The Burgin shaft is in the Chief Oxide area of the E. Tintic district, Utah, and is about a mile E. of any previously known ore bodies; workings from it are currently developing a substantial amount of commercial Pb-Zn ore in several blind ore bodies that lie in folded Paleozoic carbonate rock concealed beneath a blanket of Eocene lava. This area was mapped by Tower and Smith of the U.S. Geological Survey in 1897 and again by Lindgren and Loughlin in 1911, but no detailed work was done until after 1943 when a field party headed by T.S. Lovering began a study of the entire E. Tintic district. The history of the development of exploration concepts is summarized under Historical Summary. The E. Tintic mining district is in the E.-central part of a N.-trending fault-block mountain range near the eastern margin of the Great Basin; dominant structures of the range are a N.-trending syncline on the W. and a less well exposed anticline on the E. Both folds are cut by an intersecting system of transcurrent strike-slip faults and by minor thrust faults and normal faults of moderate displacement. A strong W.-dipping thrust fault cuts the anticline a short distance E. of the fold axis, but is hidden by Eocene lava throughout the E. Tintic district. The pre-Tertiary rocks range from Lower Cambrian to Upper Mississippian and exceed 7,000 ft. in total thickness; they are dominantly marine limestone and dolomite except for a thick basal Cambrian quartzite. The Tertiary rocks are chiefly dacitic lavas and pyroclastic deposits that are intruded by moderately persistent dikes and irregular bodies of monzonite and quartz porphyry. Nearly all the faulting and folding took place before the extrusion of the lavas on a rugged Eocene erosion surface. At about the time of the intrusion of monzonitic magma, many of the faults in the Paleozoic rock were re-opened and in the overlying lava some fracturing took place which was later accented by hydrothermal alteration. Most of the ore mined in the E. Tintic district has come from Pb-Zn-Ag replacement bodies in shattered Jasperoidized hydrothermal dolomite at the intersection of low angle faults and steep mineralized NE.-trending cross fractures. The U.S. Geological Survey studies of 1943 to 1957 concentrated on detailed mapping of geology and alteration in the E. Tintic district, together with field and laboratory studies of the relation of alteration to stages of mineralization and ore deposition. Trenching and core drilling were carried on after World War II to aid in interpreting the subrhyolite geology, and the Chief Oxide area was 1 of 4 localities tested by drilling. Study of the fossils, lithology, and alteration shown here in a deep drill core, together with the knowledge of the regional geology, led to an essentially correct interpretation of subrhyolite structure in the strongly discordant underlying Paleozoic rocks in which a mineralized tear fault cuts a strong thrust fault, and to the conclusion that ore stage mineralization was present in substantial amounts in the Paleozoic rocks below the Chief Oxide alteration patch in the quartz latite lava. Subsequent geothermal and geochemical work strengthened this conclusion, and the recent development work of the Bear Creek Mining Company, which sank the Burgin shaft, has shown the presence of Pb-Zn-Ag ore of commercial grade in substantial amount in blind ore bodies below the lava blanket in the Chief Oxide area.
No abstract available.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1960)10[1541:SOTQAE]2.0.CO;2","usgsCitation":"Scott, G., 1960, Subdivision of the quaternary alluvium east of the front range near Denver, Colorado: GSA Bulletin, v. 71, no. 10, p. 1541-1544, https://doi.org/10.1130/0016-7606(1960)10[1541:SOTQAE]2.0.CO;2.","productDescription":"4 p.","startPage":"1541","endPage":"1544","costCenters":[],"links":[{"id":375978,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado","city":"Denver","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -105.66650390625,\n 38.34165619279595\n ],\n [\n -104.447021484375,\n 38.34165619279595\n ],\n [\n -104.447021484375,\n 40.863679665481676\n ],\n [\n -105.66650390625,\n 40.863679665481676\n ],\n [\n -105.66650390625,\n 38.34165619279595\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"71","issue":"10","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Scott, Glenn R.","contributorId":33324,"corporation":false,"usgs":true,"family":"Scott","given":"Glenn R.","affiliations":[],"preferred":false,"id":791695,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220589,"text":"70220589 - 1960 - Stratigraphic and geotectonic relationships in northern Vermont and southern Quebec","interactions":[],"lastModifiedDate":"2021-05-20T18:49:24.731852","indexId":"70220589","displayToPublicDate":"1960-05-01T13:42:52","publicationYear":"1960","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":"Stratigraphic and geotectonic relationships in northern Vermont and southern Quebec","docAbstract":"Stratified rocks of early and middle Paleozoic age form a belt of northeast-trending anticlinoria and synclinoria of middle Paleozoic age, in northern Vermont and adjacent parts of southern Quebec. The foreland margin of this belt, in the Champlain and St. Lawrence valleys to the west, is cut by eastward-dipping thrust faults of middle Paleozoic age and by later northeast-trending normal faults. The Green Mountain anticlinorium, which is the dominant structure of the region, is flanked to the west, on the foreland, by the St. Albans-Hinesburg-Middlebury synclinorium and to the east, in the midst of the folded belt, by the Connecticut Valley-Gaspe synclinorium. The principal thrust faults, notably the Champlain and Philipsburg thrusts, are in the west limb of the St. Albans-Hinesburg-Middlebury synclinorium. East of the Connecticut Valley-Gaspe synclinorium is the Boundary Mountain anticlinorium, in eastern Vermont and adjacent New Hampshire and along the international boundary between Quebec and Maine. Two contrasting intergradational lithic assemblages, the graywacke-shale assemblage and the carbonate-quartzite assemblage, characterize the protolith of the bedded rocks. The graywacke-shale assemblage includes thick sections of lower Paleozoic strata, portions of which lap both gradationally and unconformably westward on the foreland, particularly in Quebec; it also includes middle Paleozoic strata that offlap eastward away from the foreland. The carbonate-quartzite assemblage laps both unconformably and gradationally eastward over the graywacke-shale assemblage in sections of the middle Paleozoic east of the axis of the Green Mountain anticlinorium. Stratigraphic correlation has become well established in the foreland belt where numerous distinctive and fossiliferous strata, chiefly of the carbonate-quartzite assemblage, have escaped metamorphism. It is also fairly clear in sections in the eastern foreland and western part of the Green Mountain anticlinorium, where the strata of the carbonate-quartzite assemblage extend eastward and interfinger with rocks of the graywacke-shale terrane. Rocks that are entirely of the graywacke-shale assemblage have been correlated in the present study. The stratified rocks west of the axis of the Green Mountain anticlinorium are of Cambrian(?), Cambrian, and Ordovician age; those to the east range in age from Cambrian to Devonian. The geotectonic setting of the region is the once mobile belt of the Appalachian orthogeosyncline, which is at the southeastern margin of the stable continental block, or craton, of North America. The orthogeosyncline was a belt, chiefly of subsidence, that embraced two parallel and adjoining longitudinal zones: the eugeosynclinal zone, which was more mobile, and the miogeosynclinal zone, which was less mobile. Second- and third-generation geosynclines are superimposed not only on the orthogeosyncline but also on adjoining parts of the craton. Uplift, and finally folding, gradually superseded subsidence in the orthogeosyncline. Local uplift, chiefly within the eugeosynclinal zone, provided most of the clastic sediments, principally those of the graywacke-shale assemblage. General stabilization of the western part of the orthogeosyncline at the end of the Ordovician was accompanied by eastward migration of the miogeosynclinal zone. Localized uplift within the eastern part of the orthogeosyncline at this time is marked by unconformities referred to the Taconic disturbance. Folding and uplift after the Early Devonian is shown by angular unconformities referred to the Acadian and Appalachian orogenies. The interpretation of the geotectonic relations of the bedded rocks is aided by critical features of the magmatic activity that began with, accompanied, and followed the diastrophism.
","language":"English","publisher":"Geological Society of America","doi":"10.1130/0016-7606(1960)71[531:SAGRIN]2.0.CO;2","usgsCitation":"Cady, W.M., 1960, Stratigraphic and geotectonic relationships in northern Vermont and southern Quebec: Economic Geology, v. 71, no. 5-6, p. 531-576, https://doi.org/10.1130/0016-7606(1960)71[531:SAGRIN]2.0.CO;2.","productDescription":"46 p.","startPage":"531","endPage":"576","costCenters":[],"links":[{"id":385800,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States, Canada","state":"Vermont, Quebec","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -73.5205078125,\n 43.37311218382002\n ],\n [\n -71.455078125,\n 43.37311218382002\n ],\n [\n -71.455078125,\n 45.98169518512228\n ],\n [\n -73.5205078125,\n 45.98169518512228\n ],\n [\n -73.5205078125,\n 43.37311218382002\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"71","issue":"5-6","noUsgsAuthors":false,"publicationStatus":"PW","contributors":{"authors":[{"text":"Cady, W. M.","contributorId":64641,"corporation":false,"usgs":true,"family":"Cady","given":"W.","middleInitial":"M.","affiliations":[],"preferred":false,"id":816102,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70220587,"text":"70220587 - 1960 - Occurrence of strontium in the surface and ground waters of Champaign county, Ohio","interactions":[],"lastModifiedDate":"2021-05-21T14:39:50.079798","indexId":"70220587","displayToPublicDate":"1960-01-01T13:30:04","publicationYear":"1960","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":"Occurrence of strontium in the surface and ground waters of Champaign county, Ohio","docAbstract":"Naturally occurring strontium was found in both surface and ground waters during an investigation of the water resources of Champaign County, Ohio. The strontium is related to the presence of celestite (strontium sulfate) in rocks associated with evaporite deposition. The principal source of celestite in Ohio is in rocks of Late Silurian age. Celestite is present also in the glacial deposits of western Ohio, which contain rock material of Late Silurian age. Total time in contact with the rock material seems to have a large effect upon concentrations of strontium in ground water. Streamflow, during low-flow periods, is made up largely of ground-water seepage and contains detectable strontium. Strontium has been found in ground water in other counties in western Ohio and in the brines of eastern Ohio.
