An extended equation to calculate NaCl contents from final clathrate melting temperatures in H2O-CO2-NaCl fluid inclusions: Implications for P-T isochore location

Darling, Robert S.

doi:10.1016/0016-7037(91)90079-k

Cited by 134 publications

(61 citation statements)

References 7 publications

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“…Errors of these measurements were ±0.2°C at and below 0°C and ±1.5°C at 340°C, respectively. Salinity data were calculated from freezing point depression in the system H 2 O-NaCl for CO 2 -free, aqueous inclusions (Bodnar, 1993), from clathrate melting temperatures for CO 2 -bearing inclusions (Darling, 1991), and from dissolution temperature for halite ± sylvite-bearing inclusions (Bodnar et al, 1989).…”

Section: Methods Of Studymentioning

confidence: 99%

Fluid inclusions and their stable isotope geochemistry of the carbonate-hosted talc deposits near the Cretaceous Muamsa Granite, South Korea

Shin

Lee

2006

Geochem. J.

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Microthermometric and stable isotope studies of fluid inclusions were conducted for the Poongjeon talc deposit which formed as alteration products of calc-silicate minerals during the retrograde stage of contact metamorphism related to the intrusion of the Cretaceous Muamsa Granite of South Korea. Two types of quartz vein are observed in the deposit. Vein I, which occurs in marble, is characterized by both mixing and unmixing process of fluid inclusions. Repeated boiling of carbonic fluids produced high X CO2 fluids abundantly and low X CO2 or aqueous fluids a little. Occasionally mixing took place between halite ± sylvite-bearing fluids and carbonic fluids. As for vein II, which occurs typically at points of amphibolite-metapelite contact, the fluid mixing model can be applied to the coexistence of abundant CH 4 ± H 2 O, H 2 O-CO 2 -CH 4 fluids with variable CH 4 /CO 2 ratios (X CH4 > 0.1), and minor high X CO2 fluid inclusions. The CH 4 -rich inclusions seem to be derived from the reheating of C-bearing metapelite during contact metamorphism.Occurrences of halite ± sylvite-bearing inclusions along trails in both vein I and II are chronologically behind other primary inclusions and are closely related to the talc mineralization. The mineralizing fluids would have been derived directly from a water-saturated crystallizing melt and the entrapment occurred between 150 and 700 bars at 260°-390°C. The δ 13 C CO2 values, 0.1-2.4‰, of inclusion fluids of vein I seem to have resulted from the isotopic exchange of magmatic carbon with 13 C-enriched CO 2 liberated from the decarbonation for calc-silicate formation. Distinctly lower δ 13 C CO2 values, -3.5 to -1.7‰, in vein II could have originated from the strong effect of metasediment-derived fluids. Higher δ 18 O H2O values of vein I and lower δD values of vein II, both of which belong to the magmatic water range, seem to have similar evolution history as δ 13 C values. Geologic structures such as faults and contacts between different rock units seem to have promoted infiltration, mixing, and unmixing of fluids of diverse origins.

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Section: Methods Of Studymentioning

confidence: 99%

Fluid inclusions and their stable isotope geochemistry of the carbonate-hosted talc deposits near the Cretaceous Muamsa Granite, South Korea

Shin

Lee

2006

Geochem. J.

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“…The density of a non-aqueous phase was calculated via the Duan et al (1992) equation of state. The salinity of the aqueous phase of carbonic-bearing inclusions was calculated using chlatrate meiting temperatures (Darling, 1991). The resuits of fluid properties calculations are shown in Table 3.…”

Section: Fluid Inclusionsmentioning

confidence: 99%

Emeralds from the Delbegetey deposit (Kazakhstan): mineralogical characteristics and fluid-inclusion study

Gavrilenko¹,

Pérez²,

Bolíbar³

et al. 2006

Mineral. mag.

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AB5TRACTThe aim of this study is to provide the first detailed mineralogical and fluid-inc1usion description of emeralds from the Delbegetey deposit (Kazakhstan). The characteristic features of Delbegetey emeralds are established: they have dissolution figures on crystal faces, bluish colour and distinct colour zoning; the refractive indices are ro = 1.566-1.570, E = 1.558-1.562, and the specific gravity is 2.65±0.005, relatively low for natural emeralds; they have very small concentrations of the impurities (Fe, Mg, Na and others) typical of other emeralds, and contain Cr and V; there is a significant preponderance of vapour in fluid inc1usions of all types and there is liquid-to-vapour homogenization of primary fluid inc1usions (at 395-420°C). The lattice oxygen isotope composition data obtained (0 18 0 SMOW value of 11.3%0) situate the deposit within the range characteristic of other granite-related emerald deposits. Emerald crystallization took place in low-density (0.40-0.55 g/cm 3 ) aqueous fluid, with the following chemical composition (mol.%): 75.6-97.4 HzO, 0.0-18.4 caz, 0.0-0.9 C~, and 4.06-9.65 wt.% NaCI equiv. salinity. According to the calculated isochores, the pressure offormation ofthe Delbegetey emeralds can be estimated at 570-1240 bar.

