The Paradox Basin region is approximately bounded by the south flank of the Uinta Basin to the north, the Uncompahgre uplift and San Juan Mountains to the east, the Four Corners structural platform to the southeast, the north rim of the Black Mesa Basin and the Grand Canyon to the south and southwest, and the Wasatch Plateau and Hurricane fault system to the west. Some of these geologic features are areas of ground-water recharge or discharge whereas others such as the Four Corners platform do not directly influence fluid movement. The aquifer systems studied were: (1) Mississippian rocks; (2) Pinkerton Trail Limestone of Wengerd and Strickland, 1954; (3) Paradox Member of the Hermosa Formation; (4) Honaker Trail Formation of Wengerd and Matheny, 1958; (5) Permian rocks.
Recharge in the Paradox Basin occurs on the west flank of the San Juan Mountains and along the west side of the Uncompahgre uplift. The direction of ground-water movement in each analyzed unit is principally southwest-ward toward the topographically low outcrop areas along the Colorado River in Arizona. However, at any point in the basin, flow may be in some other direction owing to the influence of intrabasin recharge areas or local obstructions to flow, such as faults or dikes. A series of potentiometric surface maps was prepared for the five systems studied. Material used in construction of the maps included outcrop altitudes of springs and streams, drill-stem tests, water-well records, and an electric analog model of the entire basin. Many structurally and topographically high areas within the basin are above the regional potentiometric surface; recharge in these areas will drain rapidly off the high areas and adjust to the regional water level.
With a few exceptions, most wells in formations above the Pennsylvanian contain fresh (< 1,000 mg/l T.D.S.2) to moderately saline (< 10,000 mg/l T.D.S.) water. In only a few cases are true brines (> 35,000 mg/l T.D.S.) reported. Most water samples from strata below the Permian are brines of the sodium chloride type but with large amounts of calcium sulfate or calcium chloride type water commonly occurring. Because evaporite facies occur in the Paradox Member, this unit has brines with as much as 400,000 mg/l dissolved solids content.
Previous analysis of the San Juan Basin has indicated the presence of an osmotic membrane system. The highly permeable Jurassic formations were postulated to be the outflow side of the membrane. It is also possible that the Upper Paleozoic units with known brines and with an otherwise inexplicably high potentiometric surface in the Four Corners area of New Mexico could be the outflow receptors of the San Juan membrane system.
","language":"English","publisher":"Elsevier","doi":"10.1016/0009-2541(69)90050-3","issn":"00092541","usgsCitation":"Hanshaw, B., and Hill, G., 1969, Geochemistry and hydrodynamics of the Paradox Basin region, Utah, Colorado and New Mexico: Chemical Geology, v. 4, no. 1-2, p. 263-294, https://doi.org/10.1016/0009-2541(69)90050-3.","productDescription":"32 p.","startPage":"263","endPage":"294","numberOfPages":"32","costCenters":[],"links":[{"id":221376,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"country":"United States","state":"Colorado, New Mexico, Utah","otherGeospatial":"Paradox Basin region","geographicExtents":"{\n \"type\": \"FeatureCollection\",\n \"features\": [\n {\n \"type\": \"Feature\",\n \"properties\": {},\n \"geometry\": {\n \"type\": \"Polygon\",\n \"coordinates\": [\n [\n [\n -110.390625,\n 34.32529192442733\n ],\n [\n -105.40283203124999,\n 34.32529192442733\n ],\n [\n -105.40283203124999,\n 39.30029918615029\n ],\n [\n -110.390625,\n 39.30029918615029\n ],\n [\n -110.390625,\n 34.32529192442733\n ]\n ]\n ]\n }\n }\n ]\n}","volume":"4","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a16d4e4b0c8380cd55295","contributors":{"authors":[{"text":"Hanshaw, B.B.","contributorId":25928,"corporation":false,"usgs":true,"family":"Hanshaw","given":"B.B.","email":"","affiliations":[],"preferred":false,"id":361446,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Hill, G.A.","contributorId":83666,"corporation":false,"usgs":true,"family":"Hill","given":"G.A.","email":"","affiliations":[],"preferred":false,"id":361447,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70009829,"text":"70009829 - 1969 - Determination of traces of silver in waters by anion exchange and atomic absorption spectrophotometry","interactions":[],"lastModifiedDate":"2020-11-29T20:14:54.206493","indexId":"70009829","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":760,"text":"Analytica Chimica Acta","active":true,"publicationSubtype":{"id":10}},"title":"Determination of traces of silver in waters by anion exchange and atomic absorption spectrophotometry","docAbstract":"A method has been developed for the accurate determination of 0.1–1 μg of silver per liter of water. The method permits stabilization of silver in water without loss to container walls. Optimum conditions have been established for the complete recovery of silver from water with an anion-exchange column, for quantitative elution of silver from the resin, and for measurement of silver by atomic absorption spectrophotometry after chelation with ammonium pyrrolidine dithiocarbamate and extraction of the chelate with MIBK. Silver in the 1–10
The applicability of computer-oriented techniques to assist in the interpretation of brine data is demonstrated by the use of six programs on data from two example areas. These programs include a data tabling routine; routines for producing Stiff, Piper, and Ropes diagrams; programs for calculating ionic ratios; and programs for plotting maps of chemical data. The examples illustrate: (1) the range in water quality and contamination of potable water by brines in Stafford, Pratt, and Barber Counties, and (2) the change in water quality in the Arbuckle Group from southeast to south-central Kansas.