","language":"English","publisherLocation":"Society of Economic Geologist","doi":"10.2113/gsecongeo.55.1.176","usgsCitation":"Feulner, A., and Hubble, J., 1960, Occurrence of strontium in the surface and ground waters of Champaign county, Ohio: Economic Geology, v. 55, no. 1, p. 176-186, https://doi.org/10.2113/gsecongeo.55.1.176.","productDescription":"11 p.","startPage":"176","endPage":"186","costCenters":[],"links":[{"id":385794,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Ohio","county":"Champaign County","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -83.83186340332031,\n 40.063884174719156\n ],\n [\n -83.64303588867186,\n 40.063884174719156\n ],\n [\n -83.64303588867186,\n 40.16680597002458\n ],\n [\n -83.83186340332031,\n 40.16680597002458\n ],\n [\n -83.83186340332031,\n 40.063884174719156\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"55","issue":"1","noUsgsAuthors":false,"publicationDate":"1960-01-01","publicationStatus":"PW","contributors":{"authors":[{"text":"Feulner, A.J.","contributorId":70796,"corporation":false,"usgs":true,"family":"Feulner","given":"A.J.","affiliations":[],"preferred":false,"id":816098,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hubble, J.H.","contributorId":99624,"corporation":false,"usgs":true,"family":"Hubble","given":"J.H.","email":"","affiliations":[],"preferred":false,"id":816099,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":1094,"text":"1094 - 1960 - Geology and ground-water hydrology of the Redlands-Beaumont area, California, with special reference to ground-water outflow","interactions":[],"lastModifiedDate":"2024-09-03T21:05:26.158835","indexId":"1094","displayToPublicDate":"1960-01-01T12:39:48","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"title":"Geology and ground-water hydrology of the Redlands-Beaumont area, California, with special reference to ground-water outflow","docAbstract":"The Redlands-Beaumont area is bordered by the Santa Ana River on the north, the San Bernadina River on the northeast, the Yucaipa Hills and the San Gorgonio Pass on the east, and the Badlands and the San Jacinto fault on the south and south-west. Large alluvial fans underlie much of the area, but other landforms include alluvial benches, dissected alluvial hills, plains, terraces, and bedrock hills which locally protrude above the floors of the alluvial valleys.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/1094","collaboration":"Prepared in cooperation with the San Bernardino County Flood Control District.","usgsCitation":"Burnham, W., and Dutcher, L.C., 1960, Geology and ground-water hydrology of the Redlands-Beaumont area, California, with special reference to ground-water outflow, 352 p., https://doi.org/10.3133/1094.","productDescription":"352 p.","costCenters":[],"links":[{"id":433421,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/1094/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":289641,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/1094/report-thumb.jpg"}],"country":"United States","state":"California","city":"Beaumont, Redlands","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -117.2637864386227,\n 34.105233250065254\n ],\n [\n -117.2637864386227,\n 33.87256760375355\n ],\n [\n -116.9107764193285,\n 33.87256760375355\n ],\n [\n -116.9107764193285,\n 34.105233250065254\n ],\n [\n -117.2637864386227,\n 34.105233250065254\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53be6474e4b0527d5d4097b6","contributors":{"authors":[{"text":"Burnham, W.L.","contributorId":58668,"corporation":false,"usgs":true,"family":"Burnham","given":"W.L.","email":"","affiliations":[],"preferred":false,"id":143166,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Dutcher, Lee Carlton","contributorId":32229,"corporation":false,"usgs":true,"family":"Dutcher","given":"Lee","email":"","middleInitial":"Carlton","affiliations":[],"preferred":false,"id":143165,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70160871,"text":"70160871 - 1960 - Geology and ground-water resources of the island of Kauai, Hawaii","interactions":[],"lastModifiedDate":"2016-01-06T08:58:28","indexId":"70160871","displayToPublicDate":"1960-01-01T12:15:00","publicationYear":"1960","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":4,"text":"Other Government Series"},"seriesTitle":{"id":242,"text":"Bulletin","active":false,"publicationSubtype":{"id":4}},"seriesNumber":"13","title":"Geology and ground-water resources of the island of Kauai, Hawaii","docAbstract":"Kauai is one of the oldest, and is structurally the most complicated, of the Hawaiian Islands. Like the others, it consists principally of a huge shield volcano, built up from the sea floor by many thousands of thin flows of basaltic lava. The volume of the Kauai shield was on the order of 1,000 cubic miles. Through much of its growth it must have resembled rather closely the presently active shield volcano Mauna Loa, on the island of Hawaii. When the Kauai volcano started its growth is not known with certainty, but it is believed that activity started late in the Tertiary period, possibly in the early or middle part of the Pliocene epoch. Growth of the shield was rapid and probably was completed before the end of the Pliocene.
Toward the end of the growth of the shield, its summit collapsed to form a broad caldera, the largest that has been found in the Hawaiian Islands. Like the calderas of Kilauea and Mauna Loa, that of Kauai volcano had boundaries that were, in part, rather indefinite. The principal depression was bordered by less depressed fault blocks, some of which merged imperceptibly with the outer slopes of the volcano. Elsewhere the caldera rim was low, and flows spilled over it onto the outer slopes. The well-defined central depression of the Kauai caldera was approximately 10 to 12 miles across.
At about the same time as the formation of the major caldera, another, smaller caldera was formed by collapse around a minor eruptive center on the southeastern side of the Kauai shield. Lavas accumulated in the calderas, gradually filling them and burying banks of talus that formed along the foot of the boundary cliffs. The caldera-filling lavas differed from those that built the major portion of the shield in being much thicker and more massive as a result of ponding in the depressions. The petrographic types for the most part are the same throughout. Both the flank flows that built most of the shield and the flows that filled the calderas are predominantly olivine basalt. Picrite-basalt (oceanite), containing very abundant large phenocrysts of olivine, and basalt containing little or no olivine are present but together comprise less than 10 percent of the whole. Late in the period of filling of the major caldera a small amount of basaltic andesine andesite was extruded.
Near the end of the period of filling of the major caldera further collapse occurred, forming a large graben on the southwestern side of the shield. Lava flows erupting within the caldera poured southwestward over the cliff bounding the graben and spread over the gently sloping graben floor. Near the present Waimea Canyon their advance was obstructed by the fault scarp at the west edge of the graben. The cliff along the northeast edge of the graben eventually was buried by lava flows from within the caldera, but that along the west edge continued to stand above the level of the flows in the graben. The flows that accumulated in the graben are of the same types as those that filled the caldera, and like them are mostly thick and massive because of ponding by the graben walls and of the gentle slopes of the graben floor over which they spread.
The rocks of the major Kauai shield volcano are known as the Waimea Canyon volcanic series. The thin flows that accumulated on the flanks of the shield, which compose the major portion of the volcanic edifice, are named the Napali formation of the Waimea Canyon volcanic series. The rocks that accumulated in the big summit caldera are named the Olokele formation, and those that filled the small caldera on the southeast flank of the shield are named the Haupu formation. The volcanic rocks accumulated in the graben on the southwestern side of the shield are named the Makaweli formation of the Waimea Canyon volcanic series, and sedimentary rocks interbedded with them are known as the Mokuone member of the Makaweli formation.
Few vents of the Waimea Canyon volcanic series have been recognized, probably because most of them have been destroyed by erosion or are buried by later lavas. Large numbers of dikes cut the lavas of the Napali formation along Waimea Canyon and the Napali Coast and along the east edge of the Waialeale massif. Fewer dikes are found in the other members of the series. Some tendency toward radial arrangement of the dikes is present, but the dominant trend all over the island is east-northeastward.
Another great collapse took place on the eastern flank of the volcano at about the time the major shield became extinct, or shortly afterward. A subcircular graben 6 or 7 miles across sank several thousand feet, forming a broad depression between the Waialeale massif on the west and Kalepa and Nonou ridges on the east. This collapsed structure cannot be as clearly demonstrated as the Makaweli graben on the southwest side of the shield, because its walls have been greatly eroded and its floor is deeply buried by lavas of the later Koloa volcanic series. It appears, however, to be the only reasonable explanation of the physiography of the eastern side of the island.
After the completion of the great Kauai shield came a long period of erosion during which no volcanic activity occurred. Waves cut high sea cliffs around the island, and streams cut canyons as much as 3,000 feet deep. Thick soil formed over much of the mountain.
Then volcanism was renewed. Eruption occurred from a series of minor vents arranged in nearly north-south and northeast-southwest lines across the eastern two-thirds of the island. The lavas, cinder cones, and ash beds of this period of volcanism are known as the Koloa volcanic series. Lavas of the Koloa volcanic series include olivine basalt, picrite-basalt (mimosite) with few phenocrysts of olivine, basanite, nepheline basalt, melilite-nepheline basalt, and ankaratrite (nepheline basalt very rich in pyroxene and olivine). Inclusions of dunite, composed almost entirely of olivine, are common in flows of the Koloa. Just before and during the eruption of the Koloa volcanic series, voluminous landslides and mudflows brought down a large amount of rock debris and soil from the steep slopes of the mountainous central upland and deposited it as breccias at the foot of the steep slopes in valley heads and along the border of the marginal lowland. Streams distributed part of the material across the lowland. The breccias and conglomerates thus formed, and later buried by lavas of the Koloa volcanic series, are named the Palikea formation of the Koloa volcanic series.
The structures formed at Koloa vents include cinder cones, one tuff cone, and lava cones. The latter are miniature shields resembling the major shield volcano, formed by repeated outpourings of fluid lava. The tuff cone, at the west side of Kilauea Bay, was formed by phreatomagmatic explosions caused by rising magma coming in contact with water-saturated rocks.
Volcanism during Koloa time continued for a long period but was not continuous over the entire area. Locally, long periods of quiet occurred, allowing streams to re-excavate some of the canyons filled by earlier flows of the Koloa volcanic series, and weathering to form soils later buried by new flows. Some of the canyons thus formed during the time when the Koloa was being deposited were several hundred feet deep. Volcanism probably continued throughout most of the Pleistocene epoch. The latest flow of the Koloa volcanic series appears very recent, and rests on lithified calcareous dunes formed during one of the Pleistocene low stands of the sea.
During the Pleistocene epoch stream valleys and sea cliffs were eroded to base levels governed by one or more stands of the sea more than 100 feet below present sea level. Beaches of calcareous sand were formed, and the sand blown inland to form calcareous dunes, now lithified. A test boring near Moloaa penetrated calcareous sand 160 feet below sea level, at the foot of a high sea cliff. Coral reef also was built around part or all of the island, and in part buried by lavas of the Koloa volcanic series. The explosions that built the tuff cone at Kilauea Bay threw up fragments of limestone from a buried reef. Much of the apron of lavas of the Kalna series around the northeastern side of the island probably rests on a platform formed below present sea level by wave erosion and the growth of coral reef.
As the sea rose around the island, the valley mouths were alluviated. Several levels of the sea higher than the present one probably are represented. Some stream terraces may be graded to a stand of the sea as high as 260 feet above present sea level, but no positive evidence for stands higher than 25 feet have been found. Well-preserved shorelines are recognized approximately 25 and 5 feet above sea level. Much of the present coral reef appears to have been formed when the sea stood about 5 feet higher than now, and reduced to its present level by solutional weathering and wave erosion.
The lavas of the Napali formation of the Waimea Canyon volcanic series are highly permeable. They carry basal water over much of the island, and yield it freely to wells. This water is fresh everywhere except very close to the coast on the leeward side of the island. In some areas they may contain water confined at high levels between dikes. The lavas of the Olokele and Haupu formations are moderately to poorly permeable. They probably contain fresh water at sea level, but would not yield it readily to wells. Locally, ash beds perch small bodies of fresh water at high levels in the lavas of the Olokele formation, but these are of no economic importance. The lavas of the Makaweli formation also arc moderately to poorly permeable. They carry fresh or brackish water at sea level. In general, they yield water to wells less readily than the lavas of the Napali formation, but more readily than the lavas of the Olokele. The conglomerates and breccias of the Mokuone member are poorly permeable, but are not known to perch more than a slight amount of water in the overlying lavas,
The lava flows of the Koloa volcanic series are poorly to moderately permeable. They carry fresh or brackish water at sea level, but generally yield it slowly to wells. Locally, small bodies of fresh water are perched at high levels in the lavas of the Koloa by beds of ash and soil and by breccia and conglomerate of the Palikea formation.
Both the older and the younger alluvium generally are poorly permeable, but contain small amounts of fresh or brackish water. The lithified calcareous dunes are permeable, but they appear to contain only brackish water. Lagoon deposits on the Mana plain are poorly to moderately permeable and yield brackish water to wells.
