Water from rock degassing

During the 2007 field experiments, C02 concentrations of the water samples under the reservoir pressure could not be correctly monitored due to the broken of the water sampler. This means that water samples were collected around 800m depth and a part of C02 must be degassed during ascending to the surface from the sampler. Therefore, C02 concentrations of the reservoir fluids are calculated on the basis of the observed pH and charge balance of each samples (Case 1) and the tracer concentration (Case 2). The Case 2 means that C02 in the injected water did not react with rocks. Fig.3 shows the calculated C02 concentration with iodine. Iodine concentration decreases from 1000 to 200pg/L with the elapsed time. From Fig.4, the fraction of the injected C02 water (1 wt.% C02) is almost zero. This means that... 

This was the first extinct radioactivity detected (Jeffrey and Reynolds 1961) and was made possible by the early high sensitivity of rare gas measurements and the low abrmdance of Xe in rocks. I has only one stable isotope at mass 127. Its abundance is measured as Xe after exposing a sample to an adequate neutron flux. The correlation between Xe and Xe observed in a stepwise degassing of a sample demonstrates that the excess Xe results from decay (Fig. 9h). Results in primitive meteorites and inclusions show that i29j/i2tj j.jose to 10 . Chronometry with I- Xe has been widely used in meteorite work (Reynolds 1963 Hohenberg 1967) but occasionally has some diflflculties to agree with the other chronometers due to the sensitivity of I to secondary processes and water alteration (Pravdivtseva et al. 2003 Busfleld et al. 2004 see also Swindle and Podosek (1988) for an extensive review). ... 

The oceans and the salts dissolved in them probably all formed early in the Earth s history. Although planetary degassing is occurring, as evidenced by studies of rare gases in rocks, the oceans, and the atmosphere, there is also a loss of water to the mantle via subduction. Supply from and loss to the mantle may be roughly equal at present. 

An alternative means of sulphur isotope fractionation in igneous rocks is by the degassing of SO2 from sub-aerial or shallow submarine lavas. This fractionation is controlled by the sulphate/sulphide ratio of the melt, which in turn is controlled by temperature, pressure, water content and oxygen activity. SO2 outgassed by basic lavas is enriched m relative to die melt because the dominant sulphur species in the melt is sulphide and SO2 is enriched in 5 S relative to sulphide (see Figure 7.26). The process is documented from Kilauea volcano, Hawaii, by Sakai el al (1982) and quantified by 2heng (1990). 

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