Study of several closed drainages in the Great Basin has shown that the interstitial solutions of shallow, fine-grained playa deposits store a large quantity of dissolved solids and are often more concentrated than associated lakes and ponds, except in peripheral zones of stream or ground-water inflow. These interstitial fluids, when compared with local runoff, impoundments, or spring waters, commonly have a distinctive ionic composition which sometimes cannot be explained by either simple mixing of surface and subsurface inflow or by evaporative concentration.
At Abert Lake, Oregon, the interstitial solute concentrations increased with depth to values as much as five times greater than the lake, except where springs indicate significant ground-water input. Where Na+, Cl, and CO2 species constitute more than 90% of the solutes,
In the Abert Lake area, as in other parts of the western Great Basin,
X-ray analysis of Li+- and K+-saturated samples, differential thermal analysis (DTA), thermal gravimetric analysis (TGA), and chemical analysis of 83 samples enable a distinction to be made between Wyoming, Tatatilla, Otay, Chambers, and non-ideal types of montmorillonite, and between ideal and non-ideal types of beidellite. The Greene-Kelly Li+-test differentiates between the montmorillonites and beidellites. Re-expansion with ethylene glycol after K+-saturation and heating at 300°C depends upon total net layer charge and not upon location of the charge. Wyoming-type montmorillonites characteristically have low net layer charge and re-expand to 17 Å. whereas most other montmorillonites and beidellites have a higher net layer charge and re-expand to less than 17 Å.
Major differences in dehydroxylation temperatures cannot be related consistently to the amount of Al3+-for-Si4+ substitution, nor to the amount of Mg, Fe, type of interlayer cations, or particle size. The major factor controlling temperature of dehydroxylation seems to be the amount of structural (OH). Of 19 samples analyzed by TGA, montmorillonites and the one ideal beidellite that give dehydroxylation endotherms on their DTA curves between 650° and 760°C all contain nearly the ideal amount of 4(OH) per unit cell, but the non-ideal montmorillonites and beidellites that give dehydroxylation peaks between 550° and 600°C do not. Non-ideal beidellites contain more than the ideal amount of structural (OH) and non-ideal montmorillonites seem to contain less, although the low temperature of dehydroxylation of the latter could also be due to other structural defects. Change in X-ray diffraction intensity of the 001 reflection during dehydroxylation suggests that the extra (OH) of beidellite occurs at the apex of SiO4 or AlO4 tetrahedrons with the H+ of the (OH)- polarized toward vacant cation sites in the octahedral sheet.
