Buldir Depression is a large, rectilinear basin that lies on the northern edge of the Aleutian Ridge and is aligned with the arcuate chain of active volcanoes on the ridge crest. The depression appears to be a volcanic-tectonic feature, which began to form in Late Tertiary time and which is still forming. It is a graben formed by extensional rifting and accompanied by contemporaneous volcanism on the Aleutian Ridge. Subsidence rates for the depression are estimated at 20–70 cm/1,000 years. Sediments in the depression are 300 m thick and are probably pelagic and turbidite deposits of Pleistocene age. The turbidites were apparently derived from the plateau area of the Aleutian Ridge surrounding the depression. Older sediments on the northern slope of the Aleutian Ridge have a maximum thickness of 550 m and are deformed and slumped toward the Bering Sea. These sediments are postulated to overlie a mid-flank terrace on the northern Aleutian Ridge that titled to the north during the formation of Buldir Depression.
Earthquakes generated by fluid injection near Denver, Colorado, are compared with earthquakes triggered by nuclear explosion at the Nevada Test Site. Spatial distributions of the earthquakes in both cases are compatible with the hypothesis that variation of fluid pressure in preexisting fractures controls the time distribution of the seismic events in an “aftershock” sequence. We suggest that the fluid pressure changes may also control the distribution in time and space of natural aftershock sequences and of earthquakes that have been reported near large reservoirs.
No abstract available.
","language":"English","publisher":"Elsevier","doi":"10.1016/0025-326X(70)90238-9","issn":"0025326X","usgsCitation":"Cory, R.L., and Nauman, J.W., 1970, Pollution of estuaries: Marine Pollution Bulletin, v. 1, no. 6, p. 87-91, https://doi.org/10.1016/0025-326X(70)90238-9.","productDescription":"5 p.","startPage":"87","endPage":"91","costCenters":[],"links":[{"id":219495,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Georgia","otherGeospatial":"North Newport River estuary","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -81.36659328797393,\n 31.8041599522617\n ],\n [\n -81.36659328797393,\n 31.66916693993238\n ],\n [\n -81.18408984646872,\n 31.66916693993238\n ],\n [\n -81.18408984646872,\n 31.8041599522617\n ],\n [\n -81.36659328797393,\n 31.8041599522617\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"1","issue":"6","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a7ce4e4b0c8380cd79c32","contributors":{"authors":[{"text":"Cory, R. L.","contributorId":49456,"corporation":false,"usgs":true,"family":"Cory","given":"R.","email":"","middleInitial":"L.","affiliations":[],"preferred":false,"id":357387,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Nauman, J. W.","contributorId":30630,"corporation":false,"usgs":true,"family":"Nauman","given":"J.","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":357386,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70010413,"text":"70010413 - 1970 - Coastal currents and mass transport of surface sediments over the shelf regions of Monterey Bay, California","interactions":[],"lastModifiedDate":"2025-04-16T15:08:04.716543","indexId":"70010413","displayToPublicDate":"2003-04-04T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2667,"text":"Marine Geology","active":true,"publicationSubtype":{"id":10}},"title":"Coastal currents and mass transport of surface sediments over the shelf regions of Monterey Bay, California","docAbstract":"In Monterey Bay, the highest concentrations of medium and fine sands occur nearshore between ten and thirty fathoms. Silt and clay accumulate in greater depths. Contours of median diameter roughly parallel the isobaths.
Fine-grained materials are supplied to the bay region from erosion of cliffs which partly surround Monterey Bay, from sediment laden river discharge, and from continual reworking of widespread Pleistocene and Recent sea floor sediments. These sediments in turn are picked up by coastal currents and distributed over the shelf regions by present day current regimes.
Studies of bottom currents over the shelf regions and in Monterey Canyon have revealed patterns which vary with seasonal changes. Current patterns during August and September exhibit remarkable symmetry about the axis of Monterey Submarine Canyon. Central Shelf currents north and south of Monterey Canyon flowed northwest at an average rate of 0.2 knots and south at 0.3 knots respectively. On the North Shelf between January and March currents flowed east to southeast at 0.3–0.5 knots with mirror image patterns above the South Shelf during the same period.
Irregular current flow in the canyon indicates a complex current structure with frequent shifts in counterclockwise and clockwise direction over very short periods of time. Bottom topography of the canyon complex often causes localization of canyon currents. One particular observation at a depth of 51 fathoms indicated up-canyon flow at a rate of 0.2 knots. Most of the observed currents are related to seasonal variations, upwelling, ocean swell patterns, and to changes in the California and Davidson currents.
Changes in current regimes are reflected in the patterns of sediment distribution and transport. Sediment transport is chiefly parallel to the isobaths, particularly on the North and South Shelf regions. Complex dispersal patterns are observed near Monterey Canyon and Moss Landing Harbor jetties. Longshore currents move sediments southward except near Monterey Canyon which acts as a physiographic barrier and the extreme southern end of the bay where currents are non persistent.
Some sediments are also transported offshore by rip currents and other agencies and deposited in deeper, quieter waters. Supply of sediments to the canyon head results in over-filling and steepening with subsequent mass movement of sediments seaward followed by deposition in channels and on the broad deep sea fan.