The papers comprising the various parts of this report contain preliminary results of the U. S. Geological Survey investigations in the U12b.03 and U12b.04 tunnels at the Nevada Test Site, Nye County, Nevada (fig. 1). The geologic studies were undertaken to define the structural, chemical, mineralogic, and some of the physical properties of the tuffaceous rocks that enclose the explosion chambers at the end of each tunnel.
\nThe U12b.03 and .04 tunnels are part of the U12b (Rainier) tunnel complex that was driven northwestward from the steep east slope of Rainier Mesa (a prominent topographic feature in the northwest part of the Test Site (fig . 2)). The U12b.03 tunnel trends north from a point about 980 feet from the portal of the U12b tunnel (fig. 3). The U12b.03 tunnel consists of 620 feet of tunnel, two alcoves, and a shot chamber. The tunnel is irregular, ranging from 6 to 10 feet in width, and 6 to 9 feet in height. The shot chamber at the north end of the tunnel is 22 feet on each sidee The vertical and minimum cover over the shot chamber are 610 and 510 feet, respectively.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/tem996","usgsCitation":"Diment, W., Wilmarth, V.R., McKeown, F.A., Dickey, D., Hinrichs, E., Botinelly, T., Roach, C.H., Byers, F., Hawley, C.C., Izett, G., and Clebsch, A., 1959, Geological investigations in the U12b.03 and U12b.04 tunnels, Nevada Test Site: U.S. Geological Survey Trace Elements Memorandum 996, Report: 73 p.; 4 Plates: 42.66 x 40.60 inches or smaller, https://doi.org/10.3133/tem996.","productDescription":"Report: 73 p.; 4 Plates: 42.66 x 40.60 inches or smaller","numberOfPages":"73","onlineOnly":"N","additionalOnlineFiles":"N","costCenters":[],"links":[{"id":309873,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/tem996.jpg"},{"id":310387,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tem/0996/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"}},{"id":310388,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0996/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":310389,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0996/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":310390,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0996/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":310391,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/0996/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Nevada","county":"Nye County","otherGeospatial":"Rainier Mesa","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-115.9082,39.1615],[-115.5191,38.9578],[-115.4725,38.9325],[-115.4433,38.9162],[-115.3694,38.8769],[-115.363,38.874],[-115.242,38.8093],[-115.0969,38.7309],[-115.0777,38.721],[-115.0604,38.7107],[-115.0291,38.6937],[-114.999,38.6777],[-114.9996,38.592],[-114.9997,38.4315],[-114.9994,38.3894],[-115.0004,38.0507],[-115.1185,38.0508],[-115.1436,38.0508],[-115.326,38.0515],[-115.3453,38.0514],[-115.4003,38.051],[-115.4587,38.0506],[-115.6394,38.0512],[-115.6581,38.051],[-115.8404,38.0504],[-115.8931,38.0507],[-115.8938,37.723],[-115.8969,37.5498],[-115.8975,37.2796],[-115.8982,37.1926],[-115.8942,36.8425],[-115.8941,36.686],[-115.8945,36.6702],[-115.8949,36.598],[-115.8949,36.5962],[-115.8946,36.5858],[-115.8947,36.5005],[-115.8945,36.4806],[-115.8949,36.462],[-115.8944,36.457],[-115.8948,36.3087],[-115.8945,36.2923],[-115.8943,36.1957],[-115.8945,36.1608],[-115.8948,36.1163],[-115.8948,36.0927],[-115.895,36.0015],[-115.9178,36.0192],[-115.9518,36.0457],[-115.9925,36.0773],[-116.049,36.1211],[-116.0624,36.1314],[-116.1039,36.1636],[-116.1287,36.1829],[-116.1702,36.2152],[-116.173,36.2174],[-116.2311,36.2626],[-116.2834,36.3028],[-116.2954,36.3122],[-116.3752,36.373],[-116.5107,36.4764],[-116.5247,36.4871],[-116.5589,36.5131],[-116.574,36.5245],[-116.5946,36.54],[-116.6556,36.5867],[-116.6583,36.5888],[-116.6764,36.6024],[-116.706,36.6248],[-116.7895,36.6877],[-116.8424,36.7276],[-116.8453,36.7298],[-116.8806,36.7568],[-116.8912,36.7648],[-116.9237,36.7891],[-116.9641,36.8193],[-116.9783,36.8299],[-116.981,36.8319],[-117.0046,36.8495],[-117.164,36.9688],[-117.1639,36.9698],[-117.1637,37.0182],[-117.164,37.0894],[-117.1642,37.171],[-117.1641,37.1909],[-117.1641,37.1936],[-117.1665,37.6995],[-117.1664,37.714],[-117.1663,37.7285],[-117.1663,37.7435],[-117.1662,37.7585],[-117.1657,38.0019],[-117.2198,38.0482],[-117.2397,38.0483],[-117.239,38.0641],[-117.2408,38.0705],[-117.2653,38.0932],[-117.6896,38.4731],[-118.0197,38.7599],[-118.197,38.9154],[-118.1972,38.9993],[-117.8559,39.0746],[-117.7748,39.092],[-117.7008,39.1058],[-117.6409,39.1149],[-117.5946,39.1231],[-117.4742,39.1431],[-117.3823,39.1562],[-117.3609,39.1585],[-117.3318,39.1629],[-117.3063,39.1634],[-117.2849,39.1633],[-117.1995,39.1632],[-117.0856,39.1628],[-117.0322,39.1626],[-117.0144,39.1626],[-116.9871,39.1625],[-116.9158,39.1631],[-116.7562,39.1622],[-116.7301,39.1625],[-116.5996,39.1616],[-116.5859,39.162],[-116.4815,39.1616],[-116.3497,39.1618],[-116.2358,39.1616],[-116.0548,39.1624],[-115.9082,39.1615]]]},\"properties\":{\"name\":\"Nye\",\"state\":\"NV\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"561f7cb5e4b03ee62faa8fe1","contributors":{"authors":[{"text":"Diment, W.H.","contributorId":54992,"corporation":false,"usgs":true,"family":"Diment","given":"W.H.","affiliations":[],"preferred":false,"id":577411,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Wilmarth, V. R.","contributorId":119573,"corporation":false,"usgs":true,"family":"Wilmarth","given":"V.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":577412,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"McKeown, F. A.","contributorId":106100,"corporation":false,"usgs":true,"family":"McKeown","given":"F.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":577413,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Dickey, D.D.","contributorId":15612,"corporation":false,"usgs":true,"family":"Dickey","given":"D.D.","email":"","affiliations":[],"preferred":false,"id":577414,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Hinrichs, E. N.","contributorId":98717,"corporation":false,"usgs":true,"family":"Hinrichs","given":"E. N.","affiliations":[],"preferred":false,"id":577415,"contributorType":{"id":1,"text":"Authors"},"rank":5},{"text":"Botinelly, T.","contributorId":20408,"corporation":false,"usgs":true,"family":"Botinelly","given":"T.","affiliations":[],"preferred":false,"id":577416,"contributorType":{"id":1,"text":"Authors"},"rank":6},{"text":"Roach, C. H.","contributorId":12117,"corporation":false,"usgs":true,"family":"Roach","given":"C.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":577417,"contributorType":{"id":1,"text":"Authors"},"rank":7},{"text":"Byers, F. M.","contributorId":50141,"corporation":false,"usgs":true,"family":"Byers","given":"F. M.","affiliations":[],"preferred":false,"id":577418,"contributorType":{"id":1,"text":"Authors"},"rank":8},{"text":"Hawley, C. C.","contributorId":102070,"corporation":false,"usgs":true,"family":"Hawley","given":"C.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":577419,"contributorType":{"id":1,"text":"Authors"},"rank":9},{"text":"Izett, G. A.","contributorId":21131,"corporation":false,"usgs":true,"family":"Izett","given":"G. A.","affiliations":[],"preferred":false,"id":577420,"contributorType":{"id":1,"text":"Authors"},"rank":10},{"text":"Clebsch, Alfred","contributorId":57047,"corporation":false,"usgs":true,"family":"Clebsch","given":"Alfred","affiliations":[],"preferred":false,"id":577421,"contributorType":{"id":1,"text":"Authors"},"rank":11}]}} ,{"id":76909,"text":"tem1033 - 1959 - Thickness, character, and structure of upper Permian evaporites in part of Eddy County, New Mexico","interactions":[],"lastModifiedDate":"2015-11-02T13:42:37","indexId":"tem1033","displayToPublicDate":"2013-07-23T13:26:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":338,"text":"Trace Elements Memorandum","code":"TEM","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1033","title":"Thickness, character, and structure of upper Permian evaporites in part of Eddy County, New Mexico","docAbstract":"Between Project Gnome site and the International Minerals and Chemical Corporation's plant site, in central eastern Eddy County, N. Mex., unconsolidated deposits of Quaternary age and redbeds of Triassic age attain a thickness of about 700 feet, and rest unconformably on evaporites of late Permian age. The upper Permian evaporites are 3,000 to 3,800 feet thick, and they are divided, in descending order, into the Rustler, Salado, and Castile formations. The Rustler is largely gypsum rock, the Salado is dominantly halite rock, and the Castile contains both anhydrite rock and halite rock. The salt and anhydrite beds of the Salado and Castile are intruded by narrow dikes of alkalic rock along which the evaporites are little altered. The sedimentary rocks have a generally southeastward regional dip, but locally are warped in gentle folds of low amplitude and fairly small lateral dimensions.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/tem1033","collaboration":"Submitted to San Francisco Operations Office, U.S. Atomic Energy Commission.","usgsCitation":"Jones, C.L., 1959, Thickness, character, and structure of upper Permian evaporites in part of Eddy County, New Mexico: U.S. Geological Survey Trace Elements Memorandum 1033, Report: 19 p.; 2 Plates: 19.75 x 12.88 inches; Table, https://doi.org/10.3133/tem1033.","productDescription":"Report: 19 p.; 2 Plates: 19.75 x 12.88 inches; Table","numberOfPages":"21","onlineOnly":"N","additionalOnlineFiles":"Y","costCenters":[],"links":[{"id":290813,"rank":4,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/TEM1033.jpg"},{"id":310946,"rank":1,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tem/1033/report.pdf","text":"Report","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":310947,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tem/1033/plate-2.pdf","text":"Plate 2","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 2"},{"id":310948,"rank":3,"type":{"id":27,"text":"Table"},"url":"https://pubs.usgs.gov/tem/1033/table-2.pdf","text":"Table 2","linkFileType":{"id":1,"text":"pdf"},"description":"Table 2"}],"country":"United States","state":"New Mexico","county":"Eddy County","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-103.8111,32.9663],[-103.8112,32.903],[-103.8116,32.8876],[-103.8115,32.8725],[-103.8114,32.8575],[-103.8112,32.8429],[-103.8114,32.7974],[-103.8112,32.7823],[-103.8105,32.7122],[-103.8103,32.6971],[-103.8101,32.6247],[-103.81,32.6101],[-103.8097,32.5399],[-103.8096,32.5249],[-103.789,32.5245],[-103.7716,32.5246],[-103.7493,32.5242],[-103.7194,32.524],[-103.7166,32.524],[-103.7165,32.5085],[-103.7165,32.4916],[-103.7157,32.4429],[-103.7156,32.4278],[-103.7155,32.3535],[-103.7154,32.3385],[-103.7158,32.2692],[-103.7157,32.2546],[-103.7161,32.1817],[-103.716,32.1666],[-103.716,32.0918],[-103.7162,32.0631],[-103.7164,32.0015],[-103.9574,32.0011],[-103.9757,32.001],[-103.9936,32.001],[-104.0001,32.001],[-104.0011,32.001],[-104.0109,32.001],[-104.0265,32.001],[-104.0282,32.001],[-104.0617,32.0012],[-104.1475,32.0017],[-104.4014,32.0024],[-104.7313,32.0032],[-104.7467,32.0032],[-104.8299,32.0031],[-104.8466,32.0031],[-104.8464,32.0958],[-104.8462,32.1104],[-104.8463,32.1378],[-104.8461,32.1533],[-104.8457,32.2554],[-104.8495,32.2554],[-104.8493,32.3839],[-104.8496,32.399],[-104.8492,32.4286],[-104.8495,32.4427],[-104.8491,32.5124],[-104.849,32.5188],[-104.8392,32.5196],[-104.8389,32.5351],[-104.8384,32.608],[-104.8382,32.6253],[-104.8376,32.6986],[-104.8372,32.7268],[-104.8369,32.7856],[-104.8367,32.7992],[-104.8369,32.827],[-104.8366,32.8416],[-104.8364,32.8543],[-104.8362,32.8694],[-104.8357,32.903],[-104.8354,32.9659],[-104.8332,32.9659],[-104.8189,32.9662],[-104.8162,32.9661],[-104.802,32.966],[-104.7982,32.9659],[-104.779,32.9662],[-104.7686,32.9661],[-104.7621,32.966],[-104.7511,32.9664],[-104.7178,32.9664],[-104.7118,32.9664],[-104.7003,32.9662],[-104.6844,32.9661],[-104.6336,32.9664],[-104.6254,32.9663],[-104.6084,32.9665],[-104.5986,32.9664],[-104.3487,32.9663],[-104.3416,32.9661],[-104.3071,32.9661],[-104.2973,32.966],[-104.2896,32.9663],[-104.2803,32.9662],[-104.2617,32.9663],[-104.2552,32.9662],[-104.2448,32.9661],[-104.2382,32.9664],[-104.2278,32.9663],[-104.1939,32.9662],[-104.1758,32.9664],[-104.1589,32.9661],[-104.154,32.966],[-104.1425,32.9658],[-104.1365,32.9657],[-104.1327,32.9661],[-104.108,32.9662],[-104.1042,32.9661],[-104.0807,32.9662],[-104.0741,32.966],[-104.0643,32.9659],[-104.0523,32.9661],[-104.0495,32.9661],[-104.0402,32.9664],[-104.0348,32.9663],[-104.0315,32.9662],[-103.9834,32.9649],[-103.9741,32.9648],[-103.9593,32.965],[-103.9435,32.9651],[-103.9265,32.9653],[-103.8773,32.9657],[-103.8466,32.9661],[-103.8111,32.9663]]]},\"properties\":{\"name\":\"Eddy\",\"state\":\"NM\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"561e2b3be4b0cdb063e59cfa","contributors":{"authors":[{"text":"Jones, Charles