","language":"English","publisher":"The Clay Minerals Society","doi":"10.1346/CCMN.1969.0170302","usgsCitation":"Schultz, L.G., 1969, Lithium and potassium absorption, dehydroxylation temperature, and structural water content of aluminous smectites: Clays and Clay Minerals, v. 17, no. 3, p. 115-149, https://doi.org/10.1346/CCMN.1969.0170302.","productDescription":"36 p.","startPage":"115","endPage":"149","costCenters":[],"links":[{"id":219501,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"17","issue":"3","noUsgsAuthors":false,"publicationDate":"2024-07-01","publicationStatus":"PW","scienceBaseUri":"505a4822e4b0c8380cd67c2f","contributors":{"authors":[{"text":"Schultz, Leonard Gene","contributorId":19146,"corporation":false,"usgs":true,"family":"Schultz","given":"Leonard","email":"","middleInitial":"Gene","affiliations":[],"preferred":false,"id":357730,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70011501,"text":"70011501 - 1969 - Oxygen isotope fractionation in divalent metal carbonates","interactions":[],"lastModifiedDate":"2020-11-30T13:41:37.401641","indexId":"70011501","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":2207,"text":"Journal of Chemical Physics","active":true,"publicationSubtype":{"id":10}},"title":"Oxygen isotope fractionation in divalent metal carbonates","docAbstract":"CaCO3–H2O, 1000lnα = 2.78(106T−2)− 3.39,\">CaCO3–H2O, 1000lnα = 2.78(106T−2)− 3.39,CaCO3–H2O, 1000lnα = 2.78(106T−2)− 3.39, |
SrCO3–H2O, 1000lnα = 2.69(106T−2)− 3.74,\">SrCO3–H2O, 1000lnα = 2.69(106T−2)− 3.74,SrCO3–H2O, 1000lnα = 2.69(106T−2)− 3.74, |
BaCO3–H2O, 1000lnα = 2.57(106T−2)− 4.73.\">BaCO3–H2O, 1000lnα = 2.57(106T−2)− 4.73.BaCO3–H2O, 1000lnα = 2.57(106T−2)− 4.73. |
No abstract available.
","language":"English","publisher":"American Chemical Society","doi":"10.1021/j100725a062","issn":"00223654","usgsCitation":"O’Neil, J.R., and Adami, L., 1969, Oxygen isotope partition function ratio of water and the structure of liquid water: Journal of Physical Chemistry, v. 73, no. 5, p. 1553-1558, https://doi.org/10.1021/j100725a062.","productDescription":"6 p.","startPage":"1553","endPage":"1558","numberOfPages":"6","costCenters":[],"links":[{"id":219519,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"73","issue":"5","noUsgsAuthors":false,"publicationDate":"2002-05-01","publicationStatus":"PW","scienceBaseUri":"505bae79e4b08c986b32410e","contributors":{"authors":[{"text":"O’Neil, J. R.","contributorId":69633,"corporation":false,"usgs":true,"family":"O’Neil","given":"J.","email":"","middleInitial":"R.","affiliations":[],"preferred":false,"id":358401,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Adami, L.H.","contributorId":56677,"corporation":false,"usgs":true,"family":"Adami","given":"L.H.","affiliations":[],"preferred":false,"id":358400,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70011611,"text":"70011611 - 1969 - Heat flow measurements on the southeast coast of Australia","interactions":[],"lastModifiedDate":"2020-11-29T17:55:48.524254","indexId":"70011611","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1427,"text":"Earth and Planetary Science Letters","active":true,"publicationSubtype":{"id":10}},"title":"Heat flow measurements on the southeast coast of Australia","docAbstract":"Three boreholes have been drilled for the Australian National University near the southeast coast of New South Wales, Australia. The heat flows found are 1.1, 1.0, and 1.3 μcal/cm2sec. The errors resulting from the proximity of the sea and a lake, surface temperature change, conductivity structure and water flow have been examined. The radioactive heat production in some of the intrusive rocks of the area have also been measured. The heat flows are much lower than the values of about 2.0 found elsewhere in south eastern Australia. The lower values appear to be part of a distinct heat flow province in eastern Australia.
Weathering products formed on surfaces of both potassium and plagioclase feldspar (An70), which were continuously leached in a Soxhlet extraction apparatus for 140 days with 7.21 of distilled water per day at a temperature of approximately 78°C, are morphologically identical to natural products developed on potassium feldspars weathered under conditions of good drainage in the humid tropics. The new products, which first appear as tiny bumps on the feldspar surface, start to develop mainly at exposed edges but also at apparently random sites on flat cleavage surfaces. As weathering continues, the bumps grow outward from the feldspar surface to form tapered projections, which then develop into wide-based thin films or sheets. The thin sheets of many projections merge laterally to form one continuous flame-shaped sheet. The sheets formed on potassium feldspars may then roll to form tubes that are inclined at a high angle to the feldspar surface. Etch pits of triangular outline on the artificially weathered potassium feldspars serve as sites for development of continuous, non-rolled, hollow tubes. It is inferred from its morphology that this weathering product is halloysite or its primitive form. The product of naturally weathered potassium feldspars is halloysite . 4H2O.
The flame-shaped films or sheets formed on artificially weathered plagioclase feldspar do not develop into hollow tubes, but instead give rise to a platy mineral that is most probably boehmite. These plates form within the flame-shaped films, and with continued weathering are released as the film deteriorates. There is no indication from this experiment that platy pseudohexagonal kaolinite forms from any of these minerals under the initial stage of weathering.