","language":"English","publisher":"Elsevier","doi":"10.1016/0025-3227(70)90029-0","issn":"00253227","usgsCitation":"Wolf, S.C., 1970, Coastal currents and mass transport of surface sediments over the shelf regions of Monterey Bay, California: Marine Geology, v. 8, no. 5, p. 321-336, https://doi.org/10.1016/0025-3227(70)90029-0.","productDescription":"16 p.","startPage":"321","endPage":"336","costCenters":[],"links":[{"id":219302,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"California","otherGeospatial":"Monterey Bay","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -122.23388671874999,\n 36.507428541837264\n ],\n [\n -121.57745361328125,\n 36.507428541837264\n ],\n [\n -121.57745361328125,\n 37.04202441635081\n ],\n [\n -122.23388671874999,\n 37.04202441635081\n ],\n [\n -122.23388671874999,\n 36.507428541837264\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"8","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f780e4b0c8380cd4cb4f","contributors":{"authors":[{"text":"Wolf, Stephen C.","contributorId":38148,"corporation":false,"usgs":true,"family":"Wolf","given":"Stephen","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":358862,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010436,"text":"70010436 - 1970 - The structure and origin of the large submarine canyons of the Bering Sea","interactions":[],"lastModifiedDate":"2025-04-16T15:21:45.429592","indexId":"70010436","displayToPublicDate":"2003-04-02T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2667,"text":"Marine Geology","active":true,"publicationSubtype":{"id":10}},"title":"The structure and origin of the large submarine canyons of the Bering Sea","docAbstract":"Three exceptionally large and long submarine canyons — Bering, Pribilof, and Zhemchug — incise the continental slope underlying the southeastern Bering Sea. Bering Canyon, the world's longest known slope valley, is approximately 400 km long and has a volume of 4,300 km3. The volume of Pribilof Canyon is 1,300 km3 and that of Zhemchug is 8,500 km3; Zhemchug Canyon may well be the world's largest slope valley; most other large submarine canyons have volumes less than 500 km3. Pribilof and Zhemchug canyons are further distinguished by the headward bifurcation of their slope axes to form elongated trough-shaped basins behind the regionally projected position of the shelf edge. These troughs are superimposed over structural depressions formed by down-faulted basement rocks of Mesozoic and older ages. Prior to canyon cutting these depressions were filled with as much as 2,600 m of shallow-water diatomaceous, tuffaceous, and detrital sediments largely of Tertiary age. Deposition of these sediments took place concurrently with general margin subsidence of at least 2,000 m.
The data and conclusions presented in this paper stress that the location, trend, and shape of the enormous submarine canyons cutting the Bering margin are structurally determined. However, axial cutting and headward erosion within the relatively unconsolidated Tertiary strata and the older, lithified basement rock is thought to have been caused by basinward-sliding masses of sediment; these unstable sediment bodies accumulated on the upper continental slope and outer shelf, probably near the mouths of major Alaskan rivers.
Bering Canyon was periodically cut and filled by axial sedimentation during Late Tertiary and Quaternary time. Pribilof and Zhemchug canyons, however, are thought to have been excavated entirely during the Pleistocene. It is presumed that, during one or more periods of glacially lowered sea level, the Kuskokwim and Yukon rivers emptied into or near the heads of Pribilof and Zhemchug canyons. The enormous size and unusual shape of Zhemchug Canyon resulted from the breaching of the seaward wall of an outer-shelf basement depression and the subsequent removal of nearly 4,500 km3 of Tertiary deposits filling it.
","language":"English","publisher":"Elsevier","doi":"10.1016/0025-3227(70)90043-5","issn":"00253227","usgsCitation":"Scholl, D., Buffington, E.C., Hopkins, D., and Alpha, T.R., 1970, The structure and origin of the large submarine canyons of the Bering Sea: Marine Geology, v. 8, no. 3-4, p. 187-210, https://doi.org/10.1016/0025-3227(70)90043-5.","productDescription":"24 p.","startPage":"187","endPage":"210","costCenters":[],"links":[{"id":219758,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Alaska","otherGeospatial":"Bering Sea","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -168.48632812499997,\n 54.77534585936447\n ],\n [\n -154.16015625,\n 54.77534585936447\n ],\n [\n -154.16015625,\n 60.19615576604439\n ],\n [\n -168.48632812499997,\n 60.19615576604439\n ],\n [\n -168.48632812499997,\n 54.77534585936447\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"8","issue":"3-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bb096e4b08c986b324f56","contributors":{"authors":[{"text":"Scholl, D.W.","contributorId":106461,"corporation":false,"usgs":true,"family":"Scholl","given":"D.W.","email":"","affiliations":[],"preferred":false,"id":358927,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Buffington, E. C.","contributorId":13948,"corporation":false,"usgs":true,"family":"Buffington","given":"E.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":358924,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Hopkins, D.M.","contributorId":103646,"corporation":false,"usgs":true,"family":"Hopkins","given":"D.M.","email":"","affiliations":[],"preferred":false,"id":358926,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Alpha, T. R.","contributorId":20715,"corporation":false,"usgs":true,"family":"Alpha","given":"T.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":358925,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70010274,"text":"70010274 - 1970 - Rapid changes in the head of the Rio Balsas Submarine Canyon system, Mexico","interactions":[],"lastModifiedDate":"2025-04-16T15:18:10.725351","indexId":"70010274","displayToPublicDate":"2003-04-02T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2667,"text":"Marine Geology","active":true,"publicationSubtype":{"id":10}},"title":"Rapid changes in the head of the Rio Balsas Submarine Canyon system, Mexico","docAbstract":"The investigation of a river delta and the heads of several nearby submarine canyons in western Mexico produced evidence for rapid changes in the configuration and depth of the nearshore portions of canyon tributaries. General scarcity of data on the rates of submarine canyon formation and the relationship to river discharge should make these results of special interest.
