being filled with sediment. The Cañón de Petacalco, not now receiving sediment directly from a Rio Balsas distributary, has remained active because the shoreline has not retreated far. Until about 100 years ago its head was being filled with fine-grained and highly organic sediments from a nearby rivermouth, while the coarse portion of the sediment supply joined the canyon via a tributary farther seaward. Since then the river has shifted away from this canyon, and the horizontally stratified sediments in the canyon head have been incised as much as 20–30 m, as evidenced by three 14C dates of organic material exposed in the steep to overhanging canyon walls.
The changes in the shallow portion of the Rio Balsas submarine canyons seem to be related to changes in river discharge pattern, either directly or indirectly. A shifting point source of sediment supply either activates a pre-existing, partly filled canyon, or erodes a new one near the new river mouth, whereas the canyon at the abandoned river mouth is deactivated following retreat of the shoreline.
The heads of the different tributaries form a dendritic pattern in Holocene unconsolidated sediment. Subaerial processes are not involved in the formation of these submarine canyons. Thus, a dendritic pattern of submarine canyons is not necessarily indicative of subaerial erosion.
Three exceptionally large and long submarine canyons — Bering, Pribilof, and Zhemchug — incise the continental slope underlying the southeastern Bering Sea. Bering Canyon, the world's longest known slope valley, is approximately 400 km long and has a volume of 4,300 km3. The volume of Pribilof Canyon is 1,300 km3 and that of Zhemchug is 8,500 km3; Zhemchug Canyon may well be the world's largest slope valley; most other large submarine canyons have volumes less than 500 km3. Pribilof and Zhemchug canyons are further distinguished by the headward bifurcation of their slope axes to form elongated trough-shaped basins behind the regionally projected position of the shelf edge. These troughs are superimposed over structural depressions formed by down-faulted basement rocks of Mesozoic and older ages. Prior to canyon cutting these depressions were filled with as much as 2,600 m of shallow-water diatomaceous, tuffaceous, and detrital sediments largely of Tertiary age. Deposition of these sediments took place concurrently with general margin subsidence of at least 2,000 m.
The data and conclusions presented in this paper stress that the location, trend, and shape of the enormous submarine canyons cutting the Bering margin are structurally determined. However, axial cutting and headward erosion within the relatively unconsolidated Tertiary strata and the older, lithified basement rock is thought to have been caused by basinward-sliding masses of sediment; these unstable sediment bodies accumulated on the upper continental slope and outer shelf, probably near the mouths of major Alaskan rivers.
Bering Canyon was periodically cut and filled by axial sedimentation during Late Tertiary and Quaternary time. Pribilof and Zhemchug canyons, however, are thought to have been excavated entirely during the Pleistocene. It is presumed that, during one or more periods of glacially lowered sea level, the Kuskokwim and Yukon rivers emptied into or near the heads of Pribilof and Zhemchug canyons. The enormous size and unusual shape of Zhemchug Canyon resulted from the breaching of the seaward wall of an outer-shelf basement depression and the subsequent removal of nearly 4,500 km3 of Tertiary deposits filling it.
","language":"English","publisher":"Elsevier","doi":"10.1016/0025-3227(70)90043-5","issn":"00253227","usgsCitation":"Scholl, D., Buffington, E.C., Hopkins, D., and Alpha, T.R., 1970, The structure and origin of the large submarine canyons of the Bering Sea: Marine Geology, v. 8, no. 3-4, p. 187-210, https://doi.org/10.1016/0025-3227(70)90043-5.","productDescription":"24 p.","startPage":"187","endPage":"210","costCenters":[],"links":[{"id":219758,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Bering Sea","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -168.48632812499997,\n 54.77534585936447\n ],\n [\n -154.16015625,\n 54.77534585936447\n ],\n [\n -154.16015625,\n 60.19615576604439\n ],\n [\n -168.48632812499997,\n 60.19615576604439\n ],\n [\n -168.48632812499997,\n 54.77534585936447\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"8","issue":"3-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb096e4b08c986b324f56","contributors":{"authors":[{"text":"Scholl, D.W.","contributorId":106461,"corporation":false,"usgs":true,"family":"Scholl","given":"D.W.","email":"","affiliations":[],"preferred":false,"id":358927,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Buffington, E. C.","contributorId":13948,"corporation":false,"usgs":true,"family":"Buffington","given":"E.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":358924,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hopkins, D.M.","contributorId":103646,"corporation":false,"usgs":true,"family":"Hopkins","given":"D.M.","email":"","affiliations":[],"preferred":false,"id":358926,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Alpha, T. R.","contributorId":20715,"corporation":false,"usgs":true,"family":"Alpha","given":"T.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":358925,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":2512,"text":"wsp1888 - 1970 - Hydrology of the Upper Malad River basin, southeastern Idaho","interactions":[],"lastModifiedDate":"2013-11-21T13:44:23","indexId":"wsp1888","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1970","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":"1888","title":"Hydrology of the Upper Malad River basin, southeastern Idaho","docAbstract":"The report area comprises 485 square miles in the Basin and Range physiographic province. It includes most of eastern' Oneida County and parts of Franklin, Bannock, and Power Counties of southeastern Idaho. Relief is about 5,000 feet; the floor of the Malad Valley is at an average altitude of about 4,400 feet. Agriculture is, by far, ,the principal economic .activity. In 1960 the population of the upper Malad River basin was about 3,600, of which about 60 percent resided in Malad City, the county seat of Oneida County. \n\nThe climate is semiarid throughout the Malad Valley and its principal tributary valleys; ,above 6,500 feet the climate is subhumid. Annual precipitation ranges from about 13 inches in the lower Malad Valley to more than 30 inches on the highest peaks of the Bannock and Malad ranges. Owing to ,the normally clear atmospheric conditions, large daily and seasonal temperature fluctuations are common. Topography, distance from the Pacific Ocean, .and the general atmospheric circulation are the principal factors governing the climate of the Malad River basin. The westerlies transport moisture from the P.acific Ocean toward southeastern Idaho. The north-south tren4ing mountains flanking the basin are oriented orthogonally to the moisture flux so that they are very effective in removing precipitable water from the air. A minimum uplift of 6,000 feet is required to transport moisture from the Pacific source region; accordingly, most air masses are desiccated long before they reach the Malad basin. Heaviest precipitation is generally associated with steep pressure gradients in the midtroposphere that are so oriented as to cause a deep landward penetration of moisture from the Pacific Ocean.
