{"pageNumber":"1609","pageRowStart":"40200","pageSize":"25","recordCount":40783,"records":[{"id":70173588,"text":"70173588 - 1968 - Evaporation study at Warm Springs Reservoir, Oregon","interactions":[],"lastModifiedDate":"2016-06-22T08:15:39","indexId":"70173588","displayToPublicDate":"1980-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":375,"text":"Open-File Report","active":false,"publicationSubtype":{"id":6}},"title":"Evaporation study at Warm Springs Reservoir, Oregon","docAbstract":"<p>The mass transfer-water budget method of computing reservoir evaporation was tested on Warm Springs Reservoir, whose contents and surface area change greatly from early spring to late summer. The mass-transfer coefficient computed for the reservoir is two to three times greater than expected and results in a computed evaporation much greater than that from a land pan. Because of the remoteness of the area, the recommended study technique was modified, which could have reduced the accuracy of the results.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Portland, OR","doi":"10.3133/70173588","collaboration":"Prepared in cooperation with Oregon State Engineer","usgsCitation":"Harris, D., 1968, Evaporation study at Warm Springs Reservoir, Oregon: Open-File Report, i, 17 p., https://doi.org/10.3133/70173588.","productDescription":"i, 17 p.","numberOfPages":"21","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":323086,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70173588.jpg"},{"id":324188,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70173588/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Oregon","otherGeospatial":"Warm Springs Reservoir","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -118.27709197998047,\n              43.57093929750569\n            ],\n            [\n              -118.27709197998047,\n              43.68003923450592\n            ],\n            [\n              -118.20190429687501,\n              43.68003923450592\n            ],\n            [\n              -118.20190429687501,\n              43.57093929750569\n            ],\n            [\n              -118.27709197998047,\n              43.57093929750569\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5757f034e4b04f417c24da79","contributors":{"authors":[{"text":"Harris, D.D.","contributorId":59002,"corporation":false,"usgs":true,"family":"Harris","given":"D.D.","email":"","affiliations":[],"preferred":false,"id":637376,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70114619,"text":"70114619 - 1968 - Ground-water resources of Monmouth County, New Jersey","interactions":[],"lastModifiedDate":"2015-10-17T19:43:54","indexId":"70114619","displayToPublicDate":"1970-01-01T11:02:47","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":126,"text":"New Jersey Division of Water Policy and Supply Special Report","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"23","title":"Ground-water resources of Monmouth County, New Jersey","docAbstract":"<p>Monmouth County includes an area of 538 square miles in east-central New Jersey. The climate is characterized by moderate temperature, moderate humidity, and moderate precipitation.</p>\n<p>The exposed rocks in the area are chiefly sands and clays, which range in age from Late Cretaceous through Recent. The formations strike northeast-southwest and dip gently to the southeast. These rocks range in total thickness from about 500 to 1,200 feet or more and are underlain by basement rocks of late Precambrian (?) age.</p>\n<p>The principal aquifers underlying Monmouth County occur in the Raritan and Magothy Formations, the Englishtown Formation, the Wenonah Formation and Mount Laurel Sand, the Vincentown Formation, and the Kirkwood Formation.</p>\n<p>Ground water constituted about 50 percent of the total water use in 1958. The daily withdrawal of ground water was at an average rate of 21.6 mgd (million gallons per day) in 1958 and about 32 mgd in 1965 (N. J. Division of Water Policy and Supply). The water demand is expected to increase to about 133 mgd by the year 2000. An analysis of streamflow records for the period 1932 to 1950 suggests that, excluding the Raritan and Magothy Formations, the major aquifers that occur under water-table conditions in the county discharge an average of about 178 mgd to streams.</p>\n<p>The aquifers in the Raritan and Magothy Formations contribute little or no water directly to streams in Monmouth County. These aquifers have been the most productive in the county. However, because salt water has been found in the lower parts of these formations in Ocean County, further development should proceed watchfully to assure that salt water does not threaten existing supplies.</p>\n<p>Aquifers in the Raritan and Magothy Formations and the Englishtown Formation supplied 76 percent of the ground water used in 1958. These aquifers, in conjunction with the Wenonah Formation and Mount Laurel Sand of Late Cretaceous age, are capable of providing relatively large yields to wells. The average yield of 63 large-diameter wells tapping these aquifers is 580 gpm, at depths randing from 100 to 1,140 feet. In general, the concentrations of chemical constituents in water from the aquifers would not restrict the use of the water for most purposes. High concentrations of iron do occur and require treatment. The concentrations of dissolved solids in 39 to 41 samples were 160 ppm (parts per million) or less.</p>","language":"English","publisher":"New Jersey Department of Conservation and Economic Development, Division of Water Policy and Supply","collaboration":"Prepared by the U.S. Geological Survey in cooperation with the State of New Jersey, Department of Conservation and Economic Development, Division of Water Policy and Supply","usgsCitation":"Jablonski, L.A., 1968, Ground-water resources of Monmouth County, New Jersey: New Jersey Division of Water Policy and Supply Special Report 23, ix, 117 p.","productDescription":"ix, 117 p.","numberOfPages":"130","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":290150,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":290149,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70114619/report.pdf"}],"country":"United States","state":"New Jersey","county":"Monmouth County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -74.613529,40.07913 ], [ -74.613529,40.478576 ], [ -73.972184,40.478576 ], [ -73.972184,40.07913 ], [ -74.613529,40.07913 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53ad40f2e4b0729c154181cc","contributors":{"authors":[{"text":"Jablonski, Leo A.","contributorId":16324,"corporation":false,"usgs":true,"family":"Jablonski","given":"Leo","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":495355,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70011427,"text":"70011427 - 1968 - Pedogenic formation of montmorillonite from a 2:1-2:2 intergrade clay mineral","interactions":[],"lastModifiedDate":"2018-01-25T14:39:21","indexId":"70011427","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1245,"text":"Clays and Clay Minerals","onlineIssn":"1552-8367","printIssn":"0009-8604","active":true,"publicationSubtype":{"id":10}},"title":"Pedogenic formation of montmorillonite from a 2:1-2:2 intergrade clay mineral","docAbstract":"<p>Montmorillonite was found to be the dominant clay mineral in surface horizons of certain soils of the North Carolina Coastal Plain whereas a 2:1-2:2 intergrade clay mineral was dominant in subjacent horizons. In all soils where this clay mineral sequence was found, the surface horizon was low in pH (below 4<strong>⋅</strong>5) and high in organic matter content. In contrast, data from studies of other soils of this region (Weed and Nelson, 1962) show that: (1) montmorillonite occurs infrequently; (2) maximum accumulation of the 2:1-2:2 intergrade normally occurs in the surface horizon and decreases with depth in the profile; (3) organic matter contents are low; and (4) pH values are only moderately acid (pH 5-6).</p><p>It is theorized that the montmorillonite in the surface horizon of the soils studied originated by pedogenic weathering of the 2:1-2:2 intergrade clay mineral. The combined effects of low pH (below 4<strong>⋅</strong>5) and high organic matter content in surface horizons are believed to be the agents responsible for this mineral transformation. The protonation and solubilization (reverse of hydrolysis) of Al-polymers in the interlayer of expansible clay minerals will occur at or below pH 4<strong>⋅</strong>5 depending on the charge and steric effects of the interlayer. A low pH alone may cause this solubilization and thus mineral transformation, but in the soils studied the organic matter is believed to facilitate and accelerage the transformation. The intermediates of organic matter decomposition provide an acid environment, a source of protons, and a source of watersoluble mobile organic substances (principally fulvic acids) which have the ability to complex the solubilized aluminum and move it down the profile. This continuous removal of solubilized aluminum would provide for a favorable gradient for aluminum solubilization.</p><p>The drainage class or position in a catena is believed to be less important than the chemical factors in formation of montmorillonite from 2:1-2:2 intergrade, because montmorillonite is present in all drainage classes if the surface horizon is low in pH and high in organic matter.</p>","language":"English","publisher":"The Clay Minerals Society","doi":"10.1346/CCMN.1969.0160602","usgsCitation":"Malcolm, R., Nettleton, W., and McCracken, R.J., 1968, Pedogenic formation of montmorillonite from a 2:1-2:2 intergrade clay mineral: Clays and Clay Minerals, v. 16, no. 6, p. 405-414, https://doi.org/10.1346/CCMN.1969.0160602.","productDescription":"10 p.","startPage":"405","endPage":"414","costCenters":[],"links":[{"id":221111,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"16","issue":"6","noUsgsAuthors":false,"publicationDate":"2024-07-01","publicationStatus":"PW","scienceBaseUri":"505a7629e4b0c8380cd77f6e","contributors":{"authors":[{"text":"Malcolm, Ronald L.","contributorId":46075,"corporation":false,"usgs":true,"family":"Malcolm","given":"Ronald L.","affiliations":[],"preferred":false,"id":361073,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nettleton, W.D.","contributorId":91988,"corporation":false,"usgs":true,"family":"Nettleton","given":"W.D.","email":"","affiliations":[],"preferred":false,"id":361074,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"McCracken, R. J.","contributorId":102205,"corporation":false,"usgs":false,"family":"McCracken","given":"R.","middleInitial":"J.","affiliations":[],"preferred":false,"id":361075,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70207280,"text":"70207280 - 1968 - On the maintenance of anomalous fluid pressures: I. thick sedimentary sequences","interactions":[],"lastModifiedDate":"2019-12-15T16:12:30","indexId":"70207280","displayToPublicDate":"1968-12-31T16:07:40","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1786,"text":"Geological Society of America Bulletin","active":true,"publicationSubtype":{"id":10}},"title":"On the maintenance of anomalous fluid pressures: I. thick sedimentary sequences","docAbstract":"<p><span>Various physical and chemical processes may be envisioned which will cause anomalous pressures on an underground fluid. In order to consider the maintenance of anomalous pressure, it is necessary to consider the problem as one of nonsteady fluid flow. The time rate of pressure change and maintenance depends upon the hydrodynamics of flow through porous media and the particular boundary conditions. This paper presents a series of general solutions to hydrodynamic models which are germane to the problem of creating and maintaining excess-fluid pressures in a thick sedimentary sequence. The creation and maintenance of fluid pressures approaching lithostatic pressure through a process of continuous sedimentation was evaluated. Our results indicate that a sedimentation rate of 500 m/10</span><sup>6</sup><span>&nbsp;yr (reasonable for the Gulf Coast) will create fluid pressures approaching lithostatic in a sedimentary column that has a hydraulic conductivity of 10</span><sup>-8</sup><span>&nbsp;cm sec</span><sup>-1</sup><span>, or lower. It is apparent that the creation of anomalous pressure and its maintenance depends, to a large degree, upon the hydraulic conductivity and, to a lesser extent, upon the specific storage of clay layers within the system. © 1968, The Geological Society of America, Inc.