The Rio Balsas, one of Mexico's largest rivers, empties into the ocean near the heads of a large submarine canyon that terminates in the Middle America Trench. One of the distributaries of the Rio Balsas presently is discharging at the head of Cañón de la Necesidad, which is being eroded actively. Two inactive canyons are related to former discharge channels of the river. Their heads lie at some distance from shore and are being filled with sediment. The Cañón de Petacalco, not now receiving sediment directly from a Rio Balsas distributary, has remained active because the shoreline has not retreated far. Until about 100 years ago its head was being filled with fine-grained and highly organic sediments from a nearby rivermouth, while the coarse portion of the sediment supply joined the canyon via a tributary farther seaward. Since then the river has shifted away from this canyon, and the horizontally stratified sediments in the canyon head have been incised as much as 20–30 m, as evidenced by three 14C dates of organic material exposed in the steep to overhanging canyon walls.
The changes in the shallow portion of the Rio Balsas submarine canyons seem to be related to changes in river discharge pattern, either directly or indirectly. A shifting point source of sediment supply either activates a pre-existing, partly filled canyon, or erodes a new one near the new river mouth, whereas the canyon at the abandoned river mouth is deactivated following retreat of the shoreline.
The heads of the different tributaries form a dendritic pattern in Holocene unconsolidated sediment. Subaerial processes are not involved in the formation of these submarine canyons. Thus, a dendritic pattern of submarine canyons is not necessarily indicative of subaerial erosion.
A detailed bathymetric study of Astoria Canyon and Astoria Fan provides a model for typical submarine canyon-fan systems. The present canyon head is 9 miles (17 km) west of the Columbia River mouth but buried Pleistocene channels appear to have connected the two features in the past. The canyon, which is distinguished by its relief, V-shaped profiles, and numerous tributaries, winds sinuously and is coincident with apparent structural trends across the continental shelf and slope. At the fan apex, the canyon mouth merges smoothly into Astoria Channel, which is characterized by its U-shaped profiles, lower walls of even height, and levee development. Astoria Channel and the fan valley at the base of the continental slope are the most recently active of a series of main fan valleys that appear to have: (1) progressively “hooked left”; (2) migrated from north to south across the fan during its formation; and (3) been partly responsible for the asymmetrical shape of the fan. The deep, narrow upper fan valleys that characterize the steep (> 1:100, or 0°35′) and rough (10–30 fathoms, or 18–55 m) upper fan surface break into distributaries on the middle fan, where there is the sharpest change in gradient. The main valleys become broader and shallower down the fan, while the generally concave fan surface grades to nearly a flat seafloor (to gradients < 1:1000, or 0°0.5′), (< 10 fathoms, or 18 m relief).
Similarity of Astoria Canyon-Fan system with other deep-sea fan and alluvial fan systems, suggests the hypothesis that size of drainage basin, sediment size, and sediment load control the size, gradient, and valley development of any fan system. Data from bathymetry, seismic refraction stations, and sediment load of the Columbia River indicate that the cutting of Astoria Canyon and the deposition of the unconsolidated sediment layer forming Astoria Fan could have been accomplished during the Pleistocene. A similar history can be suggested for other major submarine canyon-fan systems.