Leslie","contributorId":27790,"corporation":false,"usgs":true,"family":"Jones","given":"Charles","email":"","middleInitial":"Leslie","affiliations":[],"preferred":false,"id":288141,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":71569,"text":"tei545 - 1959 - Gravity and seismic exploration in Yucca Valley, Nevada test site, January-April, 1959","interactions":[],"lastModifiedDate":"2015-10-20T13:04:38","indexId":"tei545","displayToPublicDate":"2013-07-18T11:22:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":337,"text":"Trace Elements Investigations","code":"TEI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"545","title":"Gravity and seismic exploration in Yucca Valley, Nevada test site, January-April, 1959","docAbstract":"The thickness of the alluvial and tuffaceous deposits that overlie bedrock in Yucca Valley has been inferred from gravity and seismic measurements. Preliminary interpretations indicate that these deposits are thickest in a narrow north-trending trough in the eastern part of the valley. The gravity data delineate a buried north-trending ridge of bedrock that extends from Mine Mountain almost to Quartzite Ridge.
\nSeismic refraction measurements confirm the existence of the bedrock ridge and indicate that the bedrock is as close as 100 feet to the surface. The buried bedrock high is important because it may alter concepts of the movement of groundwater within the valley.
\nA single seismic-refraction profile was located near the area of thickest alluvium and tuff to determine the feasibility of using refraction techniques for determining the depth to bedrock where it is covered with several thousand feet of alluvium and tuff. The results are encouraging but not enough data were acquired to give a reliable depth estimate.
\nSeismic-refraction measurements were used successfully to determine the thickness of alluvium in narrow valleys partly filled with alluvium.
\nThis work was in the northwestern part of Yucca Valley and was done to choose drilling sites for studies of ground-water movement.
\n","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Washington, D.C.","doi":"10.3133/tei545","collaboration":"Work done on behalf of the Albuquerque Operations Office, U.S. Atomic Energy Commission.","usgsCitation":"Diment, W.H., Healey, D., and Roller, J., 1959, Gravity and seismic exploration in Yucca Valley, Nevada test site, January-April, 1959: U.S. Geological Survey Trace Elements Investigations 545, Report: 41 p.; 1 Plate: 21.26 x 34.69 inches, https://doi.org/10.3133/tei545.","productDescription":"Report: 41 p.; 1 Plate: 21.26 x 34.69 inches","numberOfPages":"44","onlineOnly":"N","additionalOnlineFiles":"Y","temporalStart":"1959-01-01","temporalEnd":"1959-04-30","costCenters":[],"links":[{"id":290451,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/tei545.jpg"},{"id":310154,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/tei/545/report.pdf","text":"Report","size":"14.70 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Report"},{"id":310155,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/tei/545/plate-1.pdf","text":"Plate 1","size":"12.50 MB","linkFileType":{"id":1,"text":"pdf"},"description":"Plate 1"}],"country":"United States","state":"Nevada","county":"Nye County","otherGeospatial":"Yucca Valley","geographicExtents":"{\"type\":\"FeatureCollection\",\"features\":[{\"type\":\"Feature\",\"geometry\":{\"type\":\"Polygon\",\"coordinates\":[[[-115.9082,39.1615],[-115.5191,38.9578],[-115.4725,38.9325],[-115.4433,38.9162],[-115.3694,38.8769],[-115.363,38.874],[-115.242,38.8093],[-115.0969,38.7309],[-115.0777,38.721],[-115.0604,38.7107],[-115.0291,38.6937],[-114.999,38.6777],[-114.9996,38.592],[-114.9997,38.4315],[-114.9994,38.3894],[-115.0004,38.0507],[-115.1185,38.0508],[-115.1436,38.0508],[-115.326,38.0515],[-115.3453,38.0514],[-115.4003,38.051],[-115.4587,38.0506],[-115.6394,38.0512],[-115.6581,38.051],[-115.8404,38.0504],[-115.8931,38.0507],[-115.8938,37.723],[-115.8969,37.5498],[-115.8975,37.2796],[-115.8982,37.1926],[-115.8942,36.8425],[-115.8941,36.686],[-115.8945,36.6702],[-115.8949,36.598],[-115.8949,36.5962],[-115.8946,36.5858],[-115.8947,36.5005],[-115.8945,36.4806],[-115.8949,36.462],[-115.8944,36.457],[-115.8948,36.3087],[-115.8945,36.2923],[-115.8943,36.1957],[-115.8945,36.1608],[-115.8948,36.1163],[-115.8948,36.0927],[-115.895,36.0015],[-115.9178,36.0192],[-115.9518,36.0457],[-115.9925,36.0773],[-116.049,36.1211],[-116.0624,36.1314],[-116.1039,36.1636],[-116.1287,36.1829],[-116.1702,36.2152],[-116.173,36.2174],[-116.2311,36.2626],[-116.2834,36.3028],[-116.2954,36.3122],[-116.3752,36.373],[-116.5107,36.4764],[-116.5247,36.4871],[-116.5589,36.5131],[-116.574,36.5245],[-116.5946,36.54],[-116.6556,36.5867],[-116.6583,36.5888],[-116.6764,36.6024],[-116.706,36.6248],[-116.7895,36.6877],[-116.8424,36.7276],[-116.8453,36.7298],[-116.8806,36.7568],[-116.8912,36.7648],[-116.9237,36.7891],[-116.9641,36.8193],[-116.9783,36.8299],[-116.981,36.8319],[-117.0046,36.8495],[-117.164,36.9688],[-117.1639,36.9698],[-117.1637,37.0182],[-117.164,37.0894],[-117.1642,37.171],[-117.1641,37.1909],[-117.1641,37.1936],[-117.1665,37.6995],[-117.1664,37.714],[-117.1663,37.7285],[-117.1663,37.7435],[-117.1662,37.7585],[-117.1657,38.0019],[-117.2198,38.0482],[-117.2397,38.0483],[-117.239,38.0641],[-117.2408,38.0705],[-117.2653,38.0932],[-117.6896,38.4731],[-118.0197,38.7599],[-118.197,38.9154],[-118.1972,38.9993],[-117.8559,39.0746],[-117.7748,39.092],[-117.7008,39.1058],[-117.6409,39.1149],[-117.5946,39.1231],[-117.4742,39.1431],[-117.3823,39.1562],[-117.3609,39.1585],[-117.3318,39.1629],[-117.3063,39.1634],[-117.2849,39.1633],[-117.1995,39.1632],[-117.0856,39.1628],[-117.0322,39.1626],[-117.0144,39.1626],[-116.9871,39.1625],[-116.9158,39.1631],[-116.7562,39.1622],[-116.7301,39.1625],[-116.5996,39.1616],[-116.5859,39.162],[-116.4815,39.1616],[-116.3497,39.1618],[-116.2358,39.1616],[-116.0548,39.1624],[-115.9082,39.1615]]]},\"properties\":{\"name\":\"Nye\",\"state\":\"NV\"}}]}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"53cd5f19e4b0b290850fc1de","contributors":{"authors":[{"text":"Diment, William H.","contributorId":78797,"corporation":false,"usgs":true,"family":"Diment","given":"William","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":284407,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Healey, D.L.","contributorId":52964,"corporation":false,"usgs":true,"family":"Healey","given":"D.L.","email":"","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":284406,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Roller, J.C.","contributorId":12507,"corporation":false,"usgs":true,"family":"Roller","given":"J.C.","email":"","affiliations":[],"preferred":false,"id":284405,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70047487,"text":"70047487 - 1959 - Ground-water resources of the Oakland Park area of eastern Broward County, Florida","interactions":[{"subject":{"id":24519,"text":"ofr5891 - 1958 - Ground-water resources of the Oakland Park area of eastern Broward County, Florida","indexId":"ofr5891","publicationYear":"1958","noYear":false,"title":"Ground-water resources of the Oakland Park area of eastern Broward County, Florida"},"predicate":"SUPERSEDED_BY","object":{"id":70047487,"text":"70047487 - 1959 - Ground-water resources of the Oakland Park area of eastern Broward County, Florida","indexId":"70047487","publicationYear":"1959","noYear":false,"title":"Ground-water resources of the Oakland Park area of eastern Broward County, Florida"},"id":1}],"lastModifiedDate":"2017-09-13T17:55:10","indexId":"70047487","displayToPublicDate":"2013-01-01T15:18:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":5489,"text":"Florida Geological Survey Report of Investigations","active":false,"publicationSubtype":{"id":2}},"seriesNumber":"20","title":"Ground-water resources of the Oakland Park area of eastern Broward County, Florida","docAbstract":"The Biscayne aquifer is the source of all fresh ground water in the Oakland Park area of eastern Broward County, Florida. This aquifer extends from the land surface to more than 215 feet below mean sea level and is composed chiefly of sandy marine limestone, calcareous sandstone, and beds of fine to medium quartz sand. The aquifer differs from place to place, but, in general, most of the layers of limestone and sandstone occur at depths below 60 feet. The permeability of the aquifer increases with depth.","language":"English","publisher":"Florida Geological Survey","publisherLocation":"Tallahassee, FL","collaboration":"Prepared by the United States Geological Survey in cooperation with the City of Fort Lauderdale and the Florida Geological Survey","usgsCitation":"Sherwood, C., 1959, Ground-water resources of the Oakland Park area of eastern Broward County, Florida: Florida Geological Survey Report of Investigations 20, vii, 40 p.","productDescription":"vii, 40 p.","costCenters":[],"links":[{"id":276179,"type":{"id":11,"text":"Document"},"url":"https://ufdc.ufl.edu/UF00001204/00001/pdf?search=report+%3dinvestigations"},{"id":276180,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/70047487.PNG"}],"country":"United States","state":"Florida","county":"Broward County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -80.881389,25.95675 ], [ -80.881389,26.334667 ], [ -80.015276,26.334667 ], [ -80.015276,25.95675 ], [ -80.881389,25.95675 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5203a379e4b02bdb1bc63fa6","contributors":{"authors":[{"text":"Sherwood, C. B.","contributorId":27888,"corporation":false,"usgs":true,"family":"Sherwood","given":"C. B.","affiliations":[],"preferred":false,"id":482173,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":5220549,"text":"5220549 - 1959 - Mourning dove management in Eastern United States","interactions":[],"lastModifiedDate":"2012-02-02T00:14:42","indexId":"5220549","displayToPublicDate":"2010-06-16T12:18:16","publicationYear":"1959","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3140,"text":"Proceedings of the Annual Conference of the Southeastern Association of Game and Fish Commissioners","active":true,"publicationSubtype":{"id":10}},"title":"Mourning dove management in Eastern United States","largerWorkType":{"id":2,"text":"Article"},"largerWorkTitle":"Proceedings of the Annual Conference of the Southeastern Association of Game and Fish Commissioners","largerWorkSubtype":{"id":10,"text":"Journal Article"},"language":"English","usgsCitation":"Kiel, W., 1959, Mourning dove management in Eastern United States: Proceedings of the Annual Conference of the Southeastern Association of Game and Fish Commissioners, v. 13, p. 19-21.","productDescription":"19-21","startPage":"19","endPage":"21","numberOfPages":"3","costCenters":[{"id":531,"text":"Patuxent Wildlife Research Center","active":true,"usgs":true}],"links":[{"id":197039,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"13","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b32e4b07f02db6b47d3","contributors":{"authors":[{"text":"Kiel, W.H.","contributorId":105395,"corporation":false,"usgs":true,"family":"Kiel","given":"W.H.","email":"","affiliations":[],"preferred":false,"id":331995,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":56161,"text":"ofr5976 - 1959 - Surface waters of Illinois River basin in Arkansas and Oklahoma","interactions":[],"lastModifiedDate":"2012-02-02T00:12:10","indexId":"ofr5976","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"59-76","title":"Surface waters of Illinois River basin in Arkansas and Oklahoma","docAbstract":"The estimated runoff from the Illinois River basin of 1,660 square miles has averaged 1,160,000 acre-feet per year during the water years 1938-56, equivalent to an average annual runoff depth of 13.1 inches. About 47 percent of the streamflow is contributed from drainage in Arkansas, where an average of 550,000 acre-ft per year runs off from 755 square miles, 45.5 percent of the total drainage area.