Measurements of the rates of population increase, reproduction, and mortality together with an observed age ratio, were used to analyze the population of the Herring Gull in New England. Data from sporadic censuses prior to this study, aerial censuses by the authors, and National Audubon Society Christmas Bird Count indicated that the New England breeding population has been doubling every 12 to 15 years since the early 1900's. This increase has involved founding new colonies and expanding the breeding range There is evidence that 15 to 30% of the adults do not breed in any given year. Sixty—one productivity measurements on 43 islands from 1963 through 1966, involving almost 13,000 nests, showed that from 0.8 to 1.4 young/breeding pair/year is the usual range of rate of production. The age distribution in the population was determined by classifying Herring Gulls by plumage category on an aerial census of the coast from Tampico, Mexico, to Cape Sable, Nova Scotia. Of the 622,000 gulls observed, 68% were adults, 17% were second— and third—year birds, and 15% were first—year birds. Mortality rates derived from band recovery data were too high to be consistent with the observed rate of population growth, productivity, and age structure. Loss of bands increasing to the rate of about 20%/year 5 years after banding eliminates most of the discrepancy. The age structure and rate of population increase indicate a mortality rate of 4 to 9% for gulls 2 years old or older, compared with the 25 to 30% indicated by band recoveries. The population structure we have developed fits everything we have observed about Herring Gull population dynamics, except mortality based on band recoveries.
","language":"English","publisher":"Ecological Society of America","doi":"10.2307/1935530","usgsCitation":"Kadlec, J.A., and Drury, W.H., 1968, Structure of the New England herring gull population: Ecology, v. 49, no. 4, p. 644-676, https://doi.org/10.2307/1935530.","productDescription":"33 p.","startPage":"644","endPage":"676","numberOfPages":"33","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":198016,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"49","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a80e4b07f02db649408","contributors":{"authors":[{"text":"Kadlec, John A.","contributorId":113405,"corporation":false,"usgs":true,"family":"Kadlec","given":"John","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":332008,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Drury, William H.","contributorId":20012,"corporation":false,"usgs":true,"family":"Drury","given":"William","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":332007,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70221386,"text":"70221386 - 1968 - Monitoring of changes in quality of ground water","interactions":[],"lastModifiedDate":"2021-06-14T12:07:52.93776","indexId":"70221386","displayToPublicDate":"1968-05-01T07:04:04","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Monitoring of changes in quality of ground water","docAbstract":"Ground water of acceptable quality is commonly interspersed with water of inferior quality. Water of inferior quality may be naturally occurring salty water commonly underlying fresh water, or it may be enclaves of contaminated water from wastes that lie in the fresh-water bodies. Disposal of wastes on and in the ground and pumping of water from wells cause a dispersion of contaminated water; migration of contaminated water toward wells may be spontaneously induced by the natural hydraulic gradient, or it may be induced artificially by the cone of depression about one or more wells. Economic methods of determining precisely the boundary zones between contaminated and uncontaminated water are not available. Much reliance is placed on monitoring wells.
A prerequisite to monitoring is a synthetic hydrogeologic framework or model in which the behavior of the contaminated water is conceived. Such a conceptual model, using pertinent data that are available, helps to assess the need for monitoring and to guide a monitoring program for optimum results. Unplanned, indiscriminate monitoring of water from wells is expensive, inefficient, and fallible. The need for monitoring will increase in the future; yet, the proper objective is to improve the technology of determining the distribution of contaminated water so that monitoring can be minimized and conducted with optimum results.
","language":"English","publisher":"NGWA The Groundwater Association","doi":"10.1111/j.1745-6584.1968.tb01645.x","usgsCitation":"LeGrand, H.E., 1968, Monitoring of changes in quality of ground water: Groundwater, v. 6, no. 3, p. 14-18, https://doi.org/10.1111/j.1745-6584.1968.tb01645.x.","productDescription":"5 p.","startPage":"14","endPage":"18","costCenters":[],"links":[{"id":386448,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"6","issue":"3","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"LeGrand, H. E.","contributorId":54571,"corporation":false,"usgs":true,"family":"LeGrand","given":"H.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":817476,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1001650,"text":"1001650 - 1968 - Age determination of blue-winged teal","interactions":[],"lastModifiedDate":"2025-02-14T16:45:24.957448","indexId":"1001650","displayToPublicDate":"1968-04-01T00:00:00","publicationYear":"1968","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":"Age determination of blue-winged teal","docAbstract":"Primary feather length, markings on the greater secondary coverts, and the degree of bill spotting were evaluated as characters for use in the spring to distinguish first-year, blue-winged teal (Anas discors) females from older ones. The length of the 10th primary feather did not prove suitable to separate different aged females. Extreme primary lengths might be used to determine the age of some males. In females that have been through a postnuptial molt the greater secondary coverts have a more symmetrical, and more acutely angled, white, inverted 'V'-marking. Any female with a 'V' subjectively classified as good has gone through at least one postnuptial molt, and a female with no sign of a 'V' on the coverts is a juvenile or yearling before her first postnuptial molt. By measuring the longest bill spot on the upper mandible of each known-age female, it was possible to determine the age of some female teal. Because the spots fade during the breeding season, no lower size limit could be set to delineate first-year females at that time of year, but any nest-trapped hen with a spot longer than 10 mm was considered to be older than 1 year. Upper and lower limits were also established to distinguish some yearlings and 2-year-olds in the fall.
","language":"English","publisher":"Wiley","doi":"10.2307/3798970","usgsCitation":"Dane, C., 1968, Age determination of blue-winged teal: Journal of Wildlife Management, v. 32, no. 2, p. 267-274, https://doi.org/10.2307/3798970.","productDescription":"8 p.","startPage":"267","endPage":"274","costCenters":[{"id":480,"text":"Northern Prairie Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":133672,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"32","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ae3e4b07f02db6893a0","contributors":{"authors":[{"text":"Dane, C.W.","contributorId":95003,"corporation":false,"usgs":true,"family":"Dane","given":"C.W.","email":"","affiliations":[],"preferred":false,"id":311436,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221375,"text":"70221375 - 1968 - Well logging in ground‐water hydrology","interactions":[],"lastModifiedDate":"2021-06-11T17:14:12.52318","indexId":"70221375","displayToPublicDate":"1968-01-01T12:11:27","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Well logging in ground‐water hydrology","docAbstract":"In 1966 more than 50 billion gallons of water was pumped daily from an estimated 10 to 15 million water wells in the United States. This was more than one‐sixth of the national withdrawal of water. On the basis of past rates of increase, a much greater future use of ground water is suggested. Our annual investment in water wells is one‐half to three‐quarter billion dollars, not including pumps and plumbing. In 1964 approximately 436,000 new wells were drilled; however, less than 1 percent of these wells were logged by any geophysical means. The application of _ge_o.phy.sical well logging to ground‐water hydrology is comparable to its use in petroleum exploration in the 1930's; however, we can take advantage of equipment and interpretation techniques developed in the oil industry that are available now for use in ground‐water investigations. Although most petroleum well logging techniques may be utilized in hydrology; modifications in equipment and interpretation are necessary because of basic economic and environmental differences between petroleum and ground‐water evaluation. If logging is to be widely applied to ground‐water exploration and evaluation, the expense of equipment and services must be reduced. Fortunately, this can be accomplished, because most water wells are not as deep as oil wells and the temperatures and pressures are lower. The Water Resources Division of the U. S. Geological Survey is conducting research on the application of borehole geophysics to ground‐water hydrology. The following logging devices are utilized in the evaluation of ground‐water environments: spontaneous potential, resistivity, gamma, gamma‐gamma, neutron, radioactive tracer, flowmeter, caliper, fluid resistivity, gradient and differential temperature, and sonic velocity. Lightweight logging sondes and control modules are operated by one man, either on a vehicle‐mounted 6,000‐foot logger or on a suitcase‐mounted 500‐foot logger. An inexpensive magnetic tape system has been developed and is used routinely for log recording and playback. If commercial well logging service is to be widely used in ground‐water exploration and development, water well contractors, and State and municipal agencies must be educated on the advantages of obtaining more information from each hole drilled. It will be necessary also to demonstrate how well logging can provide much of this information. In addition, the well logging industry must adapt their equipment and services to the requirements of ground‐water hydrology. The need for additional logging capability in this field exists at the present time and is expected to increase. Hopefully industry will be able to fill the gap.
","language":"English","publisher":"NGWA The Groundwater Association","doi":"10.1111/j.1745-6584.1968.tb01630.x","usgsCitation":"Keys, W., 1968, Well logging in ground‐water hydrology: Groundwater, v. 6, no. 1, p. 10-18, https://doi.org/10.1111/j.1745-6584.1968.tb01630.x.","productDescription":"9 p.","startPage":"10","endPage":"18","costCenters":[],"links":[{"id":386438,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"6","issue":"1","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Keys, W.S.","contributorId":75126,"corporation":false,"usgs":true,"family":"Keys","given":"W.S.","email":"","affiliations":[],"preferred":false,"id":817451,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70011658,"text":"70011658 - 1968 - Basalts dredged from the Amirante ridge, western Indian ocean","interactions":[],"lastModifiedDate":"2020-11-29T16:36:23.780474","indexId":"70011658","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1372,"text":"Deep-Sea Research and Oceanographic Abstracts","active":true,"publicationSubtype":{"id":10}},"title":"Basalts dredged from the Amirante ridge, western Indian ocean","docAbstract":"Oceanic tholeiitic basalts were dredged from 2500 to 3000 m depth on each flank of the Amirante Ridge, 1200 km southeast of Somalia in the western Indian Ocean, by R.V. Argo in 1964. One sample, probably shed from a flow or dike in basement beneath the coralline cap, gave a wholerock K-Ar age of 82±16×106 years. The age is similar to those reported by others for agglomerate from Providence Reef, nearer Madagascar, and for gabbro from Chain Ridge, the southwest member of Owen Fracture Zone, nearer the Somali coast. The Amirante Cretaceous-Early Tertiary occurrence lies between the “continental” 650 × 106 years granites of Seychelles Archipelago and the large Precambrian “continental” block of Madagascar.
Trends of major structures and distribution of the related topographic and magnetic-anomaly lineations in 7–8 × 106 km2of the surrounding Indian Ocean suggest that in addition to spreading of the seafloor from the seismically-active Mid-Indian Ocean Ridge-Carlsberg Ridge complex there has been, since mid-Mesozoic time, distributed left-lateral shear along 52°–54°E that has moved Madagascar at least 700 km south relative to Seychelles Bank. Measurements by other indicate the absolute movement of Madagascar has been southward as well. The emplacement of oceanic tholeiitic basalts at shallow depth, the development of volcanic topography between the sedimented Somali and Mascarene basins, and the existence of the faulted Amirante Trench and Ridge are consequences of the displacement.