","language":"English","publisher":"Elsevier","doi":"10.1016/0025-3227(70)90047-2","issn":"00253227","usgsCitation":"Nelson, C., Carlson, P., Byrne, J., and Alpha, T.R., 1970, Development of the Astoria Canyon-Fan physiography and comparison with similar systems: Marine Geology, v. 8, no. 3-4, p. 259-291, https://doi.org/10.1016/0025-3227(70)90047-2.","productDescription":"33 p.","startPage":"259","endPage":"291","costCenters":[],"links":[{"id":219362,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Oregon","otherGeospatial":"Astoria Canyon, Astoria Fan","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"coordinates\": [\n [\n [\n -121.89139364833369,\n 45.61941840485443\n ],\n [\n -121.89139364833369,\n 44.27741061960609\n ],\n [\n -119.62339339391065,\n 44.27741061960609\n ],\n [\n -119.62339339391065,\n 45.61941840485443\n ],\n [\n -121.89139364833369,\n 45.61941840485443\n ]\n ]\n ],\n \"type\": \"Polygon\"\n }\n }\n ]\n}","volume":"8","issue":"3-4","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a0067e4b0c8380cd4f74e","contributors":{"authors":[{"text":"Nelson, C.H.","contributorId":88346,"corporation":false,"usgs":true,"family":"Nelson","given":"C.H.","email":"","affiliations":[],"preferred":false,"id":358558,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Carlson, P.R.","contributorId":97055,"corporation":false,"usgs":true,"family":"Carlson","given":"P.R.","email":"","affiliations":[],"preferred":false,"id":358559,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Byrne, J.V.","contributorId":21684,"corporation":false,"usgs":true,"family":"Byrne","given":"J.V.","email":"","affiliations":[],"preferred":false,"id":358557,"contributorType":{"id":1,"text":"Authors"},"rank":3},{"text":"Alpha, T. R.","contributorId":20715,"corporation":false,"usgs":true,"family":"Alpha","given":"T.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":358556,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70010088,"text":"70010088 - 1970 - The mechanics of stick-slip","interactions":[],"lastModifiedDate":"2025-08-29T15:40:12.97049","indexId":"70010088","displayToPublicDate":"2003-03-31T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"The mechanics of stick-slip","docAbstract":"Physical mechanisms that have been proposed to explain the occurrence of stick-slip motion during frictional sliding have been examined in the light of results obtained from experiments with rocks and brittle minerals. An instability caused by sudden brittle fracture of locked regions on surfaces in contact is the most likely explanation for stick-slip during dry frictional sliding of brittle rocks at room temperature. Areas requiring further study and the uncertainties in applying the results of laboratory experiments to earthquake studies are emphasized.
Ocean-floor dredging and submarine photography in the Revillagigedo region off the west coast of Mexico reveal that the dominant exposed rock of the submarine part of the large island-forming volcanoes (Roca Partida and San Benedicto) is a uniform alkali pillow basalt; more siliceous rocks are exposed on the upper, subaerial parts of the volcanoes. Basalts dredged from smaller seamounts along the Clarion fracture zone south of the Revillagigedo Islands are tholeiitic pillow basalts. Pillows of alkali basalts are more vesicular than Hawaiian tholeiitic pillows collected from the same depths. This difference probably reflects a higher original volatile content of the alkali basalts.
Manganese-iron oxide nodules common in several dredge hauls generally contain nucleii of rhyolitic pumice or basalt pillow fragments. The pumice floated to its present site from subaerial eruptions, became waterlogged and sank, and was then coated with manganese-iron oxides. The thickness of palagonite rinds on the glassy pillow fragments is proportional to the thickness of manganese-iron oxide layers, and both are a measure of the age of the nodule. Both oldest basalts (10–100 m.y.) and youngest (less than 1 m.y.) are along the Clarion fracture zone, whereas basalts from Roca Partida and San Benedicto volcanoes are of intermediate age.
","language":"English","publisher":"Elsevier","doi":"10.1016/0025-3227(70)90022-8","issn":"00253227","usgsCitation":"Moore, J., 1970, Submarine basalt from the Revillagigedo Islands region, Mexico: Marine Geology, v. 9, no. 5, p. 331-345, https://doi.org/10.1016/0025-3227(70)90022-8.","productDescription":"15 p.","startPage":"331","endPage":"345","numberOfPages":"15","costCenters":[],"links":[{"id":218761,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"Mexico","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -111.0498046875,\n 22.268764039073968\n ],\n [\n -105.2490234375,\n 22.268764039073968\n ],\n [\n -105.2490234375,\n 24.84656534821976\n ],\n [\n -111.0498046875,\n 24.84656534821976\n ],\n [\n -111.0498046875,\n 22.268764039073968\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"9","issue":"5","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505b9d1fe4b08c986b31d65a","contributors":{"authors":[{"text":"Moore, J.G.","contributorId":67496,"corporation":false,"usgs":true,"family":"Moore","given":"J.G.","email":"","affiliations":[],"preferred":false,"id":357264,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70010240,"text":"70010240 - 1970 - Determination of iridium in mafic rocks by atomic absorption","interactions":[],"lastModifiedDate":"2025-08-13T16:34:56.26991","indexId":"70010240","displayToPublicDate":"2001-11-30T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3517,"text":"Talanta","active":true,"publicationSubtype":{"id":10}},"title":"Determination of iridium in mafic rocks by atomic absorption","docAbstract":"Iridium is determined in mineralized mafic rocks by atomic absorption after fire-assay concentration into a gold bead. Interelement interferences in the atomic-absorption determination are removed and Ir sensitivity is increased by buffering the solutions with a mixture of copper and sodium sulphates. Substantial amounts of Ag, Al, Au, Bi, Ca, Cd, Co, Cr, Fe, Ho, Hg, K, La, Mg, Mn, Mo, Ni, Pb, Te, Ti, V, Y, Zn and platinum metals can be tolerated in the atomic-absorption determination. The sensitivity and detection limits are 3.2 and 0.25 ppm of Ir, respectively.
No abstract available.