\r\nThe streamflow is highly variable. Twenty-two years of record for Illinois River near Tahlequah, Okla., shows a variation in runoff for the water year 1945 in comparison with 1954 in a ratio of almost 10 to 1. Runoff in 1927 may have exceeded that of 1945, according to records for White River at Beaver, Ark., the drainage basin just east of the Illinois River basin. Variation in daily discharge is suggested by a frequency analysis of low flows at the gaging station near Tahlequah, Okla. The mean flow at that site is 901 cfs (cubic feet per second), the median daily flow is 350 cfs, and the lowest 30-day mean flow in a year probably will be less than 130 cfs half of the time and less than 20 cfs every 10 years on the average.\r\n\r\nThe higher runoff tends to occur in the spring months, March to May, a 3-month period that, on the average, accounts for almost half of the annual flow. High runoff may occur during any month in the year, but in general, the streamflow is the lowest in the summer. The mean monthly flow of Illinois River near Tahlequah, Okla., for September is about 11 percent of that for May. Records show that there is flow throughout the year in Illinois River and its principal tributaries Osage Creek, Flint Creek and Barren Fork.\r\n\r\nThe high variability in streamflow in this region requires the development of storage by impoundment if maximum utilization of the available water supplies is to be attained. For example, a 120-day average low flow of 22 cfs occurred in 1954 at Illinois River near Tahlequah, Okla. To have maintained the flow at 350 cfs, the median daily flow during the 19-year base period, an impoundment at that site would have required a usable storage of 185,000 acre-ft to satisfy this demand during the drought years 1954-1956.\r\n\r\nThe surface waters of the Illinois River basin are excellent quality being suitable for municipal, agriculture and most industrial uses. The average concentration of the dissolved mineral content is about 105 ppm (parts per million) and the hardness about 85 ppm. The water is slightly alkaline, having a range of pH values from 7.2 to 8.0.\r\n\r\nThis report gives the estimated average discharge at gaging stations and approximations of average discharge at the State line for 3 sub-basins during the 19-year period October 1937 to September 1956, used as a base period in this report. Duration-of-flow data for various percentages of the time are shown for the period of observed record at the gaging stations; similar data are estimated for the selected base period. Storage requirements to sustain flow during the recent drought years are given for 3 stations. The streamflow records in the basin are presented on a monthly and annual basis through September 1957; provisional records for 3 stations are included through July 1958 for correlation purposes. Results of discharge measurements are given for miscellaneous sites where low-flow observations have been made.\r\n\r\n(available as photostat copy only)","language":"ENGLISH","doi":"10.3133/ofr5976","usgsCitation":"Laine, L., 1959, Surface waters of Illinois River basin in Arkansas and Oklahoma: U.S. Geological Survey Open-File Report 59-76, 65 p., 13 figs., https://doi.org/10.3133/ofr5976.","productDescription":"65 p., 13 figs.","costCenters":[],"links":[{"id":184636,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4aeee4b07f02db6912cd","contributors":{"authors":[{"text":"Laine, L.L.","contributorId":100464,"corporation":false,"usgs":true,"family":"Laine","given":"L.L.","email":"","affiliations":[],"preferred":false,"id":254854,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":1035,"text":"wsp1483 - 1959 - Geology and ground-water resources of the upper Lodgepole Creek drainage basin, Wyoming, with a section on chemical quality of the water","interactions":[],"lastModifiedDate":"2017-09-20T16:00:17","indexId":"wsp1483","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1483","title":"Geology and ground-water resources of the upper Lodgepole Creek drainage basin, Wyoming, with a section on chemical quality of the water","docAbstract":"The principal sources of ground-water supply in the upper Lodgepole Creek drainage basin-the part of the basin west of the Wyoming-Nebraska State line-are the Brule formation of Oligocene age, the Arikaree formation of Miocene age, the Ogallala formation of Pliocene age, and the unconsolidated deposits of Quaternary age. \r\n\r\nThe Brule formation is a moderately hard siltstone that generally is not a good aquifer. However, where it is fractured or where the upper part consists of pebbles of reworked siltstone, it will yield large quantities of water to wells. Many wells in the Pine Bluffs lowland, at the east end of the area, derive water from the Brule. The Arikaree formation, which consists of loosely to moderately cemented fine sand, will yield small quantities of water to wells but is not thick enough or permeable enough to supply sufficient water for irrigation. Only a few wells derive water from it. The Ogallala formation consists of lenticular beds of clay, silt, sand, and gravel which, in part, are cemented with calcium carbonate. Only the lower part of the formation is saturated. Nearly all the wells in the upland part of the area tap the Ogallala, but they supply water in amounts sufficient for domestic and stock use only. Two of the wells have a moderately large discharge, and other wells of comparable discharge probably could be drilled in those parts of the upland where the saturated part of the Ogallala is fairly thick. Most of the unconsolidated deposits of Quaternary age are very permeable and, where a sufficient thickness is saturated, will yield large quantities of water to wells. These deposits are a significant source of water supply in the southeastern part of the area. \r\n\r\nThe Chadron formation of Oligocene age, which underlies the Brule formation, is a medium- to coarse-grained sandstone where it crops out in the Islay lowland. No wells tap the Chadron, but it probably would yield small quantities of water to wells. It lies at a relatively shallow depth beneath most of the Islay lowland, near the west end of the area, and at a depth of about 800 feet beneath the Pine Bluffs lowland. In the latter area it probably is finer grained and may not be permeable enough to yield water to wells. All the ground water in the area is derived from precipitation. It is estimated that about 5 percent of the precipitation infiltrates directly to the zone of saturation. The remainder either is evaporated immediately; is retained by the soil, later to be evaporated or transpired; or is discharged by overland flow to the surface drainage courses. Most of the water that reaches the surface drainage courses eventually sinks to the zone of saturation or is evaporated. The slope of the water table and the movement of ground water are generally eastward. The depth to water ranges from less than 10 feet in parts of the valley to about 300 feet in the upland areas. In much of the Pine Bluffs lowland, the depth to water is less than 50 feet. Ground water not pumped from wells within the area is discharged by evapotranspiration where the water table is close to the land surface, by outflow into streams, or by underflow eastward beneath the State line. \r\n\r\nThe chemical quality of ground water from the principal sources is remarkably uniform, and the range in concentration of dissolved constituents is narrow. In general, the water is of the calcium bicarbonate type, is hard (hardness as CaC03 is as high as 246 ppm), and contains less than about 400 parts per million of dissolved solids, which is a moderate mineralization. Silica constitutes a large proportion of the dissolved solids. \r\n\r\nThe water is suitable for irrigation and, except for iron in water from some wells that tap the Ogallala formation, meets the drinking water standards of the U.S. Public Health Service for chemical constituents. Because the water is siliceous, alkaline, and hard, it is unsuitable for many industrial uses unless treated.","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1483","usgsCitation":"Bjorklund, L.J., Krieger, R.A., and Jochens, E.R., 1959, Geology and ground-water resources of the upper Lodgepole Creek drainage basin, Wyoming, with a section on chemical quality of the water: U.S. Geological Survey Water Supply Paper 1483, iv, 40 p. :maps (2 fold. in pocket) diagr., tables. ;25 cm., https://doi.org/10.3133/wsp1483.","productDescription":"iv, 40 p. :maps (2 fold. in pocket) diagr., tables. ;25 cm.","costCenters":[{"id":5050,"text":"WY-MT Water Science Center","active":true,"usgs":true}],"links":[{"id":137967,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1483/report-thumb.jpg"},{"id":25672,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1483/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25673,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/wsp/1483/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":25674,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1483/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad9e4b07f02db6852ae","contributors":{"authors":[{"text":"Bjorklund, Louis Jay","contributorId":21138,"corporation":false,"usgs":true,"family":"Bjorklund","given":"Louis","email":"","middleInitial":"Jay","affiliations":[],"preferred":false,"id":143068,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Krieger, R. A.","contributorId":11202,"corporation":false,"usgs":true,"family":"Krieger","given":"R.","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":143067,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Jochens, E. R.","contributorId":101250,"corporation":false,"usgs":true,"family":"Jochens","given":"E.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":143069,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":61435,"text":"mf182 - 1959 - Bedrock geology of the northern and eastern parts of the North Range, Cuyuna district, Minnesota","interactions":[],"lastModifiedDate":"2019-05-28T08:25:02","indexId":"mf182","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":325,"text":"Miscellaneous Field Studies Map","code":"MF","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"182","title":"Bedrock geology of the northern and eastern parts of the North Range, Cuyuna district, Minnesota","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/mf182","usgsCitation":"Schmidt, R.G., 1959, Bedrock geology of the northern and eastern parts of the North Range, Cuyuna district, Minnesota: U.S. Geological Survey Miscellaneous Field Studies Map 182, 1 map on 5 sheets, https://doi.org/10.3133/mf182.","productDescription":"1 map on 5 sheets","costCenters":[],"links":[{"id":182872,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mf/0182/report-thumb.jpg"},{"id":364160,"rank":3,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0182/plate-8.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":364161,"rank":4,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0182/plate-7.