\n\nAnnual water yields in the project area range from about 0.8 inch in the, lower Malad Valley to more than 19 inches on the high peaks north and east of Malad City. The mean annual water yield for the entire basin is 4 inches, or about 115,000 acre-feet. Evaporation is greatest in July when about 7 inches is lost from lakes, reservoirs, and waterlogged areas; losses from free-water surfaces may be as much .as 38 inches annually.
\n\nAn extensive ground-water reservoir consisting of sand and gravel interbedded with relatively impermeable beds of silt .and clay underlies much of the Malad Valley. Wells near the center of the valley exceeding 700 feet in depth do not reach bedrock. The Woodruff fault, which transects the constricted lower Malad Valley, is one of the main factors creating artesian conditions south of the latitude of Malad City. Recharge is obtained principally from mountain runoff which flows onto highly permeable alluvial fans surrounding the valley and from streams that flow across the valley floor. On the basis of a water balance analysis, under flow from the project area was estimated to be 28,000 acre-feet annually, surface-water outflow was 51,000 acre-feet, and transbasin imports were about 4,000 acre-feet.
\n\nThe principal tributaries of the Malad River are perennial along their upper and middle reaches and have well-sustained low flows. During the growing season, all surface water entering the Malad Valley is used for irrigation. Spine irrigation is practiced in the principal tributary valleys; however, a shortage of suitable reservoir sites has hampered surface-water development in these areas. The highly porous deposits underlying the Malad Valley tend to attenuate flood peaks. An unusual combination of meteorologic events early in 1962 effectively counteracted the high absorptive capacity of the valley and predisposed the basin to high flood risk. Subsequent rapid snowmelt combined with frozen ground produced the extraordinary flood of February 12, 1962.
\n\nCalcium and bicarbonate commonly are the most abundant ions in the surface waters of the upper Malad River basin. In August 1967, the dissolved-solids content of streamflow ranged from 200 to 350 milligrams per liter in the middle and upper parts of the basin; however, much greater values were measured in the Malad River between Woddruff and Cherry Creek Lane. With the exception of that reach, the surface water of the project area is suitable for irrigating all but the most sensitive crops.
\n\nThe total water yield is not sufficient to meet all the water needs of the basin. A comprehensive water-management plan is required to ensure optimal use of the water resource.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington D.C.","doi":"10.3133/wsp1888","usgsCitation":"Pluhowski, E.J., 1970, Hydrology of the Upper Malad River basin, southeastern Idaho: U.S. Geological Survey Water Supply Paper 1888, v, 89 p., https://doi.org/10.3133/wsp1888.","productDescription":"v, 89 p.","numberOfPages":"94","costCenters":[],"links":[{"id":138716,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1888/report-thumb.jpg"},{"id":28673,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1888/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho","otherGeospatial":"Upper Malad River Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -0.01638888888888889,0.0011111111111111111 ], [ -0.01638888888888889,0.0011111111111111111 ], [ -0.01638888888888889,0.0011111111111111111 ], [ -0.01638888888888889,0.0011111111111111111 ], [ -0.01638888888888889,0.0011111111111111111 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ee4b07f02db5fdb62","contributors":{"authors":[{"text":"Pluhowski, Edward J.","contributorId":87911,"corporation":false,"usgs":true,"family":"Pluhowski","given":"Edward","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":145318,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":23018,"text":"ofr70121 - 1970 - Geohydrology of the Cross-Florida Barge Canal area, with special reference to the Ocala vicinity","interactions":[],"lastModifiedDate":"2012-02-02T00:07:52","indexId":"ofr70121","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","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":"70-121","title":"Geohydrology of the Cross-Florida Barge Canal area, with special reference to the Ocala vicinity","docAbstract":"The Cross-Florida Barge Canal route commences at Palatka on the St. Johns River, about 75 miles upstream from the Atlantic Ocean, and extends 110 miles southwestward across Peninsular Florida into deep water in the Gulf of Mexico near Yankeetown. The canal will be equipped with five locks, each 600 feet long and 84 feet wide, and the channel will be a minimum of 12 feet deep and 150 feet wide. From near Ocala northeastward, the canal channel will replace much of the natural channel of the Oklawaha River, and will be excavated into beds of the so-called shallow sand aquifer of Miocene and younger age, which overlies limestone of the Floridan aquifer. Westward from Ocala most of the canal will be excavated below the potentiometric surface into limestone and dolomite of the Floridan aquifer. Water levels of Rodman, Eureka, and Inglis Pools will be controlled by dams and spillways with limited exchange of water between the pools and the aquifers. The water levels in the Summit Pool will fluctuate with the natural changes in the ground-water level of the Floridan aquifer, although the stage of the pool will be partially controlled by the stage held in the Eureka Pool. A dynamic inflow-outflow relationship will exist between the Sun, nit Pool and the Floridan aquifer. \r\n\r\nThe Floridan aquifer in the canal area is 1,000 to 1,200 feet thick and consists of limestone and dolomite of middle Eocene to Miocene age, including, from older to younger the Lake City, Avon Park and Ocala limestones plus permeable sandy, dolomitic limestone in the lower part of the Hawthorn Formation. It is possible that most of the flow to the two major springs in the area occurs in the upper 100 feet or so of the aquifer in the Ocala Limestone. The aquifer is underlain by the Oldsmar Limestone of early Eocene age and is overlain by sand, clayey sand, clay and shell beds of Miocene through Holocene age, ranging from a few feet to two or three hundred feet thick. The permeable beds overlying the Floridan aquifer constitute the shallow aquifer, while the poorly permeable ones act as confining beds where the Floridan aquifer is under artesian conditions. \r\n\r\nA north-south line drawn separating the head of Silver Springs on the west from the Oklawaha River on the east marks the approximate westward limit of a continuous blanket of Miocene-Pliocene(?) age materials covering the rocks of the Floridan aquifer. East of the line much of the aquifer is under artesian conditions, particularly in the Oklawaha River valley, although in some areas east of the valley direct recharge through thick permeable Miocene-Pliocene(?) sands occurs. West of the line, only scattered