</span></p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1968)79[1097:OTMOAF]2.0.CO;2","issn":"00167606","usgsCitation":"Bredehoeft, J., and Hanshaw, B., 1968, On the maintenance of anomalous fluid pressures: I. thick sedimentary sequences: Geological Society of America Bulletin, v. 79, no. 9, p. 1097-1106, https://doi.org/10.1130/0016-7606(1968)79[1097:OTMOAF]2.0.CO;2.","productDescription":"10 p. ","startPage":"1097","endPage":"1106","costCenters":[],"links":[{"id":370287,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"79","issue":"9","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Bredehoeft, J.D.","contributorId":12836,"corporation":false,"usgs":true,"family":"Bredehoeft","given":"J.D.","affiliations":[],"preferred":false,"id":777528,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hanshaw, B.B.","contributorId":25928,"corporation":false,"usgs":true,"family":"Hanshaw","given":"B.B.","email":"","affiliations":[],"preferred":false,"id":777529,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70206944,"text":"70206944 - 1968 - Resurgent cauldrons","interactions":[],"lastModifiedDate":"2019-11-30T08:22:55","indexId":"70206944","displayToPublicDate":"1968-12-31T08:18:19","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2711,"text":"Memoir of the Geological Society of America","active":true,"publicationSubtype":{"id":10}},"title":"Resurgent cauldrons","docAbstract":"<p><span>Resurgent cauldrons are defined as cauldrons (calderas) in which the cauldron block, following subsidence, has been uplifted, usually in the form of a structural dome. Seven of the best known resurgent cauldrons are: Valles, Toba, Creede, San Juan, Silverton, Lake City, and Timber Mountain. Geologic summaries of these and Long Valley, California, a probable resurgent caldera, are presented. Using the Valles caldera as a model, but augmented by information from other cauldrons, seven stages of volcanic, structural, sedimentary, and plutonic events are recognized in the development of resurgent cauldrons. They are: (I) Regional tumescence and generation of ring fractures; (II) Calderaforming eruptions; (III) Caldera collapse; (IV) Preresurgence volcanism and sedimentation; (V) Resurgent doming; (VI) Major ring-fracture volcanism; (VII) Terminal solfatara and hot-spring activity. These stages define the terminal cycle of resurgent cauldrons, which in the Valles caldera spanned more than 1 million years. The known and inferred occurrence of the seven stages in the eight cauldrons discussed, together with some time control in four cauldrons, indicates that resurgent doming is early in the postcollapse history; hence, it seems part of a pattern and not fortuitous. Doming of the cauldron block by magma pressure is preferred to doming by stock or laccolithic intrusion, although these processes may be subsidiary. Magma rise that produces doming may be explained in several ways, but the principal cause is not known. Nor is it known why some otherwise similar calderas do not have resurgent domes, although size and thickness of the cauldron block and the degree to which it was deformed during caldera collapse may be factors. All known resurgent structures are larger than 8 miles in diameter and are associated with silicic and, presumably, high-viscosity magmas. Genetically, resurgent cauldrons belong to a cauldron group in which subsidence of a central mass takes place along ring fractures and is related to eruption of voluminous ash flows, thereby differing from Kilauean-type calderas. It is proposed that typical Krakatoan-type calderas differ in that collapse is chaotic and ring fractures are not essential to their formation. Krakatoan calderas typically occur in the andesitic volcanoes of island arcs or the eugeosynclinal environment, and their sub-volcanic analogues are not known, whereas resurgent and related Glen Coe-type cauldrons are more common in cratonic or post-orogenic environments as are their sub-volcanic analogues - granitic ring complexes. Granitic ring complexes, such as Lirue, Sande, Ossipee, and Alnsj0, are probably the closest sub-volcanic analogues of resurgent calderas. The source areas of most of the ash-flow sheets of western United States and Mexico are yet to be found. It is suggested that many of them will prove to be resurgent structures. Present evidence suggests that ore deposits are more commonly associated with resurgent cauldrons than with other cauldron types.</span></p>","language":"English","publisher":"Geological Society of America","doi":"10.1130/MEM116-p613","issn":"00721069","usgsCitation":"Smith, R., and Bailey, R.A., 1968, Resurgent cauldrons: Memoir of the Geological Society of America, v. 116, p. 613-662, https://doi.org/10.1130/MEM116-p613.","productDescription":"50 p. ","startPage":"613","endPage":"662","costCenters":[],"links":[{"id":369774,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"116","noUsgsAuthors":false,"publicationDate":"1968-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Smith, R.L.","contributorId":47422,"corporation":false,"usgs":true,"family":"Smith","given":"R.L.","email":"","affiliations":[],"preferred":false,"id":776347,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bailey, R. A.","contributorId":119050,"corporation":false,"usgs":true,"family":"Bailey","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":776348,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70233751,"text":"70233751 - 1968 - A method for estimating the uncertainty of seismic velocities measured by refraction techniques","interactions":[],"lastModifiedDate":"2022-07-27T17:14:44.377534","indexId":"70233751","displayToPublicDate":"1968-12-01T12:02:26","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1135,"text":"Bulletin of the Seismological Society of America","onlineIssn":"1943-3573","printIssn":"0037-1106","active":true,"publicationSubtype":{"id":10}},"title":"A method for estimating the uncertainty of seismic velocities measured by refraction techniques","docAbstract":"<p>Time residuals from&nbsp;<i>7</i>5-km segments of 18 crustal seismic-refraction profiles in the Basin and Range province are used to investigate the validity of the linear-regression model and to make large sample estimates of the variance in the travel time distributions.</p><p>A formula for unbiased estimates of velocity uncertainty is derived, assuming a linear trend with distance for the variances of the travel-time distributions. If the recording units are symmetric about the center of the recording interval, this formula is equivalent to the one derived assuming the variances are equal.</p><p>At the 95-per cent confidence level the chi-squared test implied 84 per cent of the time-residual samples were inconsistent with the hypothesis that their parent populations had Gaussian distributions. If the number of recording locations expceeds 8, confidence limits computed without the Gaussian assumption suggest the departures from normality are not significant for velocity uncertainty estimates.</p><p>The large sample estimates of the time-residual populations may be applicable to other areas. This evidence motivated the development of a method, requiring very little numerical calculation, for estimating uncertainties in velocities. The method requires, in addition to the large sample estimates of the travel time variances, information on the quality of the data, the location of the recording interval, and the number of recording units. The method is useful for the design of new experiments and independent estimates of uncertainty reported in the literature.</p>","language":"English","publisher":"Seismological Society of America","doi":"10.1785/BSSA0580061769","usgsCitation":"Borcherdt, R.D., and Healy, J.H., 1968, A method for estimating the uncertainty of seismic velocities measured by refraction techniques: Bulletin of the Seismological Society of America, v. 58, no. 6, p. 1769-1790, https://doi.org/10.1785/BSSA0580061769.","productDescription":"22 p.","startPage":"1769","endPage":"1790","costCenters":[{"id":234,"text":"Earthquake Hazards Program","active":true,"usgs":true}],"links":[{"id":404500,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Arizona, California, Idaho, Nevada, Oregon, Utah","otherGeospatial":"Basin and Range province","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -117.57568359374999,\n              32.45415593941475\n            ],\n            [\n              -111.20361328125,\n              32.713355353177555\n            ],\n            [\n              -111.07177734375,\n              44.29240108529005\n            ],\n            [\n              -123.33251953125,\n              43.6599240747891\n            ],\n            [\n              -123.28857421875,\n              37.70120736474139\n            ],\n            [\n              -121.46484375,\n              34.32529192442733\n            ],\n            [\n              -118.67431640625,\n              32.41706632846282\n            ],\n            [\n              -117.57568359374999,\n              32.45415593941475\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"58","issue":"6","noUsgsAuthors":false,"publicationDate":"1968-12-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Borcherdt, Roger D. 0000-0002-8668-0849 borcherdt@usgs.gov","orcid":"https://orcid.org/0000-0002-8668-0849","contributorId":2373,"corporation":false,"usgs":true,"family":"Borcherdt","given":"Roger","email":"borcherdt@usgs.gov","middleInitial":"D.","affiliations":[{"id":237,"text":"Earthquake Science Center","active":true,"usgs":true}],"preferred":true,"id":847627,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Healy, J. H.","contributorId":48968,"corporation":false,"usgs":true,"family":"Healy","given":"J.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":847628,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70206752,"text":"70206752 - 1968 - Lead and strontium isotope studies of the Boulder Batholith, Southwestern Montana","interactions":[],"lastModifiedDate":"2019-11-21T08:02:13","indexId":"70206752","displayToPublicDate":"1968-12-01T07:58:55","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Lead and strontium isotope studies of the Boulder Batholith, Southwestern Montana","docAbstract":"<p><span>The isotopic composition of lead in feldspar varies widely from pluton to pluton of the Late Cretaceous Boulder batholith, encompassing the following ranges in isotopic values: 16.9-18.1 for Pb&nbsp;</span><sup>206</sup><span>/Pb&nbsp;</span><sup>204</sup><span>; 15.4-15.7 for Pb&nbsp;</span><sup>207</sup><span>/Pb&nbsp;</span><sup>204</sup><span>; and 37.7-38.5 for Pb&nbsp;</span><sup>205</sup><span>/Pb&nbsp;</span><sup>204</sup><span>. Although each pluton has a characteristic isotopic composition, the fact that Pb&nbsp;</span><sup>206</sup><span>/Pb&nbsp;</span><sup>204</sup><span>&nbsp;for the Butte Quartz Monzonite varies by 1.3 percent, compared to a range of about 8.6 percent for the batholith as a whole, suggests that perfect isotopic mixing of the magma was not always attained. Whole rock initial Sr&nbsp;</span><sup>87</sup><span>/Sr&nbsp;</span><sup>88</sup><span>&nbsp;for the entire batholith ranges from 0.705 to 0.710, comparable to ranges for the Sierra Nevada and British Columbia batholiths. Ore leads of the Butte district are isotopically very similar to feldspar leads of the host Butte Quartz Monzonite. This isotopic similarity was interpreted by Murthy and Patterson (1961a) to indicate complete mixing of independently derived feldspar lead and ore lead rather than close genetic relationship. However, detailed study of the only sample in the present investigation, from the Donald pluton, that clearly has mixed leads shows significant differences in lead isotopic composition between megacryst K-feldspar and both the groundmass K-feldspar and plagioclase, indicating that isotopic mixing of leads is not complete, even within a single hand specimen. Spatial relations of isotopic differences among the various plutons strongly suggest that complete mixing of leads of different isotopic composition from the magma did not occur in the Butte Quartz Monzonite nor in any other pluton of the batholith, and that the isotopic similarity between Butte ore and feldspar lead of the host rock indeed stems from a genetic association. Lead and strontium isotope ratios generally behave in a similar way; that is, the more radiogenic the lead in a rock, the more radiogenic the strontium. The source of the lead which could produce the isotope variations observed for the batholith is calculated to have a mean age of about 2,200 m.y., which is compatible with ages of Precambrian crystalline rocks in the region, and an isotopic makeup with U&nbsp;</span><sup>238</sup><span>/pb&nbsp;</span><sup>204</sup><span>&nbsp;&lt;9, Th/U &gt; 4, and Rb/Sr of 0.03-0.09. However, no large volumes of prebatholith rocks exposed in the Boulder batholith region are of the required isotopic composition, which is typical of basaltic-gabbroic or quartz dioritic chemical composition. Models involving complete melting of possible source materials to account for the isotope variations are considered and rejected. Mechanisms involving par.tial melting of lower crustal or upper mantle source material appear to be the most viable in explaining the observed isotopic compositions. Assimilation of upper crustal material (i.e., the Precambrian Belt and pre-Belt rocks, in which the lead and strontium are more radiogenic than in the batholith rocks) may have accompanied partial melting of the lower crust or upper mantle and indeed must have played a major role if the source material had a composition isotopically comparable to that observed for oceanic tholelites (i.e., low Th/U, U&nbsp;</span><sup>238</sup><span>/Pb&nbsp;</span><sup>204</sup><span>&nbsp;and Rb/Sr), but would be relatively unimportant if the source material were sufficiently radiogenic to begin with as might be expected from basalt, gabbro, or quartz diorite compositions 2,200 m.y. old. © 1968 Society of Economic Geologists, Inc.</span></p>","language":"English ","publisher":"Society of Economic Geologists ","doi":"10.2113/gsecongeo.63.8.884","issn":"03610128","usgsCitation":"Doe, B.R., Tilling, R., Hedge, C., and Klepper, M.R., 1968, Lead and strontium isotope studies of the Boulder Batholith, Southwestern Montana: Economic Geology, v. 63, no. 8, p. 884-906, https://doi.org/10.2113/gsecongeo.63.8.884.","productDescription":"23 p.","startPage":"884","endPage":"906","costCenters":[],"links":[{"id":369372,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States ","state":"Montana ","city":"Helena, Deer Lodge, Butte, Boulder ","otherGeospatial":"Boulder Batholith","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -112.01934814453125,\n              46.60982785835103\n            ],\n            [\n              -112.57827758789062,\n              46.5720787149159\n            ],\n            [\n              -112.72247314453124,\n              46.380096460287824\n            ],\n            [\n              -112.7197265625,\n              46.059891147620725\n            ],\n            [\n              -112.50274658203125,\n              46.01603873833416\n            ],\n            [\n              -112.36129760742188,\n              46.21785176740299\n            ],\n            [\n              -112.16903686523436,\n              46.308047059262954\n            ],\n            [\n              -112.02209472656249,\n              46.605110653248275\n            ],\n            [\n              -112.01934814453125,\n              46.60982785835103\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"63","issue":"8","noUsgsAuthors":false,"publicationDate":"1968-12-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Doe, B. R.","contributorId":52173,"corporation":false,"usgs":true,"family":"Doe","given":"B.