","language":"English","publisher":"Elsevier","doi":"10.1016/0011-7471(68)90061-2","issn":"00117471","usgsCitation":"Fisher, R., Engel, C., and Hilde, T., 1968, Basalts dredged from the Amirante ridge, western Indian ocean: Deep-Sea Research and Oceanographic Abstracts, v. 15, no. 5, p. 521-534, https://doi.org/10.1016/0011-7471(68)90061-2.","productDescription":"14 p.","startPage":"521","endPage":"534","costCenters":[],"links":[{"id":221538,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"otherGeospatial":"Amirante ridge","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n 43.154296875,\n -18.312810846425442\n ],\n [\n 67.763671875,\n -18.312810846425442\n ],\n [\n 67.763671875,\n 1.3182430568620136\n ],\n [\n 43.154296875,\n 1.3182430568620136\n ],\n [\n 43.154296875,\n -18.312810846425442\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"15","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059efc3e4b0c8380cd4a43c","contributors":{"authors":[{"text":"Fisher, R.L.","contributorId":68028,"corporation":false,"usgs":true,"family":"Fisher","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":361634,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Engel, C.G.","contributorId":18489,"corporation":false,"usgs":true,"family":"Engel","given":"C.G.","email":"","affiliations":[],"preferred":false,"id":361632,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hilde, T.W.C.","contributorId":20469,"corporation":false,"usgs":true,"family":"Hilde","given":"T.W.C.","affiliations":[],"preferred":false,"id":361633,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70011498,"text":"70011498 - 1968 - Mineralogy as a function of depth in the prehistoric Makaopuhi tholeiitic lava lake, Hawaii","interactions":[],"lastModifiedDate":"2020-11-29T16:49:47.663291","indexId":"70011498","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","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":"Mineralogy as a function of depth in the prehistoric Makaopuhi tholeiitic lava lake, Hawaii","docAbstract":"The electron probe X-ray microanalyzer has been used to determine the compositional variability of the groundmass minerals and glass in 10 specimens from a complete 225-foot section of the prehistoric tholeiitic lava lake of Makaopuhi Crater, Hawaii. The order of beginning of crystallization was: (1) chromite, (2) olivine, (3) augite, (4) plagioclase, (5) pigeonite, (6) iron-titanium oxides and orthopyroxene, (7) alkali feldspar and apatite, and (8) glass.
Although the lake is chemically tholeiitic throughout, the occurrence of ferromagnesian minerals is as though there were a gradation from alkali olivine basalt in the upper chill downwards to olivine tholeiite. Groundmass olivine decreases downwards and disappears at about 20 feet. Pigeonite is absent in the uppermost 5±2 feet, then increases in amount down to 20 feet, below which augite and pigeonite coexist in constant 2∶1 proportions. Strong zoning and metastable compositions characterize the pyroxenes of the chilled zones, but these features gradually disappear towards the interior of the lake to give way to equilibrium pyroxenes. Relatively homogeneous poikilitic orthopyroxene (≈ Ca4Mg70Fe26) occurs in the olivine cumulate zone, having formed partly at the expense of pre-existing olivine, augite, and pigeonite (≈ Ca8Mg66Fe26). The growth of orthopyroxene is believed to have been facilitated by the slower cooling rate and higher volatile pressure at depth, and by the rise in Mg/Fe ratio of the liquid due to the partial dissolution of settled olivine.
Unlike olivine and pyroxene, feldspar is least zoned in the upper and lower chilled regions. The greatest range of compositional zoning in feldspar occurs at 160 to 190 feet, where it extends continuously from Or1.0Ab22An77 to Or64Ab33An3. The feldspar fractionation trend in the An-Ab-Or triangle gradually shifts with depth toward more “equilibrium” trends, even though the zoning becomes more extreme. The variation with depth in the initial (core) composition of the plagioclase suggests the influence of either slow nucleation and growth (undercooling) or slow diffusion in the liquid, relative to the rate of cooling.
Idiomorphic opaque inclusions in olivine phenocrysts are chrome-spinels showing continuous variation from 60 percent chromite to 85 percent ulvospinel and to magnetite-rich spinel. A pre-eruption trend of increasing Al with decreasing Cr can be recognized in chromites from the upper chill. Most of the inclusions show a trend of falling Cr and Al, toward an ulvospinelmagnetite solid solution which is progressively poorer in Usp with depth. This trend was produced by solid state alteration of the chromite inclusions during cooling in the lava lake. Ilmenite (average Ilm91Hm9) coexists with variably oxidized titaniferous magnetite in the basalt groundmass. Estimated oxygen fugacities agree well with other independent determinations in tholeiitic basalt. No sulfide phase has been detected.
Fractional crystallization produced a groundmass glass of granitic composition. Average, in percent, is: SiO2, 75.5; Al2O3, 12.5; K2O, 5.7; Na2O, 3.1; CaO, 0.3; MgO, 0.05; total FeO, 1.2; and TiO2, 0.8. Normative Or> Ab. Minor changes in glass composition with depth are consistent with a greater approach towards the granite minimum. Incipient devitrification precluded reliable analysis of glass from the lower half of the section. The SiO2-phase associated with devitrification contains alkalis and Al and is believed to be cristobalite. Needle-like apatite crystals in the groundmass glass are Siand Fe-bearing fluorapatites containing appreciable rare earths (predominantly Ce) and variable Cl.
The grain-size and maximum An content of the cores of plagioclase grains were controlled by cooling rate and are at a maximum at the center of the section. The most homogeneous pyroxene (and olivine, MOORE and EVANS, 1967), most equilibrium pyroxene trends, most abundant alkali feldspar, and most equilibrium feldspar trends are found at 160 to 190 feet, which is appreciably below that part of the lake which was slowest to crystallize. Volatile pressure, increasing with depth, possibly controlled the degree of attainment of equilibrium more than cooling rate.
Since they are dependent on cooling history, some of the modal criteria commonly used for recognizing basalt types, such as the absence of Ca-poor pyroxene, presence of groundmass olivine, and the presence of alkali feldspar, should be applied with caution. Petrographic comparison of basalts from one flow, volcano, or province, with another, should recognize the possible variations due to cooling history alone.
","language":"English","publisher":"Springer","doi":"10.1007/BF00373204","issn":"00107999","usgsCitation":"Evans, B., and Moore, J., 1968, Mineralogy as a function of depth in the prehistoric Makaopuhi tholeiitic lava lake, Hawaii: Contributions to Mineralogy and Petrology, v. 17, no. 2, p. 85-115, https://doi.org/10.1007/BF00373204.","productDescription":"31 p.","startPage":"85","endPage":"115","numberOfPages":"31","costCenters":[],"links":[{"id":221175,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United 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\"}}]}","volume":"17","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a5acce4b0c8380cd6f134","contributors":{"authors":[{"text":"Evans, B.W.","contributorId":86896,"corporation":false,"usgs":true,"family":"Evans","given":"B.W.","email":"","affiliations":[],"preferred":false,"id":361266,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Moore, J.G.","contributorId":67496,"corporation":false,"usgs":true,"family":"Moore","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":361265,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70009963,"text":"70009963 - 1968 - Paleomagnetism and the compositions of highly-oxidised iron-titanium oxides in basalts","interactions":[],"lastModifiedDate":"2020-11-29T17:05:56.491169","indexId":"70009963","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3071,"text":"Physics of the Earth and Planetary Interiors","active":true,"publicationSubtype":{"id":10}},"title":"Paleomagnetism and the compositions of highly-oxidised iron-titanium oxides in basalts","docAbstract":"As a preliminary step towards determination of the source of the natural remanence in highly-oxidised basalt lava flows, electron probe microanalysis has been carried out on the two main phases in each of two types of highly-oxidised iron-titanium oxide. The discovery of the source of NRM in these basalts is important because the correlations obtained recently by several workers between high oxidation and reversed polarity in basalts appear to support the possibility of self-reversal, even though some of the rocks studied give independent indications that the reversed magnetizations are due to field reversal.
In one type of grain analysed the probe data are consistent with a titanohematite phase and a pseudobrookite phase. This agrees with previous petrographic data. In the other type of grain the probe data are consistent with one phase of titanohematite but contradict petrographic data by showing that the other phase cannot be titanomagnetite. It is concluded that significant contributions to the NRM could possibly arise from the titanohematite (whose magnetic properties in basalts are little known) or the unindentified phase (unless subsequent work rules this phase out), but not in the pseudobrookite phase. However, the NRM may not lie in the analysed grains at all; and other workers are at present investigating this possibility.
","language":"English","publisher":"Elsevier","doi":"10.1016/0031-9201(68)90052-6","issn":"00319201","usgsCitation":"Smith, P., 1968, Paleomagnetism and the compositions of highly-oxidised iron-titanium oxides in basalts: Physics of the Earth and Planetary Interiors, v. 1, no. 2, p. 88-92, https://doi.org/10.1016/0031-9201(68)90052-6.","productDescription":"5 p.","startPage":"88","endPage":"92","numberOfPages":"5","costCenters":[],"links":[{"id":219339,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"1","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a741ee4b0c8380cd77458","contributors":{"authors":[{"text":"Smith, P.J.","contributorId":6579,"corporation":false,"usgs":true,"family":"Smith","given":"P.J.","email":"","affiliations":[],"preferred":false,"id":357544,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1014189,"text":"1014189 - 1968 - Infectious pancreatic necrosis: Selection of virus-free stock from a population of carrier trout","interactions":[],"lastModifiedDate":"2025-03-04T17:00:04.647505","indexId":"1014189","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2543,"text":"Journal of the Fisheries Research Board of Canada","active":true,"publicationSubtype":{"id":10}},"title":"Infectious pancreatic necrosis: Selection of virus-free stock from a population of carrier trout","docAbstract":"Infectious pancreatic necrosis (IPN) is a virulent disease of young trouts and is easily transmitted from infected animals through water and with eggs. At present, the most effective control measure consists of propagation of specific pathogen-free stock. Methods are described for using fish cell cultures to detect IPN virus in peritoneal washes, feces, and gonadal fluids and thereby to identifiy carrier and non-carrier fish. The procedures were used to derive virus-free progeny from a hatchery trout population containing about one-third carrier fish. The progeny were reared to maturity, spawned for 3 successive years, and at each spawning they proved free of virus. Recommendations and precautions are given for those who may wish to apply the procedures.