remnants of a once continuous Miocene-Pliocene(?) cover remains. Lack of the cover is a result of erosion on the crest and flanks of the Ocala Uplift, a broad northwest-southeast trending anticlinal upwarp, the axis of which is crossed by the canal route in the Dunnellon area. Over most of this area the Floridan aquifer is unconfined, and receives direct recharge through a cover of a few tens of feet of sand and clayey sand of Quaternary age. \r\n\r\nTensional stresses during the structural evolution of the Ocala Uplift produced an intersecting system of fractures and normal faults in rocks of the Florida Aquifer. The fractures and faults are important controls for orientation of solution channels, and, therefore, for development of ground-water circulation patterns. When the system of surface streams which once drained the Barge Canal area eroded the poorly permeable Miocene-Pliocene(?) cover from the flanks of the Ocala Uplift, surface runoff was reduced and precipitation began to directly infiltrate the underlying limestones. Now only principal rivers, such as the Oklawaha and Withlacoochee Rivers, and a few short tributaries remain, while one of the most highly developed subsurface drainage systems in the world has evolved in the cavernous limestones of the Floridan aquifer. Two of the larger fresh water spr","language":"ENGLISH","publisher":"U.S. Geological Survey, Water Resources Division,","doi":"10.3133/ofr70121","issn":"0094-9140","usgsCitation":"Faulkner, G.L., 1970, Geohydrology of the Cross-Florida Barge Canal area, with special reference to the Ocala vicinity: U.S. Geological Survey Open-File Report 70-121, xii, 229 p. :ill., maps ;28 cm., https://doi.org/10.3133/ofr70121.","productDescription":"xii, 229 p. :ill., maps ;28 cm.","costCenters":[],"links":[{"id":154732,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1970/0121/report-thumb.jpg"},{"id":52403,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1970/0121/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b1be4b07f02db6a89d8","contributors":{"authors":[{"text":"Faulkner, Glen L.","contributorId":58302,"corporation":false,"usgs":true,"family":"Faulkner","given":"Glen","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":189288,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2683,"text":"wsp1990 - 1970 - Annotated bibliography on artificial recharge of ground water, 1955-67","interactions":[],"lastModifiedDate":"2017-06-12T13:47:02","indexId":"wsp1990","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","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":"1990","title":"Annotated bibliography on artificial recharge of ground water, 1955-67","docAbstract":"Artificial ground-water recharge has become more important as water use by agriculture, industry, and municipalities increases. Water management agencies are increasingly interested in potential use of recharge for pollution abatement, waste-water disposal, and re-use and reclamation of locally available supplies. Research projects and theoretical analyses of operational recharge systems show increased scientific emphasis on the practice. Overall ground-water basin management systems generally now contain considerations of artificial recharge, whether by direct or indirect methods. Artificial ground-water recharge is a means of conserving surface runoff for future use in places where it would otherwise be lost, of protecting ground-water basins from salt-water encroachment along coastal areas, and of storing and distributing imported water. The biblio-graphy emphasizes technology; however, annotations of articles on waste-water reclamation, ground-water management and ground-water basin management are included. Subjects closely related to artificial recharge, including colloidal flow through porous media, field or laboratory instrumentation, and waste disposal by deep well injection are included where they specifically relate to potential recharge problems. Where almost the same material has been published in several journals, all references are included on the assumption that some publications may be more readily available to interested persons than others. Other publications, especially those of foreign literature, provided abstracts that were used freely as time limitations precluded obtaining and annotating all materials. Abstracts taken from published sources are noted. These are: \"Abstracts of North American Geology,\" U.S. Department of the Interior, Geological Survey; \"Abstracts of Recent Published Material on Foil and Water Conservation,\" ARS-41 series, Agricultural F.esearch Service, U.S. Department of Agriculture; \"Water and1 Water Engineering,\" published by Fuel and Metallurgical Journals, Ltd., London, England; \"Journal of Geophysical Research,\" American Geophysical Union, Washington, D.C.; \"American Society of Civil Engineers Transactions,\" New York; \"Selected Bibliography of Hydrology, United Kingdom, for the Years 1955-59,\" International Association of Scientific Hydrology; \"Water Wells, an Annotated Bibliography,\" California University Water Resources Center Archives Report 13; \"Re-use of Effluent in the Future With an Annotated Bibliography,\" by G. A. Whetstone, Texas Water Development Board Report 8, Austin, Tex.; \"Journal of Water Pollution Control Federation,\" Washington, D.C.; and \"A List of Selected Technical References on Artificial Recharge of Ground-Water Reservoirs,\" compiled by Roy W. Graves, Tulsa University, Information Services Department, Tulsa, Okla. Other notations are self-explanatory, and initials are those of the authors (DCS, DJG, WK). An unpublished compilation of recharge references by Arnon Arad sponsored by the United Nations Educational, Scientific, and Cultural Organization during a training period with the U.S. Geological Survey was also used. The bibliography is arranged alphabetically by author. Where an author has more than one publication, the arrangement is chronological; where an author has more than one publication in a given year, a, b, c, . . . are added. The indexing is by subject and geographic location. Each article was assigned the key words or phrases to best characterize its contents. Units of measure are as they were in the original article; abbreviations retained are generally those in common use such as mg/1 (milligrams per liter), ppm (parts per million), gpm (gallons per minute), km (kilometers), m (meters), cu m per hr (cubic meters p^r hour), cfs (cubic feet per second), me/1 (milliequivalents per liter), psi (pounds per square inch), BOD (biochemical oxygen demand), sq m (square meters), gpd (gallons per day), and mgd (million gallons per day). The bibliography was prepared because of the worldwide interest in the field of artificial recharge and the need for a single source of references to the literature published since 1954. The work is a sequel to the \"Annotated Bibliography on Artificial Recharge of Ground Water Through 1954,\" by D. K. Todd, U.S. Geological Survey Water-Supply Paper 1477, published in 1959.