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":364159,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0182/plate-9.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":364163,"rank":6,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0182/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":364162,"rank":5,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0182/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"7200","country":"United States","state":"Minnesota","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -94.1,46.45 ], [ -94.1,46.55 ], [ -93.81694444444445,46.55 ], [ -93.81694444444445,46.45 ], [ -94.1,46.45 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a5ee4b07f02db633f4b","contributors":{"authors":[{"text":"Schmidt, R. G.","contributorId":107690,"corporation":false,"usgs":true,"family":"Schmidt","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":265637,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":13682,"text":"ofr5941 - 1959 - Geology of the State of Morelos and contiguous areas in south-central Mexico","interactions":[],"lastModifiedDate":"2012-02-02T00:07:01","indexId":"ofr5941","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"59-41","title":"Geology of the State of Morelos and contiguous areas in south-central Mexico","docAbstract":"The area described lies in south-central Mexico and embraces all but the southeastern corner and easternmost border of the State of Moreles, the second smallest State in the Mexican Republic. It includes small contiguous parts of the State of Mexico, in the northeastern corner, and of the State of Guerrero in the southwestern corner. Limiting geographic coordinates are 98 45\u0019 to 99 39\u001D west longitude and 18 18\u0019 to 19 08\u0019 north latitude, the northern boundary being only 35 km south of Mexico City, capital of the Republic. The geological map does not cover the entire rectangle outlined, but is irregular in form and measures roughly 4150 sq. km, three-quarters of it representing two0thirds of the State of Moreles and the rest lying outside the State.\r\n\r\nThe region ranges in altitude from 730 m above sea level at Iguala near the south edge of the map, to a general level of about 3000 m at the north edge, although individual peaks rise to 3900 m and Popocatepetl Volcano, a few kilometers east of the northeastern border of the map, rises to 5452 m above sea level. Annual rainfall ranges from a minimum of about 640 mm in the low country, to 1200 mm and more at altitudes above 2000 m. Most of it falls in summer between June and September. Winter frosts are rare below 1800 m. The climate is of savanna to steppe type; soils are thin and may be classified as belonging to the tachernoses group, with strong development of calcareous evaporates (caliche) at altitudes below 1800 m.\r\n\r\nThe northern border of the area forms the southern half of the late Pliocene to Recent Neo-volcanic Belt of basic volcanism that crosses Mexico in the direction N. 80 W., and thus has constructional topography. The rest of the area belongs to the Balsas Basin physiographic province, which is characterized by maturely dissected terrain tributary to the large Balsas River. All but the southwestern corner of the area drains southward via the Amacuzac River into the Mexcala-Balsas River, and thence westward into the Pacific Ocean. The southwestern corner drains directly into the Balsas River via the Iguala River. Local relief is of the order of 300 to 600 m. The mature topography was partly buried by late Pliocene alluvium in the central part of the area, owing largely to local volcanism. Dissolution of limestone, dolomite, and anhydrite of the Cretaceous formations has produced sinks and poljes, some of which contain small lakes. Other karst features are also common, such as caves, caverns, underground rivers, and surficial lapies or karren. Drainage blocking by lava and polje development in late Pleistocene and Recent time produced new alluvial flats in this otherwise dissected region.\r\n\r\nThe oldest rock unit in the region is the Texco schist series of late Paleozoic (?) age. It was folded, metamorphosed, foliated, intruded by dikes, and strongly eroded before the next unit, the Texco Viejo green volcanic series of Late Triassic (?) age, was deposited. Another period of metamorphism and erosion followed before the calcareous clastic sediments of the Upper Jurassic (?) Acahuizotla formation were laid down. The next unit consists of the partly phyllitic calcareous shale of the Acuitlapan formation, which is of Neocenian (?) age and rests with at least disconformity on the Acahuizotla formation. The overlying Aptian-Barresian Kochicalco formation of thin-bedded limestone appears to grade upward from the Acuitlapan formation, locally, but it seems to be unconformable elsewhere. All these units have small outcrops in the area mapped and were not studied in detail.\r\n\r\nWarping and erosion occurred before the overlying Morelos formation began to accumulate in early Albian time. The basal member is anhydrite in the eastern part of the area mapped, but limestone and dolomite were deposited elsewhere. The formation consists largely of shallow-water calcareous bank deposits, with a maximum thickness of about 900 m. Deposition ceased in early Cenomanian time and further warpi","language":"ENGLISH","publisher":"U.S. Geological Survey],","doi":"10.3133/ofr5941","usgsCitation":"Fries, C.F., 1959, Geology of the State of Morelos and contiguous areas in south-central Mexico: U.S. Geological Survey Open-File Report 59-41, xi, 210 p., 22 plates :ill., maps ;27 cm., https://doi.org/10.3133/ofr5941.","productDescription":"xi, 210 p., 22 plates :ill., maps ;27 cm.","costCenters":[],"links":[{"id":147587,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1959/0041/report-thumb.jpg"},{"id":42230,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1959/0041/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42231,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1959/0041/plate-2.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42232,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1959/0041/plate-3.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42233,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/of/1959/0041/plate-4.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":42234,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1959/0041/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acce4b07f02db67e421","contributors":{"authors":[{"text":"Fries, Carl F.","contributorId":107299,"corporation":false,"usgs":true,"family":"Fries","given":"Carl","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":168226,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":33740,"text":"b1077 - 1959 - Geology of the Lake Mary quadrangle, Iron County, Michigan","interactions":[{"subject":{"id":12610,"text":"ofr565 - 1956 - Preliminary report on the geology of Lake Mary quadrangle, Iron County, Michigan","indexId":"ofr565","publicationYear":"1956","noYear":false,"title":"Preliminary report on the geology of Lake Mary quadrangle, Iron County, Michigan"},"predicate":"SUPERSEDED_BY","object":{"id":33740,"text":"b1077 - 1959 - Geology of the Lake Mary quadrangle, Iron County, Michigan","indexId":"b1077","publicationYear":"1959","noYear":false,"title":"Geology of the Lake Mary quadrangle, Iron County, Michigan"},"id":1}],"lastModifiedDate":"2016-08-26T14:32:11","indexId":"b1077","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1077","title":"Geology of the Lake Mary quadrangle, Iron County, Michigan","docAbstract":"
The Lake Mary quadrangle is in eastern Iron County, in the west part of the Upper Peninsula of Michigan. The quadrangle is underlain by Lower and Middle Precambrian rocks, formerly designated Archean and Algonkian rocks, and is extensively covered by Pleistocene glacial deposits. A few Upper Precambrian (Keweenawan) diabase dikes and two remnants of sandstone and dolomite of early Paleozoic age are also found in the area.
The major structural feature is the Holmes Lake anticline, the axis of which strikes northwest through the northeast part of the quadrangle. Most of the quadrangle, therefore, is underlain by rock of the west limb of the anticline. To the northwest along the fold axis, the Holmes Lake anticline is separated from the Amasa oval by a saddle of transverse folds in the vicinity of Michigamme Mountain in the Kiernan quadrangle.
The Lower Precambrian rocks are represented by the Dickinson group and by porphyritic red granite whose relation to the Dickinson group is uncertain, but which may be older. The rocks of the Dickinson group are chiefly green to black metavolcanic schist and red felsite, some of the latter metarhyolite. The dark schist is commonly magnetic. The Dickinson group underlies the core area of the Holmes Lake anticline, which is flanked by steeply dipping Middle Precambrian formations of the Animikie series.
A major unconformity separates the Lower Precambrian rocks from the overlying Middle Precambrian rocks. In ascending order the formations of the Middle Precambrian are the Randville dolomite, the Hemlock formation, which includes the Mansfield iron-bearing slate member, and the Michigamme slate. An unconformity occurs between the Hemlock formation and Michigamme slate. The post-Hemlock unconformity is thought to be represented in the Lake Mary quadrangle by the absence of iron-formation of the Amasa formation, which is known to lie between the Hemlock and the Michigamme to the northwest of the Lake Mary quadrangle in the Crystal Falls quadrangle. Post-Hemlock erosion may account also for the absence of iron-formation of the Fence River formation on the east limb of the Holmes Lake anticline within the Lake Mary quadrangle.
The Randville dolomite is not exposed and is known only from diamond drilling in the northeast part of the area where it occurs in the east and west limbs of the Holmes Lake anticline. The formation has a maximum thickness of about 2,100 feet; this includes a lower arkosic phase, some of which is quartz pebble conglomerate, a medial dolomitic phase, and an upper slate phase. The triad is gradational. Included within the formation are a few beds of chloritic schist thought to be of volcanic origin. An unconformity between the Randville and the succeeding Hemlock is not indicated in the quadrangle, but is probably present.
The Hemlock formation is best exposed in the northwest and south-central parts of the area. The apparent thickness of the formation is 10,000- 17,000 feet. It is composed mainly of mafic metavolcanic rocks and intercalated slate and iron-formation. In the north part of the quadrangle the volcanic rocks are greenstone, which includes altered basaltic flow rocks, volcanic breccia, tuff, and slate. Pillow structures are common in the metabasalt. It is not certain if any Hemlock rocks are present in the east limb of the Holmes Lake anticline. In the south part of the quadrangle, the rocks of the Hemlock are chiefly chlorite and hornblende schist and hornfels. Pyroxene hornfels is sparingly present.
At least two sedimentary slate belts are included in the Hemlock formation. One of these, the Mansfield iron-bearing slate member, includes in its upper part an altered chert-siderite iron-formation 30 to over 150 feet thick from which iron ore has been mined at the Mansfield location. The position of the iron-bearing rocks has been determined magnetically, and past explorations for iron ore are discussed.
Though probably; unconformable, the contact between the Hemlock and the Michigamme formations appears conformable. The Michigamme slate consists of at least 4,000 feet of interbedded mica schist and granulite, the altered equivalents of the slate and graywacke characteristic of the Michigamme in adjacent areas. The Michigamme rocks are best exposed in the south part of the quadrangle in the vicinity of Peavy Pond.