","language":"English","publisher":"The Clay Minerals Society","doi":"10.1346/CCMN.1969.0170104","usgsCitation":"Parham, W.E., 1969, Formation of halloysite from feldspar: Low temperature, artificial weathering versus natural weathering: Clays and Clay Minerals, v. 17, no. 1, p. 13-22, https://doi.org/10.1346/CCMN.1969.0170104.","productDescription":"10 p.","startPage":"13","endPage":"22","costCenters":[],"links":[{"id":221753,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"17","issue":"1","noUsgsAuthors":false,"publicationDate":"2024-07-01","publicationStatus":"PW","scienceBaseUri":"505a1350e4b0c8380cd545eb","contributors":{"authors":[{"text":"Parham, Walter E.","contributorId":58022,"corporation":false,"usgs":false,"family":"Parham","given":"Walter","email":"","middleInitial":"E.","affiliations":[],"preferred":false,"id":361181,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70011612,"text":"70011612 - 1969 - Surface area of vermiculite with nitrogen and carbon dioxide as adsorbates","interactions":[],"lastModifiedDate":"2018-01-25T14:36:50","indexId":"70011612","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1245,"text":"Clays and Clay Minerals","onlineIssn":"1552-8367","printIssn":"0009-8604","active":true,"publicationSubtype":{"id":10}},"title":"Surface area of vermiculite with nitrogen and carbon dioxide as adsorbates","docAbstract":"Surface-area studies were made on several homoionic vermiculites with both nitrogen and carbon dioxide as adsorbates. These studies show that only very slight penetration occurs between individual vermiculite platelets. This is in contrast to an earlier investigation of montmorillonite where it was found that the degree of penetration between layers is quite high, particularly for carbon dioxide, and is governed by the size and charge of the interlayer cation. The inability of these adsorbates to penetrate substantially between vermiculite platelets is due primarily to this mineral's high surface-charge density.
The extent of penetration of nitrogen and carbon dioxide at the edges of vermiculite platelets, though slight, is influenced by the coordinated water retained within the sample at a given degassing temperature. Forces between layers are weakened with increasing water content, which permits slightly greater penetration by adsorbate gases. Thus, the surface area of vermiculite, as determined by gas adsorption, is larger than the calculated external surface area based upon particle size and shape considerations. In addition, \"extra\" surface is provided by the lifting and scrolling of terminal platelets. These morphological features are shown in scanning electron micrographs of a naturally occuring vermiculite.
","language":"English","publisher":"The Clay Minerals Society","doi":"10.1346/CCMN.1969.0170403","usgsCitation":"Thomas, J., and Bohor, B., 1969, Surface area of vermiculite with nitrogen and carbon dioxide as adsorbates: Clays and Clay Minerals, v. 17, no. 4, p. 205-209, https://doi.org/10.1346/CCMN.1969.0170403.","productDescription":"5 p.","startPage":"205","endPage":"209","costCenters":[],"links":[{"id":220851,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"17","issue":"4","noUsgsAuthors":false,"publicationDate":"2024-07-01","publicationStatus":"PW","scienceBaseUri":"505b9f95e4b08c986b31e6b0","contributors":{"authors":[{"text":"Thomas, Josephus Jr.","contributorId":11755,"corporation":false,"usgs":false,"family":"Thomas","given":"Josephus","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":361541,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Bohor, Bruce F.","contributorId":104823,"corporation":false,"usgs":true,"family":"Bohor","given":"Bruce F.","affiliations":[],"preferred":false,"id":361542,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70011674,"text":"70011674 - 1969 - Blueschist-facies metamorphism related to regional thrust faulting","interactions":[],"lastModifiedDate":"2020-11-29T17:48:28.255922","indexId":"70011674","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":3525,"text":"Tectonophysics","active":true,"publicationSubtype":{"id":10}},"title":"Blueschist-facies metamorphism related to regional thrust faulting","docAbstract":"Rocks of the blueschist (glaucophane schist) facies occur throughout the world in narrow tectonic belts associated with ultramafic rocks. In the Coast Range province of California, blueschist rocks are devloped in the eugeosynclinal Franciscan Formation of Late Mesozoic age. The blueschist rocks form a narrow belt for more than 800 km along the eastern margin of this province and commonly are separated from rocks of an overlying thrust plate by serpentinite. Increasing metamorphism upward toward the thrust fault is indicated mineralogically by a transition from pumpellyite to lawsonite and texturally by a transition from metagraywacke to schist. The blueschist metamorphism probably occurred during thrusting in a zone of anomalously high water pressure in the lower plate along the sole of the thrust fault. This tectonic mode of origin for blueschist differs from the generally accepted hypothesis involving extreme depth of burial. Other belts of blueschist-facies rocks, including the Sanbagawa belt of Japan, the marginal synclinal belt of New Zealand, and the blueschist-ultramafic belts of Venezuela, Kamchatka, Ural mountains, and New Caledonia have similar geologic relations and might be explained in the same manner.