","language":"English","publisher":"U.S. Government Printing Office","doi":"10.3133/wsp1990","usgsCitation":"Signor, D.C., Growitz, D.J., and Kam, W., 1970, Annotated bibliography on artificial recharge of ground water, 1955-67: U.S. Geological Survey Water Supply Paper 1990, iii, 141 p. ;24 cm., https://doi.org/10.3133/wsp1990.","productDescription":"iii, 141 p. ;24 cm.","costCenters":[{"id":532,"text":"Pennsylvania Water Science Center","active":true,"usgs":true}],"links":[{"id":138781,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1990/report-thumb.jpg"},{"id":29040,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1990/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67bdba","contributors":{"authors":[{"text":"Signor, Donald C.","contributorId":13220,"corporation":false,"usgs":true,"family":"Signor","given":"Donald","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":145603,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Growitz, Douglas J.","contributorId":83503,"corporation":false,"usgs":true,"family":"Growitz","given":"Douglas","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":145604,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Kam, William","contributorId":85159,"corporation":false,"usgs":true,"family":"Kam","given":"William","email":"","affiliations":[],"preferred":false,"id":145605,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70112296,"text":"70112296 - 1970 - Using radar imagery for crop discrimination: a statistical and conditional probability study","interactions":[],"lastModifiedDate":"2017-03-27T14:05:38","indexId":"70112296","displayToPublicDate":"1990-06-12T13:38:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3254,"text":"Remote Sensing of Environment","printIssn":"0034-4257","active":true,"publicationSubtype":{"id":10}},"title":"Using radar imagery for crop discrimination: a statistical and conditional probability study","docAbstract":"A number of the constraints with which remote sensing must contend in crop studies are outlined. They include sensor, identification accuracy, and congruencing constraints; the nature of the answers demanded of the sensor system; and the complex temporal variances of crops in large areas. Attention is then focused on several methods which may be used in the statistical analysis of multidimensional remote sensing data.
Crop discrimination for radar K-band imagery is investigated by three methods. The first one uses a Bayes decision rule, the second a nearest-neighbor spatial conditional probability approach, and the third the standard statistical techniques of cluster analysis and principal axes representation.
Results indicate that crop type and percent of cover significantly affect the strength of the radar return signal. Sugar beets, corn, and very bare ground are easily distinguishable, sorghum, alfalfa, and young wheat are harder to distinguish. Distinguishability will be improved if the imagery is examined in time sequence so that changes between times of planning, maturation, and harvest provide additional discriminant tools. A comparison between radar and photography indicates that radar performed surprisingly well in crop discrimination in western Kansas and warrants further study.
","language":"English","publisher":"Elsevier","publisherLocation":"New York, NY","doi":"10.1016/S0034-4257(70)80015-3","usgsCitation":"Haralick, R.M., Caspall, F., and Simonett, D., 1970, Using radar imagery for crop discrimination: a statistical and conditional probability study: Remote Sensing of Environment, v. 1, no. 2, p. 131-142, https://doi.org/10.1016/S0034-4257(70)80015-3.","productDescription":"12 p.","startPage":"131","endPage":"142","numberOfPages":"12","costCenters":[{"id":222,"text":"Earth Resources Observation and Science (EROS) Center","active":true,"usgs":true}],"links":[{"id":288502,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":288501,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://dx.doi.org/10.1016/S0034-4257(70)80015-3"}],"volume":"1","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"539acc5ce4b0e83db6d09050","contributors":{"authors":[{"text":"Haralick, R. M.","contributorId":63728,"corporation":false,"usgs":true,"family":"Haralick","given":"R.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":494647,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Caspall, F.","contributorId":35652,"corporation":false,"usgs":true,"family":"Caspall","given":"F.","email":"","affiliations":[],"preferred":false,"id":494646,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Simonett, D.S.","contributorId":102499,"corporation":false,"usgs":true,"family":"Simonett","given":"D.S.","affiliations":[],"preferred":false,"id":494648,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70112295,"text":"70112295 - 1970 - The airborne infrared scanner as a geophysical research tool","interactions":[],"lastModifiedDate":"2017-03-27T14:04:54","indexId":"70112295","displayToPublicDate":"1990-06-12T13:35:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2952,"text":"Optical Spectra","active":true,"publicationSubtype":{"id":10}},"title":"The airborne infrared scanner as a geophysical research tool","docAbstract":"The infrared scanner is proving to be an effective anomaly-mapping tool, albeit one which depicts surface emission directly and heat mass transfer from depths only indirectly and at a threshold level 50 to 100 times the normal conductive heat flow of the earth. Moreover, successive terrain observations are affected by time-dependent variables such as the diurnal and seasonal warming and cooling cycle of a point on the earth's surface. In planning precise air borne surveys of radiant flux from the earth's surface, account must be taken of background noise created by variations in micrometeorological factors and emissivity of surface materials, as well as the diurnal temperature cycle. The effect of the diurnal cycle may be minimized by planning predawn aerial surveys. In fact, the diurnal change is very small for most water bodies and the emissivity factor for water (e) =~ 1 so a minimum background noise is characteristic of scanner records of calm water surfaces.