Two periods of regional metamorphism have resulted in the alteration of almost all of the rocks of the quadrangle. The Lower Precambrian rocks underwent at least one period of metamorphism, uplift, and erosion before the deposition of the Randville dolomite. After the deposition of the Michigamme slate, a post-Middle Precambrian period of regional metamorphism occurred with attending deformation and igneous intrusion. The grade of metamorphism rises toward the south in the area. The rocks in the northern two-thirds of the quadrangle are representative of greenschist facies of regional metamorphism, whereas the rocks in the southern onethird of the quadrangle are representative of the albite-epidote-amphibolite, the amphibolite, and the pyroxene hornfels facies, the metamorphic node centering about the intrusive Peavy Pond complex in the Peavy Pond area.
The Precambrian sedimentary and volcanic rocks are cut by intrusive igneous rocks of different types and several different ages. Gabbroic sills and dikes invaded the Hemlock rocks at some time after the Hemlock was deposited and before the post-Middle Precambrian orogeny and metamorphism. Some contact metamorphism attended the intrusion of the major sills. One of the sills, the West Kiernan sill, is well differentiated. A syntectonic igneous body, composed of gabbro and minor ultramafic parts and fringed with intermediate and felsic differentiates and hybrids, the Peavy; Pond complex, was intruded into the Hemlock and Michigamme formations during the post-Middle Precambrian orogeny. The complex is situated in the Peavy Pond area at the crest of the regional metamorphic node. Contact-altered sedimentary and volcanic rocks margin the complex.
The effects of regional metamorphism have been superposed on the contact metamorphic rocks peripheral to the complex and on the igneous rocks of the complex as well. The mafic augite-bearing rocks of the complex emplaced early in the orogeny were deformed by granulation at the peak of the deformation and subsequently metamorphosed to hornblende rocks. Some of the intermediate and felsic rocks of the complex were foliated by the deformation, while the more fluid, felsic parts of the complex were intruded under orogenic stress and crystallized after the peak of deformation. The deformation culminated in major faulting during which the formations were dislocated, and some of the granite of the complex was extremely brecciated.
A few diabase dikes, probably of Keweenawan age, have intruded the deformed and altered Animikie rocks.
The only known metallic resource is iron ore. The Mansfield mine produced 1¥2 million tons of high-grade iron ore between the years 1890 and 1913. Sporadic exploration since 1913 has failed to reveal other ore deposits of economic importance.
","language":"English","publisher":"U. S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/b1077","collaboration":"Prepared in cooperation with the Geological Survey Division Michigan Department of Conservation","usgsCitation":"Bayley, R.W., 1959, Geology of the Lake Mary quadrangle, Iron County, Michigan: U.S. Geological Survey Bulletin 1077, Document: v, 112 p.; 7 Plates: 38.91 x 33.74 inches or smaller, https://doi.org/10.3133/b1077.","productDescription":"Document: v, 112 p.; 7 Plates: 38.91 x 33.74 inches or smaller","costCenters":[{"id":382,"text":"Michigan Water Science Center","active":true,"usgs":true}],"links":[{"id":96076,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-1.pdf","size":"5234","linkFileType":{"id":1,"text":"pdf"}},{"id":96077,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-2.pdf","size":"3204","linkFileType":{"id":1,"text":"pdf"}},{"id":96078,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-3.pdf","size":"3526","linkFileType":{"id":1,"text":"pdf"}},{"id":96079,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-4.pdf","size":"981","linkFileType":{"id":1,"text":"pdf"}},{"id":96080,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-5.pdf","size":"2776","linkFileType":{"id":1,"text":"pdf"}},{"id":96081,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-6.pdf","size":"2526","linkFileType":{"id":1,"text":"pdf"}},{"id":96082,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1077/plate-7.pdf","size":"289","linkFileType":{"id":1,"text":"pdf"}},{"id":109296,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20736.htm","linkFileType":{"id":5,"text":"html"},"description":"20736"},{"id":61608,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1077/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":163861,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1077/report-thumb.jpg"}],"country":"United States","state":"Michigan","county":"Iron County","otherGeospatial":"Lake Mary quadrangle","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -88.25,\n 46.125\n ],\n [\n -88.25,\n 46\n ],\n [\n -88.125,\n 46\n ],\n [\n -88.125,\n 46.125\n ],\n [\n -88.25,\n 46.125\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4acee4b07f02db67f91d","contributors":{"authors":[{"text":"Bayley, Richard W.","contributorId":106084,"corporation":false,"usgs":true,"family":"Bayley","given":"Richard","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":211857,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":36259,"text":"b1072K - 1959 - Geology and oil and gas possibilities of upper Mississippian rocks of southwestern Virginia, southern West Virginia and eastern Kentucky","interactions":[],"lastModifiedDate":"2022-10-27T18:46:47.689656","indexId":"b1072K","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":306,"text":"Bulletin","code":"B","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1072","chapter":"K","title":"Geology and oil and gas possibilities of upper Mississippian rocks of southwestern Virginia, southern West Virginia and eastern Kentucky","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/b1072K","usgsCitation":"Wilpolt, R.H., and Marden, D.W., 1959, Geology and oil and gas possibilities of upper Mississippian rocks of southwestern Virginia, southern West Virginia and eastern Kentucky: U.S. Geological Survey Bulletin 1072, Report: iv, 70 p.; 3 Plates: 55.00 × 40.21 inches or smaller, https://doi.org/10.3133/b1072K.","productDescription":"Report: iv, 70 p.; 3 Plates: 55.00 × 40.21 inches or smaller","startPage":"587","endPage":"656","costCenters":[],"links":[{"id":109284,"rank":700,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_20723.htm","linkFileType":{"id":5,"text":"html"},"description":"20723"},{"id":64205,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/bul/1072k/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":165048,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/bul/1072k/report-thumb.jpg"},{"id":97333,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072k/plate-29.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":97332,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072k/plate-28.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":97331,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/bul/1072k/plate-27.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Kentucky, Virginia, West Virginia","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -81,\n 38\n ],\n [\n -84,\n 38\n ],\n [\n -84,\n 36.5\n ],\n [\n -81,\n 36.5\n ],\n [\n -81,\n 38\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad8e4b07f02db684817","contributors":{"authors":[{"text":"Wilpolt, Ralph H.","contributorId":42244,"corporation":false,"usgs":true,"family":"Wilpolt","given":"Ralph","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":216022,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Marden, Douglas W.","contributorId":74030,"corporation":false,"usgs":true,"family":"Marden","given":"Douglas","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":216023,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":15345,"text":"ofr5992 - 1959 - Geology of the upper Killik-Itkillik region, Alaska","interactions":[{"subject":{"id":15345,"text":"ofr5992 - 1959 - Geology of the upper Killik-Itkillik region, Alaska","indexId":"ofr5992","publicationYear":"1959","noYear":false,"title":"Geology of the upper Killik-Itkillik region, Alaska"},"predicate":"SUPERSEDED_BY","object":{"id":39101,"text":"pp303G - 1964 - Geology of the Killik-Itkillik region, Alaska","indexId":"pp303G","publicationYear":"1964","noYear":false,"chapter":"G","title":"Geology of the Killik-Itkillik region, Alaska"},"id":1}],"supersededBy":{"id":39101,"text":"pp303G - 1964 - Geology of the Killik-Itkillik region, Alaska","indexId":"pp303G","publicationYear":"1964","noYear":false,"title":"Geology of the Killik-Itkillik region, Alaska"},"lastModifiedDate":"2025-04-02T13:49:47.460719","indexId":"ofr5992","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"59-92","title":"Geology of the upper Killik-Itkillik region, Alaska","docAbstract":"The upper Killik-Itkillik map area is a 2,500 square mile segment of foothills along the north front of the Brooks Range on the Arctic Slope of Alaska. The rocks exposed in this area include eleven formations of sedimentary rocks, three types of surficial deposits, and one igneous rock unit. The oldest rocks are a 2,500-foot sequence of limestone which belongs to the Lisburne group (Mississippian). The Lisburne is succeeded by the Siksikpuk formation (Permian ?), a 300-foot unit of variegated shale and siltstone. The Shublik formation (Triassic), composed of 200 to 750 feet of fossiliferous dark shale, limestone, and chart, rests upon the Siksikpuk. Next above the Shublik is a sequence, more than 13,000 feet thick, of marine shale and graywacke which is subdivided into four formations: Tiglukpuk (Late Jurassic), Okpikruak (earliest Cretaceous), Fortress Mountain (late Early Cretaceous), and Torok (late Early Cretaceous). The youngest rocks comprise the Nanushuk group (late Early to Late Cretaceous) which consists of 5,000 feet of interfingering marine and non-marine clastic rocks and is subdivided into three formations: Tuktu, Chandler, and Ninuluk.
Small diabase sills, thought to be of latest Jurassic age, intrude the Tiglukpuk and older formations in the western part of the map area.
The rocks of the map area have been deformed by north-south tectonic forces in such a way that the upper part of the crust appears to have moved northward relative to deeper parts. Five east-trending zones of distinctive lithology and structure are recognizable: zone I, at the mountain front-massive strata of the Lisburne group sliced by southward dipping imbricate faults and locally thrust upon the younger strata of the dipping imbricate faults and locally thrust upon the younger strata of the foothills, zone II—relatively incompetent interfolded late Paleozoic and Mesozoic strata characterized by isoclinal folds and by small, closely spaced high-angle faults, zone III--chiefly rocks of the Fortress Mountain formation which, although folded and faulted, are not as complexly deformed as the rocks of zone II, zone IV - highly crenulated shale of the Torok formation, and zone V, at the northern edge of the map area--gently folded strata of the Nanushuk group.
A seismograph survey across zone IV suggests that, although the incompetent Torok formation is highly crenulated, the subsurface strata lie nearly flat.
The character of the subsurface structure in zones II and III is uncertain. However, it is believed that some of the high-angle faults in these two zones may flatten in the subsurface and merge into large sole faults beneath thrust plates of Paleozoic limestone. Such a fault pattern has been found in the foothills of the Alberta Rockies, where the surface structure, stratigraphy and geologic history are remarkably similar.
The depositional history of the Paleozoic and Mesozoic strata is divided into a shelf phase during late Paleozoic and Triassic and a geosynclinal phase during Late Jurassic and Cretaceous. The shelf sediments were chiefly marine carbonates and fine clastics, apparently derived largely from the north. The geosynclinal sediments consisted of marine graywacke \"flysch\" deposits overlain by littoral marine and non-marine coal-bearing \"molasse\" deposits and were derived mainly from the south. Several periods of emergence and erosion interrupted the shelf and geosynclinal deposition; evidently some folding and faulting occurred during deposition of the \"flysch\". The principal deformation is believed to have coincided with the Laramide orogeny in Late Cretaceous or Tertiary.
In the Pleistocene the Brooks Range was intensively glaciated, and at times of maximum advance, ice tongues along the major river valleys pushed northward into the foothills.