","language":"English","publisher":"Elsevier","doi":"10.1016/0040-1951(69)90100-0","issn":"00401951","usgsCitation":"Blake, M., Irwin, W., and Coleman, R.G., 1969, Blueschist-facies metamorphism related to regional thrust faulting: Tectonophysics, v. 8, no. 3, p. 237-246, https://doi.org/10.1016/0040-1951(69)90100-0.","productDescription":"10 p.","startPage":"237","endPage":"246","costCenters":[{"id":312,"text":"Geology, Minerals, Energy, and Geophysics Science Center","active":true,"usgs":true}],"links":[{"id":220718,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"8","issue":"3","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"5059f1eee4b0c8380cd4aee2","contributors":{"authors":[{"text":"Blake, M.C. Jr.","contributorId":27094,"corporation":false,"usgs":true,"family":"Blake","given":"M.C.","suffix":"Jr.","affiliations":[],"preferred":false,"id":361680,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Irwin, W. P.","contributorId":82347,"corporation":false,"usgs":true,"family":"Irwin","given":"W. P.","affiliations":[],"preferred":false,"id":361682,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Coleman, R. G.","contributorId":75170,"corporation":false,"usgs":true,"family":"Coleman","given":"R.","email":"","middleInitial":"G.","affiliations":[],"preferred":false,"id":361681,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70011622,"text":"70011622 - 1969 - Ion association in natural brines","interactions":[],"lastModifiedDate":"2020-11-29T17:53:53.104347","indexId":"70011622","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":2,"text":"Article"},"publicationSubtype":{"id":10,"text":"Journal Article"},"seriesTitle":{"id":1213,"text":"Chemical Geology","active":true,"publicationSubtype":{"id":10}},"title":"Ion association in natural brines","docAbstract":"Natural brines, both surface and subsurface, are highly associated aqueous solutions. Ion complexes in brines may be ion pairs in which the cation remains fully hydrated and the bond between the ions is essentially electrostatic, or coordination complexes in which one or more of the hydration water molecules are replaced by covalent bonds to the anion. Except for Cl−, the major simple ions in natural brines form ion pairs; trace and minor metals in brines form mainly coordination complexes.
Limitations of the Debye-Hückel relations for activity coefficients and lack of data on definition and stability of all associated species in concentrated solutions tend to produce underestimates of the degree of ion association, except where the brines contain a very high proportion of Cl−. Data and calculations on closed basin brines of highly varied composition have been coupled with electrode measurements of single-ion activities in an attempt to quantify the degree of ion association. Such data emphasize the role of magnesium complexes.
Trace metal contents of closed basin brines are related to complexes formed with major anions. Alkaline sulfo- or chlorocarbonate brines (western Great Basin) carry significant trace metal contents apparently as hydroxides or hydroxy polyions. Neutral high chloride brines (Bonneville Basin) are generally deficient in trace metals.
With a knowledge of the thermodynamic properties of a natural water, many possible reactions with other phases (solids, gases, other liquids) may be predicted. A knowledge of these reactions is particularly important in the study of natural brines which may be saturated with many solid phases (silicates, carbonates, sulfates, etc.), which may have a high pH and bring about dissolution of other phases (silica, amphoteric hydroxides, CO2, etc.), and which because of their high density may form relatively stable interfaces with dilute waters.