","language":"English","publisher":"Optical Pub. Co.","publisherLocation":"Pittsfield, MA","usgsCitation":"Friedman, J.D., 1970, The airborne infrared scanner as a geophysical research tool: Optical Spectra, v. 4, no. 6, p. 35-44.","productDescription":"10 p.","startPage":"35","endPage":"44","numberOfPages":"10","costCenters":[{"id":222,"text":"Earth Resources Observation and Science (EROS) Center","active":true,"usgs":true}],"links":[{"id":288500,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"4","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"539acc58e4b0e83db6d09027","contributors":{"authors":[{"text":"Friedman, Jules D.","contributorId":79464,"corporation":false,"usgs":true,"family":"Friedman","given":"Jules","email":"","middleInitial":"D.","affiliations":[],"preferred":false,"id":494645,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70206956,"text":"70206956 - 1970 - Volcanic history of the San Juan Mountains, Colorado, as indicated by potassium-argon dating","interactions":[],"lastModifiedDate":"2021-06-29T16:02:47.66598","indexId":"70206956","displayToPublicDate":"1970-12-31T19:36:04","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1723,"text":"GSA Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"Volcanic history of the San Juan Mountains, Colorado, as indicated by potassium-argon dating","docAbstract":"Volcanic rocks in the San Juan Mountains constitute the largest erosional remnant of a once nearly continuous volcanic field that extended over much of the southern Rocky Mountains and adjacent areas in Oligocene and later time. Recent regional studies have shown that the gross petrologic evolution throughout the San Juan remnant of this field was relatively simple, with initial intermediate lavas and breccias, followed closely in time by more silicic ash-flow tuffs, and ending with a bimodal association of basalt and rhyolite. More limited data from other remnants of the original field indicate a similar evolution. In the San Juan field, voluminous early lavas and breccias - mainly alkali andesite, rhyodacite, and mafic quartz latite - were erupted from numerous scattered central volcanoes onto an eroded tectonically stable terrane. They formed mostly during the interval 35 to 30 m.y. ago, but some probably were erupted earlier and others up to several million years later. About 30 m.y. ago, major volcanic activity changed to explosive ash-flow eruptions of quartz latite and low-silica rhyolite that persisted until about 26 m.y. ago. Source areas for the ash flows are marked by large calderas in the central and western San Juan Mountains. Two groups of lavas and associated rocks of intermediate composition intertongue with the ash-flow sequence: (1) quartz latitic lavas that were erupted in and adjacent to caldera structures and are genetically related to the ash-flow activity; and (2) other, generally more mafic lavas and related rocks that are widely distributed without evident structural relation to the ash-flow eruptive centers. The second group apparently represents a continuation of the early intermediate activity into the period of major ash-flow eruption. In the early Miocene the character of volcanism changed notably. Whereas the Oligocene volcanics are predominantly intermediate lavas and related silicic differentiates, the younger rocks are largely a bimodal association of basalt and high-silica alkali rhyolite. Basalt and minor rhyolite were erupted intermittently through the Miocene and Pliocene, and at one time formed a widespread thin veneer over the older volcanic terrane. The marked contrast between the Oligocene intermediate to low-silica rhyolitic magmas and the later basaltic and rhyolitic magmas implies either different conditions of magma generation or processes of differentiation for the two suites. This petrologic change coincides approximately in time with nearby development of the Rio Grande depression, a major rift that is the local expression of widespread late Cenozoic crustal extension. Whatever the cause of the petrologic change, the progression from predominantly intermediate to bimodal basalt-rhyolite volcanism, approximately concurrent with initiation of late Tertiary crustal extension, appears characteristic of Cenozoic volcanism for much of the western interior United States. © 1970, The Geological Society of America, Inc.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1970)81[2329:VHOTSJ]2.0.CO;2","issn":"00167606","usgsCitation":"Lipman, P.W., Steven, T.A., and Mehnert, H.H., 1970, Volcanic history of the San Juan Mountains, Colorado, as indicated by potassium-argon dating: GSA Bulletin, v. 81, no. 8, p. 2329-2352, https://doi.org/10.1130/0016-7606(1970)81[2329:VHOTSJ]2.0.CO;2.","productDescription":"24 p.","startPage":"2329","endPage":"2352","costCenters":[{"id":218,"text":"Denver Federal Center","active":false,"usgs":true}],"links":[{"id":369782,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado","otherGeospatial":"San Juan Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -108.87451171875,\n 37.1165261849112\n ],\n [\n -105.16113281249999,\n 37.1165261849112\n ],\n [\n -105.16113281249999,\n 38.453588708941375\n ],\n [\n -108.87451171875,\n 38.453588708941375\n ],\n [\n -108.87451171875,\n 37.1165261849112\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"81","issue":"8","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Lipman, Peter W. 0000-0001-9175-6118 plipman@usgs.gov","orcid":"https://orcid.org/0000-0001-9175-6118","contributorId":3486,"corporation":false,"usgs":true,"family":"Lipman","given":"Peter","email":"plipman@usgs.gov","middleInitial":"W.","affiliations":[{"id":617,"text":"Volcano Science Center","active":true,"usgs":true},{"id":5079,"text":"Pacific Regional Director's Office","active":true,"usgs":true}],"preferred":true,"id":776373,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Steven, Thomas A.","contributorId":82977,"corporation":false,"usgs":true,"family":"Steven","given":"Thomas","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":776374,"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":776375,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70226754,"text":"70226754 - 1970 - Quartz gabbro and anorthositic gabbro: Markers of offset along the San Andreas fault in the California Coast Ranges","interactions":[],"lastModifiedDate":"2021-12-09T14:37:39.803124","indexId":"70226754","displayToPublicDate":"1970-12-01T08:26:26","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":"Quartz gabbro and anorthositic gabbro: Markers of offset along the San Andreas fault in the California Coast Ranges","docAbstract":"Large-scale lateral movement on the San Andreas fault zone is suggested by the distribution of gabbroic rocks that may be slivered remnants of oceanic crust. Distinctive and unusual hornblende quartz gabbro and anorthositic gabbro that are virtually identical both petrographically and chemically are exposed at Logan and Gold Hill in the Coast Ranges along the San Andreas fault. The hornblende quartz gabbro is made up of labradorite to bytownite plagioclase, hornblende, and quartz, with very minor biotite and pyroxene, and accessory metallic opaques and apatite. The coarse-grained anorthositic gabbro with anorthositic layers and associated gneiss is made up mainly of labradorite to bytownite plagioclase, hornblende, lesser clinopyroxene, and, locally, orthopyroxene.