","language":"English","publisher":"Canadian Science Publishing","doi":"10.1139/f68-030","usgsCitation":"Wolf, K., Quimby, M.C., Carlson, C.P., and Bullock, G.L., 1968, Infectious pancreatic necrosis: Selection of virus-free stock from a population of carrier trout: Journal of the Fisheries Research Board of Canada, v. 25, no. 2, p. 383-391, https://doi.org/10.1139/f68-030.","productDescription":"9 p.","startPage":"383","endPage":"391","numberOfPages":"9","costCenters":[{"id":365,"text":"Leetown Science Center","active":true,"usgs":true}],"links":[{"id":197309,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"25","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49f1e4b07f02db5ee939","contributors":{"authors":[{"text":"Wolf, K.","contributorId":16344,"corporation":false,"usgs":true,"family":"Wolf","given":"K.","email":"","affiliations":[],"preferred":false,"id":319932,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Quimby, M. C.","contributorId":14334,"corporation":false,"usgs":true,"family":"Quimby","given":"M.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":319931,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Carlson, C. P.","contributorId":7229,"corporation":false,"usgs":false,"family":"Carlson","given":"C.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":319930,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bullock, G. L.","contributorId":69498,"corporation":false,"usgs":true,"family":"Bullock","given":"G.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":319933,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70011537,"text":"70011537 - 1968 - Geologic history of the continental margin of North America in the Bering Sea","interactions":[],"lastModifiedDate":"2020-11-29T16:41:09.795945","indexId":"70011537","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","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":"Geologic history of the continental margin of North America in the Bering Sea","docAbstract":"The North American continental margin beneath the Bering Sea is nearly 1,300 km long and extends from Alaska to eastern Siberia. The margin is a canyon-scarred 3,200–3,400-m high escarpment separating one of the world's largest epicontinental seas (the shallow Bering Sea) and the Aleutian Basin (the deep-water Bering Sea), a marginal oceanic basin distinguished by having its southern boundary formed by the Aleutian Ridge.
Three geomorphic provinces can be recognized: a southeastern province characterized by a gentle continental slope (lacking V-shaped canyons) and an outlying continental borderland (formed by Umnak Plateau); a central province distinguished by a steep canyon-scarred slope, and a northwestern province having a gentler and, apparently, less eroded continental slope.
Continuous seismic reflection profiles show that the margin is constructed of three major structural-stratigraphic units: (1) an acoustic basement underlying the outer shelf and upper slope; (2) an overlying main layered sequence; and (3) a stratified rise unit underlying and forming the continental rise at the base of the slope.
The existing margin evolved with downbowing and faulting of the acoustic basement, an older margin probably of Late Mesozoic age, consisting in part of well-indurated siltstone and mudstone, in Early Tertiary time. Concomitant with subsidence as much as 1,500 m of main-layered-sequence strata were draped over the basement. Intense canyon cutting, presumed to have been caused by the rapid deposition of unstable masses of riverborn sediment over the outer shelf and upper slope, is thought to have begun in Late Tertiary and Quaternary time. Concurrent with canyon cutting, submarine fans, consisting of turbidites forming the rise unit, accrued at the base of the continental slope.
Subsidence of the continental margin during the Tertiary may be related to foundering (“oceanization”) of a continental block to form the Aleutian Basin, or to simple isostatic depression of a former segment of the North Pacific oceanic floor in response to sediment infilling north of the Aleutian Ridge.
The activity product constant of cryolite (Na3AlF6) at 25°C and 1 atm total pressure was calculated from data for solutions from which synthetic cryolite or mixtures of cryolite and a solid apparently related to ralstonite had precipitated. The activities of fluoride and of sodium were estimated using specific ion electrodes. The activity of Al3+ was calculated from aluminum concentrations using equations which involve aluminum species existing in water solutions containing fluoride and hydroxide ions.
\nFor the reaction Na3AlF6(c) = 3Na(aq)+ + Al3+(aq) + 6E-(aq) the activity product constant Kso is 10−33.84, and the standard free energy of formation at 25°C is -745.4±1.0 kcal mole−1. This latter is identical to a value from the literature which is based on calorimetric data.
\nAlthough cryolite and related minerals are easily precipitated in the laboratory, their relative scarcity in nature suggests that the effect of influences, perhaps solutes other than those occurring in the structure, may inhibit or prevent the formation of cryolite.
","language":"English","publisher":"Elsevier","doi":"10.1016/0016-7037(68)90033-1","issn":"00167037","usgsCitation":"Roberson, C.E., and Hem, J., 1968, Activity product constant of cryolite at 25°C and one atmosphere using selective-ion electrodes to estimate sodium and fluoride activities: Geochimica et Cosmochimica Acta, v. 32, no. 12, p. 1343-1351, https://doi.org/10.1016/0016-7037(68)90033-1.","productDescription":"9 p.","startPage":"1343","endPage":"1351","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":221761,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"32","issue":"12","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059e6d0e4b0c8380cd4764a","contributors":{"authors":[{"text":"Roberson, C. E.","contributorId":40190,"corporation":false,"usgs":true,"family":"Roberson","given":"C.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":361336,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hem, J.D.","contributorId":54576,"corporation":false,"usgs":true,"family":"Hem","given":"J.D.","affiliations":[],"preferred":false,"id":361337,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":38846,"text":"pp542E - 1967 - Effects of the earthquake of March 27, 1964, at Seward, Alaska","interactions":[{"subject":{"id":38846,"text":"pp542E - 1967 - Effects of the earthquake of March 27, 1964, at Seward, Alaska","indexId":"pp542E","publicationYear":"1967","noYear":false,"chapter":"E","title":"Effects of the earthquake of March 27, 1964, at Seward, Alaska"},"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":"2022-03-31T18:47:27.868901","indexId":"pp542E","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1967","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":"E","title":"Effects of the earthquake of March 27, 1964, at Seward, Alaska","docAbstract":"Seward, in south-central Alaska, was one of the towns most devastated by the Alaska earthquake of March 27, 1964. The greater part of Seward is built on an alluvial fan-delta near the head of Resurrection Bay on the southeast coast of the Kenai Peninsula. It is one of the few ports in south-central Alaska that is ice free all year, and the town’s economy is almost entirely dependent upon its port facilities.
\n\nThe Alaska earthquake of March 27, 1964, magnitude approximately 8.3–8.4, began at 6:36 p.m. Its epicenter was in the northern part of the Prince William Sound area; focal depth was 20–50 km.
\n\nStrong ground motion at Seward lasted 3–4 minutes. During the shaking, a strip of land 50–400 feet wide along the Seward waterfront, together with docks and other harbor facilities, slid into Resurrection Bay as a result of large-scale submarine landsliding. Fractures ruptured the ground for'severa1 hundred feet back from the landslide scarps. Additional ground was fractured in the Forest Acres subdivision and on the alluvial floor of the Resurrection River valley; fountaining and sand boils accompanied the ground fracturing. Slide-generated wares, possibly seiche waves, and seismic sea waves crashed onto shore; ware runup was as much as 30 feet above mean lower low water and caused tremendous damage; fire from burning oil tanks added to the destruction. Damage from strong ground motion itself was comparatively minor. Tectonic subsidence of about 3.6 feet resulted in low areas being inundated at high tide.
\n\nThirteen people were killed and five were injured as a result of the earthquake. Eighty-six houses were totally destroyed and 260 were heavily damaged. The harbor facilities were almost completely destroyed, and the entire economic base of the town was wiped out. The total cost to replace the destroyed public and private facilities was estimated at $22 million.
\n\nSeward lies on the axis of the Chugach Mountains geosyncline. The main structural trend in the mapped area, where the rocks consist almost entirely of graywacke and phyllite, is from near north to N. 20° E. Beds and cleavage of the rocks commonly dip 70° W. or NW. to near vertical. Locally, the rocks are complexly folded or contorted. So major faults were found in the mapped area, but small faults, shear zones, and joints are common.
\n\nSurficial deposits of the area hare been divided for mapping into the following units: drift deposits, alluvial fan deposits, valley alluvium, intertidal deposits, landslide deposits, and artificial fill. Most of these units intergrade and were deposited more or less contemporaneously.
\n\nThe drift deposits consist chiefly of till that forms moraines along the lower flanks of the Resurrection River valley and up tributary valleys. The till is predominantly silt and sand and lesser amounts of clay-size particles, gravel, cobbles, and boulders. Glacial outwash and stratified ice-contact deposits constitute the remainder of the drift deposits.
\n\nFans and fan-deltas have been deposited at the valley mouths of tributary streams. Some, including the one upon which Seward built, project into Resurrection Bay, and deltaic-type deposits form their distal edges. The larger fans—composed chiefly of loosely compacted and poorly sorted silt, sand, and gravel—form broad aprons having low gradients. The fan deposits range in thickness from about 100 feet to possibly several hundred feet and, at least in some places, lie on a platform of compact drift. Smaller fans at the mouths of several canyons have steep gradients and considerable local relief.
\n\nValley alluvium, deposited chiefly by the Resurrection River, consists mostly of coarse sand and fine to medium gravel. In the axial part of the valley it is probably more than 100 feet thick. Near the head of Resurrection Bay, the alluvium is underlain by at least 75 feet of marine deltaic sediments, which are in turn underlain by 600 or more feet of drift in the deepest part of the bedrock valley.
\n\nBeach, deltaic, and estuarine sediments, deposited on intertidal flats at the head of the bay and along far1 margins that extend into the bay, arc mapped as intertidal deposits. They consist mostly of silt, sand, and fine gravel, and lesser amounts of clay-size particles.
\n\nThe earthquake reactivated old slides and trigged new ones in the mountains. Rock and snow avalanches, debris flows, and creep of talus deposits characterized slide activity on the steeper slops. The Seward waterfront had been extended before the earthquake by adding artificial fill consisting of loose sand and gravel; part of the lagoon area had been filled with refuse. After the earth- quake, fill, consisting of silt and sand dredged from the head of the bay, was pumped onto part of the lagoon area and also on land at the northwest corner of the bay.
\n\nResponse to the disaster was immediate and decisive. City, State, and Federal agencies, as well as other organizations and individuals, gave unstintingly of their time and facilities. Within a few days, there was temporary restoration of water, sewerage, and electrical facilities.
\n\nThe U.S. Army Corps of Engineers was authorized to select sites and construct a new dock for the Alaska Railroad, a new small-boat basin, and related facilities. The firm of Shannon and Wilson, Inc., under contract to the Corps of Engineers, investigated subsurface soils extensively to determine the factors responsible for the sliding along the Seward waterfront and to assist in site selection for reconstruction of the destroyed harbor facilities. Borings also made along the Seward waterfront and at the head of the bay, and laboratory tests were conducted on pertinent samples. These studies were augmented by geophysical studies both on land and in the bay. In addition, the Corps of Engineers made shallow borings on the intertidal flats at the head of the bay and performed pile-driving and load tests. Borings also were drilled and test pits were dug in the subdivision of Forest Acres.
\n\nSliding along the Seward waterfront markedly deepened the water along the former shoreline. Post-earthquake slopes of the bay floor immediately offshore also are steeper in places than before the earthquake. The strong ground motion of the earthquake triggered the landsliding, but several factors may have contributed to the magnitude and characteristics of the slides. These factors are: (1) the long duration of strong ground motion, (2) the grain size and texture of the material involved in the sliding, (3) the probability that the finer grained materials liquefied and flowed seaward, and (4) the added load of manmade facilities built on the edge of the shore, Secondary effects of the slides themselves—sudden drawdown of water, followed by the weight of returning waves—also may have contributed to the destruction.