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":775673,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tilling, R.I. 0000-0003-4263-7221","orcid":"https://orcid.org/0000-0003-4263-7221","contributorId":98311,"corporation":false,"usgs":true,"family":"Tilling","given":"R.I.","affiliations":[],"preferred":false,"id":775674,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hedge, C. E.","contributorId":73611,"corporation":false,"usgs":true,"family":"Hedge","given":"C. E.","affiliations":[],"preferred":false,"id":775675,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Klepper, M. R.","contributorId":64278,"corporation":false,"usgs":true,"family":"Klepper","given":"M.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":775676,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":70221374,"text":"70221374 - 1968 - Electric‐analog and digital‐computer model analysis of stream depletion by wells","interactions":[],"lastModifiedDate":"2021-06-11T17:06:43.201817","indexId":"70221374","displayToPublicDate":"1968-11-01T12:03:21","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":"Electric‐analog and digital‐computer model analysis of stream depletion by wells","docAbstract":"<p>Electric<span>‐</span>analog<span>&nbsp;or&nbsp;</span>digital<span>‐</span>computer<span>&nbsp;models are used to compute the effect of ground‐water withdrawal or recharge on streamflow. The results can be generalized on a map showing lines of equal elapsed time. The lines indicate the time of recharging or discharging that is needed to affect the streamflow by a given fraction of the amount pumped or injected. The generalization is based on the similarity in shape of the relations between pumping time and&nbsp;</span>stream<span>&nbsp;</span>depletion<span>&nbsp;for (1) semi‐infinite homogeneous aquifers drained by a straight, fully penetrating&nbsp;</span>stream<span>, and (2) complex heterogeneous aquifers. Response curves from a&nbsp;</span>model<span>&nbsp;reflect the combined effect of&nbsp;</span>stream<span>&nbsp;sinuosity, irregular impermeable boundaries, areal variation in aquifer properties, and imperfect hydraulic connection between the&nbsp;</span>stream<span>&nbsp;and aquifer. The elapsed‐cime lines are identified by sdf (</span>stream<span>&nbsp;</span>depletion<span>&nbsp;factor) values. These values can be calculated from observations made on an&nbsp;</span>electric<span>‐</span>analog<span>&nbsp;</span>model<span>&nbsp;and then may be used in a&nbsp;</span>digital<span>‐</span>computer<span>&nbsp;program for determining the effects of ground‐water pumping or recharge on streamflow.</span></p>","language":"English","publisher":"NGWA The Groundwater Association","doi":"10.1111/j.1745-6584.1968.tb01258.x","usgsCitation":"Jenkins, C., 1968, Electric‐analog and digital‐computer model analysis of stream depletion by wells: Groundwater, v. 6, no. 6, p. 27-34, https://doi.org/10.1111/j.1745-6584.1968.tb01258.x.","productDescription":"8 p.","startPage":"27","endPage":"34","costCenters":[],"links":[{"id":386437,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"6","issue":"6","noUsgsAuthors":false,"publicationDate":"2006-07-06","publicationStatus":"PW","contributors":{"authors":[{"text":"Jenkins, C.T.","contributorId":106099,"corporation":false,"usgs":true,"family":"Jenkins","given":"C.T.","email":"","affiliations":[],"preferred":false,"id":817450,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70221364,"text":"70221364 - 1968 - A lead isotope study of galenas and selected feldspars from mining Districts in Utah","interactions":[],"lastModifiedDate":"2021-06-11T15:12:05.825137","indexId":"70221364","displayToPublicDate":"1968-11-01T10:07:55","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"A lead isotope study of galenas and selected feldspars from mining Districts in Utah","docAbstract":"<p><span>The leads&nbsp;</span>in<span>&nbsp;</span>feldspars<span>&nbsp;from the main Tertiary intrusive bodies&nbsp;</span>in<span>&nbsp;each of three&nbsp;</span>mining<span>&nbsp;regions&nbsp;</span>in<span>&nbsp;</span>Utah<span>&nbsp;are isotopically similar to the&nbsp;</span>lead<span>&nbsp;deposits immediately associated with them. These deposits are the largest and also the least radiogenic&nbsp;</span>in<span>&nbsp;each region, whereas the smaller deposits are more radiogenic. Throughout each region the 'ore leads appear to be mixtures&nbsp;</span>in<span>&nbsp;various proportions of&nbsp;</span>lead<span>&nbsp;derived from the intrusive magma and&nbsp;</span>a<span>&nbsp;radiogenic&nbsp;</span>lead<span>&nbsp;component derived from the upper crustal rocks through which the mineralizing fluids passed. Linear relationships are exhibited between the&nbsp;</span>lead<span>&nbsp;</span>isotope<span>&nbsp;ratios within each&nbsp;</span>mining<span>&nbsp;region, and these enable the ages of the upper crustal basement rocks to be determined.&nbsp;</span>A<span>&nbsp;simple tvo-stage model theory for the development of the&nbsp;</span>lead<span>&nbsp;ores yields the folloving data: Oquirrh Mountains region, t 1,650 4-150 m.y., p-Cottonwood-Park City region, t = 2,415 4-30 m.y., p- = 8.87. Tintlc region, t 2,075 4-30 m.y., Milford region, t 1 765 4-70 m.y., p-T ( Us ) = , = 8.83. An alternative \"mixing\" model is also proposed which requires only 1,650-m.y. and 2,400-m.y. events&nbsp;</span>in<span>&nbsp;these regions.&nbsp;</span>In<span>&nbsp;either case these ages confirm and supplement our present geochronological knowledge of the basement rocks of&nbsp;</span>Utah<span>.&nbsp;</span></p>","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.63.7.796","usgsCitation":"Stacey, J.S., Zartman, R., and Nkomo, I.T., 1968, A lead isotope study of galenas and selected feldspars from mining Districts in Utah: Economic Geology, v. 63, no. 7, p. 796-814, https://doi.org/10.2113/gsecongeo.63.7.796.","productDescription":"19 p.","startPage":"796","endPage":"814","costCenters":[],"links":[{"id":386427,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United  States","state":"Utah","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -111.0498046875,\n              42.049292638686836\n            ],\n            [\n              -114.08203125,\n              42.049292638686836\n            ],\n            [\n              -114.08203125,\n              37.020098201368114\n            ],\n            [\n              -109.00634765625,\n              37.00255267215955\n            ],\n            [\n              -109.0283203125,\n              41.04621681452063\n            ],\n            [\n              -111.09374999999999,\n              41.07935114946899\n            ],\n            [\n              -111.0498046875,\n              42.049292638686836\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"63","issue":"7","noUsgsAuthors":false,"publicationDate":"1968-11-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Stacey, J. S.","contributorId":72785,"corporation":false,"usgs":true,"family":"Stacey","given":"J.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":817431,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zartman, R. E.","contributorId":15632,"corporation":false,"usgs":true,"family":"Zartman","given":"R. E.","affiliations":[],"preferred":false,"id":817432,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Nkomo, Ignatius T.","contributorId":61044,"corporation":false,"usgs":true,"family":"Nkomo","given":"Ignatius","email":"","middleInitial":"T.","affiliations":[],"preferred":false,"id":817433,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}}
,{"id":70175860,"text":"70175860 - 1968 - Field test results of the Model B panametrics radioisotope gage for monitoring suspended-sediment concentration in rivers and streams","interactions":[],"lastModifiedDate":"2018-04-02T10:40:24","indexId":"70175860","displayToPublicDate":"1968-10-29T13:45:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":1,"text":"Federal Government Series"},"title":"Field test results of the Model B panametrics radioisotope gage for monitoring suspended-sediment concentration in rivers and streams","docAbstract":"<p>No abstract available</p>","language":"English","publisher":"Federal Inter-Agency Sedimentation Project","usgsCitation":"Skinner, J.V., 1968, Field test results of the Model B panametrics radioisotope gage for monitoring suspended-sediment concentration in rivers and streams, 37 p.","productDescription":"37 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":392,"text":"Minnesota Water Science Center","active":true,"usgs":true}],"links":[{"id":327044,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57b82db6e4b03fd6b7da36a5","contributors":{"authors":[{"text":"Skinner, J. V.","contributorId":32504,"corporation":false,"usgs":true,"family":"Skinner","given":"J.","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":646459,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70221368,"text":"70221368 - 1968 - Temperature, salinity, and origin of the ore-forming fluids at Pine Point, Northwest Territories, Canada, from fluid inclusion studies","interactions":[],"lastModifiedDate":"2021-06-11T15:57:58.424528","indexId":"70221368","displayToPublicDate":"1968-08-01T10:53:30","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1472,"text":"Economic Geology","active":true,"publicationSubtype":{"id":10}},"title":"Temperature, salinity, and origin of the ore-forming fluids at Pine Point, Northwest Territories, Canada, from fluid inclusion studies","docAbstract":"<p><span>Although the&nbsp;</span>Pine<span>&nbsp;</span>Point<span>&nbsp;</span>ore<span>&nbsp;is relatively poor in useable&nbsp;</span>fluid<span>&nbsp;inclusions, some sphalerite crystals from replacements, vugs, and from \" colloform\" crusts were found to contain primary or pseudosecondary liquid-gas inclusions adequate for&nbsp;</span>study<span>. Most (132 of 133) of these had low freezing temperatures, indicating exceedingly saline brines. The 112 inclusions suitable for filling-</span>temperature<span>&nbsp;determination homogenized&nbsp;</span>at<span>&nbsp;+51° to +97° C. A very small pressure correction must be added to obtain the trapping&nbsp;</span>temperature<span>.Dolomite crystals from some of the same vugs contain large numbers of primary inclusions, many of which have leaked. The twenty-three that presumably have not leaked had filling temperatures of 90°-100° C, but somewhat lower salinities. Inclusions in late calcite appeared to have similar gas-liquid ratios, but had still lower salinities.The significance of these data lies in the limitations they place on the choice of possible mechanisms of&nbsp;</span>origin<span>&nbsp;of these large deposits. This choice, in turn, may influence the success in prospecting for blind&nbsp;</span>ore<span>&nbsp;bodies. There is general agreement that the deposits are of Mississippi Valley type. Although the high salinities may reflect solution of salts from evaporites, as are now found to the south, the elevated temperatures seem to require deep circulation, perhaps through known faults in the underlying Pre-cambrian. The densities of these brines, even&nbsp;</span>at<span>&nbsp;their elevated temperatures, are well above that of fresh, cold surface water, thus restricting the possible modes of circulation during&nbsp;</span>ore<span>&nbsp;deposition.</span></p>","language":"English","publisher":"Society of Economic Geologists","doi":"10.2113/gsecongeo.63.5.439","usgsCitation":"Roedder, E., 1968, Temperature, salinity, and origin of the ore-forming fluids at Pine Point, Northwest Territories, Canada, from fluid inclusion studies: Economic Geology, v. 63, no. 5, p. 439-450, https://doi.org/10.2113/gsecongeo.63.5.439.","productDescription":"12 p.","startPage":"439","endPage":"450","costCenters":[],"links":[{"id":386431,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Canada","otherGeospatial":"northwest Canada","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -140.9765625,\n              57.51582286553883\n            ],\n            [\n              -112.14843749999999,\n              57.51582286553883\n            ],\n            [\n              -112.14843749999999,\n              70.8446726342528\n            ],\n            [\n              -140.9765625,\n              70.8446726342528\n            ],\n            [\n              -140.9765625,\n              57.51582286553883\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"63","issue":"5","noUsgsAuthors":false,"publicationDate":"1968-08-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Roedder, E.","contributorId":100986,"corporation":false,"usgs":true,"family":"Roedder","given":"E.","affiliations":[],"preferred":false,"id":817438,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70180877,"text":"70180877 - 1968 - Analog simulation of ground-water development of the Saginaw Formation, Lansing metropolitan area, Michigan","interactions":[],"lastModifiedDate":"2022-11-22T16:16:20.031731","indexId":"70180877","displayToPublicDate":"1968-07-17T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":375,"text":"Open-File Report","active":false,"publicationSubtype":{"id":6}},"title":"Analog simulation of ground-water development of the Saginaw Formation, Lansing metropolitan area, Michigan","docAbstract":"<p>This report was prepared as a part of the study of the water resources of Clinton, Eaton and Ingham Counties being made for the Tri-County Planning Commission by the Water Resources Division of the U. S. Geological Survey. The report describes one phase of the investigation, that is, the projections of future time-withdrawal-drawdown relationships obtained from an electric analog model study of the Saginaw Formation, the principal aquifer in the Lansing Metropolitan area.