","language":"English","publisher":"Elsevier","doi":"10.1016/0039-9140(70)80168-0","issn":"00399140","usgsCitation":"Engels, J.C., and Inamells, C., 1970, Use of LiBO2 flux for K-Ar dating: Talanta, v. 17, no. 8, p. 783-784, https://doi.org/10.1016/0039-9140(70)80168-0.","productDescription":"2 p.","startPage":"783","endPage":"784","costCenters":[],"links":[{"id":219293,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"17","issue":"8","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505bbe7de4b08c986b3295f6","contributors":{"authors":[{"text":"Engels, J. C.","contributorId":92246,"corporation":false,"usgs":true,"family":"Engels","given":"J.","email":"","middleInitial":"C.","affiliations":[],"preferred":false,"id":358363,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Inamells, C.O.","contributorId":63525,"corporation":false,"usgs":true,"family":"Inamells","given":"C.O.","email":"","affiliations":[],"preferred":false,"id":358362,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70200882,"text":"wdrID691 - 1970 - Water resources data for Idaho, water year 1969: Part 1. Surface water records","interactions":[],"lastModifiedDate":"2025-05-22T20:26:18.01434","indexId":"wdrID691","displayToPublicDate":"1999-01-01T12:16:06","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":340,"text":"Water Data Report","code":"WDR","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"ID-69-1","title":"Water resources data for Idaho, water year 1969: Part 1. Surface water records","docAbstract":"Surface-water records for the 1969 water year for gaging stations, partial-record stations, and miscellaneous sites within the State of Idaho are given in this report and their locations shown in figures 2 and 3. Records for a few selected gaging stations in bordering States also are included. The records were collected and computed by the Water Resources Division of the U.S. Geological Survey, under the direction of W. L. Burnham, district chief, Water Resources Division.
Through September 30, 1960, the records of discharge and stage of streams and contents and stage of lakes or reservoirs were published in an annual series of U.S. Geological Survey water-supply papers entitled \"Surface Water Supply of the United States.\" Since 1951 there have been 20 volumes in the series; each volume covered an area whose boundaries coincided with those of certain natural drainage areas. The records in Idaho were contained in Parts 10, 12, and 13 of that series.
Beginning with the 1961 water year, streamflow records and related data have been released by the Geological Survey in annual reports on a State-boundary basis. Distribution of these basic-data reports is limited and primarily for local needs. Records will be published in Geological Survey water-supply papers at 5-year intervals. These 5-year water-supply papers will show daily discharge and will be compiled on the same geographical areas previously used for the annual series; however, some of the 14 parts of conterminous United States will be further subdivided.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/wdrID691","collaboration":"Prepared in cooperation with the State of Idaho and with other agencies","usgsCitation":"U.S. Geological Survey, 1970, Water resources data for Idaho, water year 1969: Part 1. Surface water records: U.S. Geological Survey Water Data Report ID-69-1, ix, 299 p., https://doi.org/10.3133/wdrID691.","productDescription":"ix, 299 p.","costCenters":[],"links":[{"id":486229,"rank":1,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wdr/1969/id-69-1/report-thumb.jpg"},{"id":486442,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wdr/1969/id-69-1/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United 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Reprinted in 1982.","costCenters":[],"links":[{"id":94735,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/twri/03c02-1970/report.pdf","size":"11967","linkFileType":{"id":1,"text":"pdf"}},{"id":139160,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/twri/03c02-1970/report-thumb.jpg"}],"edition":"1970","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e49fce4b07f02db5f56cb","contributors":{"authors":[{"text":"Guy, Harold P.","contributorId":6434,"corporation":false,"usgs":true,"family":"Guy","given":"Harold P.","affiliations":[],"preferred":false,"id":149620,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Norman, Vernon W.","contributorId":22325,"corporation":false,"usgs":true,"family":"Norman","given":"Vernon","email":"","middleInitial":"W.","affiliations":[],"preferred":false,"id":149621,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":67169,"text":"i571 - 1970 - Geologic map of the Jemez Mountains, New Mexico","interactions":[],"lastModifiedDate":"2012-02-10T00:11:11","indexId":"i571","displayToPublicDate":"1996-08-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":320,"text":"IMAP","code":"I","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"571","subseriesTitle":"NONE","title":"Geologic map of the Jemez Mountains, New Mexico","language":"ENGLISH","doi":"10.3133/i571","usgsCitation":"Smith, R.L., Bailey, R., and Ross, C.S., 1970, Geologic map of the Jemez Mountains, New Mexico: U.S. Geological Survey IMAP 571, 1 map :col. ;79 x 67 cm. on sheet 100 x 129 cm., https://doi.org/10.3133/i571.","productDescription":"1 map :col. ;79 x 67 cm. on sheet 100 x 129 cm.","costCenters":[],"links":[{"id":106842,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_9357.htm","linkFileType":{"id":5,"text":"html"},"description":"9357"},{"id":189984,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/usgs_thumb.jpg"},{"id":14263,"rank":9999,"type":{"id":14,"text":"Image"},"url":"https://store.usgs.gov/b2c_usgs/b2c/usgs/netfile?file=//igskahcigssap05/MOD/StoreFiles/PDF/I-0571_Geologic_Map_of_the_Jemez_Mountains_NM_125K_1970.pdf","linkFileType":{"id":5,"text":"html"}}],"scale":"250000","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -107,35.25 ], [ -107,36.25 ], [ -106,36.25 ], [ -106,35.25 ], [ -107,35.25 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afee4b07f02db69783f","contributors":{"authors":[{"text":"Smith, R. L.","contributorId":93904,"corporation":false,"usgs":true,"family":"Smith","given":"R.","email":"","middleInitial":"L.","affiliations":[{"id":595,"text":"U.S. Geological Survey","active":false,"usgs":true}],"preferred":false,"id":275702,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bailey, R. A.","contributorId":87531,"corporation":false,"usgs":true,"family":"Bailey","given":"R. A.","affiliations":[],"preferred":false,"id":275701,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Ross, C. S.","contributorId":18337,"corporation":false,"usgs":true,"family":"Ross","given":"C.","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":275700,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":12705,"text":"ofr7029 - 1970 - Geology of the Bushrod Island-New Georgia clay deposit near Monrovia, Liberia","interactions":[],"lastModifiedDate":"2022-02-04T19:28:37.396536","indexId":"ofr7029","displayToPublicDate":"1994-01-01T09:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":330,"text":"Open-File Report","code":"OFR","onlineIssn":"2331-1258","printIssn":"0196-1497","active":true,"publicationSubtype":{"id":5}},"seriesNumber":"70-29","title":"Geology of the Bushrod Island-New Georgia clay deposit near Monrovia, Liberia","docAbstract":"The Bushrod Island-New Georgia clay deposit near Monrovia, Liberia, consisted of interlensing clay and very fine to fine quartz sand; it was deposited in elongate subparallel troughs that had been eroded in coarse-grained sediments. The troughs are interpreted as abandoned stream channels on a former delta of the St. Paul River. The clay of the deposit is essentially a quartz-rich kaolinitic clay that has undergone sufficient weathering in the upper part of the deposit to redistribute iron and alumina.