","language":"English","publisher":"Elsevier","doi":"10.1016/0009-2541(69)90039-4","issn":"00092541","usgsCitation":"Truesdell, A., and Jones, B., 1969, Ion association in natural brines: Chemical Geology, v. 4, no. 1-2, p. 51-62, https://doi.org/10.1016/0009-2541(69)90039-4.","productDescription":"12 p.","startPage":"51","endPage":"62","numberOfPages":"12","costCenters":[],"links":[{"id":221054,"rank":0,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"}],"volume":"4","issue":"1-2","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"505a3ed4e4b0c8380cd64089","contributors":{"authors":[{"text":"Truesdell, A.H.","contributorId":52566,"corporation":false,"usgs":false,"family":"Truesdell","given":"A.H.","email":"","affiliations":[{"id":6672,"text":"former: USGS Southwest Biological Science Center, Colorado Plateau Research Station, Flagstaff, AZ. Current address: TN-SCORE, Univ of Tennessee, Knoxville, TN, e-mail: jennen@gmail.com","active":true,"usgs":false}],"preferred":false,"id":361563,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Jones, B.F.","contributorId":52156,"corporation":false,"usgs":true,"family":"Jones","given":"B.F.","email":"","affiliations":[],"preferred":false,"id":361562,"contributorType":{"id":1,"text":"Authors"},"rank":2}]}} ,{"id":70045464,"text":"70045464 - 1969 - Hydrology of the San Luis Valley, south-central Colorado","interactions":[],"lastModifiedDate":"2013-05-23T11:41:05","indexId":"70045464","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":6,"text":"USGS Unnumbered Series"},"seriesTitle":{"id":375,"text":"Open-File Report","active":false,"publicationSubtype":{"id":6}},"title":"Hydrology of the San Luis Valley, south-central Colorado","docAbstract":"An investigation of the water resources of the Colorado part of the San Luis Valley was begun in 1966 by the U.S. Geological Survey, in cooperation with the Colorado Water Conservation Board. (See index map, fig. 1). The purpose of the investigation is to provide information for planning and implementing improved water-development and management practices. The major water problems in the San Luis Valley include (1) waterlogging, (2) waste of water by nonbeneficial evapotranspiration, (3) deterioration of ground-water chemical quality, and (4) failure of Colorado to deliver water to New Mexico and Texas in accordance with the Rio Grande Compact. This report describes the hydrologic environment, extent of water-resource development, and some of the problems related to that development. Information presented is based on data collected from 1966 to 1968 and on previous studies. Subsequent reports are planned as the investigation progresses. The San Luis Valley extends about 100 miles from Poncha Pass near the northeast corner of Saguache County, Colo., to a point about 16 miles south of the Colorado-New Mexico State line. The total area is 3,125 square miles, of which about 3,000 are in Colorado. The valley is nearly flat except for the San Luis Hills and a few other small areas. The Colorado part of the San Luis Valley, which is described in this report, has an average altitude of about 7,700 feet. Bounding the valley on the west are the San Juan Mountains and on the east the Sangre de Cristo Mountains. Most of the valley floor is bordered by alluvial fans deposited by streams originating in the mountains, the most extensive being the Rio Grande fan (see block diagram, fig. 2 in pocket). Most of the streamflow is derived from snowmelt from 4,700 square miles of watershed in the surrounding mountains. The northern half of the San Luis Valley is internally drained and is referred to as the closed basin. The lowest part of this area is known locally as the \"sump.\" The remainder of the valley is drained by the Rio Grande and its tributaries. The climate of the San Luis Valley is arid, and a successful agricultural economy would not be possible without irrigation. It is characterized by cold winters, moderate summers, and much sunshine. The average annual precipitation on the valley floor ranges from 7 to 10 inches. More than half the precipitation occurs from July to September. Moisture deficiency in the valley is shown by the graph comparing pan evaporation and precipitation {fig. 3}. For the years 1961-67 average pan evaporation for the period April through September was 52.25 inches, but average precipitation for the period was only 5.02 inches. Average annual precipitation was 7.8 inches. Owing to the short growing season (90-120 days), crops a.re restricted mainly to barley, oats, potatoes, and other vegetables.","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Denver, CO","doi":"10.3133/70045464","collaboration":"Prepared in cooperation with the Colorado Water Conservation Board","usgsCitation":"Emery, P.A., Boettcher, A.J., Snipes, R., and Mcintyre, H., 1969, Hydrology of the San Luis Valley, south-central Colorado: Open-File Report, ii, 22 p.; 3 Plates: 23.79 x 27.78 inches or smaller, https://doi.org/10.3133/70045464.","productDescription":"ii, 22 p.; 3 Plates: 23.79 x 27.78 inches or smaller","numberOfPages":"26","additionalOnlineFiles":"Y","temporalStart":"1966-01-01","temporalEnd":"1968-12-31","costCenters":[{"id":191,"text":"Colorado Water Science