The deuterium content of hydrous minerals from the East-Central Sierra Nevada and Yosemite National Park

Godfrey, J.D.

doi:10.1016/0016-7037(62)90053-4

Cited by 193 publications

(66 citation statements)

References 8 publications

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“…Hydrogen for isotopic analysis was obtained from 50 mg samples of pure kaolinite using a procedure modified after Bigeleisen et al (1952) and Godfrey (1962). Samples were degassed at 150 ~ for 2 h under vacuum, and then maintained under vacuum at room temperature for 12 h. The samples were then reheated under vacuum for 30 min at 200 ~ prior to extraction of the hydroxyl group and hydrogen.…”

Section: Methodsmentioning

confidence: 99%

Origin of Cretaceous and Oligocene Kaolinites from the Iwaizumi Clay Deposit, Iwate, Northeastern Japan

Mizota

Longstaffe

1996

Clays and clay miner.

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Abstract--Hydrogen-(3D = -106 to -97%0 and oxygen-(3180 = +14.0 to +16.6%0 isotope compositions of kaolinite from late Cretaceous and Oligocene deposits at Iwaizumi, northeastern Japan, indicate that these clays formed by weathering of volcanic parent rocks, rather than during hydrothermal (>100 ~ alteration. The Iwaizumi kaolinites also are depleted of D and 180 relative to kaolinite formed during modern, tropical weathering, suggesting that the kaolinite developed under cool or cool-temperate conditions. The oxygen-isotope compositions of the kaolinite increase slightly upward through the deposits, perhaps implying a modest increase in temperature from late Cretaceous to Oligocene time. The 8D and 8~sO results for kaolinite from the Oligocene deposits closely follow the kaolinite weathering line. However, a small but systematic deviation from this line for the Cretaceous kaolinites is most simply explained by post-formational, hydrogen-isotope exchange between these clays and downward percolating meteoric water.

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Section: Methodsmentioning

confidence: 99%

Origin of Cretaceous and Oligocene Kaolinites from the Iwaizumi Clay Deposit, Iwate, Northeastern Japan

Mizota

Longstaffe

1996

Clays and clay miner.

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“…Hydrogen was extracted from whole-rock samples for analysis by dehydrating whole-rock samples under vacuum with an induction furnace and converting the evolved water to hydrogen gas by reaction with uranium at 850øC (Godfrey, 1962). Carbon dioxide was liberated from the carbonates for 6•sO and 6•3C analyses by reaction with phosphoric acid at 25øC for calcites and dolomites and at 50øC for siderites (McCrea, 1950 Samples show a marked correlation between blaC and stratigraphic position for both dolomites (Fig.…”

Section: Stable Isotopesmentioning

confidence: 99%

Stable isotope study of water-rock interaction and ore formation, Bayhorse base and precious metal district, Idaho

Seal¹,

Rye²

1992

Economic Geology

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“…The extracted 02 was converted quantitatively to CO2 and the gas analyzed on a mass spectrometer. Hydroxyl hydrogen was expelled as H~O by heating the sample up to 1300~ after removing interlayer and adsorbed water by heating under vacuum for about 24 hr at 250 ~ 300~ Hydrogen was formed by reacting the H20 vapor with uranium (Godfrey, 1962), and the D/H ratio was determined using a mass spectrometer (Friedman, 1953). The ~O is values are based on single analyses; from past experience, the standard deviation is probably better than 0.2%~ Most of the samples were analyzed twice for D/H and the precision of these analyses is ---2%~ All of the analyses presented here are in the usual notation and are relative to Standard Mean Ocean Water (SMOW) (Craig, 1961).…”

Section: Analytical Techniquesmentioning

confidence: 99%

Mineralogy, O18/O16, and D/H Ratios of Clay-Rich Sediments from Deep Sea Drilling Project Site 180, Aleutian Trench1

Eslinger

Yeh

1981

Clays and Clay Minerals

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Abstract--Mineralogy, O18/O 16, and D/H ratios have been determined in five size fractions (<0.1,0.1-0.5, 0.5-1.0, 1.0-2.0, and >2.0/zm) of seven samples taken from 500 m of Pleistocene deep-sea sediments cored at Deep Sea Drilling Project Site 180 in the Aleutian Trench. The depositional age of the samples spans the last 300,000 years; the samples have been interpreted by others to be continental detritus weathered from a mixed igneous, metamorphic, and sedimentary source area and then deposited by ice-rafting and turbidity currents. The minerals present are quartz, feldspar, illite, chlorite and/or non-expandable vermiculite, and expandable vermiculite and/or mixed-layer iUite/expandable vermiculite. The relative amounts of quartz, feldspar, and total clay vary with particle size, but are nearly constant from sample to sample for a given particle size. 80 is values of the four coarser size fractions range from +9.7 to + 12.0%~ with variations attributable to changes in quartz/feldspar and clay/(quartz + feldspar) abundances. Values of 80 is for the expandable vermiculite-rich <0.1-/.tm size fraction range from + 12.1 to + 16.3%o which indicates some oxygen isotope exchange at surface temperatures between meteoric waters and the parent rock during vermiculite formation. Values of 8D range from -46 to -74%0 with variations attributable to changes in amounts of different clay minerals present. There is no mineralogic or isotopic evidence ofpost-depositional reactions in the coarser size fractions, but a general change in 6D of the vermiculite-rich, <0.1-/zm size fraction from about -50%~ to about -70%0 with increasing depth may be due either to post-depositional isotopic exchange or to climatic changes in the terrestrial weathering environment.

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The deuterium content of hydrous minerals from the East-Central Sierra Nevada and Yosemite National Park

Cited by 193 publications

References 8 publications

Origin of Cretaceous and Oligocene Kaolinites from the Iwaizumi Clay Deposit, Iwate, Northeastern Japan

Origin of Cretaceous and Oligocene Kaolinites from the Iwaizumi Clay Deposit, Iwate, Northeastern Japan

Stable isotope study of water-rock interaction and ore formation, Bayhorse base and precious metal district, Idaho

Mineralogy, O18/O16, and D/H Ratios of Clay-Rich Sediments from Deep Sea Drilling Project Site 180, Aleutian Trench1

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