The clay may be divided into three groups: an iron-rich group (A) in which total iron expressed as Fe2O3 averages 6.5 percent and ranges from 4.4 to 9.2 percent, a group (B) relatively lower in iron in which total iron expressed as Fe2O3 averages 2.7 percent and ranges from 1.6 to 7.4 percent, and a group (C) high in both organic material and iron in which total iron expressed as Fe2O3 averages 3.9 percent and ranges from 3.3 to 4.9 percent.
Potential indicated reserves for the three groups are estimated at 1,800,000, 5,300,000, and 470,000 tons, respectively.
Tests of the physical properties of the raw and fired clay indicate the clay is suitable for the following commercial uses: building brick, hollow tile, drain tile, roofing tile, quarry tile, flower pots, porous earthenware, low to intermediate duty refractory products, and probably stoneware and small diameter sewer pipe.
","language":"English","publisher":"U.S. Geological Survey","doi":"10.3133/ofr7029","usgsCitation":"Blade, L.V., 1970, Geology of the Bushrod Island-New Georgia clay deposit near Monrovia, Liberia: U.S. Geological Survey Open-File Report 70-29, 35 p., https://doi.org/10.3133/ofr7029.","productDescription":"35 p.","costCenters":[],"links":[{"id":143798,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/of/1970/0029/report-thumb.jpg"},{"id":395464,"rank":2,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/of/1970/0029/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"Liberia","city":"Monrovia","otherGeospatial":"Bushrod Island","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -10.809345245361328,\n 6.332189609907789\n ],\n [\n -10.763339996337889,\n 6.332189609907789\n ],\n [\n -10.763339996337889,\n 6.395824732995197\n ],\n [\n -10.809345245361328,\n 6.395824732995197\n ],\n [\n -10.809345245361328,\n 6.332189609907789\n ]\n ]\n ]\n }\n }\n ]\n}","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4ad4e4b07f02db683294","contributors":{"authors":[{"text":"Blade, Lawrence Vernon","contributorId":51748,"corporation":false,"usgs":true,"family":"Blade","given":"Lawrence","email":"","middleInitial":"Vernon","affiliations":[],"preferred":false,"id":166572,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":2512,"text":"wsp1888 - 1970 - Hydrology of the Upper Malad River basin, southeastern Idaho","interactions":[],"lastModifiedDate":"2013-11-21T13:44:23","indexId":"wsp1888","displayToPublicDate":"1994-01-01T07:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":341,"text":"Water Supply Paper","code":"WSP","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1888","title":"Hydrology of the Upper Malad River basin, southeastern Idaho","docAbstract":"The report area comprises 485 square miles in the Basin and Range physiographic province. It includes most of eastern' Oneida County and parts of Franklin, Bannock, and Power Counties of southeastern Idaho. Relief is about 5,000 feet; the floor of the Malad Valley is at an average altitude of about 4,400 feet. Agriculture is, by far, ,the principal economic .activity. In 1960 the population of the upper Malad River basin was about 3,600, of which about 60 percent resided in Malad City, the county seat of Oneida County. \n\nThe climate is semiarid throughout the Malad Valley and its principal tributary valleys; ,above 6,500 feet the climate is subhumid. Annual precipitation ranges from about 13 inches in the lower Malad Valley to more than 30 inches on the highest peaks of the Bannock and Malad ranges. Owing to ,the normally clear atmospheric conditions, large daily and seasonal temperature fluctuations are common. Topography, distance from the Pacific Ocean, .and the general atmospheric circulation are the principal factors governing the climate of the Malad River basin. The westerlies transport moisture from the P.acific Ocean toward southeastern Idaho. The north-south tren4ing mountains flanking the basin are oriented orthogonally to the moisture flux so that they are very effective in removing precipitable water from the air. A minimum uplift of 6,000 feet is required to transport moisture from the Pacific source region; accordingly, most air masses are desiccated long before they reach the Malad basin. Heaviest precipitation is generally associated with steep pressure gradients in the midtroposphere that are so oriented as to cause a deep landward penetration of moisture from the Pacific Ocean.
