Hot spring waters

Fig. 2.13. (A) Temperature dependence of pH in Japanese thermal waters. Lines indicate the temperature dependence of pH when pH is buffered by the K-feldspar-K-mica-quartz (or chalcedony at less than 200°C) assemblage at a Na + K concentration of 0.1 and 0.01 mol/kg H2O. Symbols are as in Fig. 2.11. (B) Temperature dependence of pH of Icelandic thermal waters. Large circles indicate well discharges. Small dots represent hot spring waters (Chiba, 1991).

Chemical analytical data on the hot spring waters are given in Table 2.5 (Aoki and Thompson, 1990). Gold is precipitating from H2S-rich, diluted chloride and neutral hot springs (Aoki, 1992b). 

Chemical composition of some typical hot spring waters at Osorezan (concentration in ppm Aoki, 1992b)... 

The Arima hot spring waters are classified into three types (1) Na-Ca-Cl type brine which is high in salinity and CO2 and medium to low in temperature (2) highly saline Na-Ca-Cl-type water of high temperature and low CO2 concentration and (3) dilute and C02-rich water of low temperature (Table 2.8). 

The total amount of discharged hot spring water is 50,000 ton/day, indicating a huge geothermal system (Taguchi et al., 1988). 

The hot spring waters are divided into sulfate-rich steam heated water, chloride-rich deep-water, bicarbonate-dominated water and their intermediate types. 

Fournier, R.O. and Truesdell, A.H. (1970) Chemical indicators of subsurface temperatures applied to hot spring waters of Yellowstone National Park, Wyoming, U.S.A. Geothermics, 2, 529-535. 

Koga, A. (1961) Gold distribution in the hot springs water in Beppu. J. Chem. Soc. Japan, 82, 1476-1478 (in Japanese). 

Fig. 23.6. Calculated saturation indices (log Q/K) of aluminum-bearing minerals plotted versus temperature for a hot spring water from Gjogur, Hveravik, Iceland. Lines for most of the minerals are not labeled, due to space limitations. Sampling temperature is 72 °C and predicted equilibrium temperature (arrow) is about 80 °C. Clinoptilolite (zeolite) minerals are the most supersaturated minerals below this temperature and saponite (smectite clay) minerals are the most supersaturated above it.

Fig. 23.7. Calculated saturation indices (log Q/K) of silica minerals for Gjogur hot spring water. Chalcedony is approximately in equilibrium at 80 °C, but quartz is supersaturated at this temperature.

Combinations of mineral reactions at lower temperatures and mixing with more dilute fluids are likely to result in the variations in concentration and isotopic composition in many of the continental thermal spring waters but not seen in their marine relatives. The extreme manifestation of this difference may have been generated in the dilute hot spring waters from around Lake Baikal, whose heavy isotopic compositions required extensive re-equilibration at temperatures 100-150°C (Falkner et al. 1997). 

A long-standing geochemical problem is the source of water in volcanic eruptions and geothermal systems how much is derived from the magma itself and how much is recycled meteoric water One of the principal and unequivocal conclusions drawn from stable isotope studies of fluids in volcanic hydrothermal systems is that most hot spring waters are meteoric waters derived from local precipitation (Craig et al. 1956 Clayton et al. 1968 Clayton and Steiner 1975 Truesdell and Hulston 1980, and others). 

Most hot spring waters have deuterium contents similar to those of local precipitation, but are usually emiched in as a result of isotopic exchange with the country rock at elevated temperatures. The magnitude of the oxygen isotope shift depends on the O-isotope composition of both water and rock, the mineralogy of the rock, temperature, water/rock ratio, and the time of interaction. 

Seawater, hot-spring water, coal, coal fly ash, slag... 

Kubota, Y., Yokota, D. and Ishiyama, Y. (2001) Arsenic concentration in hot spring waters from the Niigata plain and Shinji lowland, Japan source supply of arsenic in arsenic contaminated ground water problem Part 2. Earth Science, 55(1), 11-22. 

The material from the Hector area of California is believed to have formed by the action of hot spring waters containing Li and F on clinoptiolite. The Mg was obtained from the alkaline lake waters (Ames and Goldich, 1958). The material from Morocco is associated with marls and is believed to be authigenic. These two types of trioctahedral smectite appear to be the only ones with a relatively pure Si tetrahedral sheet. No analyses were found which indicated tetrahedral Al values between 0.02 and 0.30. Analyses of saponite indicate there is complete isomorphous substitution between the range Si3.70 Al0.3o and Si3.0s Al0.92 (Table XXXIX). Caillere and Henin (1951) reported an analysis of a fibrous expanded clay (diabantite) which had a tetrahedral composition of Si3.i7 Alo.49 Fe3+0.34. There is some question as to whether this should be classified as a smectite regardless, it indicates the possibility of Fe3+ substitution in the tetrahedral sheets of the trioctahedral 2 1 clays. 

Keller et al. (1971) reported on the occurrence of halloysite formed by the action of hot spring waters on rhyolitic volcanic rock in Michoacan, Mexico and suggested that high concentrations of Si and Al in solution, low pH (about 3.5) and sulfate as the solvent anion allows the formation of halloysite rather than other kaolinite minerals. 

Toshio [23] determined copper in hot spring waters by cation exchange chromatography in ammoniacal pyrophosphate solution. A procedure may be included to overcome iron interference. 

Fig. 8. Spontaneous fission activity in hot spring water at the Cheleken peninsula after concentration by ion exchange and precipitation methods. Shown is the measured neutron multiplicity distribution (dots) compared with measured distributions for 238U, 246Cm and 252Cf spontaneous fission and calculated distributions for sets of v and a2, the average number of neutrons per fission and its variance. Reproduced from G.N. Flerov et al. [48], Fig. 1, copyright (2002), with permission from Springer-Verlag.

There are more kinds of insects on earth than all other living animals combined. They are fonnd in soil, hot springs, water, snow, air, and inside plants and animals. They eat the choicest foods from our table. They can even eat the table. 

Morey et al. (1964) collected samples of silica-rich hot spring waters from Yellowstone National Park and stored them in the laboratory at about 25°C. Silica concentrations in their samples stored for 2 years showed a strong pH dependence, from about 250 ppm as Si02(aq) at pH 1.5, to 150 ppm at pH 3, and 115 ppm at pH 6. Silica levels in the pH 3 sample had dropped from about 450 to 150 ppm in 2 years. 

River water Water Water Water Radioactive waste streams Water Sea water Sea water Dead Sea brine ASP Sea water and hot springs water... 

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