\n\nSubmarine sliding at the northwest corner of the bay occurred in fine-grained deltaic deposits whose frontal slopes probably were in metastable equilibrium under static conditions. Uplift pressures from aquifers under hydrostatic head, combined with the probable liquefaction characteristics of the sediments when vibrated by strong ground motion, probably caused the material to slide and flow seaward as a heavy slurry.
\n\nUnder static conditions, no major shoreline or submarine landsliding is expected in the Seward area; in the event of another severe earthquake, however, additional sliding is likely along the Seward waterfront and also in the deltaic deposits at the northwest corner of the bay. Fractured ground in back of the present shoreline along the Seward waterfront is an area of incipient landslides that would be unstable under strong shaking. For this reason the Scientific and Engineering Task Force placed the area in a high-risk classification and recommended no repair, rehabilitation, or new construction in this area involving use of Federal funds; it was further recommended that the area should be reserved for park or other uses that do not involve large congregations of people. The deltaic deposits at the head of the bay probably also would be susceptible to sliding during another large earthquake. This sliding would result in further landward retreat of the present shoreline toward the new railroad dock. Specifications for the new dock, whose seaward end is now approximately 1,100 feet from the back scarp of the subaqueous landslide, require design pro- visions to withstand seismic shock up to certain limits.
\n\nEarthquake-induced fracturing of the ground in the subdivision of Forest Acres was confined to the lower part of a broad alluvial fan. There, sewer and water lines were ruptured and the foundations of some homes were heavily damaged. Landsliding, such as occurred along the shoreline of the bay, was not a contributing cause of the fracturing. Two hypotheses are offered to explain the fracturing:
\n\n1. Seismic energy was transformed into visible surface waves of such amplitude that the strength of surface layer was exceeded and rupturing occurred; tensional and compressional stresses alternately opened and closed the fractures and forced out water and mud.
\n\n2. Compaction by vibration of the fine-grained deposits of the fan caused ground settlement and fracturing; ground water under temporary hydrostatic head was forced to the surface as fountains and carried the finer material with it.
\n\nWater waves that crashed onto shore, while shaking was still continuing, were generated chiefly by onshore and offshore landsliding. Waves that overran the shores about 25 minutes after shaking stopped and that continued to arrive for the next several hours are believed to be seismic sea waves (tsunamis) that originated in an uplifted area in the Gulf of Alaska. During the time of seismic sea-wave activity and perhaps preceding it, seiche wares also may have been generated within Resurrection Bay and complicated the wave effects along the shoreline.
","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/pp542E","usgsCitation":"Lemke, R., 1967, Effects of the earthquake of March 27, 1964, at Seward, Alaska: U.S. Geological Survey Professional Paper 542, Report: viii, 43 p.; 2 Plates: 20.5 x 21.5 inches and 25.57 x 19.78 inches, https://doi.org/10.3133/pp542E.","productDescription":"Report: viii, 43 p.; 2 Plates: 20.5 x 21.5 inches and 25.57 x 19.78 inches","numberOfPages":"53","additionalOnlineFiles":"Y","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":170343,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0542e/report-thumb.jpg"},{"id":113268,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542e/pp542e_plate2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":397947,"rank":6,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4587.htm"},{"id":113267,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542e/pp542e_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":113266,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0542e/pp542e_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":104504,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0542e/index.html","linkFileType":{"id":5,"text":"html"},"description":"4587"}],"scale":"63360","datum":"Mean Sea Level","country":"United States","state":"Alaska","city":"Seward","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -149.4778,\n 60.0622\n ],\n [\n -149.3333,\n 60.0622\n ],\n [\n -149.3333,\n 60.1856\n ],\n [\n -149.4778,\n 60.1856\n ],\n [\n -149.4778,\n 60.0622\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a27e4b07f02db610336","contributors":{"authors":[{"text":"Lemke, Richard W.","contributorId":59409,"corporation":false,"usgs":true,"family":"Lemke","given":"Richard W.","affiliations":[],"preferred":false,"id":220533,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":985,"text":"wsp1849 - 1967 - Roughness characteristics of natural channels","interactions":[],"lastModifiedDate":"2017-06-21T09:54:47","indexId":"wsp1849","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1849","title":"Roughness characteristics of natural channels","docAbstract":"Color photographs and descriptive data are presented for 50 stream channels for which roughness coefficients have been determined. \r\n\r\nAll hydraulic computations involving flow in open channels require an evaluation of the roughness characteristics of the channel. In the absence of a satisfactory quantitative procedure this evaluation remains chiefly an art. The ability to evaluate roughness coefficients must be developed through experience. One means of gaining this experience is by examining and becoming acquainted with the appearance of some typical channels whose roughness coefficients are known. \r\n\r\nThe photographs and data contained in this report represent a wide range of channel conditions. Familiarity with the appearance, geometry, and roughness characteristics of these channels will improve the engineer's ability to select roughness coefficients for other channels .","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1849","usgsCitation":"Barnes, H.H., 1967, Roughness characteristics of natural channels: U.S. Geological Survey Water Supply Paper 1849, vi, 213 p. :illus. (part col.) ;24 cm., https://doi.org/10.3133/wsp1849.","productDescription":"vi, 213 p. :illus. (part col.) ;24 cm.","costCenters":[],"links":[{"id":136116,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":342703,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/wsp_1849/pdf/wsp_1849.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":8,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.water.usgs.gov/wsp1849/","linkFileType":{"id":5,"text":"html"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ee4b07f02db5fe1e9","contributors":{"authors":[{"text":"Barnes, Harry Hawthorne","contributorId":64630,"corporation":false,"usgs":true,"family":"Barnes","given":"Harry","email":"","middleInitial":"Hawthorne","affiliations":[],"preferred":false,"id":142968,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":4072,"text":"cir545 - 1967 - Marine sediment sample preparation for analysis for low concentrations of fine detrital gold","interactions":[],"lastModifiedDate":"2017-08-27T17:54:55","indexId":"cir545","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":307,"text":"Circular","code":"CIR","onlineIssn":"2330-5703","printIssn":"1067-084X","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"545","title":"Marine sediment sample preparation for analysis for low concentrations of fine detrital gold","docAbstract":"Analyses by atomic absorption for detrital gold in more than 2,000 beach, offshore, marine-terrace, and alluvial sands from southern Oregon have shown that the values determined from raw or unconcentrated sediment containing small amounts of gold are neither reproducible nor representative of the initial sample. This difficulty results from a 'particle sparsity effect', whereby the analysis for gold in a given sample depends more upon the occurrence of random flakes of gold in the analyzed portion than upon the actual gold content of the sample. \r\n\r\nThe particle sparsity effect can largely be eliminated by preparing a gold concentrate prior to analysis. A combination of sieve, gravimetric, and magnetic separation produces a satisfactory concentrate that yields accurate and reproducible analyses. In concentrates of nearly every marine and beach sand studied, the gold occurs in the nonmagnetic fraction smaller than 0.124 mm and with a specific gravity greater than 3.3. The grain size of gold in stream sediments is somewhat more variable. \r\n\r\nAnalysis of concentrates provides a means of greatly increasing the sensitivity of the analytical technique in relation to the initial sample. Gold rarely exceeds 1 part per million in even the richest black sand analyzed; to establish the distribution of gold (and \r\nplatinum) in marine sediments and its relationship to source and environmental factors, one commonly needs to know their content to the part per billion range. Analysis of a concentrate and recalculation to the value in the initial sample permits this degree of sensitivity.","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/cir545","usgsCitation":"Clifton, H.E., Hubert, A., and Phillips, R.L., 1967, Marine sediment sample preparation for analysis for low concentrations of fine detrital gold: U.S. Geological Survey Circular 545, 11 p. :map ;26 cm., https://doi.org/10.3133/cir545.","productDescription":"11 p. :map ;26 cm.","costCenters":[],"links":[{"id":124628,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/circ/1967/0545/report-thumb.jpg"},{"id":31166,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/circ/1967/0545/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a17e4b07f02db604414","contributors":{"authors":[{"text":"Clifton, H. Edward","contributorId":46503,"corporation":false,"usgs":true,"family":"Clifton","given":"H.","email":"","middleInitial":"Edward","affiliations":[],"preferred":false,"id":148120,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hubert, Arthur","contributorId":17977,"corporation":false,"usgs":true,"family":"Hubert","given":"Arthur","affiliations":[],"preferred":false,"id":148119,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Phillips, R. Lawrence","contributorId":81478,"corporation":false,"usgs":true,"family":"Phillips","given":"R.","email":"","middleInitial":"Lawrence","affiliations":[],"preferred":false,"id":148121,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":40718,"text":"ofr673 - 1967 - Geohydrologic reconnaissance of the Soquel-Aptos area, Santa Cruz County, California","interactions":[],"lastModifiedDate":"2018-02-14T17:04:47","indexId":"ofr673","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"67-3","title":"Geohydrologic reconnaissance of the Soquel-Aptos area, Santa Cruz County, California","docAbstract":"This report summarizes existing knowledge on the geohydrology of the Soquel-Aptos area, near, and including the eastern part, of Santa Cruz, California, and outlines work necessary for making a complete appraisal of the water resources of the area.
The area is underlain mostly by marine and continental sedimentary deposits of Tertiary and Quaternary age. A small section in the northeastern part of the area on the eastern side of the San Andreas fault is underlain by sedimentary and metamorphic rocks of Cretaceous or older age. Quartz diorite, probably of Cretaceous age, underlies a considerable part of the area, but crops out only in small exposures along canyon bottom south of the Zayante fault.
The Soquel-Aptos area consists of two main structural blocks?one, downthrown on the northeast side of the Zayante fault; the other, upthrown on the southwest side of the fault. The main water-bearing formations in the southwestern structural block are the Santa Margarita and Purisima Formations. The Purisima, the most widespread of these units in this area, contains water under water-table and artesian conditions and furnishes water to most wells. The water-bearing character of the rocks in the northern structural block is unknown.
Presently available geohydrologic data are too limited for detailed evaluation of the ground-water potential in the Soquel-Aptos area. Work needed for a detailed evaluation includes: (1) Geophysical exploration and test drilling at selected locations, (2) pumping tests of selected existing wells and possibly of specially drilled test wells, (3) study and reconnaissance measurements of spring and streamflow, (4) chemical analysis of water samples from selected wells, and (5) establishment of a program for monitoring water quality and water levels in key wells.
