Oxygen isotope exchange between quartz and water

Clayton, Robert N.; O’Neil, James R.; Mayeda, T. K.

doi:10.1029/jb077i017p03057

Cited by 1,311 publications

(531 citation statements)

References 37 publications

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“…The results of the tests BK-1 and BK-2B (see Table 3) indicated no contamination of Fr -, Ac -, and Pr -, and insignificant contamination of Ox 2-, F -, Cl -and SO 4 2-. In addition, the effect of adsorption of minerals surfaces on the determination of species in leachates is negligible, within the uncertainty of Clayton et al (1972 T -2 ) -3.40. BK-1 0.00 ± 0.00 0.00 ± 0.00 0.00 ± 0.00 0.02 ± 0.02 0.04 ± 0.00 0.11 ± 0.01 0.04 ± 0.02 BK-2B 0.00 ± 0.00 0.00 ± 0.00 0.00 ± 0.00 0.06 ± 0.02 0.08 ± 0.02 0.18 ± 0.03 0.11 ± 0.02 BK-3 1.97 ± 0.04 1.85 ± 0.03 2.07 ± 0.03 1.98 ± 0.02 0.92 ± 0.01 2.00 ± 0.07 1.99 ± 0.04 STD 2.00 2.00 2.00 2.00 2.00 2.00 2.00…”

Section: Leaching Tests Of Inclusions In Mineralsmentioning

confidence: 88%

Short-chain carboxylates in high-temperature ore fluids of W-Sn deposits in south China.

2002

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The Xihuashan, Dangping and Piaotang deposits in the Jiangxi Province, south China can be considered as typical high-temperature hydrothermal quartz vein-type W-Sn mineralization, that is temporally and spatially related to Mesozoic S-type granite. Microthermometric studies of fluid inclusions in various minerals from these deposits were conducted to obtain homogenization temperature and salinity data. Major organic and inorganic aqueous components of the fluid inclusions were extracted by a crush-leaching, and concentrations of short-chain carboxylate (formate, acetate, propionate, oxalate), fluoride, chloride and sulfate anions in the leachates were determined using ion chromatography. The results indicate the presence of formate and acetate as well as minor amounts of oxalate and propionate in leachates, and the dominance of formate over other carboxylates. The molar ratio of acetate to formate appears to be a potential indicator of the redox state for the ore fluid system. Oxygen and hydrogen isotopic data show that inclusion water in quartz is mainly magmatic in origin. It is postulated that the dissolved carboxylate anions in the ore fluids for the deposits probably were generated by the breakdown of kerogen in "primitive sedimentary rocks" during the formation of S-type granites. The possibility of inorganic synthesis of the carboxylate species in a C-H-O system can not be excluded.organic complexes including metal-carboxylate complexes in hydrothermal solutions. Most studies, up to the present time, that looked at the role of organic matter in ore-formation were mainly focused on ore deposits formed at temperatures less than 200-250°C (Giordano, 1985200-250°C (Giordano, , 1994 and related to sedimentation and diagenesis, or those occurring in sedimentary rocks (e.g., Mississippi Valley type and red-bed type base-metal deposits). Lewan and Pittman (1994) pointed out the importance of identifying and quantifying organic acids in fluid inclusions of ore and related gangue minerals in developing and testing models for oreforming systems. Analysis of the aqueous organic components of fluid inclusions in ore and gangue minerals is the only direct method of providing

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Section: Leaching Tests Of Inclusions In Mineralsmentioning

confidence: 88%

Short-chain carboxylates in high-temperature ore fluids of W-Sn deposits in south China.

2002

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“…Analytical reproducibility is better than ± 0.2‰ for δ 18 O, ± 2‰ for δD. δ 18 O H2O was calculated according to oxygen isotope compositions of the quartz using the equilibrium fractionation equation 1000lnα Quartz-H2O = 3.38 × 10 6 /T 2 -3.4 (Clayton et al, 1972) In-situ zircon Hf isotopic analysis was carried out on zircon grains from the Early Jurassic quartz diorite porphyry that were previously analyzed for U-Pb isotopes by Lang et al (2014a). Hf isotopes of those zircons were obtained using a Nu Plasma Multi-Collector MC-ICP-MS instrument, which is coupled to a 193 nm ArF Excimer laser-ablation system.…”

Section: Sampling and Analytical Methodsmentioning

confidence: 99%

Geology and Geochemistry Constraints on the Genesis of the NO.2 Porphyry Copper-Gold Deposit in the Xiongcun District, Gangdese Porphyry Copper Belt, Tibet, China