</p><p>The study of the Tri-County Region is a part of the continuing program of water resources investigation conducted by the U. S. Geological Survey in cooperation with the Geological Survey Division of the Michigan Department of Conservation and other state and local agencies.</p>","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/70180877","collaboration":"Prepared in cooperation with Tri-County Planning Commission and Michigan Geological Survey","usgsCitation":"Vanlier, K., and Wheeler, M., 1968, Analog simulation of ground-water development of the Saginaw Formation, Lansing metropolitan area, Michigan: Open-File Report, ii, 40 p., https://doi.org/10.3133/70180877.","productDescription":"ii, 40 p.","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":409544,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70180877/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":334825,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70180877/report-thumb.jpg"}],"country":"United States","state":"Michigan","otherGeospatial":"Saginaw Formation","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"58999946e4b0efcedb71a0c6","contributors":{"authors":[{"text":"Vanlier, K.E.","contributorId":24332,"corporation":false,"usgs":true,"family":"Vanlier","given":"K.E.","affiliations":[],"preferred":false,"id":662668,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wheeler, M.L.","contributorId":179105,"corporation":false,"usgs":false,"family":"Wheeler","given":"M.L.","email":"","affiliations":[],"preferred":false,"id":662669,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70227018,"text":"70227018 - 1968 - Chapter 3: Television observations from Surveyor VII","interactions":[],"lastModifiedDate":"2021-12-27T15:53:37.120928","indexId":"70227018","displayToPublicDate":"1968-05-01T09:29:10","publicationYear":"1968","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"title":"Chapter 3: Television observations from Surveyor VII","docAbstract":"<p>Surveyor VII, the last spacecraft of the Surveyor series, successfully landed at 01:05:36 GMT, January 10, 1968, on the outer rim flank of the large crater Tycho, in the southern part of the Moon. The spacecraft landed about 30 hours after local lunar sunrise and transmitted about 21,000 pictures during the remainder of the first lunar day of operation. On January 22, after local sunset, almost 700 pictures were taken of the Earth, the Sun's corona and parts of the lunar surface illuminated by earthlight. On February 12, Surveyor VII was revived for operation on the second lunar day approximately 120 hours after local lunar sunrise. The camera was then operated in the 200-line (low-resolution) mode because of loss in horizontal sweep in the 600-line (high-resolution) mode. About 45 pictures were taken in the 200-line mode during the second lunar day before loss of power caused suspension of camera operation.<br></p>","largerWorkType":{"id":18,"text":"Report"},"largerWorkTitle":"Surveyor VII: A preliminary report","largerWorkSubtype":{"id":1,"text":"Federal Government Series"},"language":"English","publisher":"National Aeronautics and Space Administration","usgsCitation":"Shoemaker, E.M., Batson, R.M., Holt, H.E., Morris, E.C., Rennilson, J.J., and Whitaker, E.A., 1968, Chapter 3: Television observations from Surveyor VII, chap. <i>of</i> Surveyor VII: A preliminary report, p. 13-81.","productDescription":"NASA SP-173, 69 p.","startPage":"13","endPage":"81","costCenters":[],"links":[{"id":393426,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":393425,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://ntrs.nasa.gov/api/citations/19680024081/downloads/19680024081.pdf","size":"688 MB","linkFileType":{"id":1,"text":"pdf"}}],"otherGeospatial":"Moon, Tycho","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"compilers":[{"text":"National Aeronautics and Space Administration","contributorId":128140,"corporation":true,"usgs":false,"organization":"National Aeronautics and Space Administration","id":829242,"contributorType":{"id":3,"text":"Compilers"},"rank":1}],"authors":[{"text":"Shoemaker, Eugene Merle","contributorId":20342,"corporation":false,"usgs":true,"family":"Shoemaker","given":"Eugene","email":"","middleInitial":"Merle","affiliations":[],"preferred":false,"id":829236,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Batson, R. M.","contributorId":76714,"corporation":false,"usgs":true,"family":"Batson","given":"R.","email":"","middleInitial":"M.","affiliations":[],"preferred":false,"id":829237,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Holt, H. E.","contributorId":64694,"corporation":false,"usgs":true,"family":"Holt","given":"H.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":829238,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Morris, E. C.","contributorId":84381,"corporation":false,"usgs":true,"family":"Morris","given":"E.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":829239,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Rennilson, J. J.","contributorId":107336,"corporation":false,"usgs":true,"family":"Rennilson","given":"J.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":829240,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Whitaker, E. A.","contributorId":43086,"corporation":false,"usgs":true,"family":"Whitaker","given":"E.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":829241,"contributorType":{"id":1,"text":"Authors"},"rank":6}]}}
,{"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":"<p>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.</p><p>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.</p>","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":70209028,"text":"70209028 - 1968 - Flow Structure and Composition of the Southern Coulee, Mono Craters, California—A Pumiceous Rhyolite Flow","interactions":[],"lastModifiedDate":"2020-03-11T18:31:29","indexId":"70209028","displayToPublicDate":"1968-01-01T18:24:50","publicationYear":"1968","noYear":false,"publicationType":{"id":5,"text":"Book chapter"},"publicationSubtype":{"id":24,"text":"Book Chapter"},"title":"Flow Structure and Composition of the Southern Coulee, Mono Craters, California—A Pumiceous Rhyolite Flow","docAbstract":"<p>The Southern Coulee is the southernmost and largest of the four Recent pumiceous rhyolitic coulees, or stubby flows, of the Mono Craters, eastern California. It is one of the youngest volcanic deposits of the Mono Craters and is largely bare and uneroded. The coulee is 3.6 km long and averages 1.2 km in width and 75 m in thickness. It was protruded from a north-trending fissure beneath the crest of the Mono Craters ridge. About two-thirds of the lava flowed west and one-third flowed east.</p><p>The coulee has three main parts: the dome, located over the orifice, where flow was about vertical; the flow, where movement was lateral; and the talus slope, which surrounds the coulee and formed from the advancing steep-flow front. In addition, three small areas of air-fall pumice ash occur on the coulee and appear to be remnants of an ash eruption that took place during an early phase of the coulee eruption.</p><p>Three distinctive lithologic units based on rock density related to the degree of vesicularity have been mapped: a unit of lowest density (average ρ = 0.65); a unit of intermediate density (average ρ = 1.20); and a unit of highest density (average ρ = 1.75). The contacts between the units are abrupt despite the fact that core drilling has shown the coulee to be a jumbled mass of blocks down to a depth of at least 45 m. The two less dense units, which consist of highly inflated thick-bedded pumice, form two connecting boat-shaped bodies along the entire south margin of the coulee. These units are probably not over 25 m thick and are underlain by the unit of highest density, which appears to form the rest of coulee. The dense unit consists of thin- to medium-bedded dense pumice and lesser amounts of obsidian. The above distribution of the lithologic units in the coulee was probably caused by the eruption of rocks characteristic of all the units from, the southern part of the north-trending fissure, while only rocks of the unit of highest density erupted from the northern part. The protrusion of the coulee involved several subordinate and, in places, interfering streams that had slightly different courses and levels. This complex flow resulted in a modification or disruption of the original spatial relations of the lithologic units, as they erupted from the orifice.</p><p>The petrographic and chemical data indicate a uniform composition for the lava that belies its heterogeneous aspect. The lava is composed almost entirely of clear glass (average n<sub>D</sub><span>&nbsp;</span>= 1.488 ± 0.001), and contains only trace amounts of microlites and cristobalite-sanidine spherulites. Eight chemical anlyses show a silica range from 74.7 to 76.2 percent and indicate a rhyolite composition of the sodipotassic subrang. This composition is characteristic of glassy-fluidal rhyolites.</p>","largerWorkType":{"id":4,"text":"Book"},"largerWorkTitle":"Studies in Volcanology","largerWorkSubtype":{"id":15,"text":"Monograph"},"language":"English","publisher":"Geological Society of America","doi":"10.1130/MEM116-p415","usgsCitation":"Loney, R.A., 1968, Flow Structure and Composition of the Southern Coulee, Mono Craters, California—A Pumiceous Rhyolite Flow, chap. <i>of</i> Studies in Volcanology, v. 116, p. 415-440, https://doi.org/10.1130/MEM116-p415.","productDescription":"27 p.","startPage":"415","endPage":"440","costCenters":[],"links":[{"id":373149,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Mono Craters, Southern Coulee","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -119.2071533203125,\n              37.63815995799935\n            ],\n            [\n              -118.79104614257811,\n              37.63815995799935\n            ],\n            [\n              -118.79104614257811,\n              37.899239630600185\n            ],\n            [\n              -119.2071533203125,\n              37.899239630600185\n            ],\n            [\n              -119.2071533203125,\n              37.63815995799935\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","volume":"116","noUsgsAuthors":false,"publicationDate":"1968-01-01","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":784577,"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":"<p>In<span>&nbsp;1966 more than 50 billion gallons of&nbsp;</span>water<span>&nbsp;was pumped daily from an estimated 10 to 15 million&nbsp;</span>water<span>&nbsp;wells&nbsp;</span>in<span>&nbsp;the United States. This was more than one‐sixth of the national withdrawal of&nbsp;</span>water<span>. On the basis of past rates of increase, a much greater future use of&nbsp;</span>ground<span>&nbsp;</span>water<span>&nbsp;is suggested. Our annual investment&nbsp;</span>in<span>&nbsp;</span>water<span>&nbsp;wells is one‐half to three‐quarter billion dollars, not including pumps and plumbing.&nbsp;</span>In<span>&nbsp;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&nbsp;</span>well<span>&nbsp;</span>logging<span>&nbsp;to&nbsp;</span>ground‐water<span>&nbsp;</span>hydrology<span>&nbsp;is comparable to its use&nbsp;</span>in<span>&nbsp;petroleum exploration&nbsp;</span>in<span>&nbsp;the 1930's; however, we can take advantage of equipment and interpretation techniques developed&nbsp;</span>in<span>&nbsp;the oil industry that are available now for use&nbsp;</span>in<span>&nbsp;</span>ground‐water<span>&nbsp;investigations. Although most petroleum&nbsp;</span>well<span>&nbsp;</span>logging<span>&nbsp;techniques may be utilized&nbsp;</span>in<span>&nbsp;</span>hydrology<span>; modifications&nbsp;</span>in<span>&nbsp;equipment and interpretation are necessary because of basic economic and environmental differences between petroleum and&nbsp;</span>ground‐water<span>&nbsp;evaluation. If&nbsp;</span>logging<span>&nbsp;is to be widely applied to&nbsp;</span>ground‐water<span>&nbsp;exploration and evaluation, the expense of equipment and services must be reduced. Fortunately, this can be accomplished, because most&nbsp;</span>water<span>&nbsp;wells are not as deep as oil wells and the temperatures and pressures are lower. The&nbsp;</span>Water<span>&nbsp;Resources Division of the U. S. Geological Survey is conducting research on the application of borehole geophysics to&nbsp;</span>ground‐water<span>&nbsp;</span>hydrology<span>. The following&nbsp;</span>logging<span>&nbsp;devices are utilized&nbsp;</span>in<span>&nbsp;the evaluation of&nbsp;</span>ground‐water<span>&nbsp;environments: spontaneous potential, resistivity, gamma, gamma‐gamma, neutron, radioactive tracer, flowmeter, caliper, fluid resistivity, gradient and differential temperature, and sonic velocity. Lightweight&nbsp;</span>logging<span>&nbsp;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&nbsp;</span>well<span>&nbsp;</span>logging<span>&nbsp;service is to be widely used&nbsp;</span>in<span>&nbsp;</span>ground‐water<span>&nbsp;exploration and development,&nbsp;</span>water<span>&nbsp;</span>well<span>&nbsp;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&nbsp;</span>well<span>&nbsp;</span>logging<span>&nbsp;can provide much of this information.&nbsp;</span>In<span>&nbsp;addition, the&nbsp;</span>well<span>&nbsp;</span>logging<span>&nbsp;industry must adapt their equipment and services to the requirements of&nbsp;</span>ground‐water<span>&nbsp;</span>hydrology<span>. The need for additional&nbsp;</span>logging<span>&nbsp;capability&nbsp;</span>in<span>&nbsp;this field exists at the present time and is expected to increase. Hopefully industry will be able to fill the gap.