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“…Clynne & Potter (1977) demonstrated that if the salinity of saline fluids in nature were converted to NaCl equivalents, the difference would not exceed 5%. Therefore, we calculated the salinity of type-IA fluid inclusions according to Oakes et al (1990), i.e., on the basis of the system of H 2 O-NaCl-CaCl 2 , that of type-IB and type-II inclusions by freezing points for aqueous sodium chloride solutions (Potter et al 1978), and that of CO 2 -bearing type-III inclusions by clathrate-melting temperature (Darling 1991). The salinity of the fluid in inclusions containing halite and sylvite as daughter minerals can be determined by dissolution of these daughter minerals , Sterner et al 1988.…”

Section: Microthermometric Datamentioning

confidence: 99%

HYDROTHERMAL As Bi MINERALIZATION IN THE NAKDONG DEPOSITS, SOUTH KOREA: INSIGHT FROM FLUID INCLUSIONS AND STABLE ISOTOPES

Shin¹,

Park²,

Lee³

et al. 2004

The Canadian Mineralogist

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At the Nakdong As-Bi deposits, South Korea, Cambro-Ordovician sedimentary sequences are cut by numerous dykes of quartz monzodiorite and porphyritic granite. In the deposit, stage I involves arsenic mineralization, chiefly associated with arsenopyrite, pyrite, sphalerite and chalcopyrite, whereas bismuth mineralization characterizes stage II, with the coprecipitation of pyrrhotite, chalcopyrite, galena, bismuth, bismuthinite, cosalite, matildite, schirmerite, Au-Ag alloy, and argentite. The mineralization was initiated with the introduction of heterogeneous fluids of high salinity, presumably owing to the prominence of Ca, Mg, Na and K. At stage II, fluid immiscibility, which led to bismuth mineralization, produced (halite ± sylvite)-bearing highsalinity fluids of 27.6 to 49.3 wt.% NaCl equivalents, as well as low-salinity vapor-rich fluids. The homogenization temperatures of mineralizing fluids decreased only slightly from stage I, 283-416°C, to stage II, 222-395°C. A decrease in 18 O as well as 13 C in going from calcite in fresh limestone (␦ 18 O in the range +17.5 to +22.4‰, ␦ 13C in the range +2.3 to +4.4‰) to silicified limestone (␦ 18 O in the range +13.3 to +18.3‰, ␦ 13 C in the range -2.5 to +1.3‰) were promoted not only by Rayleigh volatilization, but also by fluid-rock interaction, with the influx of magmatic fluids into carbonate rocks during the mineralization process. The fluid-rock interaction contributed to the CO 2 and CH 4 components in type-III fluids and also to the Ca-enrichment in type-I fluid inclusions. The prevailing species of sulfur in the mineralizing fluids is estimated to have been H 2 S. The ␦ 34S H2S values obtained from the sulfide minerals increased from stage I, +3.2 to +4.4‰, to stage II, +4.1 to +4.8‰, values typical of magmatic sulfur, and the temperatures of homogenization of fluid inclusions increased as well. The decrease of sulfur fugacities, from 10 -9.1 -10 -6.4 atm at stage I to 10 -15.7 -10 -9.2 atm at stage II, through sulfide precipitation and H 2 S loss, induced the destabilization of bisulfide complexes and characterized the change of mineral stabilities from arsenopyrite -pyrite -sphalerite to bismuthinite -native bismuth assemblages.

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An extended equation to calculate NaCl contents from final clathrate melting temperatures in H2O-CO2-NaCl fluid inclusions: Implications for P-T isochore location

Cited by 134 publications

References 7 publications

Fluid inclusions and their stable isotope geochemistry of the carbonate-hosted talc deposits near the Cretaceous Muamsa Granite, South Korea

Fluid inclusions and their stable isotope geochemistry of the carbonate-hosted talc deposits near the Cretaceous Muamsa Granite, South Korea

Emeralds from the Delbegetey deposit (Kazakhstan): mineralogical characteristics and fluid-inclusion study

HYDROTHERMAL As Bi MINERALIZATION IN THE NAKDONG DEPOSITS, SOUTH KOREA: INSIGHT FROM FLUID INCLUSIONS AND STABLE ISOTOPES

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