","language":"English","publisher":"U.S. geological Survey","publisherLocation":"Menlo Park, CA","doi":"10.3133/ofr673","collaboration":"Prepared in cooperation with the Soquel Creek County [Watershed District?], the City of Santa Cruz, and the county of Santa Cruz","usgsCitation":"Akers, J.P., and Hickey, J., 1967, Geohydrologic reconnaissance of the Soquel-Aptos area, Santa Cruz County, California: U.S. Geological Survey Open-File Report 67-3, Report: 58 p.; 1 Figure: 27.84 x 32.26 inches, https://doi.org/10.3133/ofr673.","productDescription":"Report: 58 p.; 1 Figure: 27.84 x 32.26 inches","costCenters":[{"id":154,"text":"California Water Science Center","active":true,"usgs":true}],"links":[{"id":77992,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1967/0003/plate-1.pdf","text":"Figure 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Geologic map of the Soquel-Aptos area, California, showing location of hydrologic data stations"},{"id":77993,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1967/0003/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":110367,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_53760.htm","linkFileType":{"id":5,"text":"html"},"description":"53760"},{"id":171208,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1967/0003/report-thumb.jpg"}],"country":"United States","state":"California","county":"Santa Cruz County","otherGeospatial":"Soquel-Aptos area","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b25e4b07f02db6aedf1","contributors":{"authors":[{"text":"Akers, J. P.","contributorId":82678,"corporation":false,"usgs":true,"family":"Akers","given":"J.","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":223850,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hickey, J.J.","contributorId":57010,"corporation":false,"usgs":true,"family":"Hickey","given":"J.J.","email":"","affiliations":[],"preferred":false,"id":223849,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1112,"text":"wsp1836 - 1967 - Ground-water conditions and geologic reconnaissance of the Upper Sevier River basin, Utah","interactions":[],"lastModifiedDate":"2017-09-04T17:41:05","indexId":"wsp1836","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1967","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":"1836","title":"Ground-water conditions and geologic reconnaissance of the Upper Sevier River basin, Utah","docAbstract":"The upper Sevier River basin is in south-central Utah and includes an area of about 2,400 .square miles of high plateaus and valleys. It comprises the entire Sevier River drainage basin above Kingston, including the East Fork Sevier River and its tributaries. The basin was investigated to determine general ground-water conditions, the interrelation of ground water and surface water, the effects of increasing the pumping of ground water, and the amount of ground water in storage.
The basin includes four main valleys - Panguitch Valley, Circle Valley, East Fork Valley, and Grass Valley - which are drained by the Sevier River, the East Fork Sevier River, and Otter Creek. The plateaus surrounding the valleys consist of sedimentary and igneous rocks that range in age from Triassic to Quaternary. The valley fill, which is predominantly alluvial gravel, sand, silt, and clay, has a maximum thickness of more than 800 feet.
The four main valleys constitute separate ground-water basins. East Fork Valley basin is divided into Emery Valley, Johns Valley, and Antimony subbasins, and Grass Valley basin is divided into Koosharem and Angle subbasins. Ground water occurs under both artesian and water-table conditions in all the basins and subbasins except Johns Valley, Emery Valley, and Angle subbasins, where water is only under water-table conditions. The water is under artesian pressure in beds of gravel and sand confined by overlying beds of silt and clay in the downstream parts of Panguitch Valley basin, Circle Valley basin, and Antimony subbasin, and in most of Koosharem subbasin. Along the sides and upstream ends of these basins, water is usually under water-table conditions.
About 1 million acre-feet of ground water that is readily available to wells is stored in the gravel and sand of the upper 200 feet of saturated valley fill. About 570,000 acre-feet is stored in Panguitch Valley basin, about 210,000 in Circle Valley basin, about 6,000 in Emery Valley subbasin, about 90,000 in Johns Valley subbasin, about 36,000 in Antimony subbasin, about 90,000 in Koosharem subbasin, and about 60,000 in Angle subbasin. Additional water, although it is not readily available to wells, is stored in beds of silt and clay. Some ground water also is available in the bedrock underlying and surrounding the basins, although the bedrock formations generally are poor aquifers.
The principal source of recharge to the valley fill in the upper Sevier River basin is infiltration from streams, canals, and irrigated fields. Some ground water also miles into the valley till from the bedrock surrounding the basins.
The basin contains about 300 wells, most of which are less than 4 inches in diameter, are less than 250 feet deep, and are used for domestic purposes and stock watering. More than half the wells are flowing wells in Koosharem subbasin.
Approximately 82,000 acre-feet of ground water was discharged in 1962 from the valley till. Springs discharged about 33,000 acre-feet, wells about 3,000, and drains about 3,000; and evapotranspiration from phreatophyte areas about 43,000 acre-feet. Springs in bedrock discharged an additional 75,000 acre-feet. Most of the water discharged by springs, wells, and drains was used for irrigation.
The ground water in the basin generally is of good chemical quality. The water is excellent for irrigation and stock but is not as desirable for most domestic and industrial uses because of its hardness. The dissolved-solids content of the ground water generally increases slightly from the upstream end of the individual ground-water basins to. the downstream end owing mostly to repeated use of the water for irrigation.
Surface water and ground water in the upper Sevier River basin are inter- connected, and the base flows of streams are affected by changes in ground- water levels. Increased pumping of ground water would result in (1) an increase in the recharge to the aquifers from surface-water sources or (2) a decrease in the discharge from streams, springs, flowing wells, and areas of phreatophytes or (3) a combination of these.
About 43,000 acre-feet of ground water is now discharged annually by evapotranspiration from phreatophyte areas, and perhaps one-third of this loss, or about 14,000 acre-feet, could be salvaged by eliminating wet areas and phreatophytes. The areas where water could be salvaged are at the downstream ends of Panguitch Valley basin, Circle Valley basin, and Antimony subbasin. Most of the 14,000 acre-feet 'of water could be pumped from large-diameter wells or developed by properly designed drains without greatly affecting stream- flow and with only moderate effect on 'spring discharge. If the wells were properly located, the pumping would lower water levels and dry up wet areas where phreatophytes grow. Conjunctive use of ground water and surface water would facilitate the more efficient use of all water resources in the basin
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/wsp1836","collaboration":"Prepared in cooperation with the Utah State Engineer","usgsCitation":"Carpenter, C.H., Robinson, G., and Bjorklund, L.J., 1967, Ground-water conditions and geologic reconnaissance of the Upper Sevier River basin, Utah: U.S. Geological Survey Water Supply Paper 1836, Report: vi, 91 p.; 3 Plates: 35.00 in. x 49.87 in. or smaller, https://doi.org/10.3133/wsp1836.","productDescription":"Report: vi, 91 p.; 3 Plates: 35.00 in. x 49.87 in. or smaller","numberOfPages":"98","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":138011,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1836/report-thumb.jpg"},{"id":25869,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1836/plate-1.pdf","text":"Plate 1","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Reconnaissance geologic map and sections of the Upper Sevier River Basin, Utah"},{"id":25870,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1836/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Map showing hydrologic data and phreatophyte areas in the Upper Sevier River Basin, Utah"},{"id":25871,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1836/plate-3.pdf","text":"Plate 3","linkFileType":{"id":1,"text":"pdf"},"linkHelpText":"Graphs of water levels in selected wells and selected analyses of ground and surface water in the Upper Sevier River Basin, Utah"},{"id":25872,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1836/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Utah","otherGeospatial":"Upper Sevier River Basin","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aafe4b07f02db66d2be","contributors":{"authors":[{"text":"Carpenter, Carl H.","contributorId":46074,"corporation":false,"usgs":true,"family":"Carpenter","given":"Carl","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":143197,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Robinson, Gerald B.","contributorId":46497,"corporation":false,"usgs":true,"family":"Robinson","given":"Gerald B.","affiliations":[],"preferred":false,"id":143198,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Bjorklund, Louis Jay","contributorId":21138,"corporation":false,"usgs":true,"family":"Bjorklund","given":"Louis","email":"","middleInitial":"Jay","affiliations":[],"preferred":false,"id":143196,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70221317,"text":"70221317 - 1967 - Time and space relationships of the taconic allochthon and autochthon","interactions":[],"lastModifiedDate":"2021-06-09T18:42:14.902827","indexId":"70221317","displayToPublicDate":"1967-12-01T13:38:56","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3459,"text":"Special Paper of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Time and space relationships of the taconic allochthon and autochthon","docAbstract":"The Taconic rock sequence extends from near Sudbury, Vermont, to near Poughkeepsie, New York, a length of about 150 miles; and from just west of the Green Mountain Range and Berkshire Highlands to the valleys of the Hudson River and Lake Champlain, a width of about 20 miles. The Taconic rocks are now in the axial region of the Middlebury synclinorium and its southward extension. The Taconic sequence consists of about 2000 feet of slate, with subsidiary graywacke, quartzite, and limestone; many of the rock units are turbidites. Fossils from the rocks include forms of Early, Middle, and Late Cambrian and Early and Middle Ordovician age. Evidence of stratigraphic tops derived from the fossils and from primary sedimentary features agrees with structural data and demonstrates that the Taconic rocks are geometrically the highest strata within the Middlebury synclinorium. The underlying rocks of the synclinorium (the synclinorium sequence) are right side up; they also range in age from Early Cambrian to Middle Ordovician but belong to a different sedimentary lithofacies (dominantly carbonate and orthoquartzite). The relation between the Taconic sequence and the synclinorium sequence, therefore, is a baffling problem. Lithostratigraphically, the Taconic sequence falls into three groups: (1) the pre- Normanskill \"low Taconic\" sequence, occurring in the area between the main Taconic Range and the Hudson River, as far south as Rhinebeck, New York; (2) the Normanskill Shale in the same area, as well as in the area south of Rhinebeck at least as far as Poughkeepsie, New York, and also west of the Hudson River; and (3) the \"high Taconic\" sequence, occupying the main Taconic Range from Dorset Mountain, Vermont, south to Indian Mountain in Sharon, Connecticut, as well as Mount Greylock in Massachusetts. Rocks of (1) and (2) are fossiliferous, but to date no fossil has been found in (3). Rocks of (1) and that part of (2) areally coextensive with (1) thus are of known age but uncertain three-dimensional geometric configuration, whereas rocks of (3) are of known configuration (in the centers of open synclinoria) but unknown age. Only that part of (2) beyond the areal confines of (1) is both of