</span></p>","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":70175606,"text":"70175606 - 1968 - Records of wells, water levels, and chemical quality of water in the lower Santiam River basin, middle Willamette Valley, Oregon","interactions":[],"lastModifiedDate":"2020-10-09T17:48:48.446583","indexId":"70175606","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":115,"text":"Ground Water Report","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"13","title":"Records of wells, water levels, and chemical quality of water in the lower Santiam River basin, middle Willamette Valley, Oregon","docAbstract":"<p><span class=\"EXLDetailsDisplayVal\">Basic <span class=\"searchword\">water</span> data on the <span class=\"searchword\">lower</span> <span class=\"searchword\">Santiam</span> <span class=\"searchword\">River</span> <span class=\"searchword\">basin</span> is preliminary to a comprehensive hydrologic study of this productive and intensely irrigated area where expanding population and industry increases the demand for <span class=\"searchword\">water</span>. Highest yielding <span class=\"searchword\">wells</span> are in shallow alluvial aquifers near the main streams; yields range from several hundred to more than a thousand gpm. <span class=\"searchword\">Wells</span> in lacustrine and older alluvial aquifers that underlie low, flat terraces have yields from a few tens to a few hundred gpm. <span class=\"searchword\">Wells</span> in the Salem Hills and in the Cascade Range foothills yield moderate to small quantities of <span class=\"searchword\">water</span> and tap a variety of geologic units. Tabulated material includes <span class=\"searchword\">records</span> of representative <span class=\"searchword\">wells</span>, drillers' logs, and <span class=\"searchword\">chemical</span> and spectrographic analyses of the ground <span class=\"searchword\">water</span>.</span></p>","language":"English","publisher":"State of Oregon","usgsCitation":"Helm, D.C., 1968, Records of wells, water levels, and chemical quality of water in the lower Santiam River basin, middle Willamette Valley, Oregon: Ground Water Report 13, ii, 186 p.","productDescription":"ii, 186 p.","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[{"id":518,"text":"Oregon Water Science Center","active":true,"usgs":true}],"links":[{"id":326677,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":379286,"rank":2,"type":{"id":15,"text":"Index Page"},"url":"https://www.worldcat.org/title/records-of-wells-water-levels-and-chemical-quality-of-water-in-the-lower-santiam-river-basin-middle-willamette-valley-oregon/oclc/981926200&referer=brief_results"}],"country":"United States","state":"Oregon","otherGeospatial":"Willamette Valley","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -123.28308105468749,\n              44.07574700247845\n            ],\n            [\n              -122.420654296875,\n              44.07574700247845\n            ],\n            [\n              -122.420654296875,\n              45.57944511437787\n            ],\n            [\n              -123.28308105468749,\n              45.57944511437787\n            ],\n            [\n              -123.28308105468749,\n              44.07574700247845\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"57b58b58e4b03bcb0104bc61","contributors":{"authors":[{"text":"Helm, Donald C.","contributorId":49792,"corporation":false,"usgs":true,"family":"Helm","given":"Donald","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":645812,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70011540,"text":"70011540 - 1968 - Effects of selective fusion on the thermal history of the earth's mantle","interactions":[],"lastModifiedDate":"2020-03-19T08:15:15","indexId":"70011540","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1427,"text":"Earth and Planetary Science Letters","active":true,"publicationSubtype":{"id":10}},"title":"Effects of selective fusion on the thermal history of the earth's mantle","docAbstract":"<p>A comparative study on the thermal history of the earth's mantle was made by numerical solutions of the heat equation including and excluding selective fusion of silicates. Selective fusion was approximated by melting in a multicomponent system and redistribution of radioactive elements. Effects of selective fusion on the thermal models are (1) lowering (by several hundred degrees centigrade) and stabilizing the internal temperature distribution, and (2) increasing the surface heat-flow. It was found that models with selective fusion gave results more compatible with observations of both present temperature and surface heat-flow. The results therefore suggest continuous differentiation of the earth's mantle throughout geologic time, and support the hypothesis that the earth's atmosphere, oceans, and crust have been accumulated throughout the earth's history by degassing and selective fusion of the mantle.</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0012-821X(68)90087-3","issn":"0012821X","usgsCitation":"Lee, W., 1968, Effects of selective fusion on the thermal history of the earth's mantle: Earth and Planetary Science Letters, v. 4, no. 4, p. 270-276, https://doi.org/10.1016/0012-821X(68)90087-3.","productDescription":"7 p.","startPage":"270","endPage":"276","numberOfPages":"7","costCenters":[],"links":[{"id":220845,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"4","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a07c8e4b0c8380cd51821","contributors":{"authors":[{"text":"Lee, W.H.K.","contributorId":35303,"corporation":false,"usgs":true,"family":"Lee","given":"W.H.K.","affiliations":[],"preferred":false,"id":361358,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"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":"<p>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.</p><p>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 (≈ Ca<sub>4</sub>Mg<sub>70</sub>Fe<sub>26</sub>) occurs in the olivine cumulate zone, having formed partly at the expense of pre-existing olivine, augite, and pigeonite (≈ Ca<sub>8</sub>Mg<sub>66</sub>Fe<sub>26</sub>). 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.</p><p>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 Or<sub>1.0</sub>Ab<sub>22</sub>An<sub>77</sub><span>&nbsp;</span>to Or<sub>64</sub>Ab<sub>33</sub>An<sub>3</sub>. 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.</p><p>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 Ilm<sub>91</sub>Hm<sub>9</sub>) 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.</p><p>Fractional crystallization produced a groundmass glass of granitic composition. Average, in percent, is: SiO<sub>2</sub>, 75.5; Al<sub>2</sub>O<sub>3</sub>, 12.5; K<sub>2</sub>O, 5.7; Na<sub>2</sub>O, 3.1; CaO, 0.3; MgO, 0.05; total FeO, 1.2; and TiO<sub>2</sub>, 0.8. Normative Or&gt; 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 SiO<sub>2</sub>-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.</p><p>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,<span>&nbsp;</span><span class=\"u-small-caps\">MOORE</span><span>&nbsp;</span>and<span>&nbsp;</span><span class=\"u-small-caps\">EVANS</span>, 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.</p><p>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.</p>","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 States","state":"Hawaii","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"MultiPolygon\",\"coordinates\":[[[[-155.778234,20.245743],[-155.772734,20.245409],[-155.746893,20.232325],[-155.737004,20.222773],[-155.735822,20.212417],[-155.732704,20.205392],[-155.653966,20.16736],[-155.630382,20.146916],[-155.624565,20.145911],[-155.607797,20.137987],[-155.600909,20.126573],[-155.598033,20.124539],[-155.590923,20.122497],[-155.58168,20.123617],[-155.568368,20.130545],[-155.558933,20.13157],[-155.523661,20.120028],[-155.516795,20.11523],[-155.502561,20.114155],[-155.468211,20.104296],[-155.443957,20.095318],[-155.405459,20.078772],[-155.4024,20.075541],[-155.387578,20.067119],[-155.33021,20.038517],[-155.29548,20.024438],[-155.282629,20.021969],[-155.270316,20.014525],[-155.240933,19.990173],[-155.204486,19.969438],[-155.194593,19.958368],[-155.179939,19.949372],[-155.149215,19.922872],[-155.144394,19.920523],[-155.131235,19.906801],[-155.124618,19.897288],[-155.12175,19.886099],[-155.107541,19.872467],[-155.098716,19.867811],[-155.095032,19.867882],[-155.086341,19.855399],[-155.084357,19.849736],[-155.085674,19.838584],[-155.088979,19.826656],[-155.094414,19.81491],[-155.09207,19.799409],[-155.091216,19.776368],[-155.093517,19.771832],[-155.093387,19.737751],[-155.087118,19.728013],[-155.079426,19.726193],[-155.063972,19.728917],[-155.045382,19.739824],[-155.006423,19.739286],[-154.997278,19.72858],[-154.987168,19.708524],[-154.981102,19.690687],[-154.984718,19.672161],[-154.983778,19.641647],[-154.974342,19.633201],[-154.963933,19.627605],[-154.950359,19.626461],[-154.947874,19.62425],[-154.947718,19.621947],[-154.951014,19.613614],[-154.947106,19.604856],[-154.93394,19.597505],[-154.928205,19.592702],[-154.924422,19.586553],[-154.903542,19.570622],[-154.875,19.556797],[-154.852618,19.549172],[-154.837384,19.538354],[-154.826732,19.537626],[-154.814417,19.53009],[-154.809561,19.522377],[-154.809379,19.519086],[-154.822968,19.48129],[-154.838545,19.463642],[-154.86854,19.438126],[-154.887817,19.426425],[-154.928772,19.397646],[-154.944185,19.381852],[-154.964619,19.365646],[-154.980861,19.349291],[-155.020537,19.331317],[-155.061729,19.316636],[-155.113272,19.290613],[-155.1337,19.276099],[-155.159635,19.268375],[-155.172413,19.26906],[-155.187427,19.266156],[-155.19626,19.261295],[-155.205892,19.260907],[-155.243961,19.271313],[-155.264619,19.274213],[-155.296761,19.266289],[-155.303808,19.261835],[-155.31337,19.250698],[-155.341268,19.234039],[-155.349148,19.217756],[-155.360631,19.20893],[-155.378638,19.202435],[-155.390701,19.201171],[-155.417369,19.187858],[-155.427093,19.179546],[-155.432519,19.170623],[-155.453516,19.151952],[-155.465663,19.146964],[-155.505281,19.137908],[-155.51474,19.132501],[-155.51214,19.128174],[-155.512137,19.124296],[-155.519652,19.117025],[-155.526136,19.115889],[-155.528902,19.11371],[-155.544806,19.091059],[-155.551129,19.08878],[-155.557817,19.08213],[-155.555326,19.069377],[-155.555177,19.053932],[-155.557371,19.046565],[-155.566446,19.032531],[-155.576599,19.027412],[-155.581903,19.02224],[-155.596032,18.998833],[-155.596521,18.980654],[-155.601866,18.971572],[-155.613966,18.970399],[-155.625256,18.961951],[-155.625,18.959934],[-155.638054,18.941723],[-155.658486,18.924835],[-155.672005,18.917466],[-155.681825,18.918694],[-155.687716,18.923358],[-155.690171,18.932195],[-155.693117,18.940542],[-155.726043,18.969437],[-155.763598,18.981837],[-155.806109,19.013967],[-155.853943,19.023762],[-155.88155,19.036644],[-155.884077,19.039266],[-155.886278,19.05576],[-155.903693,19.080777],[-155.908355,19.081138],[-155.921389,19.121183],[-155.917292,19.155963],[-155.903339,19.217792],[-155.90491,19.230147],[-155.902565,19.258427],[-155.895435,19.274639],[-155.890842,19.298905],[-155.887356,19.337101],[-155.888701,19.348031],[-155.898792,19.377984],[-155.913849,19.401107],[-155.909087,19.415455],[-155.921707,19.43055],[-155.924269,19.438794],[-155.925166,19.468081],[-155.922609,19.478611],[-155.924124,19.481406],[-155.930523,19.484921],[-155.935641,19.485628],[-155.936403,19.481905],[-155.939145,19.481577],[-155.95149,19.486649],[-155.952897,19.488805],[-155.953663,19.510003],[-155.960457,19.546612],[-155.962264,19.551779],[-155.965211,19.554745],[-155.96935,19.555963],[-155.970969,19.586328],[-155.978206,19.608159],[-155.997728,19.642816],[-156.028982,19.650098],[-156.032928,19.653905],[-156.034994,19.65936],[-156.033326,19.66923],[-156.027427,19.672154],[-156.029281,19.678908],[-156.036079,19.690252],[-156.04796,19.698938],[-156.051652,19.703649],[-156.052485,19.718667],[-156.064364,19.730766],[-156.05722,19.742536],[-156.052315,19.756836],[-156.049651,19.780452],[-156.021732,19.8022],[-156.006267,19.81758],[-155.982821,19.845651],[-155.976651,19.85053],[-155.964817,19.855183],[-155.949251,19.857034],[-155.945297,19.853443],[-155.940311,19.852305],[-155.925843,19.858928],[-155.926938,19.870221],[-155.92549,19.875],[-155.915662,19.887126],[-155.901987,19.912081],[-155.894099,19.923135],[-155.894474,19.926927],[-155.892533,19.932162],[-155.866919,19.954172],[-155.856588,19.968885],[-155.840708,19.976952],[-155.838692,19.975527],[-155.835312,19.976078],[-155.831948,19.982775],[-155.828965,19.995542],[-155.825473,20.025944],[-155.828182,20.035424],[-155.850385,20.062506],[-155.866931,20.078652],[-155.88419,20.10675],[-155.899149,20.145728],[-155.906035,20.205157],[-155.901452,20.235787],[-155.890663,20.25524],[-155.882631,20.263026],[-155.873921,20.267744],[-155.853293,20.271548],[-155.811459,20.26032],[-155.783242,20.246395],[-155.778234,20.245743]]],[[[-157.789581,21.438396],[-157.789734,21.437679],[-157.789276,21.435833],[-157.790543,21.434313],[-157.791718,21.434881],[-157.793045,21.43391],[-157.793167,21.43574],[-157.791565,21.43651],[-157.791779,21.437752],[-157.793289,21.437658],[-157.791779,21.438435],[-157.791092,21.438442],[-157.790741,21.43874],[-157.789581,21.438396]]],[[[-160.125,21.95909],[-160.122262,21.962881],[-160.112746,21.995245],[-160.09645,22.001489],[-160.072123,22.003334],[-160.058543,21.99638],[-160.051992,21.983681],[-160.052729,21.980321],[-160.056336,21.977939],[-160.060549,21.976729],[-160.063349,21.978354],[-160.065811,21.976562],[-160.078393,21.955153],[-160.085787,21.927295],[-160.080012,21.910808],[-160.079065,21.89608],[-160.098897,21.884711],[-160.124283,21.876789],[-160.147609,21.872814],[-160.16162,21.864746],[-160.174796,21.846923],[-160.189782,21.82245],[-160.205211,21.789053],[-160.200427,21.786479