\n\nAnnual water yields in the project area range from about 0.8 inch in the, lower Malad Valley to more than 19 inches on the high peaks north and east of Malad City. The mean annual water yield for the entire basin is 4 inches, or about 115,000 acre-feet. Evaporation is greatest in July when about 7 inches is lost from lakes, reservoirs, and waterlogged areas; losses from free-water surfaces may be as much .as 38 inches annually.
\n\nAn extensive ground-water reservoir consisting of sand and gravel interbedded with relatively impermeable beds of silt .and clay underlies much of the Malad Valley. Wells near the center of the valley exceeding 700 feet in depth do not reach bedrock. The Woodruff fault, which transects the constricted lower Malad Valley, is one of the main factors creating artesian conditions south of the latitude of Malad City. Recharge is obtained principally from mountain runoff which flows onto highly permeable alluvial fans surrounding the valley and from streams that flow across the valley floor. On the basis of a water balance analysis, under flow from the project area was estimated to be 28,000 acre-feet annually, surface-water outflow was 51,000 acre-feet, and transbasin imports were about 4,000 acre-feet.
\n\nThe principal tributaries of the Malad River are perennial along their upper and middle reaches and have well-sustained low flows. During the growing season, all surface water entering the Malad Valley is used for irrigation. Spine irrigation is practiced in the principal tributary valleys; however, a shortage of suitable reservoir sites has hampered surface-water development in these areas. The highly porous deposits underlying the Malad Valley tend to attenuate flood peaks. An unusual combination of meteorologic events early in 1962 effectively counteracted the high absorptive capacity of the valley and predisposed the basin to high flood risk. Subsequent rapid snowmelt combined with frozen ground produced the extraordinary flood of February 12, 1962.
\n\nCalcium and bicarbonate commonly are the most abundant ions in the surface waters of the upper Malad River basin. In August 1967, the dissolved-solids content of streamflow ranged from 200 to 350 milligrams per liter in the middle and upper parts of the basin; however, much greater values were measured in the Malad River between Woddruff and Cherry Creek Lane. With the exception of that reach, the surface water of the project area is suitable for irrigating all but the most sensitive crops.
\n\nThe total water yield is not sufficient to meet all the water needs of the basin. A comprehensive water-management plan is required to ensure optimal use of the water resource.
","language":"English","publisher":"U.S. Government Printing Office","publisherLocation":"Washington D.C.","doi":"10.3133/wsp1888","usgsCitation":"Pluhowski, E.J., 1970, Hydrology of the Upper Malad River basin, southeastern Idaho: U.S. Geological Survey Water Supply Paper 1888, v, 89 p., https://doi.org/10.3133/wsp1888.","productDescription":"v, 89 p.","numberOfPages":"94","costCenters":[],"links":[{"id":138716,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/wsp/1888/report-thumb.jpg"},{"id":28673,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/wsp/1888/report.pdf","linkFileType":{"id":1,"text":"pdf"}}],"country":"United States","state":"Idaho","otherGeospatial":"Upper Malad River Basin","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -0.01638888888888889,0.0011111111111111111 ], [ -0.01638888888888889,0.0011111111111111111 ], [ -0.01638888888888889,0.0011111111111111111 ], [ -0.01638888888888889,0.0011111111111111111 ], [ -0.01638888888888889,0.0011111111111111111 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a0ee4b07f02db5fdb62","contributors":{"authors":[{"text":"Pluhowski, Edward J.","contributorId":87911,"corporation":false,"usgs":true,"family":"Pluhowski","given":"Edward","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":145318,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":62074,"text":"a1 - 1970 - Reconnaissance geologic map of the Mount Rabot Quadrangle, Transantarctic mountains, Antarctica","interactions":[],"lastModifiedDate":"2012-02-10T00:10:45","indexId":"a1","displayToPublicDate":"1994-01-01T01:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":305,"text":"Antarctic Map","code":"A","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"1","title":"Reconnaissance geologic map of the Mount Rabot Quadrangle, Transantarctic mountains, Antarctica","language":"ENGLISH","publisher":"U.S. Geological Survey","publisherLocation":"Reston, VA","doi":"10.3133/a1","usgsCitation":"Barrett, P.J., Lindsay, J., and Gunner, J., 1970, Reconnaissance geologic map of the Mount Rabot Quadrangle, Transantarctic mountains, Antarctica: U.S. Geological Survey Antarctic Map 1, 1 sheet, https://doi.org/10.3133/a1.","productDescription":"1 sheet","costCenters":[],"links":[{"id":112498,"rank":100,"type":{"id":15,"text":"Index