known age and known configuration; these rocks are in sedimentary contact above the older rocks of the synclinorium sequence and are autochthonous. At the north end of the Taconic sequence in western Vermont, rocks of group (1) are beyond reasonable doubt allochthonous. Because of the southward geometric continuity of the structural elements, all the Taconic rocks of group (1), and that part of group (2) areally coextensive with it, are interpreted as allochthonous. The structure of group (3), the high Taconic sequence, is inferred by topography and by detailed lithostratigraphic matching with rocks of the east Vermont sequence; on this basis, as well as on the basis of the broad lithic similarity with rocks of group (1), rocks of group (3) are concluded to be also allochthonous. A discontinuous polymict conglomerate underlies and surrounds the allochthon on all sides and is interpreted here as a record that dates the imminent arrival of the allochthon at each locality. The conglomerate contains unsorted blocks of rocks of both the Taconic sequence and the synclinorium sequence; the matrix is the autochthonous upper Normanskill Shale or its equivalent. Fossils from the matrix shale date the event as Trenton, probably Sherman Fall in age. The geologic history of the area is reconstructed as follows: The pre-Normanskill Taconic rocks were deposited in the area of the present Precambrian massifs of the Green Mountains-Berkshire Highlands belt between the clastic, eugeosynclinal east Vermont sequence to the east and the miogeosynclinal synclinorium sequence to the west; they constitute the transitional facies between these two belts. Conditions were relatively stable until early Middle Ordovician time, when the Green Mountain- Berkshire Highlands area began to rise and the area of the present Middlebury synclinorium began to subside. Subsidence took place largely by a series of high-angle longitudinal faults that, as a whole, step down to the west. Argillaceous sediments (the Normanskill Shale) began to inundate the former miogeosynclinal area; because the conditions of sedimentation had become similar, the sediments resembled, in facies, the synchronous Taconic rocks that were being deposited to the east. Continued rise of the Green Mountains-Berkshire Highlands area led in middle Trenton time to the decollement of the Cambrian and Ordovician sediments into the area of the present Middlebury synclinorium in a series of giant submarine slides. Sedimentation continued at the receiving site throughout the event; sedimentation may also have persisted on the moving slides. The record is found today in the turbidite-laden shale and graywacke in the upper part of the Normanskill Shale of both the allochthon and the autochthon. Restoration of the allochthonous rocks to the original site of deposition leads to correlations between rocks of the Taconic sequence and of the largely autochthonous east Vermont sequence. The lithic correlation can be carried to the level of individual formations and is confirmed by a few known ages in the east Vermont sequence. Several lines of reasoning lead to a plausible correlation of part of the Cavendish Formation of southeastern Vermont with the oldest part of the Taconic sequence. This correlation leads further to the conclusion that in this area the contacts between the Green Mountain massif and the Cavendish Formation and between the Cavendish and the overlying east Vermont sequence must both be thrust faults of large displacements. This conclusion is in fact inevitable because one of the Taconic thrust slices that extends without interruption between the latitudes corresponding to the gap in the Precambrian massifs has been shown by local structural evidence to be allochthonous; an outside original depositional site must be found for it. The present Taconic allochthon is coextensive with an area of marked negative Bouguer gravity anomaly; the Green Mountains-Berkshire massifs constitute a belt of positive anomaly. It is here proposed that these anomalies resulted from a deepseated transfer of material; subcrustal addition of material caused the rise of the Green Mountains-Berkshire Highlands area, and the concurrent subtraction of material caused subsidence in the Middlebury synclinorium area through a series of faults which were the near-surface expression of an episode of crustal collapse. If this interpretation is correct, then the regional gravity anomaly represents an uncompensated feature that has persisted since Middle Ordovician time.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/SPE97-p1","usgsCitation":"Zen, E., 1967, Time and space relationships of the taconic allochthon and autochthon: Special Paper of the Geological Society of America, v. 97, p. 1-82, https://doi.org/10.1130/SPE97-p1.","productDescription":"82 p.","startPage":"1","endPage":"82","costCenters":[],"links":[{"id":386363,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"97","noUsgsAuthors":false,"publicationDate":"1967-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Zen, E.","contributorId":101381,"corporation":false,"usgs":true,"family":"Zen","given":"E.","email":"","affiliations":[],"preferred":false,"id":817294,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70205789,"text":"70205789 - 1967 - Salt resources of Thailand","interactions":[],"lastModifiedDate":"2019-10-03T11:37:29","indexId":"70205789","displayToPublicDate":"1967-10-03T11:33:49","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":5868,"text":"Report of Investigation - Thailand, Department of Mineral Resources","printIssn":" 0563-353","active":false,"publicationSubtype":{"id":10}},"title":"Salt resources of Thailand","docAbstract":"In recent years beds of rock salt, as much as 820 feet thick, have been found in the subsurface of northeastern Thailand in a thick sequence of 'red beds' of the Maha Sarakam formation at the top of the Korat group of Mesozoic age. These salt-bearing rocks are widespread in the subsurface of northeastern Thailand and extend under the Mekong river into Laos to form one of the major salt-bearing regions of the world. The Korat group was deposited during Triassic, Jurassic and Cretaceous times on floodplains and in shallow estuaries, bays, or partly isolated coastal lakes over a large arid or semiarid region that lay near sea level and sank very slowly under remarkably uniform conditions. Total reserves are estimated at more than 2,700 billion tons of inferred rock salt in seven areas or deposits that include only about 20 percent of the total area of about 40,000 square kilometers probably underlain by salt-bearing rocks.
","language":"English","publisher":"Thailand Department of Mineral Resources","publisherLocation":"Bangkok, Thailand","issn":"0563-3532","usgsCitation":"Gardner, L.S., 1967, Salt resources of Thailand: Report of Investigation - Thailand, Department of Mineral Resources, v. 11, 100 p.","productDescription":"100 p.","costCenters":[],"links":[{"id":367963,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Thailand","otherGeospatial":"Northeastern Thailand","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[102.58493,12.18659],[101.68716,12.64574],[100.83181,12.62708],[100.97847,13.41272],[100.0978,13.40686],[100.01873,12.307],[99.47892,10.84637],[99.15377,9.96306],[99.2224,9.23926],[99.87383,9.20786],[100.27965,8.29515],[100.45927,7.42957],[101.01733,6.85687],[101.62308,6.74062],[102.14119,6.22164],[101.81428,5.81081],[101.15422,5.69138],[101.07552,6.20487],[100.2596,6.64282],[100.08576,6.46449],[99.69069,6.84821],[99.51964,7.34345],[98.98825,7.90799],[98.50379,8.38231],[98.33966,7.79451],[98.15001,8.35001],[98.25915,8.97392],[98.55355,9.93296],[99.03812,10.96055],[99.58729,11.89276],[99.19635,12.80475],[99.21201,13.26929],[99.09776,13.8275],[98.43082,14.62203],[98.19207,15.1237],[98.53738,15.3085],[98.90335,16.17782],[98.49376,16.83784],[97.85912,17.56795],[97.3759,18.44544],[97.79778,18.62708],[98.25372,19.7082],[98.95968,19.75298],[99.54331,20.1866],[100.11599,20.41785],[100.54888,20.10924],[100.60629,19.50834],[101.28201,19.46258],[101.03593,18.40893],[101.05955,17.5125],[102.11359,18.1091],[102.413,17.93278],[102.99871,17.96169],[103.20019,18.30963],[103.95648,18.24095],[104.71695,17.42886],[104.77932,16.44186],[105.58904,15.57032],[105.54434,14.72393],[105.21878,14.27321],[104.28142,14.41674],[102.98842,14.22572],[102.3481,13.39425],[102.58493,12.18659]]]},\"properties\":{\"name\":\"Thailand\"}}]}","volume":"11","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Gardner, Louis S.","contributorId":81581,"corporation":false,"usgs":true,"family":"Gardner","given":"Louis","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":772354,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70221316,"text":"70221316 - 1967 - Test hold in aquifer with many water-bearing zones at Jacksonville, Florida","interactions":[],"lastModifiedDate":"2021-06-09T18:35:59.361297","indexId":"70221316","displayToPublicDate":"1967-10-01T13:30:27","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Test hold in aquifer with many water-bearing zones at Jacksonville, Florida","docAbstract":"One of the deepest water‐exploration wells in the southeastern United States was completed in 1966 at Jacksonville, Florida. It was drilled to a depth of nearly 2,500 feet to supply geologic and hydrologic information on the deeper unexplored part of the Floridan aquifer. This aquifer consists of a series of water producing zones separated by nonproducing zones. An important new fresh‐water producing zone was found, and the contact between the fresh water and salt water was located. The well was completed in three separate zones so that it could be used to monitor the the deeper part of the aquifer to detect any salt‐water encroachment. This paper describes the objectives, techniques, and results of drilling the test well.
","language":"English","publisher":"Wiley","doi":"10.1111/j.1745-6584.1967.tb01621.x","usgsCitation":"Leve, G., and Goolsby, D.A., 1967, Test hold in aquifer with many water-bearing zones at Jacksonville, Florida: Groundwater, v. 5, no. 4, p. 18-22, https://doi.org/10.1111/j.1745-6584.1967.tb01621.x.","productDescription":"5 p.","startPage":"18","endPage":"22","costCenters":[],"links":[{"id":386362,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Florida","city":"Jacksonville","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -82.1337890625,\n 30.088107753367257\n ],\n [\n -81.2109375,\n 30.088107753367257\n ],\n [\n -81.2109375,\n 30.543338954230222\n ],\n [\n -82.1337890625,\n 30.543338954230222\n ],\n [\n -82.1337890625,\n 30.088107753367257\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"5","issue":"4","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Leve, G.W.","contributorId":64294,"corporation":false,"usgs":true,"family":"Leve","given":"G.W.","affiliations":[],"preferred":false,"id":817292,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Goolsby, D. A.","contributorId":50508,"corporation":false,"usgs":true,"family":"Goolsby","given":"D.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":817293,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1000180,"text":"1000180 - 1967 - Some oligochaetes from Lake Michigan","interactions":[],"lastModifiedDate":"2026-03-12T15:26:52.872993","indexId":"1000180","displayToPublicDate":"1967-10-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3625,"text":"Transactions of the American Microscopical Society","active":true,"publicationSubtype":{"id":10}},"title":"Some oligochaetes from Lake Michigan","docAbstract":"Twenty-six species of Tubificidae, 12 Naididae, and 1 Lumbriculidae were found in three regions of Lake Michigan- Green Bay, the southern end of the lake proper, and the harbor at Ludington, Michigan. One new naidid species is described. Methods of identification of some species are discussed and illustrated. The abundance of oligochaetes and distribution of certain species vary with depth and location. Data are presented on the effects of the environment on the distribution of certain species. The presence or absence of some species reflected the quality of the environment; some were prevalent in polluted waters whereas others were restricted or absent. Possible changes in composition and abundance of species are outlined if organic enrichment increases in Lake Michigan.