],[-160.205851,21.779518],[-160.218044,21.783755],[-160.23478,21.795418],[-160.24961,21.815145],[-160.244943,21.848943],[-160.231028,21.886263],[-160.228965,21.889117],[-160.21383,21.899193],[-160.205528,21.907507],[-160.202716,21.912422],[-160.190158,21.923592],[-160.167471,21.932863],[-160.13705,21.948632],[-160.127302,21.955508],[-160.125,21.95909]]],[[[-159.431707,22.220015],[-159.40732,22.230555],[-159.388119,22.223252],[-159.385977,22.220009],[-159.367563,22.214906],[-159.359842,22.214831],[-159.357227,22.217744],[-159.353795,22.217669],[-159.339964,22.208519],[-159.315613,22.186817],[-159.308855,22.155555],[-159.297808,22.149748],[-159.295875,22.144547],[-159.295271,22.13039],[-159.297143,22.113815],[-159.317451,22.080944],[-159.321667,22.063411],[-159.324775,22.05867],[-159.333267,22.054639],[-159.337996,22.046575],[-159.341401,22.028978],[-159.333224,21.973005],[-159.333109,21.964176],[-159.334714,21.961099],[-159.350828,21.950817],[-159.356613,21.939546],[-159.382349,21.924479],[-159.408284,21.897781],[-159.425862,21.884527],[-159.446599,21.871647],[-159.471962,21.88292],[-159.490914,21.888898],[-159.517973,21.890996],[-159.555415,21.891355],[-159.574991,21.896585],[-159.577784,21.900486],[-159.584272,21.899038],[-159.610241,21.898356],[-159.637849,21.917166],[-159.648132,21.93297],[-159.671872,21.957038],[-159.681493,21.960054],[-159.705255,21.963427],[-159.72014,21.970789],[-159.758218,21.980694],[-159.765735,21.986593],[-159.788139,22.018411],[-159.790932,22.031177],[-159.786543,22.06369],[-159.780096,22.072567],[-159.748159,22.100388],[-159.741223,22.115666],[-159.733457,22.142756],[-159.726043,22.152171],[-159.699978,22.165252],[-159.66984,22.170782],[-159.608794,22.207878],[-159.591596,22.219456],[-159.583965,22.22668],[-159.559643,22.229185],[-159.554166,22.228212],[-159.548594,22.226263],[-159.54115,22.216764],[-159.534594,22.219403],[-159.523769,22.217602],[-159.51941,22.215646],[-159.518348,22.211182],[-159.515574,22.208008],[-159.507811,22.205987],[-159.501055,22.211064],[-159.500821,22.225538],[-159.488558,22.23317],[-159.480158,22.232715],[-159.467007,22.226529],[-159.45619,22.228811],[-159.441809,22.226321],[-159.431707,22.220015]]],[[[-157.014553,21.185503],[-156.999108,21.182221],[-156.991318,21.18551],[-156.987768,21.18935],[-156.982343,21.207798],[-156.984464,21.210063],[-156.984032,21.212198],[-156.974002,21.218503],[-156.969064,21.217018],[-156.962847,21.212131],[-156.951654,21.191662],[-156.950808,21.182636],[-156.946159,21.175963],[-156.918248,21.168279],[-156.903466,21.16421],[-156.898174,21.16594],[-156.89613,21.169561],[-156.896537,21.172208],[-156.867944,21.16452],[-156.841592,21.167926],[-156.821944,21.174693],[-156.771495,21.180053],[-156.742231,21.176214],[-156.738341,21.17202],[-156.736648,21.16188],[-156.719386,21.163911],[-156.712696,21.161547],[-156.714158,21.152238],[-156.726033,21.13236],[-156.748932,21.1086],[-156.775995,21.089751],[-156.790815,21.081686],[-156.794136,21.075796],[-156.835351,21.06336],[-156.865795,21.057801],[-156.877137,21.0493],[-156.891946,21.051831],[-156.89517,21.055771],[-156.953719,21.067761],[-157.00295,21.083282],[-157.02617,21.089015],[-157.032045,21.091094],[-157.037667,21.097864],[-157.079696,21.105835],[-157.095373,21.10636],[-157.125,21.1026],[-157.143483,21.096632],[-157.254061,21.090601],[-157.298054,21.096917],[-157.313343,21.105755],[-157.299187,21.132488],[-157.299471,21.135972],[-157.293774,21.146127],[-157.284346,21.157755],[-157.276474,21.163175],[-157.274504,21.162762],[-157.259911,21.174875],[-157.254709,21.181376],[-157.251007,21.190952],[-157.25026,21.207739],[-157.256935,21.215665],[-157.261457,21.217661],[-157.263163,21.220873],[-157.26069,21.225684],[-157.257085,21.227268],[-157.241534,21.220969],[-157.226445,21.220185],[-157.212082,21.221848],[-157.202125,21.219298],[-157.192439,21.207644],[-157.185553,21.205602],[-157.157103,21.200706],[-157.148125,21.200745],[-157.144627,21.202555],[-157.128207,21.201488],[-157.113438,21.197375],[-157.097971,21.198012],[-157.064264,21.189076],[-157.053053,21.188754],[-157.047757,21.190739],[-157.039987,21.190909],[-157.014553,21.185503]]],[[[-156.544169,20.522802],[-156.550016,20.520273],[-156.559994,20.521892],[-156.586238,20.511711],[-156.603844,20.524372],[-156.631143,20.514943],[-156.642347,20.508285],[-156.647464,20.512017],[-156.668809,20.504738],[-156.682939,20.506775],[-156.703673,20.527237],[-156.702265,20.532451],[-156.696662,20.541646],[-156.6801,20.557021],[-156.651567,20.565574],[-156.614598,20.587109],[-156.610734,20.59377],[-156.576871,20.60657],[-156.56714,20.604895],[-156.553604,20.594729],[-156.543034,20.580115],[-156.542808,20.573674],[-156.548909,20.56859],[-156.556021,20.542657],[-156.553018,20.539382],[-156.540189,20.534741],[-156.539643,20.527644],[-156.544169,20.522802]]],[[[-156.612012,21.02477],[-156.612065,21.027273],[-156.606238,21.034371],[-156.592256,21.03288],[-156.580448,21.020172],[-156.562773,21.016167],[-156.549813,21.004939],[-156.546291,21.005082],[-156.528246,20.967757],[-156.518707,20.954662],[-156.512226,20.95128],[-156.510391,20.940358],[-156.507913,20.937886],[-156.49948,20.934577],[-156.495883,20.928005],[-156.493263,20.916011],[-156.481055,20.898199],[-156.474796,20.894546],[-156.422668,20.911631],[-156.386045,20.919563],[-156.374297,20.927616],[-156.370729,20.932669],[-156.352649,20.941414],[-156.345655,20.941596],[-156.342365,20.938737],[-156.332817,20.94645],[-156.324578,20.950184],[-156.307198,20.942739],[-156.286332,20.947701],[-156.275116,20.937361],[-156.263107,20.940888],[-156.242555,20.937838],[-156.230159,20.931936],[-156.230089,20.917864],[-156.226757,20.916677],[-156.222062,20.918309],[-156.217953,20.916573],[-156.216341,20.907035],[-156.173103,20.876926],[-156.170458,20.874605],[-156.166746,20.865646],[-156.132669,20.861369],[-156.129381,20.847513],[-156.115735,20.827301],[-156.100123,20.828502],[-156.090291,20.831872],[-156.059788,20.81054],[-156.033287,20.808246],[-156.003532,20.795545],[-156.002947,20.789418],[-155.987944,20.776552],[-155.984587,20.767496],[-155.986851,20.758577],[-155.985413,20.744245],[-155.987216,20.722717],[-155.991534,20.713654],[-156.00187,20.698064],[-156.01415,20.685681],[-156.020044,20.686857],[-156.030702,20.682452],[-156.040341,20.672719],[-156.043786,20.664902],[-156.053385,20.65432],[-156.059753,20.652044],[-156.081472,20.654387],[-156.089365,20.648519],[-156.120985,20.633685],[-156.129898,20.627523],[-156.142665,20.623605],[-156.144588,20.624032],[-156.148085,20.629067],[-156.156772,20.629639],[-156.169732,20.627358],[-156.173393,20.6241],[-156.184556,20.629719],[-156.192938,20.631769],[-156.210258,20.628518],[-156.225338,20.62294],[-156.236145,20.61595],[-156.265921,20.601629],[-156.284391,20.596488],[-156.288037,20.59203],[-156.293454,20.588783],[-156.302692,20.586199],[-156.322944,20.588273],[-156.351716,20.58697],[-156.359634,20.581977],[-156.370725,20.57876],[-156.377633,20.578427],[-156.415313,20.586099],[-156.417523,20.589728],[-156.415746,20.594044],[-156.417799,20.598682],[-156.423141,20.602079],[-156.427708,20.598873],[-156.431872,20.598143],[-156.438385,20.601337],[-156.444242,20.607941],[-156.442884,20.613842],[-156.450651,20.642212],[-156.445894,20.64927],[-156.443673,20.656018],[-156.448656,20.704739],[-156.451038,20.725469],[-156.452895,20.731287],[-156.458438,20.736676],[-156.462242,20.753952],[-156.462058,20.772571],[-156.464043,20.781667],[-156.473562,20.790756],[-156.489496,20.798339],[-156.501688,20.799933],[-156.506026,20.799463],[-156.515994,20.794234],[-156.525215,20.780821],[-156.537752,20.778408],[-156.631794,20.82124],[-156.678634,20.870541],[-156.688969,20.888673],[-156.687804,20.89072],[-156.688132,20.906325],[-156.691334,20.91244],[-156.697418,20.916368],[-156.69989,20.920629],[-156.69411,20.952708],[-156.680905,20.980262],[-156.665514,21.007054],[-156.652419,21.008994],[-156.645966,21.014416],[-156.642592,21.019936],[-156.644167,21.022312],[-156.642809,21.027583],[-156.619581,21.027793],[-156.612012,21.02477]]],[[[-157.010001,20.929757],[-156.989813,20.932127],[-156.971604,20.926254],[-156.937529,20.925274],[-156.91845,20.922546],[-156.897169,20.915395],[-156.837047,20.863575],[-156.825237,20.850731],[-156.809576,20.826036],[-156.808469,20.820396],[-156.809463,20.809169],[-156.817427,20.794606],[-156.838321,20.764575],[-156.846413,20.760201],[-156.851481,20.760069],[-156.869753,20.754701],[-156.890295,20.744855],[-156.909081,20.739533],[-156.949009,20.738997],[-156.96789,20.73508],[-156.984747,20.756677],[-156.994001,20.786671],[-156.988933,20.815496],[-156.991834,20.826603],[-157.006243,20.849603],[-157.010911,20.854476],[-157.054552,20.877219],[-157.059663,20.884634],[-157.061128,20.890635],[-157.062511,20.904385],[-157.05913,20.913407],[-157.035789,20.927078],[-157.025626,20.929528],[-157.010001,20.929757]]],[[[-158.044485,21.306011],[-158.0883,21.2988],[-158.1033,21.2979],[-158.1127,21.3019],[-158.1211,21.3169],[-158.1225,21.3224],[-158.111949,21.326622],[-158.114196,21.331123],[-158.119427,21.334594],[-158.125459,21.330264],[-158.13324,21.359207],[-158.1403,21.3738],[-158.149719,21.385208],[-158.161743,21.396282],[-158.1792,21.4043],[-158.181274,21.409626],[-158.181,21.420868],[-158.182648,21.430073],[-158.192352,21.44804],[-158.205383,21.459793],[-158.219446,21.46978],[-158.233,21.4876],[-158.231171,21.523857],[-158.23175,21.533035],[-158.234314,21.540058],[-158.250671,21.557373],[-158.27951,21.575794],[-158.277679,21.578789],[-158.254425,21.582684],[-158.190704,21.585892],[-158.17,21.5823],[-158.12561,21.586739],[-158.10672,21.596577],[-158.106689,21.603024],[-158.1095,21.6057],[-158.108185,21.607487],[-158.079895,21.628101],[-158.0668,21.6437],[-158.066711,21.65234],[-158.0639,21.6584],[-158.0372,21.6843],[-158.018127,21.699955],[-157.9923,21.708],[-157.98703,21.712494],[-157.968628,21.712704],[-157.947174,21.689568],[-157.939,21.669],[-157.9301,21.6552],[-157.924591,21.651183],[-157.9228,21.6361],[-157.9238,21.6293],[-157.910797,21.611183],[-157.900574,21.605885],[-157.87735,21.575277],[-157.878601,21.560181],[-157.872528,21.557568],[-157.8669,21.5637],[-157.85614,21.560661],[-157.85257,21.557514],[-157.836945,21.529945],[-157.837372,21.512085],[-157.849579,21.509598],[-157.852625,21.499971],[-157.84549,21.466747],[-157.84099,21.459483],[-157.82489,21.455379],[-157.8163,21.4502],[-157.8139,21.4403],[-157.8059,21.4301],[-157.786513,21.415633],[-157.779846,21.417309],[-157.774455,21.421352],[-157.772209,21.431236],[-157.774905,21.453698],[-157.772209,21.457741],[-157.764572,21.461335],[-157.754239,21.461335],[-157.737617,21.459089],[-157.731777,21.455944],[-157.731328,21.444713],[-157.73582,21.438424],[-157.740762,21.424048],[-157.741211,21.414614],[-157.7386,21.4043],[-157.730191,21.401871],[-157.728221,21.402104],[-157.726421,21.402845],[-157.724324,21.403311],[-157.723794,21.40329],[-157.723286,21.403227],[-157.722735,21.403121],[-157.722544,21.403036],[-157.721845,21.401596],[-157.721083,21.399541],[-157.7189,21.3961],[-157.7089,21.3833],[-157.7087,21.3793],[-157.7126,21.3689],[-157.7106,21.3585],[-157.7088,21.3534],[-157.6971,21.3364],[-157.6938,21.3329],[-157.6619,21.3131],[-157.6518,21.3139],[-157.652629,21.308709],[-157.6537,21.302],[-157.6946,21.2739],[-157.6944,21.2665],[-157.7001,21.264],[-157.7097,21.2621],[-157.7139,21.2638],[-157.7142,21.2665],[-157.7114,21.272],[-157.7122,21.2814],[-157.7143,21.2845],[-157.7213,21.2869],[-157.7572,21.278],[-157.765,21.2789],[-157.7782,21.2735],[-157.7931,21.2604],[-157.8096,21.2577],[-157.8211,21.2606],[-157.8241,21.2646],[-157.8253,21.2714],[-157.8319,21.2795],[-157.8457,21.29],[-157.89,21.3065],[-157.894518,21.319632],[-157.898969,21.327391],[-157.90482,21.329172],[-157.918939,21.318615],[-157.917921,21.313781],[-157.913469,21.310983],[-157.910925,21.305768],[-157.952263,21.306531],[-157.950736,21.312509],[-157.951881,21.318742],[-157.967971,21.327986],[-157.973334,21.327426],[-157.989424,21.317984],[-158.0245,21.3093],[-158.044485,21.306011]]]]},\"properties\":{\"name\":\"Hawaii\",\"nation\":\"USA  \"}}]}","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":70009856,"text":"70009856 - 1968 - Lead isotopes and the origin of granulite and eclogite inclusions in deep-seated pipes","interactions":[],"lastModifiedDate":"2020-11-29T17:16:20.083757","indexId":"70009856","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1427,"text":"Earth and Planetary Science Letters","active":true,"publicationSubtype":{"id":10}},"title":"Lead isotopes and the origin of granulite and eclogite inclusions in deep-seated pipes","docAbstract":"<p>The isotopic composition of lead and the concentrations of lead, uranium, and thorium in Delegate basic pipes from Australia and in South African kimberlite pipes have been determined. The observed<sup>238</sup>U/<sup>204</sup>Pb and observed<sup>232</sup>Th/<sup>238</sup>U of eclogite inclusions in the pipes range from 2.9 to 18.7 and from 3.5 to 5.9, respectively. This result as well as the isotopic composition of lead suggests that the upper mantle is chemically heterogeneous with regard to the trace elements.</p><p>Pyrochemically extracted leads from eclogite inclusions in the Delegate basic pipes and in a South African kimberlite pipe appear to be different in isotopic compositions from leads extracted from the host rock (matrix). These data are consistent with the hypothesis that the eclogitic inclusions in deep-seated pipes are of “accidental” origin and represent upper mantle materials caught up in the host materials during their intrusion.</p><p>Lead extracted from a two-pyroxene granulite inclusion in one of the Delegate pipes has an isotopic composition indistinguishable from lead in the host rock. This observation is consistent either with a “cognate” origin for the granulite inclusion or with a modified “accidental” origin in which the isotopic composition of the original lead in the inclusion has been contaminated by lead from the host magma. Other evidence would indicate that an “accidental” origin be preferred.