Yin¹

2017

Appl Ecol Env Res

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Abstract. The Xiongcun district is located in the western segment of the Gangdese porphyry copper belt (GPCB). The No.2 deposit in the Xiongcun district hosts a measured and indicated resource of 1.34 Mt copper, 76.34 t gold, and 193.78 t silver. The copper-gold mineralization of the No.2 deposit is mainly hosted in the Early Jurassic quartz diorite porphyry which intruded volcano-sedimentary rocks of the Early Jurassic Xiongcun Formation. S and Pb isotopic compositions of the ore sulfides and Re contents of molybdenite suggest a mantle source with minor contamination of subducted sediments for the ore-forming materials. Hydrogen and oxygen isotopic compositions of quartz from the quartz -sulfide veins suggest that the ore-forming fluid was a mixture of magmatic and meteoric water. Geochemical and Sr-Nd-Hf isotopic compositions of the Early Jurassic quartz diorite porphyry suggest that the mineralization of the No.2 deposit formed in an intra-oceanic island arc setting. The magmas of the Early Jurassic quartz diorite porphyry were likely sourced from partial melting of mantle with limited contamination by subducted sediments (ca. 5%). The formation of the porphyry and the No.2 deposit were related to the northward intra-oceanic subduction of the Neo-Tethys oceanic slab during the Early Jurassic.

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“…An estimate of the bulk isotopic composition of the ore-forming fluid may be gained from the isotopic data to help define the source of fluids and vein components and the evolution of the mineralising system. For O-and H-isotope data, if we assume that equilibrium was achieved between minerals and the precipitating fluid, the corresponding 8180 and 6D values of the fluid can be calculated using established mineral-water fractionation factors (O'Neil and Taylor, 1969;Clayton et al, 1972;Sakai and Tsutsumi, 1978). For a temperature of 300~ the 8180 composition of the fluid in equilibrium with the early generations of quartz is calculated to have ranged from 8.2-10.2%o.…”

Section: Stable Isotope Geochemistrymentioning

confidence: 99%

Nature and evolution of metamorphic fluids associated with turbidite-hosted gold deposits: Hill End goldfield, NSW, Australia

Seccombe¹

1993

Mineral. mag.

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The Hill goldfield, NSW, Australia, is an example of a syntectonic, slate-belt gold deposit formed in a multiply deformed, Late Silurian slate-metagreywacke turbidite sequence. Gold is confined to bedding-parallel veins and discordant leader veins composed of as many as four generations of quartz, accompanied by phyllosilicates, carbonates and minor sulphides. Vein formation and gold deposition was apparently synchronous with Early Carboniferous metamorphism and deformation. Homogenisation temperatures (Th) for fluid inclusions in vein quartz demonstrate five groupings in the temperature intervals 350-280 ~ 280-250 ~ 250-190 ~ 190-150 ~ and 150-110 ~ corresponding to a variety of primary and secondary inclusions developed during four periods of vein quartz deposition under a generally declining temperature regime. Inclusion fluids are characterised by a low salinity of around 0.1 to 3.6 wt. % NaC1 equivalent. The dominant gas phase present in the inclusion fluids varies from N2 in the early stages of the paragenesis, through CH 4 during the main episode of gold deposition, to CO2-rich fluids associated with late-stage mineralisation. ~a80 values for vein quartz (range 15.1-17.1%o) and vein carbonate (range 11.3-13.4%o) are typical of metamorphic mineralisation. 6D composition of hydrous minerals and inclusion fluids (range -53 to -138%o) suggest an influx of meteoric water in the later mineralising fluids. This conclusion is supported by 613C data for vein calcite (range -2.5 to -9.7%0). 634S composition of vein pyrrhotite and pyrite ranges from 6.9 to 7.8%0 early in the paragenesis, to lighter values (around 4.2 to 5.8%0) accompanying late gold deposition from more oxidising fluids. Sulphur isotope data imply a sulphur source from underlying turbidites and an increase in fluid oxidation state during mineralisation . Lead isotope measurements on vein pyrite, arseno py rite, galena and gold are characterised by two isotope populations with 2~176 ratios of 0.862 and 0.860, which define two discrete mineralising events during vein formation. Consistency between data from vein minerals and lead isotope signatures for potential source rocks indicate that lead was derived from the sedimentary pile.

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Oxygen isotope exchange between quartz and water

Cited by 1,311 publications

References 37 publications

Short-chain carboxylates in high-temperature ore fluids of W-Sn deposits in south China.

Short-chain carboxylates in high-temperature ore fluids of W-Sn deposits in south China.

Geology and Geochemistry Constraints on the Genesis of the NO.2 Porphyry Copper-Gold Deposit in the Xiongcun District, Gangdese Porphyry Copper Belt, Tibet, China

Nature and evolution of metamorphic fluids associated with turbidite-hosted gold deposits: Hill End goldfield, NSW, Australia

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