","language":"English","publisher":"Wiley","doi":"10.2307/3224267","usgsCitation":"Hiltunen, J.K., 1967, Some oligochaetes from Lake Michigan: Transactions of the American Microscopical Society, v. 86, no. 4, p. 433-454, https://doi.org/10.2307/3224267.","productDescription":"22 p.","startPage":"433","endPage":"454","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":324,"text":"Great Lakes Science Center","active":true,"usgs":true}],"links":[{"id":130511,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.er.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Illinois, Indiana, Michigan, Wisconsin","otherGeospatial":"Lake Michigan","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -87.97025984791705,\n 45.20587410008886\n ],\n [\n -88.14054252464355,\n 41.50726553497216\n ],\n [\n -86.33381625694446,\n 41.50940165221235\n ],\n [\n -85.83636960569008,\n 44.47722673256698\n ],\n [\n -85.09881343279604,\n 44.956609541015666\n ],\n [\n -84.6020024557969,\n 45.768004056882816\n ],\n [\n -84.97649940103136,\n 46.22260358684156\n ],\n [\n -86.6882000784625,\n 46.0039491403779\n ],\n [\n -87.97025984791705,\n 45.20587410008886\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"86","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e8e4b07f02db5e8f3f","contributors":{"authors":[{"text":"Hiltunen, Jarl K.","contributorId":27820,"corporation":false,"usgs":true,"family":"Hiltunen","given":"Jarl","email":"","middleInitial":"K.","affiliations":[],"preferred":false,"id":308199,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70205377,"text":"70205377 - 1967 - Exploration for artesian water in the Sokoto Basin, Nigeria","interactions":[],"lastModifiedDate":"2024-03-22T00:11:13.530478","indexId":"70205377","displayToPublicDate":"1967-09-16T13:20:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3825,"text":"Groundwater","active":true,"publicationSubtype":{"id":10}},"title":"Exploration for artesian water in the Sokoto Basin, Nigeria","docAbstract":"The Sokoto basin in semiarid northwestern Nigeria contains Cretaceous and Tertiary semiconsolidated deposits that dip gently northwest off an oldland of pre-Cretaceous crystalline rocks. Until recent years the dug well has been the chief source of ground water for the Hausa cultivators and the pastoral Fulani inhabitants of the region. Borehole exploration sponsored by US AID and the Geological Survey of Nigeria with technical guidance from the writers of the U. S. Geological Survey has revealed that the basal section of the Gwandu Formation contains a productive artesian sand aquifer throughout a 5,700 square mile area. Transmissibilities of the aquifer proved to be as high as 180,000 Imperial gallons a day per foot but generally decrease towards the west. The free flow areas total about 1,000 square miles with pressure heads in boreholes up to + 83 feet above land surface and individual flows as great as 12,000 gallons per hour. Beneath the Gwandu, pressure aquifers in the Rima Group and the Gundumi Formation also produce flowing water in the lowland (fadama) of the Sokoto River. In the southern part of the basin, however, only one aquifer is present in the Cretaceous sequence, because the Gundumi aquifer is absent and the Rima aquifer apparently grades into the upper permeable section of the Illo Group. The quality of the water from all the pressure aquifers is generally quite good, although the iron content is high in places and salinity increases in the very deep aquifers.
","language":"English","publisher":"National Groundwater Association","doi":"10.1111/j.1745-6584.1967.tb03670.x","usgsCitation":"Anderson, H., and Ogilbee, W., 1967, Exploration for artesian water in the Sokoto Basin, Nigeria: Groundwater, v. 5, no. 3, p. 42-46, https://doi.org/10.1111/j.1745-6584.1967.tb03670.x.","productDescription":"5 p.","startPage":"42","endPage":"46","costCenters":[],"links":[{"id":367442,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Nigeria","otherGeospatial":"Sokoto Province","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[8.50029,4.77198],[7.46211,4.41211],[7.0826,4.46469],[6.69807,4.24059],[5.89817,4.26245],[5.3628,4.88797],[5.03357,5.6118],[4.32561,6.27065],[3.57418,6.2583],[2.6917,6.25882],[2.74906,7.87073],[2.72379,8.50685],[2.91231,9.13761],[3.22035,9.44415],[3.70544,10.06321],[3.60007,10.33219],[3.79711,10.73475],[3.57222,11.32794],[3.61118,11.66017],[3.68063,12.5529],[3.96728,12.95611],[4.10795,13.53122],[4.36834,13.74748],[5.44306,13.86592],[6.44543,13.49277],[6.82044,13.11509],[7.33075,13.09804],[7.80467,13.34353],[9.01493,12.82666],[9.52493,12.8511],[10.11481,13.27725],[10.70103,13.24692],[10.98959,13.38732],[11.5278,13.32898],[12.30207,13.03719],[13.08399,13.59615],[13.3187,13.55636],[13.99535,12.46157],[14.18134,12.48366],[14.57718,12.08536],[14.46819,11.90475],[14.41538,11.57237],[13.57295,10.79857],[13.30868,10.16036],[13.1676,9.64063],[12.95547,9.41777],[12.75367,8.71776],[12.21887,8.30582],[12.06395,7.79981],[11.83931,7.39704],[11.74577,6.98138],[11.05879,6.64443],[10.49738,7.05536],[10.11828,7.03877],[9.52271,6.45348],[9.23316,6.44449],[8.75753,5.47967],[8.50029,4.77198]]]},\"properties\":{\"name\":\"Nigeria\"}}]}","volume":"5","issue":"3","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Anderson, H. R.","contributorId":67487,"corporation":false,"usgs":true,"family":"Anderson","given":"H. R.","affiliations":[],"preferred":false,"id":770966,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Ogilbee, William","contributorId":106093,"corporation":false,"usgs":true,"family":"Ogilbee","given":"William","email":"","affiliations":[],"preferred":false,"id":770967,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70011660,"text":"70011660 - 1967 - Holocene changes in sea level: Evidence in Micronesia","interactions":[],"lastModifiedDate":"2026-02-09T16:06:55.109181","indexId":"70011660","displayToPublicDate":"1967-08-04T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3338,"text":"Science","active":true,"publicationSubtype":{"id":10}},"title":"Holocene changes in sea level: Evidence in Micronesia","docAbstract":"Investigation of 33 islands, scattered widely across the Caroline and Marshall Island groups in the Central Pacific revealed no emerged reefs in which corals had unquestionably formed in situ, or other direct evidence of postglacial high stands of sea level. Low unconsolidated rock terraces and ridges of reefflat islands, mostly lying between tide levels, were composed of rubble conglomerates; carbon-14 dating of 11 samples from the conglomerates so far may suggest a former slightly higher sea level (nine samples range between 1890 and 3450 and one approaches 4500 years ago). However, recent hurricanes have produced ridges of comparable height and material, and in the same areas relics from World War II have been found cemented in place. Thus these datings do not in themselves necessarily indicate formerly higher sea levels. Rubble tracts are produced by storms under present conditions without any change in datum, and there seems to be no compelling evidence that they were not so developed during various periods in the past.
","language":"English","publisher":"American Association for the Advancement of Science","doi":"10.1126/science.157.3788.542","issn":"00368075","usgsCitation":"Shepard, F., Curray, J.R., Newman, W., Bloom, A., Newell, N., Tracey, J.I., and Veeh, H., 1967, Holocene changes in sea level: Evidence in Micronesia: Science, v. 157, no. 3788, p. 542-544, https://doi.org/10.1126/science.157.3788.542.","productDescription":"3 p.","startPage":"542","endPage":"544","costCenters":[],"links":[{"id":221603,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"otherGeospatial":"Caroline Islands, Marshall Islands","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n 133.1239933290849,\n 9.7892225885888\n ],\n [\n 133.1239933290849,\n -0.2640485063964064\n ],\n [\n 148.38286324801322,\n -0.2640485063964064\n ],\n [\n 148.38286324801322,\n 9.7892225885888\n ],\n [\n 133.1239933290849,\n 9.7892225885888\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"157","issue":"3788","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a31d8e4b0c8380cd5e296","contributors":{"authors":[{"text":"Shepard, F.P.","contributorId":75684,"corporation":false,"usgs":true,"family":"Shepard","given":"F.P.","email":"","affiliations":[],"preferred":false,"id":361643,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Curray, Joseph R.","contributorId":92424,"corporation":false,"usgs":false,"family":"Curray","given":"Joseph","email":"","middleInitial":"R.","affiliations":[{"id":6728,"text":"Scripps Inst Oceanography","active":true,"usgs":false}],"preferred":false,"id":361644,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Newman, W.A.","contributorId":94434,"corporation":false,"usgs":true,"family":"Newman","given":"W.A.","email":"","affiliations":[],"preferred":false,"id":361645,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Bloom, A.L.","contributorId":67219,"corporation":false,"usgs":true,"family":"Bloom","given":"A.L.","email":"","affiliations":[],"preferred":false,"id":361642,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Newell, N.D.","contributorId":52324,"corporation":false,"usgs":true,"family":"Newell","given":"N.D.","email":"","affiliations":[],"preferred":false,"id":361641,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Tracey, J. I. Jr.","contributorId":17205,"corporation":false,"usgs":true,"family":"Tracey","given":"J.","suffix":"Jr.","email":"","middleInitial":"I.","affiliations":[],"preferred":false,"id":361639,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Veeh, H.H.","contributorId":31906,"corporation":false,"usgs":true,"family":"Veeh","given":"H.H.","email":"","affiliations":[],"preferred":false,"id":361640,"contributorType":{"id":1,"text":"Authors"},"rank":7}]}} ,{"id":70221306,"text":"70221306 - 1967 - Epifauna of the Patuxent River Estuary, Maryland, for 1963 and 1964","interactions":[],"lastModifiedDate":"2021-06-09T16:38:55.813498","indexId":"70221306","displayToPublicDate":"1967-06-01T11:32:11","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1228,"text":"Chesapeake Science","active":true,"publicationSubtype":{"id":10}},"title":"Epifauna of the Patuxent River Estuary, Maryland, for 1963 and 1964","docAbstract":"Methods of collection and analysis of epifaunal communities from six stations in the Patuxent estuary are described. The stations were distributed from Solomons near the mouth of the estuary, upstream to Lower Marlboro, near the limit of salt water intrusion. Species composition and abundance, seasons of attachment, and production of the epifaunal community were determined on material collected from panels submerged for 1, 3, and 12 month periods covering the years 1963 and 1964. Salinity was highest downstream, as was the number of species. Salinity decreased rapidly between the Patuxent River Bridge station and Lower Marlboro, where the number of species was reduced to half. Seasons of attachment corresponded with seasonal temperature changes, with the greatest attachment taking place during the summer months. Over 40 species were identified with 7 of them comprising the bulk of the biomass produced. For the 7 most productive species, seasons of attachment and total numbers collected from areas of one square decimeter from monthly and quarterly panels from each station are shown. The seven species were the barnacle Balanus improvisus; the tunicate, Molgula manhattensis; the hydroids, Cordylophora lacustris and Bimeria franciscana; the amphipod, Corophium lacustre; the anemone Sagartia leucolena; the tubeworm, Polydora ligni. Their respective importance varied with seasons of attachment and location. Comments on the distribution and abundance of the less significant forms are included. Dry and ash-free dry weight (organic carbon) production of the epifaunal community varied from month to month depending on the seasons of attachment of the various species. The highest production for a single month was observed at the upriver station, Lower Marlboro, where barnacles and amphipods produced 2,754 g/m2/30 days dry weight and 351 gc/m2/30 days organic weight during August 1963. At the same station, barnacles, amphipods, and hydroids produced, on quarterly panels, the highest yearly average weight of about 1150 gc/m2/yr organic carbon and on monthly panels, about 6,500 g/m2/yr dry weight or about 3.5 times the least organic weight and 8 times the least dry weight produced at the downriver Station, Queentree Landing.