The present 100 mi of separation between these two gabbro bodies is probably due to displacement along the San Andreas fault of what was originally one gabbro mass. Somewhat similar quartz gabbro and anorthositic gabbro associated with ultramafic rocks near Eagle Rest Peak in the San Emigdio Mountains may represent a source for the Logan and Gold Hill slivers. This suggests a minimum right-lateral movement of about 200 mi on the San Andreas fault zone. Anorthositic gabbro clasts from Cretaceous conglomerate in the Gualala area have strong resemblance to gabbroic rocks at Logan, Gold Hill, and Eagle Rest Peak and speculatively suggest 350 mi of right-lateral movement on the fault zone.
It is tentatively suggested that the gabbro clasts of Gualala may have been shed from a large area of exposed gabbroic oceanic crust, pieces of which occur as fault slivers at Gold Hill and Logan. It is further suggested that the Eagle Rest Peak locality may be a relatively in-place exposure of this gabbroic oceanic crust that lies near a continental-oceanic interface. This interface, thought to represent a fossil subduction zone between Franciscan and Sierran basements, appears to be overlain depositionally by Eocene sedimentary rocks. If these Eocene deposits do “seal over” the possible subduction zone, it suggests that movement on such a zone ceased before the Eocene deposition, and that the new and different pattern of right-lateral movement on the San Andreas fault zone probably began sometime later.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1970)81[3647:QGAAGM]2.0.CO;2","usgsCitation":"Ross, D.C., 1970, Quartz gabbro and anorthositic gabbro: Markers of offset along the San Andreas fault in the California Coast Ranges: Bulletin of the Geological Society of America, v. 81, no. 12, p. 3647-3661, https://doi.org/10.1130/0016-7606(1970)81[3647:QGAAGM]2.0.CO;2.","productDescription":"15 p.","startPage":"3647","endPage":"3661","costCenters":[],"links":[{"id":392677,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Coast Ranges, San Andreas fault","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -117.2900390625,\n 32.52828936482526\n ],\n [\n -115.13671875,\n 32.65787573695528\n ],\n [\n -119.37744140625,\n 35.06597313798418\n ],\n [\n -121.9482421875,\n 38.54816542304656\n ],\n [\n -122.62939453125001,\n 40.49709237269567\n ],\n [\n -124.38720703124999,\n 40.34654412118006\n ],\n [\n -123.92578125,\n 39.690280594818034\n ],\n [\n -123.94775390625,\n 38.993572058209466\n ],\n [\n -122.25585937500001,\n 36.65079252503471\n ],\n [\n -121.97021484374999,\n 36.08462129606931\n ],\n [\n -120.87158203125,\n 35.02999636902566\n ],\n [\n -120.87158203125,\n 34.470335121217474\n ],\n [\n -119.50927734374999,\n 34.23451236236987\n ],\n [\n -117.88330078125,\n 33.33970700424026\n ],\n [\n -117.2900390625,\n 32.52828936482526\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"81","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Ross, Donald C.","contributorId":146987,"corporation":false,"usgs":true,"family":"Ross","given":"Donald","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":828164,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010150,"text":"70010150 - 1970 - Brines and interstitial brackish water in drill cores from the deep Gulf of Mexico","interactions":[],"lastModifiedDate":"2026-01-29T16:46:16.445095","indexId":"70010150","displayToPublicDate":"1970-10-02T00:00:00","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":"Brines and interstitial brackish water in drill cores from the deep Gulf of Mexico","docAbstract":"Marked increases in interstitial salinity occur in two drill holes located in the Gulf of Mexico at a water depth of more than 3500 meters. The increases probably arose through diffusion of salt from buried evaporites. In one hole, however, brackish water was encountered on penetrating the oil-permeated cap rock of a salt dome. The phenomenon is attributed to production of fresh water during oxidation of petroleum hydrocarbons and decomposition of gypsum to form native sulfur.","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.170.3953.57","issn":"00368075","usgsCitation":"Manheim, F., and Sayles, F., 1970, Brines and interstitial brackish water in drill cores from the deep Gulf of Mexico: Science, v. 170, no. 3953, p. 57-61, https://doi.org/10.1126/science.170.3953.57.","productDescription":"5 p.","startPage":"57","endPage":"61","costCenters":[],"links":[{"id":219356,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -95.78387916948623,\n 29.54413740231888\n ],\n [\n -97.43864547128346,\n 27.242578131972927\n ],\n [\n -97.46077793013689,\n 25.961607264239774\n ],\n [\n -81.98918531110581,\n 25.852858348792083\n ],\n [\n -82.27113796673324,\n 28.544243690230644\n ],\n [\n -83.68685304614004,\n 30.179559981046587\n ],\n [\n -85.5275784639827,\n 30.652175207940914\n ],\n [\n -95.78387916948623,\n 29.54413740231888\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"170","issue":"3953","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f283e4b0c8380cd4b1f9","contributors":{"authors":[{"text":"Manheim, F.T. 0000-0003-4005-4524","orcid":"https://orcid.org/0000-0003-4005-4524","contributorId":55421,"corporation":false,"usgs":true,"family":"Manheim","given":"F.T.","affiliations":[],"preferred":false,"id":358133,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Sayles, F.L.","contributorId":77657,"corporation":false,"usgs":true,"family":"Sayles","given":"F.L.","email":"","affiliations":[],"preferred":false,"id":358134,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":5220517,"text":"5220517 - 1970 - Woodcock feeding habits as related to summer field usage in central Maine","interactions":[],"lastModifiedDate":"2025-02-19T17:08:17.7057","indexId":"5220517","displayToPublicDate":"1970-10-02T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2508,"text":"Journal of Wildlife Management","active":true,"publicationSubtype":{"id":10}},"title":"Woodcock feeding habits as related to summer field usage in central Maine","docAbstract":"In 1968 and 1969, 60 American woodcock (Philohela minor) were collected before and after alighting on summer fields in central Maine. A comparison of stomach contents from these birds showed that woodcock fed prior to entering fields at dusk. No evidence was found to indicate that any substantial amount of food was eaten by birds remaining on fields throughout the night. In 1968, the availability and abundance of known woodcock foods were measured in 30 soil samples from one field. Few woodcock foods were found in samples located randomly and at flush sites, thus providing no evidence that birds selected sites where soil invertebrates were concentrated.