Page"},"url":"https://repository.agic.umn.edu/maps/usgs/geologic/a1_mount_rabot/","linkFileType":{"id":5,"text":"html"}},{"id":248264,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/a/01/report.pdf","size":"49","linkFileType":{"id":1,"text":"pdf"}},{"id":248265,"rank":400,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/a/01/plate-1.pdf","size":"4337","linkFileType":{"id":1,"text":"pdf"}},{"id":253082,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/a/01/report-thumb.jpg"}],"scale":"250000","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ 154,-84 ], [ 154,-83 ], [ 165,-83 ], [ 165,-84 ], [ 154,-84 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a70e4b07f02db641b93","contributors":{"authors":[{"text":"Barrett, P. J.","contributorId":96347,"corporation":false,"usgs":false,"family":"Barrett","given":"P.","email":"","middleInitial":"J.","affiliations":[],"preferred":false,"id":266868,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Lindsay, J.F.","contributorId":54666,"corporation":false,"usgs":true,"family":"Lindsay","given":"J.F.","email":"","affiliations":[],"preferred":false,"id":266866,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Gunner, John","contributorId":58345,"corporation":false,"usgs":true,"family":"Gunner","given":"John","email":"","affiliations":[],"preferred":false,"id":266867,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":37460,"text":"ssrw137 - 1970 - Mammals imported into the United States in 1968","interactions":[],"lastModifiedDate":"2012-02-02T00:09:40","indexId":"ssrw137","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":1,"text":"Federal Government Series"},"seriesTitle":{"id":83,"text":"Special Scientific Report - Wildlife","active":false,"publicationSubtype":{"id":1}},"seriesNumber":"137","title":"Mammals imported into the United States in 1968","language":"ENGLISH","publisher":"U.S. Fish and Wildlife Service","usgsCitation":"Jones, C., 1970, Mammals imported into the United States in 1968: Special Scientific Report - Wildlife 137, 30 p.","productDescription":"30 p.","costCenters":[],"links":[{"id":94655,"rank":9999,"type":{"id":10,"text":"Digital Object Identifier"},"url":"https://hdl.handle.net/2027/mdp.39015077573130?urlappend=%3Bseq=3"},{"id":166946,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4a81e4b07f02db64a069","contributors":{"authors":[{"text":"Jones, Clyde","contributorId":73258,"corporation":false,"usgs":true,"family":"Jones","given":"Clyde","email":"","affiliations":[],"preferred":false,"id":218115,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":62218,"text":"gq856 - 1970 - Geologic map of the Midway quadrangle, central Kentucky","interactions":[{"subject":{"id":42733,"text":"ofr69210 - 1969 - Preliminary structure map of the Midway Quadrangle, central Kentucky","indexId":"ofr69210","publicationYear":"1969","noYear":false,"title":"Preliminary structure map of the Midway Quadrangle, central Kentucky"},"predicate":"SUPERSEDED_BY","object":{"id":62218,"text":"gq856 - 1970 - Geologic map of the Midway quadrangle, central Kentucky","indexId":"gq856","publicationYear":"1970","noYear":false,"title":"Geologic map of the Midway quadrangle, central Kentucky"},"id":1}],"lastModifiedDate":"2012-02-10T00:10:44","indexId":"gq856","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":316,"text":"Geologic Quadrangle","code":"GQ","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"856","title":"Geologic map of the Midway quadrangle, central Kentucky","language":"ENGLISH","doi":"10.3133/gq856","usgsCitation":"Pomeroy, J.S., 1970, Geologic map of the Midway quadrangle, central Kentucky: U.S. Geological Survey Geologic Quadrangle 856, 1 map., https://doi.org/10.3133/gq856.","productDescription":"1 map.","costCenters":[],"links":[{"id":103572,"rank":700,"type":{"id":15,"text":"Index Page"},"url":"https://ngmdb.usgs.gov/Prodesc/proddesc_2158.htm","linkFileType":{"id":5,"text":"html"},"description":"2158"},{"id":248402,"rank":300,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/gq/0856/report.pdf","size":"33","linkFileType":{"id":1,"text":"pdf"}},{"id":253380,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/gq/0856/report-thumb.jpg"}],"scale":"24000","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -84.75,38.1175 ], [ -84.75,38.25 ], [ -84.61749999999999,38.25 ], [ -84.61749999999999,38.1175 ], [ -84.75,38.1175 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"4f4e4afce4b07f02db696a0b","contributors":{"authors":[{"text":"Pomeroy, John S.","contributorId":18329,"corporation":false,"usgs":true,"family":"Pomeroy","given":"John","email":"","middleInitial":"S.","affiliations":[],"preferred":false,"id":267090,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":4670,"text":"twri05A1_1970 - 1970 - Methods for collection and analysis of water samples for dissolved minerals and gases","interactions":[],"lastModifiedDate":"2021-05-28T18:23:38.769076","indexId":"twri05A1_1970","displayToPublicDate":"1994-01-01T00:00:00","publicationYear":"1970","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":5,"text":"USGS Numbered Series"},"seriesTitle":{"id":336,"text":"Techniques of Water-Resources Investigations","code":"TWRI","active":false,"publicationSubtype":{"id":5}},"seriesNumber":"05-A1","title":"Methods for collection and analysis of water samples for dissolved minerals and gases","docAbstract":"No abstract available.
","language":"English","publisher":"U.S. Govt. Print. 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