Investigations of bauxite deposits on Kauai by the U. S. Geological Survey in cooperation with the State of Hawaii were begun July 1, 1959. The investigations, as planned, are to consist of two phases, each of two years duration. The geological investigations of the bauxite and associated rocks in the field and a considerable amount of chemical and mineralogical work in the laboratory are planned for completion during the first two years of the project. During this phase, a geologist and an assistant will be working on Kauai and geologists, mineralogists, and chemists will be analyzing and studying samples of the bauxite in laboratories of the Geological Survey at Beltsville, Maryland, and Washington, D. C. The work during the second phase of the investigations will be carried on at Beltsville and Washington and will consist of completion of chemical and mineralogical investigations, compilation of maps, analysis of field and laboratory data including determination of the size and quality of the bauxite deposits in the eastern part of Kauai, mineralogical research on bauxite samples, and preparation of a final geological report.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr60109","usgsCitation":"Patterson, S.H., 1959, Progress report on the investigations of bauxite deposits in the eastern part of Kauai, Hawaii: U.S. Geological Survey Open-File Report 60-109, 12 p., https://doi.org/10.3133/ofr60109.","productDescription":"12 p.","costCenters":[],"links":[{"id":430541,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1960/0109/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":147997,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1960/0109/report-thumb.jpg"}],"country":"United States","state":"Hawaii","otherGeospatial":"eastern Kauai","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -159.50513794376542,\n 22.23123347395571\n ],\n [\n -159.50513794376542,\n 21.87358021194069\n ],\n [\n -159.2806096009181,\n 21.87358021194069\n ],\n [\n -159.2806096009181,\n 22.23123347395571\n ],\n [\n -159.50513794376542,\n 22.23123347395571\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a9be4b07f02db65db85","contributors":{"authors":[{"text":"Patterson, Sam H.","contributorId":62996,"corporation":false,"usgs":true,"family":"Patterson","given":"Sam","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":170985,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":39758,"text":"pp309 - 1959 - The Geology of the Upper Mississippi Valley Zinc-Lead District","interactions":[],"lastModifiedDate":"2017-10-26T14:34:21","indexId":"pp309","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"309","title":"The Geology of the Upper Mississippi Valley Zinc-Lead District","docAbstract":"The upper Mississippi Valley zinc-lead district includes the southwest part of Wisconsin, the northwest corner of Illinois, and a narrow fringe of Iowa extending from Bellevue to McGregor, just west of the Mississippi River. The total area of the district is 4,000 square miles. The entire district is drained by the Mississippi River and its tributaries. The central part is a rolling plain dissected to a depth of about 300 feet by the larger stream valleys. Marginal parts of the district are relatively hilly. Most of the district lies within the so-called \"Driftless Area\", but glacial deposits occur in the eastern, southeastern, and western fringes of the district.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington, D.C.","doi":"10.3133/pp309","collaboration":"Prepared in cooperation with the Wisconsin Geological and Natural History Survey, the Iowa Geological Survey, and the Illinois State Geological Survey","usgsCitation":"Heyl, A.V., Agnew, A.F., Lyons, E.J., Behre, C.H., and Flint, A., 1959, The Geology of the Upper Mississippi Valley Zinc-Lead District: U.S. Geological Survey Professional Paper 309, Report: x, 310 p.; 24 Plates: 61.5 x 37.5 inches or smaller, https://doi.org/10.3133/pp309.","productDescription":"Report: x, 310 p.; 24 Plates: 61.5 x 37.5 inches or smaller","costCenters":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"links":[{"id":67616,"rank":423,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-24.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67617,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0309/report.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67608,"rank":415,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-16.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67609,"rank":416,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-17.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67593,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-01.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67594,"rank":401,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-02.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67595,"rank":402,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-03.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67596,"rank":403,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-04.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67597,"rank":404,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-05.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67598,"rank":405,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-06.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67599,"rank":406,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-07.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67600,"rank":407,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-08.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67601,"rank":408,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-09.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67602,"rank":409,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-10.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67603,"rank":410,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-11.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67604,"rank":411,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-12.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67605,"rank":412,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-13.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67606,"rank":413,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-14.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67607,"rank":414,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-15.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":104425,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_4291.htm","linkFileType":{"id":5,"text":"html"},"description":"4291"},{"id":172773,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0309/report-thumb.jpg"},{"id":67615,"rank":422,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-23.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67610,"rank":417,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-18.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67611,"rank":418,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-19.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67612,"rank":419,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-20.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67613,"rank":420,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-21.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":67614,"rank":421,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/pp/0309/plate-22.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Illinois, Iowa, Wisconsin","otherGeospatial":"Upper Mississippi Valley","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -91.51885986328125,\n 42.02481360781777\n ],\n [\n -89.26391601562499,\n 42.02481360781777\n ],\n [\n -89.26391601562499,\n 43.23719944365308\n ],\n [\n -91.51885986328125,\n 43.23719944365308\n ],\n [\n -91.51885986328125,\n 42.02481360781777\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ac9e4b07f02db67c671","contributors":{"authors":[{"text":"Heyl, Allen V. Jr.","contributorId":81168,"corporation":false,"usgs":true,"family":"Heyl","given":"Allen","suffix":"Jr.","email":"","middleInitial":"V.","affiliations":[],"preferred":false,"id":222105,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Agnew, Allen F.","contributorId":105702,"corporation":false,"usgs":true,"family":"Agnew","given":"Allen","email":"","middleInitial":"F.","affiliations":[],"preferred":false,"id":222107,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Lyons, Erwin J.","contributorId":87124,"corporation":false,"usgs":true,"family":"Lyons","given":"Erwin","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":222106,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Behre, Charles H. Jr.","contributorId":14880,"corporation":false,"usgs":true,"family":"Behre","given":"Charles","suffix":"Jr.","email":"","middleInitial":"H.","affiliations":[],"preferred":false,"id":222103,"contributorType":{"id":1,"text":"Authors"},"rank":4},{"text":"Flint, Arthur E.","contributorId":45300,"corporation":false,"usgs":true,"family":"Flint","given":"Arthur E.","affiliations":[],"preferred":false,"id":222104,"contributorType":{"id":1,"text":"Authors"},"rank":5}]}} ,{"id":61459,"text":"mf210 - 1959 - Preliminary geologic and structure map of the east-central part of the Cascade Springs quadrangle, Fall River County, South Dakota","interactions":[],"lastModifiedDate":"2018-12-14T11:15:19","indexId":"mf210","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":325,"text":"Miscellaneous Field Studies Map","code":"MF","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"210","title":"Preliminary geologic and structure map of the east-central part of the Cascade Springs quadrangle, Fall River County, South Dakota","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/mf210","usgsCitation":"Post, E., and Lane, D.W., 1959, Preliminary geologic and structure map of the east-central part of the Cascade Springs quadrangle, Fall River County, South Dakota: U.S. Geological Survey Miscellaneous Field Studies Map 210, 36.46 x 31.65 inches, https://doi.org/10.3133/mf210.","productDescription":"36.46 x 31.65 inches","costCenters":[],"links":[{"id":182681,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/mf/0210/report-thumb.jpg"},{"id":360306,"rank":2,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/mf/0210/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"South Dakota","county":"Fall River County","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -130.5,43.284166666666664 ], [ -130.5,43.333333333333336 ], [ -103.55111111111111,43.333333333333336 ], [ -103.55111111111111,43.284166666666664 ], [ -130.5,43.284166666666664 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4b05e4b07f02db699b77","contributors":{"authors":[{"text":"Post, Edwin V.","contributorId":80330,"corporation":false,"usgs":true,"family":"Post","given":"Edwin V.","affiliations":[],"preferred":false,"id":265690,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lane, Donald W.","contributorId":15511,"corporation":false,"usgs":true,"family":"Lane","given":"Donald","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":265691,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":39043,"text":"pp321 - 1959 - Cenozoic echinoids of eastern United States","interactions":[],"lastModifiedDate":"2013-02-26T14:56:35","indexId":"pp321","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","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":"321","title":"Cenozoic echinoids of eastern United States","language":"ENGLISH","doi":"10.3133/pp321","usgsCitation":"Cooke, C.W., 1959, Cenozoic echinoids of eastern United States: U.S. Geological Survey Professional Paper 321, 106 p., https://doi.org/10.3133/pp321.","productDescription":"106 p.","costCenters":[],"links":[{"id":165559,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/pp/0321/report-thumb.jpg"},{"id":268409,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/pp/0321/report.pdf"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49e5e4b07f02db5e6a52","contributors":{"authors":[{"text":"Cooke, C. Wythe","contributorId":81538,"corporation":false,"usgs":true,"family":"Cooke","given":"C.","email":"","middleInitial":"Wythe","affiliations":[],"preferred":false,"id":220847,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2948,"text":"wsp1504 - 1959 - Surface water supply of the United States, 1957, Part II-B, South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River","interactions":[],"lastModifiedDate":"2012-02-02T00:05:33","indexId":"wsp1504","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1504","title":"Surface water supply of the United States, 1957, Part II-B, South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River","language":"ENGLISH","publisher":"U.S. Govt. Print. Off.,","doi":"10.3133/wsp1504","usgsCitation":"Wells, J.V., 1959, Surface water supply of the United States, 1957, Part II-B, South Atlantic slope and eastern Gulf of Mexico basins, Ogeechee River to Pearl River: U.S. Geological Survey Water Supply Paper 1504, x, 436 p. :ill. ;25 cm., https://doi.org/10.3133/wsp1504.","productDescription":"x, 436 p. :ill. ;25 cm.","costCenters":[],"links":[{"id":139135,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1504/report-thumb.jpg"},{"id":29657,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1504/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afbe4b07f02db69610f","contributors":{"authors":[{"text":"Wells, J. V. B.","contributorId":57037,"corporation":false,"usgs":true,"family":"Wells","given":"J.","email":"","middleInitial":"V. B.","affiliations":[],"preferred":false,"id":146034,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":64315,"text":"gp205 - 1959 - Aeromagnetic map of the East Greenville quadrangle, Berks, Lehigh, and Montgomery Counties, Pennsylvania","interactions":[],"lastModifiedDate":"2021-12-06T22:24:35.22011","indexId":"gp205","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1959","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":317,"text":"Geophysical Investigations Map","code":"GP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"205","title":"Aeromagnetic map of the East Greenville quadrangle, Berks, Lehigh, and Montgomery Counties, Pennsylvania","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/gp205","usgsCitation":"Bromery, R.W., and Zandle, G.L., 1959, Aeromagnetic map of the East Greenville quadrangle, Berks, Lehigh, and Montgomery Counties, Pennsylvania: U.S. Geological Survey Geophysical Investigations Map 205, 1 Plate: 22.90 × 26.96 inches, https://doi.org/10.3133/gp205.","productDescription":"1 Plate: 22.90 × 26.96 inches","costCenters":[],"links":[{"id":392532,"rank":4,"type":{"id":36,"text":"NGMDB Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_3124.htm"},{"id":251708,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gp/0205/report-thumb.jpg"},{"id":250953,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/gp/0205/plate-1.pdf","linkFileType":{"id":1,"text":"pdf"}},{"id":250952,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gp/0205/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"scale":"24000","country":"United States","state":"Pennsylvania","county":"Berks County, Lehigh County, Montgomery County","otherGeospatial":"East Greenville quadrangle","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -75.625,40.375 ], [ -75.625,40.5 ], [ -75.5,40.5 ], [ -75.5,40.375 ], [ -75.625,40.375 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db6974fd","contributors":{"authors":[{"text":"Bromery, Randolph Wilson","contributorId":22746,"corporation":false,"usgs":true,"family":"Bromery","given":"Randolph","email":"","middleInitial":"Wilson","affiliations":[],"preferred":false,"id":270542,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Zandle, G. L.","contributorId":39863,"corporation":false,"usgs":true,"family":"Zandle","given":"G.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":270543,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ]}