","language":"English","publisher":"Wiley","doi":"10.2307/3799142","usgsCitation":"Krohn, W., 1970, Woodcock feeding habits as related to summer field usage in central Maine: Journal of Wildlife Management, v. 34, no. 4, p. 769-775, https://doi.org/10.2307/3799142.","productDescription":"7 p.","startPage":"769","endPage":"775","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":193488,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Maine","county":"Penobscot County","otherGeospatial":"central Maine","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-68.8196,46.3958],[-68.6951,46.3951],[-68.6945,46.3818],[-68.5068,46.3831],[-68.4363,46.3819],[-68.436,46.2692],[-68.437,46.0714],[-68.4379,46.043],[-68.4327,46.0352],[-68.4315,45.9519],[-68.4276,45.9445],[-68.4271,45.9313],[-68.4277,45.7803],[-68.4278,45.7684],[-68.4279,45.7597],[-68.4318,45.7597],[-68.4327,45.5796],[-68.4249,45.5763],[-68.4126,45.5726],[-68.2568,45.597],[-68.2587,45.6048],[-68.2547,45.6062],[-68.0479,45.6401],[-67.9938,45.4664],[-67.9547,45.3537],[-67.9663,45.352],[-67.9392,45.2673],[-67.9995,45.2595],[-68.0559,45.2553],[-68.1805,45.2369],[-68.303,45.2216],[-68.27,45.1004],[-68.3968,45.0837],[-68.375,44.9982],[-68.5022,44.9814],[-68.4902,44.9448],[-68.464,44.8361],[-68.446,44.7639],[-68.5335,44.7515],[-68.6081,44.7426],[-68.6171,44.7408],[-68.6242,44.7317],[-68.6475,44.7039],[-68.6911,44.7218],[-68.7137,44.7037],[-68.7265,44.6959],[-68.7298,44.69],[-68.744,44.6608],[-68.7716,44.6641],[-68.7664,44.6759],[-68.7812,44.6787],[-68.785,44.6782],[-68.7857,44.6865],[-68.7927,44.6856],[-68.7946,44.6874],[-68.7979,44.6874],[-68.7985,44.6888],[-68.8024,44.6878],[-68.8158,44.6838],[-68.8184,44.6874],[-68.8223,44.6874],[-68.8389,44.6934],[-68.8364,44.697],[-68.8376,44.702],[-68.8665,44.697],[-68.8659,44.6943],[-68.8717,44.6934],[-68.8961,44.6893],[-68.8967,44.6916],[-68.9038,44.6907],[-69.1157,44.6546],[-69.1272,44.6528],[-69.1837,44.6441],[-69.1979,44.6997],[-69.1986,44.702],[-69.2051,44.7298],[-69.2674,44.7219],[-69.2864,44.8081],[-69.2812,44.8086],[-69.2819,44.8122],[-69.356,45.0736],[-69.3431,45.0755],[-69.3398,45.0755],[-69.2049,45.0936],[-69.1752,45.0982],[-69.0531,45.1147],[-68.9775,45.127],[-68.8566,45.143],[-68.881,45.2247],[-68.8746,45.2261],[-68.7761,45.2401],[-68.8468,45.4902],[-68.8577,45.5267],[-68.9644,45.5126],[-68.952,45.5812],[-68.9507,45.6356],[-68.9597,45.6621],[-68.9408,45.6653],[-68.8255,45.6844],[-68.8229,45.9351],[-68.8212,46.2908],[-68.8196,46.3958]]]},\"properties\":{\"name\":\"Penobscot\",\"state\":\"ME\"}}]}","volume":"34","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49d9e4b07f02db5dfa0b","contributors":{"authors":[{"text":"Krohn, W.B.","contributorId":64355,"corporation":false,"usgs":true,"family":"Krohn","given":"W.B.","email":"","affiliations":[],"preferred":false,"id":331942,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70226577,"text":"70226577 - 1970 - Seismic refraction study of crustal structure in the western United States","interactions":[],"lastModifiedDate":"2021-11-29T20:24:45.381369","indexId":"70226577","displayToPublicDate":"1970-09-01T14:04:01","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":"Seismic refraction study of crustal structure in the western United States","docAbstract":"A network of 64 seismic-refraction profiles recorded by the U.S. Geological Survey in California and Nevada and adjacent areas of Idaho, Wyoming, Utah, and Arizona from 1961 to 1963 was re-interpreted. From record sections compiled for all profiles, a basic travel-time diagram can be derived. In addition to the first arrivals on profiles in the Snake River Plain, the northern Basin and Range province, and the middle Rocky Mountains, two dominant phases can be correlated in secondary arrivals, whereas the profiles in other areas show only one dominant phase in later arrivals. Based on velocity-depth functions calculated for each profile after the method of Giese, the crustal structure of the western United States is presented on contour maps and on a fence diagram that is composed of 15 crustal cross sections.