Center","active":true,"usgs":true}],"links":[{"id":271022,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/unnumbered/70045464/report-thumb.jpg"},{"id":272738,"type":{"id":11,"text":"Document"},"url":"https://pubs.usgs.gov/unnumbered/70045464/report.pdf"},{"id":272739,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70045464/plate-2.pdf"},{"id":272740,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70045464/plate-4.pdf"},{"id":272741,"type":{"id":17,"text":"Plate"},"url":"https://pubs.usgs.gov/unnumbered/70045464/plate-7.pdf"}],"country":"United States","state":"Colorado","county":"Alamosa;Conejos;Costilla;Custer;Huerfano;Rio Grande;Saguache","otherGeospatial":"San Luis Valley","geographicExtents":"{ \"type\": \"FeatureCollection\", \"features\": [ { \"type\": \"Feature\", \"properties\": {}, \"geometry\": { \"type\": \"Polygon\", \"coordinates\": [ [ [ -105.25,37.0 ], [ -105.25,38.5 ], [ -106.75,38.5 ], [ -106.75,37.0 ], [ -105.25,37.0 ] ] ] } } ] }","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"516fc466e4b05024ef3cd408","contributors":{"authors":[{"text":"Emery, P. 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Jr.","contributorId":34027,"corporation":false,"usgs":true,"family":"Mcintyre","given":"H.J.","suffix":"Jr.","email":"","affiliations":[],"preferred":false,"id":477542,"contributorType":{"id":1,"text":"Authors"},"rank":4}]}} ,{"id":70190816,"text":"70190816 - 1969 - Hydrologic and climatologic data, 1968, Salt Lake County, Utah","interactions":[],"lastModifiedDate":"2018-03-26T15:42:29","indexId":"70190816","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":5498,"text":"Utah Basic-Data Release","active":true,"publicationSubtype":{"id":2}},"seriesNumber":"17","title":"Hydrologic and climatologic data, 1968, Salt Lake County, Utah","docAbstract":"An investigation of the water resources of Salt Lake County, Utah, was undertaken by the Water Resources Division of the U.S. Geological Survey in July 1963. This investigation is a cooperative project financed chiefly by equal contributions of the State of Utah and the Federal Government in accordance with an agreement between the Division of Water Rights, Utah Department of Natural Resources, and the Geological Survey. The investigation was financed during the period covered by this report by the following organizations: Utah Division of Water Rights (formerly State Engineer), Utah Division of Water Resources (formerly Water and Power Board), Salt Lake County, Salt Lake County Water Conservancy District, Central Utah Water Conservancy District, Metropolitan Water District of Salt Lake City, City of Murray, Granger-Hunter Improvement District, Taylorsville-Bennion Improvement District, Holladay Water Company, Magna Water and Sewer District, U.S. Bureau of Reclamation, U.S. Geological Survey
The investigation encompasses the collection and interpretation of a large variety of climatologic, hydrologic, and geologic data in and near Salt Lake County. Utah Basic-Data Releases 11-13 and 15 contain data collected through 1967. This release contains climatologic and surface-water data for the 1968 water year (October 1967 to September 1968) and ground-water data collected during the 1968 calendar year. This is the final annual release of basic data for this investigation. Interpretive reports summarizing the results are in preparation. Organizations that furnished data are acknowledged in station descriptions and footnotes to tables.
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Much of the basic data was collected by the U.S. Geological Survey in cooperation with the Utah Department of Natural Resources, Division of Water Rights, during the years 1935-67. Data collected by other organizations are also included in this report.
","language":"English","publisher":"U.S. Geological Survey","publisherLocation":"Salt Lake City, UT","collaboration":"Prepared in cooperation with The Utah Department of Natural Resources, Division of Water Rights","usgsCitation":"Cordova, R., 1969, Selected hydrologic data, southern Utah and Goshen Valleys, Utah: Utah Basic-Data Release 16, iii, 35 p.","productDescription":"iii, 35 p.","numberOfPages":"41","costCenters":[{"id":610,"text":"Utah Water Science Center","active":true,"usgs":true}],"links":[{"id":345822,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":345821,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://www.waterrights.utah.gov/cgi-bin/docview.exe?Folder=TP21-1-310&Title=Basic+Data+Report+16"}],"country":"United States","state":"Utah","otherGeospatial":"Goshen Valley, Utah Valley","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"59bf899de4b091459a5e0893","contributors":{"authors":[{"text":"Cordova, R.M.","contributorId":77511,"corporation":false,"usgs":true,"family":"Cordova","given":"R.M.","email":"","affiliations":[],"preferred":false,"id":710667,"contributorType":{"id":1,"text":"Authors"},"rank":1}]}} ,{"id":70191027,"text":"70191027 - 1969 - Water in Kentucky","interactions":[],"lastModifiedDate":"2017-09-21T15:15:18","indexId":"70191027","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","noYear":false,"publicationType":{"id":18,"text":"Report"},"publicationSubtype":{"id":2,"text":"State or Local Government Series"},"seriesTitle":{"id":5503,"text":"Kentucky Geological Survey Special Publication","active":true,"publicationSubtype":{"id":2}},"seriesNumber":"16-10","title":"Water in Kentucky","docAbstract":"No abstract available.