</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0012-821X(68)90062-9","issn":"0012821X","usgsCitation":"Lovering, J., and Tatsumoto, M., 1968, Lead isotopes and the origin of granulite and eclogite inclusions in deep-seated pipes: Earth and Planetary Science Letters, v. 4, no. 5, p. 350-356, https://doi.org/10.1016/0012-821X(68)90062-9.","productDescription":"7 p.","startPage":"350","endPage":"356","numberOfPages":"7","costCenters":[],"links":[{"id":218975,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"4","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a45c3e4b0c8380cd674b1","contributors":{"authors":[{"text":"Lovering, J.F.","contributorId":19282,"corporation":false,"usgs":true,"family":"Lovering","given":"J.F.","email":"","affiliations":[],"preferred":false,"id":357292,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Tatsumoto, M.","contributorId":76798,"corporation":false,"usgs":true,"family":"Tatsumoto","given":"M.","email":"","affiliations":[],"preferred":false,"id":357293,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":70009893,"text":"70009893 - 1968 - Effects of selective fusion on the thermal history of the Moon, Mars, and Venus","interactions":[],"lastModifiedDate":"2020-11-29T17:15:06.12172","indexId":"70009893","displayToPublicDate":"1968-01-01T00:00:00","publicationYear":"1968","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1427,"text":"Earth and Planetary Science Letters","active":true,"publicationSubtype":{"id":10}},"title":"Effects of selective fusion on the thermal history of the Moon, Mars, and Venus","docAbstract":"<p>A comparative study on the thermal history of the Moon, Mars, and Venus was made by numerical solutions of the heat equation including and excluding selective fusion of silicates. Selective fusion was approximated by melting in a multicomponent system and redistribution of radioactive elements. Effects on selective fusion on the thermal models are (1) lowering (by several hundred degrees centigrade) and stabilizing the internal temperature distribution, and (2) increasing the surface heat-flow.&nbsp;</p>","language":"English","publisher":"Elsevier","doi":"10.1016/0012-821X(68)90088-5","issn":"0012821X","usgsCitation":"Lee, W., 1968, Effects of selective fusion on the thermal history of the Moon, Mars, and Venus: Earth and Planetary Science Letters, v. 4, no. 4, p. 277-283, https://doi.org/10.1016/0012-821X(68)90088-5.","productDescription":"7 p.","startPage":"277","endPage":"283","numberOfPages":"7","costCenters":[],"links":[{"id":219575,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"4","issue":"4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a07c8e4b0c8380cd5181e","contributors":{"authors":[{"text":"Lee, W.H.K.","contributorId":35303,"corporation":false,"usgs":true,"family":"Lee","given":"W.H.K.","affiliations":[],"preferred":false,"id":357393,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":70038229,"text":"70038229 - 1967 - Water resources inventory of Connecticut Part 2: Shetucket River Basin","interactions":[],"lastModifiedDate":"2014-04-09T12:35:29","indexId":"70038229","displayToPublicDate":"2012-04-22T09:08:00","publicationYear":"1967","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":108,"text":"Connecticut Water Resources Bulletin","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"11","title":"Water resources inventory of Connecticut Part 2: Shetucket River Basin","docAbstract":"The Shetucket River basin has a relatively abundant supply of water of generally good quality which is derived from precipitation that has fallen on the basin. Annual precipitation has ranged from about 30 inches to 75 inches and has averaged about 45 inches over a 35-year period. Approximately 20 inches of water are returned to the atmosphere each year by evaporation and transpiration; the remainder of the annual precipitation either flows overland to streams or percolates downward to the water table and ultimately flows out of the basin in the Shetucket River or as underflow through the deposits beneath. During the autumn and winter months precipitation normally is sufficient to cause a substantial increase in the amount of water stored underground and in surface reservoirs within the basins whereas in the summer most of the precipitation is lost through evaporation and transpiration, resulting in sharply reduced streamflow and lowered groundwater levels. The mean monthly storage of water in the basin on an average is 3.5 inches higher in November than it is in June.\nThe amount of water that flows out of the\nbasin in the Shetucket River represents the total\namount of water potentlally available for use by man.\nAnnual runoff from the entire basin above the\nQuinebaug River has ranged from about 13 to 42\ninches since 1929, and has averaged about 23\ninches (300 billion gallons). Although runoff\nindicates the total amount of water potentially\navailable, it is usually not economically or\nlegally feasible for man to use all of it. On\nthe other hand, with increased development, It\nis possible that some water will be reused several\ntimes.\nThe water available may be tapped as it flows\nthrough the area or is temporarily stored in\nstreams, lakes, and aquifers. The amounts that\ncan be developed vary from place to place and\ntime to time, depending on the amount of precipitation,\non the size of drainage area, on the\nthickness, permeability and areal extent of aquifers,\nand on the variations in chemical and\nphysical quality of the water.\nDifferences in streamflow from point to\npoint are due primarily to differences in the\nproportion of stratified drift in the drainage\nbasin above each point, which affect the timing\nof streamflow, and to differences in precipitation,\nwhich affect the amount of streamflow.\nInformation on streamflow from gaging stations\nmay be extended to ungaged sites by accounting\nfor both of these factors ,in calculations.\nFuture floods on the upper Willimantic\nRiver or the Shetucket River are unlikely to\ncause major damage so long as buildings are not\nconstructed below the highest flood elevations to\nbe expected with the present system of reservoirs\nfor flood control.\nGround water can be obtained from wells\nalmost anywhere in the Shetucket River basin, but\nthe amount obtainable from individual wells at\nany particular point depends upon the type and\nwater-bearing properties of the aquifers present.\nFor practical purposes, the earth materials in\nthe basin comprise three aquifers--stratified\ndrift, till, and bedrock,\nStratified drift is the only aquifer generally capable of yielding more than 100 gpm to\nindividual wells. This aquifer covers about 18\npercent of the basin and occurs chiefly In lowlands\nwhere it overlies till or bedrock. Coefficient\nof permeability of the coarse-grained unit\nof stratified drift averages about 1,900 gpd per\nsq ft. Drilled, screened wells tapping this unit,\nare known to yield from 200 to 675 gpm. Dug wells\nin coarse-grained stratified drift should supply\nat least 2 gpm per foot of drawdown over an 8-hour\nperiod. Fine-grained stratified drift has an\naverage coefficient of permeability of about 400\ngpd per sq ft and can usually yield to dug wells\nsupplies sufficient for household use.\nTill and bedrock are widespread in extent but\ncan provide only small to moderate water supplies.\nTill is tapped chiefly by dug wells; permanent\nsupplies of more than 200 gpd can be obtained from\ndug wells at a majority of sites in areas of till,\nbut there are many sites where the till is too\nimpermeable or too thin to provide this much water\nthroughout the year. The coefficient of permeability of till ranges from about 0.2 gpd per sq ft to\n55 gpd per sq it. Bedrock Is tapped chiefly by\ndrilled wells, about 90 percent of which will\nsupply at least 3 gpm. Very few, however, will\nsupply more than 50 gpm.\nThe amount of ground water potentially available\nIn an area depends upon the amount of groundwater\noutflow, the amount of ground water in storage,\nand the quantity of water available by Induced\ninfiltration from streams and lakes. From\ndata on permeability, saturated thickness, recharge,\nyield from aquifer storage, well performance, and\nstreamflow, preliminary estimates of ground-water\navailability can be made for any point in the\nbasin. Long-term yields estimated for 15 areas\nespecially favorable for development of large\nground-water supplies ranged from 1.3 to 61.8 mgd.\nDetailed site studies to determine optimum yields,\ndrawdowns, and spacing of individual wells are\nneeded before major ground-water development is\nundertaken In these or other areas.\nThe chemical quality of water in the Shetucket\nbasin Is generally good to excellent. Samples of\nnaturally occurring surface water collected from\n32 sites contained less than 61 ppm of dissolved\nsolids and less than 32 ppm of hardness. Water\nfrom wells is more highly mineralized than naturally\noccurring water from streams. Even so only\n7 percent of wells sampled yielded water with more\nthan 200 ppm of dissolved sol-ids and only 9 percent\nyielded water with more than 120 ppm of hardness.\nEven in the major rivers, which are used to\ntransport industrial waste, the dissolved mineral\ncontent is less than 100 ppm and hardness rarely\nexceeds 40 ppm. One notable exception occurs in\nthe lower reaches of Little River where an\nexceptional amount of industrial waste is discharged\ninto the river near Versailles. This\nwaste is particularly noticeable during low\nstreamflow.\nIron and manganese In both ground water and\nsurface water are the only constituents whose concentrations\ncommonly exceed recommended limits for\ndomestic and industrial use. Most wells in the\n basin yield clear water with little or no iron or\nmanganese, but distributed among them are wells\nwith ground water that contains enough of these dissolved\nconstituents to be troublesome for most uses.\niron concentrations in naturally occurring\nstream water exceeded 0.3 ppm under tow-flow conditions\nat 20 percent of the sites sampled. Large\nconcentrations of iron in stream water result\nfrom discharge of iron-bearing ground water or\nfrom the discharge of water from swamps. In\nswamps the iron is released largely from decaying\nvegetation.\nGround water more than 30 feet below the\nland surface has a relatively constant temperature,\nusually between 48°F and 50°F. Water\ntemperature in very shallow wells may fluctuate\nfrom about 38°F in February or March to about\n55°F in late summer. Water temperature in the\nlarger streams fluctuates much more widely,\nranging from 32°F at least for brief periods\nin winter, to about 85°F occasionally during\nThe quantity of suspended sediment transported\nby streams in the basin is negligible,\nthough amounts large enough to be troublesome\nmay occur locally at times.\nThe total amount of water used In the\nShetucket Rlver basin for all purposes during\n1961 was about 5,810 million gallons~ which is\nequivalent to 208 gpd per person, Public water\nsystems supplied the domestic needs of nearly\nhalf the population of the basin; 10 systems\nwere sampled, all of which provided water of\nbetter quality than the U.S. Public Health Service\nsuggests for drinking water standards.","language":"English","publisher":"Connecticut Water Resources Commission","collaboration":"Prepared by the U.S. Geological Survey in cooperation with the Connecticut Water Resource Commission","usgsCitation":"Thomas, M.P., Bednar, G.A., Thomas, C.E., and Wilson, W.E., 1967, Water resources inventory of Connecticut Part 2: Shetucket River Basin: Connecticut Water Resources Bulletin 11, Report: viii, 96 p.; 4 Plates: 36.00 x 58.00 inches and smaller.","productDescription":"Report: viii, 96 p.; 4 Plates: 36.00 x 58.00 inches and smaller","numberOfPages":"112","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":258791,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/ctwrb/0011/report.pdf","size":"22651","linkFileType":{"id":1,"text":"pdf"}},{"id":258792,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/ctwrb/0011/report-thumb.jpg"},{"id":285972,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038229/plate-c.pdf"},{"id":285973,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038229/plate-d.pdf"},{"id":285970,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038229/plate-a.pdf"},{"id":285971,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70038229/plate-b.pdf"}],"scale":"48000","country":"United States","state":"Connecticut","otherGeospatial":"Shetucket River Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -72.466667,41.533333 ], [ -72.466667,42.066667 ], [ -72.0,42.066667 ], [ -72.0,41.533333 ], [ -72.466667,41.533333 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bcb78e4b08c986b32d681","contributors":{"authors":[{"text":"Thomas, Mendall P.","contributorId":104314,"corporation":false,"usgs":true,"family":"Thomas","given":"Mendall","email":"","middleInitial":"P.","affiliations":[],"preferred":false,"id":463693,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bednar, Gene A.","contributorId":81881,"corporation":false,"usgs":true,"family":"Bednar","given":"Gene","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":463692,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Thomas, Chester E. Jr.","contributorId":37182,"corporation":false,"usgs":true,"family":"Thomas","given":"Chester","suffix":"Jr.","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":463690,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Wilson, William E.","contributorId":46478,"corporation":false,"usgs":true,"family":"Wilson","given":"William","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":463691,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}}