","language":"English","publisher":"Estuarine Research Federation","doi":"10.2307/1351152","usgsCitation":"Cory, R.L., 1967, Epifauna of the Patuxent River Estuary, Maryland, for 1963 and 1964: Chesapeake Science, v. 8, no. 2, p. 71-89, https://doi.org/10.2307/1351152.","productDescription":"19 p.","startPage":"71","endPage":"89","costCenters":[],"links":[{"id":386353,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Maryland","otherGeospatial":"Patuxent River","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -76.80541992187499,\n 38.238180119798635\n ],\n [\n -76.39617919921875,\n 38.238180119798635\n ],\n [\n -76.39617919921875,\n 38.839707613545144\n ],\n [\n -76.80541992187499,\n 38.839707613545144\n ],\n [\n -76.80541992187499,\n 38.238180119798635\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"8","issue":"2","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Cory, R. L.","contributorId":49456,"corporation":false,"usgs":true,"family":"Cory","given":"R.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":817282,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70209344,"text":"70209344 - 1967 - Post-paleozoic radiometric ages and their relevance to fault movements, Northern Southeastern Alaska","interactions":[],"lastModifiedDate":"2020-04-01T12:13:03","indexId":"70209344","displayToPublicDate":"1967-04-01T12:02:43","publicationYear":"1967","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":"Post-paleozoic radiometric ages and their relevance to fault movements, Northern Southeastern Alaska","docAbstract":"Recently determined lead-alpha and potassium-argon ages from northern southeastern Alaska indicate major plutonic events in the Paleozoic, Mesozoic, and Tertiary; in contrast, previous studies suggested that only one complex Jurassic and Cretaceous event occurred. The ages presented in this paper indicate the following Mesozoic and Tertiary plutonic events: Middle or Late Jurassic (144–164 m.y.); Early Cretaceous (103–117 m.y.); Eocene (42–48 m.y.); and Oligocene to Miocene (24–31 m.y.). The present data show no distinctive a real pattern for the Mesozoic plutons, but those of known Tertiary age are restricted to Baranof and Kruzof islands, a distribution that suggests a belt of Tertiary plutonism along the margin of the Pacific Ocean.
Stratigraphic evidence and radiometric ages indicate that Baranof Island and possibly Chichagof Island have been uplifted several kilometers since Miocene time, whereas Admiralty Island to the east appears to have been relatively stable since Paleocene time. This movement apparently took place on the north-striking Chatham Strait fault, which separates the islands, and probably also had a large right-lateral component. Northwest-striking faults in Chichagof and Baranof islands were probably active during at least part of the movement on the Chatham Strait fault. Movement on one of the northwest-striking faults, the Patterson Bay fault of Baranof Island, took place some time between the Eocene and the Miocene and produced a 5-km, right-lateral separation.
The inferred uplift of Baranof Island relative to Admiralty Island is based on the present-day exposure on Baranof Island of mesozonal Tertiary plutons, which were probably intruded at a depth of several kilometers, contrasted with the present-day exposure on Admiralty Island of continental sedimentary and volcanic rocks that were being deposited near sea level during the Tertiary. The uplift of the Baranof Island plutons to the surface in post-Miocene time contrasts sharply with the stable or weakly negative tectonic conditions that have prevailed on Admiralty Island since the Paleocene.
","language":"English","publisher":"GSA","doi":"10.1130/0016-7606(1967)78[511:PRAATR]2.0.CO;2","usgsCitation":"Loney, R.A., Brew, D.A., and Lanphere, M.A., 1967, Post-paleozoic radiometric ages and their relevance to fault movements, Northern Southeastern Alaska: GSA Bulletin, v. 78, no. 4, p. 511-526, https://doi.org/10.1130/0016-7606(1967)78[511:PRAATR]2.0.CO;2.","productDescription":"16 p.","startPage":"511","endPage":"526","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":373712,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Northern Southeastern Alaska","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -136.7138671875,\n 54.09806018306312\n ],\n [\n -131.94580078125,\n 54.09806018306312\n ],\n [\n -131.94580078125,\n 58.297944045474146\n ],\n [\n -136.7138671875,\n 58.297944045474146\n ],\n [\n -136.7138671875,\n 54.09806018306312\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"78","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Loney, R. A.","contributorId":90757,"corporation":false,"usgs":true,"family":"Loney","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":786217,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Brew, David A. dbrew@usgs.gov","contributorId":3244,"corporation":false,"usgs":true,"family":"Brew","given":"David","email":"dbrew@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":786218,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lanphere, Marvin A. alder@usgs.gov","contributorId":2696,"corporation":false,"usgs":true,"family":"Lanphere","given":"Marvin","email":"alder@usgs.gov","middleInitial":"A.","affiliations":[],"preferred":true,"id":786219,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70114650,"text":"70114650 - 1967 - Results of the second phase of the drought-disaster test-drilling program near Morristown, N.J.","interactions":[],"lastModifiedDate":"2018-01-08T18:31:02","indexId":"70114650","displayToPublicDate":"1967-01-01T13:17:37","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":149,"text":"New Jersey Division of Water Policy and Supply Water Resources Circular","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"17","title":"Results of the second phase of the drought-disaster test-drilling program near Morristown, N.J.","docAbstract":"The continued drought in northeastern New Jersey through the summer of 1966 with its attendant water-supply problems resulted in an extension of the drought-disaster test-drilling program originally requested by the Office of Emergency Planning on August 30, 1965. Authorization to continue test drilling was fiven by the Office of Emergency Planning on September 26, 1966, with the stipulation that all field work be complete by January 31, 1977. Contractural costs were paid by the Office of Emergency Planning, whereas personnel costs were shared by the U.S. Geological Survey and the New Jersey Department of Conservation and Economic Development, Division of Water Policy and Supply.
The work undertaken in 1965 by the Geological Survey was \"...to preform the necessary drilling and testing of wells to identify the extent and nature of a reserve ground-water source in the vicinity of the Passaic River near the northern New Jersey metropolitan area.\" Results of this first phase were made available in the fall of 1966 in Water Resources Circular 16 of the New Jersey Department of Conservation and Economic Development. Three of the five areas tested (figure 1)--two in Parsippany-Troy Hills Township (areas 2 and 4) and one in East Hanover Township (area 1), Morris County--proved capable of providing an aggregate sustained yield of 7.5 million gallons daily (mgd) from wells constructed in sand and gravel deposits. Because significant supplies of ground water for emergency use were located in the first phase of the exploratory test-drilling program, it was though desirable to extend the originally planned studies so as to obtain maximum practicable information on emergency supplies.
During this second phase of the investigation, drilling was conducted in 16 sites in Chatham, Madison, and Florham Park Boroughs and in Hanover and East Hanover Townships, Morris County. (See figure 2.) The drilling in Hanover and East Hanover Townships, and part of the drilling done in Florham Park was to explore the availability of large undeveloped ground-water supplies. Drilling in Chatham, Madison, and Florham Park Boroughs was done primarily to determine the extent and continuity of buried valley-fill aquifers, so that a full evaluation of the effects of pumpage from other areas on these already heavily pumped areas could be made. In addition, it was anticipated that the drilling could help in defining the feasibility of artificial recharge of the heavily pumped areas and in the determination of the prospective method of recharge and points of emplacement.
Arrangements for easements with landowners, preparation of specifications for well drilling and seismic work, and supervision of well drilling and seismic contracts were all performed by the New Jersey District, Water Resources Division of the Geological Survey.
Prior to the test drilling, seismic exploration under contract with Alpine Geophysical Associates of Norwood, N. J. was conducted at five locations in the Chatham-Madison-Florham Park area and at one place in Parsippany-Troy Hills Township. The seismic work was done to determine the most favorable location for a test well at several potential test-well sites and to help in the interpretation of subsurface geology between test sites.
Contracts for the drilling of the test holes were awarded during November and drilling commences on November 30. Kaye Well drilling, Inc. of Jackson, N. J. was the recipient of a contract for eight of the test holes, and a second contract was awarded to Rinbrand Well Drilling Co., Inc. of Glen Rock, N. J.--also for eight test holes.
Acknowledgment is due to the many public officials of Chatham, Madison, Florham Park, Morristown, and East Hanover Township as well as officials of the Braidburn Corporation and Esso Research and Engineering Co., who cooperated by making their lands available for exploration.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Trenton, NJ","collaboration":"Prepared by the State of New Jersey Department of Conservation and Economic Development, Division of Water Policy and Supply, in cooperation with United States Department of the Interior Geological Survey","usgsCitation":"Vecchioli, J., Nichols, W., and Nemickas, B., 1967, Results of the second phase of the drought-disaster test-drilling program near Morristown, N.J.: New Jersey Division of Water Policy and Supply Water Resources Circular 17, Report: v, 23 p.; 3 Plates: 34.65 x 21.48 inches or smaller.","productDescription":"Report: v, 23 p.; 3 Plates: 34.65 x 21.48 inches or smaller","numberOfPages":"30","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":290164,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":327417,"rank":5,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70114650/figure-4.pdf","text":"Figure 4","linkFileType":{"id":1,"text":"pdf"}},{"id":327415,"rank":3,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70114650/figure-2.pdf","text":"Figure 2","linkFileType":{"id":1,"text":"pdf"}},{"id":327416,"rank":4,"type":{"id":29,"text":"Figure"},"url":"https://pubs.usgs.gov/unnumbered/70114650/figure-3.pdf","text":"Figure 3","linkFileType":{"id":1,"text":"pdf"}},{"id":290163,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70114650/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"New Jersey","city":"Morristown","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -74.501444,40.780231 ], [ -74.501444,40.818361 ], [ -74.456181,40.818361 ], [ -74.456181,40.780231 ], [ -74.501444,40.780231 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53ad40f9e4b0729c154181d6","contributors":{"authors":[{"text":"Vecchioli, John","contributorId":36113,"corporation":false,"usgs":true,"family":"Vecchioli","given":"John","email":"","affiliations":[],"preferred":false,"id":495394,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nichols, William D.","contributorId":98296,"corporation":false,"usgs":true,"family":"Nichols","given":"William D.","affiliations":[],"preferred":false,"id":495395,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Nemickas, Bronius","contributorId":105733,"corporation":false,"usgs":true,"family":"Nemickas","given":"Bronius","email":"","affiliations":[],"preferred":false,"id":495396,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70009781,"text":"70009781 - 1967 - An operational theory of laser-radar selenodesy","interactions":[],"lastModifiedDate":"2025-02-28T17:11:24.058801","indexId":"70009781","displayToPublicDate":"1967-01-01T00:00:00","publicationYear":"1967","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1963,"text":"Icarus","active":true,"publicationSubtype":{"id":10}},"title":"An operational theory of laser-radar selenodesy","docAbstract":"