","language":"English","publisher":"Kentucky Geological Survey","usgsCitation":"Krieger, R.A., Cushman, R.V., and Thomas, N., 1969, Water in Kentucky: Kentucky Geological Survey Special Publication 16-10, 51 p.","productDescription":"51 p.","costCenters":[],"links":[{"id":345994,"type":{"id":24,"text":"Thumbnail"},"url":"https://pubs.usgs.gov/thumbnails/outside_thumb.jpg"},{"id":345993,"rank":1,"type":{"id":15,"text":"Index Page"},"url":"https://kgs.uky.edu/kgsweb/pubs/pubsearch.asp","text":"Available from the Kentucky Geological Survey"}],"country":"United States","state":"Kentucky","noUsgsAuthors":false,"publicationStatus":"PW","scienceBaseUri":"59c4cf9ae4b017cf313d3cce","contributors":{"authors":[{"text":"Krieger, Robert A.","contributorId":99954,"corporation":false,"usgs":true,"family":"Krieger","given":"Robert","email":"","middleInitial":"A.","affiliations":[],"preferred":false,"id":711006,"contributorType":{"id":1,"text":"Authors"},"rank":1},{"text":"Cushman, Robert Vittum","contributorId":96661,"corporation":false,"usgs":true,"family":"Cushman","given":"Robert","email":"","middleInitial":"Vittum","affiliations":[],"preferred":false,"id":711007,"contributorType":{"id":1,"text":"Authors"},"rank":2},{"text":"Thomas, N.O.","contributorId":99962,"corporation":false,"usgs":true,"family":"Thomas","given":"N.O.","email":"","affiliations":[],"preferred":false,"id":711008,"contributorType":{"id":1,"text":"Authors"},"rank":3}]}} ,{"id":70185803,"text":"pp669D - 1969 - The rapids and the pools - Grand Canyon: Chapter D in The Colorado River region and John Wesley Powell (Professional Paper 669)","interactions":[{"subject":{"id":70185803,"text":"pp669D - 1969 - The rapids and the pools - Grand Canyon: Chapter D in The Colorado River region and John Wesley Powell (Professional Paper 669)","indexId":"pp669D","publicationYear":"1969","noYear":false,"chapter":"D","title":"The rapids and the pools - Grand Canyon: Chapter D in The Colorado River region and John Wesley Powell (Professional Paper 669)"},"predicate":"IS_PART_OF","object":{"id":25022,"text":"pp669 - 1969 - The Colorado River region and John Wesley Powell","indexId":"pp669","publicationYear":"1969","noYear":false,"title":"The Colorado River region and John Wesley Powell"},"id":1}],"isPartOf":{"id":25022,"text":"pp669 - 1969 - The Colorado River region and John Wesley Powell","indexId":"pp669","publicationYear":"1969","noYear":false,"title":"The Colorado River region and John Wesley Powell"},"lastModifiedDate":"2017-03-29T10:46:45","indexId":"pp669D","displayToPublicDate":"1969-01-01T00:00:00","publicationYear":"1969","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":"669","chapter":"D","title":"The rapids and the pools - Grand Canyon: Chapter D in The Colorado River region and John Wesley Powell (Professional Paper 669)","docAbstract":"Through the Grand Canyon the Colorado drops in elevation about 2,200 feet in 280 miles; most of this drop occurs in rapids that account for only 10 percent of the distance. Despite the importance of rapids, there are no waterfalls. Depth measurements made at 1/10-mile intervals show that the bed profile is highly irregular, but the apparent randomness masks an organized alternation of deeps and shallows. Measurement of the age of a lava flow that once blocked the canyon near Toroweap shows that no appreciable deepening of the canyon has taken place during the last million years. It is reasoned that the river has had both the time and the ability to eliminate the rapids. The long-continued existence and the relative straightness of the longitudinal profile indicate that the river maintains a state of quasi-equilibrium which provides the hydraulic requirements for carrying the debris load brought in from upstream without continued erosion of the canyon bed. The maintenance of the alternating pools and rapids seems to be a necessary part of this poised or equilibrium condition.
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