,{"id":38847,"text":"pp542F - 1967 - Effects of the earthquake of March 27, 1964 on the communities of Kodiak and nearby islands","interactions":[{"subject":{"id":38847,"text":"pp542F - 1967 - Effects of the earthquake of March 27, 1964 on the communities of Kodiak and nearby islands","indexId":"pp542F","publicationYear":"1967","noYear":false,"chapter":"F","title":"Effects of the earthquake of March 27, 1964 on the communities of Kodiak and nearby islands"},"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":"2022-02-15T20:39:34.466499","indexId":"pp542F","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":"F","title":"Effects of the earthquake of March 27, 1964 on the communities of Kodiak and nearby islands","docAbstract":"<p>The great earthquake (Richter magnitude of 8.4–8.5) that struck south-central Alaska at 5:36 p.m., Alaska standard time, on March 27, 1964 (03:36, March 28, Greenwich mean time), was felt in every community on Kodiak Island and the nearby islands. It was the most severe earthquake to strike this part of Alaska in modern time, and took the lives of 18 persons in the area by drowning; this includes two in Kodiak and three at Kaguyak. Property damage and loss of income to the communities is estimated at more than $45 million.</p>\n</br>\n<p>The largest community, Kodiak, had the greatest loss from the earthquake. Damage was caused chiefly by 5.6 feet of tectonic subsidence and a train of 10 seismic sea waves that inundated the low-lying areas of the town. The seismic sea waves destroyed all but one of the docking facilities and more than 215 structures; many other structures were severely damaged. The waves struck the town during the evening hours of March 27 and early morning hours of March 28. They moved from the southwest and northeast: and reached their maximum height of 20–30 feet above mean lower low water at Shahafka Cove between 11:00 and 11:45 p.m., March 27. The violently destructive seismic sea waves not only severely damaged homes, shops, and naval-station structures but also temporarily crippled the fishing industry in Kodiak by destroying the processing plants and most of the fishing vessels. The waves scoured out 10 feet of sediments in the channel between Kodiak Island and Near Island and exposed bedrock. This bedrock presented a major post-earthquake construction problem because no sediments remained into which piles could be driven for foundations of waterfront facilities.</p>\n</br>\n<p>Because of tectonic subsidence, high tides now flood Mission and Potatopatch Lakes which, before the earthquake, had not been subject to tidal action. The subsidence also accelerated erosion of the unconsolidated sediments along the shoreline in the city of Kodiak.</p>\n</br>\n<p>Seismic shaking lasted 4½–5½ minutes at Kodiak and had a rolling motion. Inasmuch as most of Kodiak is underlain by bedrock or by only a thin veneer of unconsolidated sediments, very little if any damage occurred from ground motion or seismic shaking. The ground motion, however, did cause a massive short circuit and power failure at Kodiak.</p>\n</br>\n<p>The Kodiak Naval Station, 5 miles southwest of Kodiak, was also severely damaged by the earthquake. The station was inundated by at least 10 seismic sea waves which reached a maximum height of 25 feet above post-earthquake mean lower low water between 11:16 and 11:34 p.m. on March 27, 1964. The first seismic sea wave that inundated the station did not do severe damage because it behaved much like a rapid rise of tide, but the subsequent and more violent waves destroyed most of the docking facilities and several other shoreline structures. The waves struck the station from the southwest and from the east.</p>\n</br>\n<p>The shoreline structures that were not destroyed required rehabilitation because the 5.6 feet of tectonic subsidence put them under water during the highest tides. Furthermore the subsidence accelerated erosion during high tide of the soft unconsolidated sediments and fill in the low-lying areas of the station.</p>\n</br>\n<p>Seismic shaking did little damage to the station housing facility, but it was responsible for compaction of sediments, lateral displacement of a seawall, and the development of fissures in the aircraft parking area. The ground motion was as south-southeast–north-northwest to north-south in direction.</p>\n</br>\n<p>An unusual case of radioactive contamination was reported at the naval station. The inundating seismic sea waves entered a building in which radionuclides were stored. The contamination was restricted to the building only, however, and did not spread throughout the station.</p>\n</br>\n<p>Afognak was abandoned because of the extensive damage incurred from tectonic subsistence and seismic sea waves. The seismic effects, estimated Mercalli intensity VI-VII, did not directly cause any significant property damage at Afognak Serious long-term damage, however, resulted from tectonic subsidence estimated to be from 3½ to 5½ feet. The subsidence has resulted in rapid erosion of the coast, landward shift and building up of bench berms to the new higher sea levels, and flooding of extensive low-lying areas behind the barrier beaches. Inundation of low-lying parts of the village by a train of seismic sea waves having maximum heights of 10.8 feet above post-earthquake tide level (14.5 ft above post-earthquake mean lower low water) caused losses of about half a million dollars to homes, vehicles, bridges, and personal possessions.</p>\n</br>\n<p>Uzinki was damaged by tectonic subsidence and seismic sea waves. No significant damage resulted from the ground motion during the earthquake; the Mercalli intensity was about VI. However, tectonic subsidence, estimated to be 5 feet, caused inundation of a narrow zone along the waterfront. Structures and vessels were damaged as a result of the seismic sea waves that repeatedly flooded the waterfront area after the earthquake.</p>\n</br>\n<p>Old Harbor was damaged by seismic shock, subsidence, and seismic sea waves. The tremors, which had a Mercalli intensity estimated at VII-VIII, toppled two concrete-block chimneys, cracked interior walls, and caused minor breakage of personal property in the homes. Regional tectonic subsidence and superficial subsidence of the unconsolidated deposits on which the village is situated apparently caused incursion of salt water into the school well. A quarter of million yards of fill was required to raise the waterfront areas to their pre-earthquake elevations relative to sea level. Seismic sea waves having a maximum runup of about 12 feet above tide level (16 ft above post-earthquake mean lower low water) destroyed 34 of the 35 residences in the village and presumably drowned one man who lived immediately across the strait from Old Harbor.</p>\n</br>\n<p>At Kaguyak, seismic sea waves having a maximum runup of about 25 feet above mean lower low water carried away all 10 buildings in the village, took three lives, and damaged an unknown number of fishing vessels. The village site has been abandoned. The communities of Akhiok, Karluk, and Larsen Bay were virtually undamaged by the earthquake tremors, which had estimated Mercalli intensities of VI-VII, but tectonic subsidence of about 2–2½ feet at Larsen Bay made it necessary to raise the cannery dock level at an estimated cost of $80,000.</p>","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/pp542F","usgsCitation":"Kachadoorian, R., and Plafker, G., 1967, Effects of the earthquake of March 27, 1964 on the communities of Kodiak and nearby islands: U.S. Geological Survey Professional Paper 542, Report: vi, 41 p.; 1 Plate: 20.53 x 16.53 inches, https://doi.org/10.3133/pp542F.","productDescription":"Report: vi, 41 p.; 1 Plate: 20.53 x 16.53 inches","numberOfPages":"49","additionalOnlineFiles":"Y","costCenters":[{"id":380,"text":"Menlo ParkCalif. Office-Earthquake Science Center","active":false,"usgs":true}],"links":[{"id":396001,"rank":5,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4588.htm"},{"id":170406,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0542f/report-thumb.jpg"},{"id":113270,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0542f/pp542f_plate1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":113269,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0542f/pp542f_text.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":111458,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://pubs.usgs.gov/pp/0542f/index.html","linkFileType":{"id":5,"text":"html"}}],"country":"United States","state":"Alaska","otherGeospatial":"Kodiak Island","geographicExtents":"{\n  \"type\": \"FeatureCollection\",\n  \"features\": [\n    {\n      \"type\": \"Feature\",\n      \"properties\": {},\n      \"geometry\": {\n        \"type\": \"Polygon\",\n        \"coordinates\": [\n          [\n            [\n              -153.34442138671875,\n              57.671848402248166\n            ],\n            [\n              -152.10296630859375,\n              57.671848402248166\n            ],\n            [\n              -152.10296630859375,\n              58.1793925460941\n            ],\n            [\n              -153.34442138671875,\n              58.1793925460941\n            ],\n            [\n              -153.34442138671875,\n              57.671848402248166\n            ]\n          ]\n        ]\n      }\n    }\n  ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a27e4b07f02db610277","contributors":{"authors":[{"text":"Kachadoorian, Reuben","contributorId":24336,"corporation":false,"usgs":true,"family":"Kachadoorian","given":"Reuben","email":"","affiliations":[],"preferred":false,"id":220535,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Plafker, George","contributorId":3920,"corporation":false,"usgs":false,"family":"Plafker","given":"George","email":"","affiliations":[],"preferred":false,"id":220534,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}}
,{"id":41275,"text":"ofr68328 - 1967 - Preliminary geologic map of Ellipse II-2-1 and vicinity","interactions":[{"subject":{"id":41275,"text":"ofr68328 - 1967 - Preliminary geologic map of Ellipse II-2-1 and vicinity","indexId":"ofr68328","publicationYear":"1967","noYear":false,"title":"Preliminary geologic map of Ellipse II-2-1 and vicinity"},"predicate":"SUPERSEDED_BY","object":{"id":67387,"text":"i617 - 1970 - (ORB II-2(25)) Geologic map of Apollo landing site 1, part of Maskelyne DA region southeastern Mare Tranquillitatis","indexId":"i617","publicationYear":"1970","noYear":false,"title":"(ORB II-2(25)) Geologic map of Apollo landing site 1, part of Maskelyne DA region southeastern Mare Tranquillitatis"},"id":1}],"supersededBy":{"id":67387,"text":"i617 - 1970 - (ORB II-2(25)) Geologic map of Apollo landing site 1, part of Maskelyne DA region southeastern Mare Tranquillitatis","indexId":"i617","publicationYear":"1970","noYear":false,"title":"(ORB II-2(25)) Geologic map of Apollo landing site 1, part of Maskelyne DA region southeastern Mare Tranquillitatis"},"lastModifiedDate":"2022-05-27T21:11:46.233469","indexId":"ofr68328","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":"68-328","title":"Preliminary geologic map of Ellipse II-2-1 and vicinity","docAbstract":"<p>The map area contains landing ellipse II-2-1 and lies near the southern edge of southeastern embayment of Mare Tranquillitatis, a region of typical flat mare and terrain of gently undulating relief and moderate albedo.</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr68328","collaboration":"Prepared in cooperation with the Manned Spacecraft Center, National Aeronautics and Space Administration","usgsCitation":"Wilhelms, D., 1967, Preliminary geologic map of Ellipse II-2-1 and vicinity: U.S. Geological Survey Open-File Report 68-328, 1 Plate: 45.60 x 32.33 inches, https://doi.org/10.3133/ofr68328.","productDescription":"1 Plate: 45.60 x 32.33 inches","costCenters":[],"links":[{"id":170615,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0328/report-thumb.jpg"},{"id":401341,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0328/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"25000","projection":"Mercator Projection","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67c07f","contributors":{"authors":[{"text":"Wilhelms, D.E.","contributorId":82302,"corporation":false,"usgs":true,"family":"Wilhelms","given":"D.E.","email":"","affiliations":[],"preferred":false,"id":224754,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
,{"id":41232,"text":"ofr68118 - 1967 - Preliminary geologic map of Ellipse III-12-1 and vicinity","interactions":[],"lastModifiedDate":"2022-05-20T15:34:44.580292","indexId":"ofr68118","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":"68-118","title":"Preliminary geologic map of Ellipse III-12-1 and vicinity","docAbstract":"<p>Ellipse III-12-1 is in the northwestern part of the Flamsteed P ring, about 35 km north-northeast of the crater Flamsteed E. The area is a moderately cratered, undulating mare plain.&nbsp;</p>","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr68118","collaboration":"Prepared in cooperation with the Manned Spacecraft Center, National Aeronautics and Space Administration","usgsCitation":"Harbour, J., 1967, Preliminary geologic map of Ellipse III-12-1 and vicinity: U.S. Geological Survey Open-File Report 68-118, 1 Plate: 31.61 x 33.03 inches, https://doi.org/10.3133/ofr68118.","productDescription":"1 Plate: 31.61 x 33.03 inches","costCenters":[],"links":[{"id":170903,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1968/0118/report-thumb.jpg"},{"id":400861,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1968/0118/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"25000","projection":"Mercator Projection","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac8e4b07f02db67c072","contributors":{"authors":[{"text":"Harbour, Jerry","contributorId":68379,"corporation":false,"usgs":true,"family":"Harbour","given":"Jerry","email":"","affiliations":[],"preferred":false,"id":224688,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}}
]}