Crustal thickness reaches maxima under the Sierra Nevada (42 km), the Transverse Ranges of southern California (37 km), and in southwestern Nevada (36 km), whereas the crust is relatively thin under the Coast Ranges of California (24–26 km), under the Mojave Desert (28 km), and under parts of the central Basin and Range province in Nevada and Utah (29–30 km). The base of the crust dips generally from the Basin and Range province toward greater depths in the Colorado Plateau (43 km), the middle Rocky Mountains (45 km), and the Snake River Plain (44 km). The upper-mantle velocity is less than 8.0 kmps under the Great Basin of the Basin and Range province, the Sierra Nevada, and the Colorado Plateau, but it is equal to or greater than 8.0 kmps under the Coast Ranges of California, the Mojave Desert, and the middle Rocky Mountains. Velocity inversions within the upper crust are indicated under the southern Cascade Mountains and the middle Rocky Mountains, but not under the Sierra Nevada. The average velocity of the upper crust beneath the Basin and Range province is 6.1 to 6.2 kmps to a depth of 15 to 20 km. Only beneath the middle Rocky Mountains, the Snake River Plain, and the northern part of the Basin and Range province can a boundary zone between upper and lower crust be determined confidently.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1970)81[2629:SRSOCS]2.0.CO;2","usgsCitation":"Prodehl, C., 1970, Seismic refraction study of crustal structure in the western United States: Bulletin of the Geological Society of America, v. 81, no. 9, p. 2629-2645, https://doi.org/10.1130/0016-7606(1970)81[2629:SRSOCS]2.0.CO;2.","productDescription":"17 p.","startPage":"2629","endPage":"2645","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":392193,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona, California, Idaho, Nevada, Utah, Wyoming","otherGeospatial":"Cascade Mountains, Coast Ranges, Colorado Plateau, Great Basin, Mojave Desert, Rocky Mountains, Sierra Nevada, Snake River Plain, Transverse Ranges","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.51953124999999,\n 37.84015683604136\n ],\n [\n -120.7672119140625,\n 35.24113278166642\n ],\n [\n -118.2843017578125,\n 33.6420625047537\n ],\n [\n -116.13922119140624,\n 34.687427949314845\n ],\n [\n -114.01611328125,\n 35.137879119634185\n ],\n [\n -109.522705078125,\n 36.11125252076156\n ],\n [\n -109.51995849609375,\n 41.04207384890103\n ],\n [\n -112.686767578125,\n 43.104993581605505\n ],\n [\n -116.27929687499999,\n 43.866218006556394\n ],\n [\n -118.66882324218751,\n 39.60145584096999\n ],\n [\n -122.607421875,\n 41.07935114946899\n ],\n [\n -122.51953124999999,\n 37.84015683604136\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"81","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Prodehl, Claus","contributorId":224738,"corporation":false,"usgs":false,"family":"Prodehl","given":"Claus","affiliations":[],"preferred":false,"id":827396,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70226793,"text":"70226793 - 1970 - The Uralides and the motion of the Russian and Siberian Platforms","interactions":[],"lastModifiedDate":"2021-12-13T18:24:45.080549","indexId":"70226793","displayToPublicDate":"1970-09-01T12:12:00","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":"The Uralides and the motion of the Russian and Siberian Platforms","docAbstract":"The Uralides—the late Precambrian and Paleozoic orogenic terrane between the Russian and Siberian Platforms—in part are exposed in the Ural Mountains, in the central Soviet Arctic, along the west edge of the Siberian Platform, and in southern Siberia and Kazakhstan, and in part are buried beneath the fill of the West Siberian Lowlands and other basins. Paleomagnetic orientations suggest that the Russian and Siberian Platforms were far apart during the early Paleozoic, converged during the middle Paleozoic, and collided in the Permian or Triassic. The geology of the Uralides accords with the concept that the two subcontinents approached and collided as the intervening oceanic plate slid beneath them along subduction (Benioff) zones.
The medial eugeosyncline of the Uralides consists largely of what may be oceanic material scraped off against the edges of the opposed subcontinents. Basalt-and-spilite belts may represent ocean-floor abyssal tholeiite, and the manganiferous cherts and other sediments upon them may be pelagic oozes. Andesite belts may have formed as island arcs within the ocean, swept subsequently against the continents. Fossil subduction zones are recorded by great faults soled by, or containing tectonic injections of, mafic and ultramafic rocks from the lower oceanic crust and upper mantle, and containing high-pressure metamorphic rocks. Granitic and silicic-volcanic rocks may have formed above the subduction zones in the accreted parts of the continental plates. Both these continental-margin magmatic rocks and the island-arc complexes display ratios of potassium to silicon that vary across strike and so indicate the directions of dip of the subduction zones.
From the distribution of such indicators of various ages, a history of the continental margins can be deduced. An active subduction zone dipped beneath the Siberian Platform during at least parts of late Precambrian and early, middle, and late Paleozoic time. The late Precambrian and Cambrian history of the Russian side is unclear, but in the Ordovician and Silurian the Russian continental margin was stable, while somewhere offshore an island arc was present whose trench was on the Russian side; the last of the intervening oceanic plate vanished down the subduction zone in about the Early Devonian, and the island arc became part of the continental margin. During the remainder of the Devonian and during the Carboniferous and Early Permian, a subduction zone was present along the margin of the enlarged Russian continent and dipped beneath it.
Each subcontinent grew oceanward as oceanic material was accreted against it, and the subduction zones stepped oceanward correspondingly. The continental magmatic zones migrated oceanward behind the accreting edges of the continental plates, so the tectonic and magmatic progression with time at any one place is analogous to the variations present across the entire orogenic belt at any one time.
Severe right-lateral deformation of the Uralides, the Russian side having moved northward relative to the Siberian side during Mesozoic and early Cenozoic time, is inferred from structural and magnetic-anomaly patterns. The deformation was accomplished by oroclinal folding, strike-slip faulting, and tensional thinning of the crust.
The Uralides may have been continuous in early Mesozoic time with the Ellesmerides of North Greenland and the Canadian Arctic islands. The Cenozoic (and late Mesozoic?) opening of the Arctic Ocean was accomplished by spreading of the Eurasia Basin, and by opening of the Canada Basin behind a counterclockwise-rotating Alaska.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1970)81[2553:TUATMO]2.0.CO;2","usgsCitation":"Hamilton, W.B., 1970, The Uralides and the motion of the Russian and Siberian Platforms: Bulletin of the Geological Society of America, v. 81, no. 9, p. 2553-2576, https://doi.org/10.1130/0016-7606(1970)81[2553:TUATMO]2.0.CO;2.","productDescription":"24 p.","startPage":"2553","endPage":"2576","costCenters":[],"links":[{"id":392794,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Kazakhstan, Russia","otherGeospatial":"Siberia, Ural Mountains","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n 44.6484375,\n 44.715513732021336\n ],\n [\n 77.34374999999999,\n 44.715513732021336\n ],\n [\n 77.34374999999999,\n 77.11803181203176\n ],\n [\n 44.6484375,\n 77.11803181203176\n ],\n [\n 44.6484375,\n 44.715513732021336\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"81","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Hamilton, Warren B.","contributorId":74664,"corporation":false,"usgs":true,"family":"Hamilton","given":"Warren","email":"","middleInitial":"B.","affiliations":[],"preferred":false,"id":828289,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ]}