Variation in fumarolic H2 gas and volcanic activity at Nasudake in Japan

Kiyosu, Yasuhiro; Okamoto, Yasunori

doi:10.1016/s0377-0273(97)00039-5

Cited by 7 publications

(3 citation statements)

References 24 publications

Supporting

Mentioning

Contrasting

Order By: Relevance

“…Data from Yellowstone (14°C/hr model fit) are highlighted for discussion (see Section 4.5). Data sources by locality: Iceland (Arnason, 1977;Arnason and Sigurgeirsson, 1968), Japan (Kiyosu, 1983;Kiyosu and Okamoto, 1998;Mizutani, 1983;Tsunogai et al, 2011), Socorro Island (Taran et al, 2010), Kamchatka (Taran et al, 1992), Greece, shallow Aegean Sea (Botz et al, 1996), Yellowstone (Gunter and Musgrave, 1971;Welhan, 1981), New Zealand (Lyon and Hulston, 1984). Of New Zealand samples, measured T not reported for geothermal wells at Wairakei, nor Broadlands, isotopic values were therefore averaged and plotted against known reservoir temperatures, 255 and 290°C, respectively (Glover and Mroczek, 2009;Simmons et al, 2016).…”

Section: Continental Volcanic and Geothermal Systemsmentioning

confidence: 99%

Kinetics of D/H isotope fractionation between molecular hydrogen and water

Pester

Conrad

Knauss

et al. 2018

Geochimica et Cosmochimica Acta

View full text Add to dashboard Cite

At equilibrium, the D/H isotope fractionation factor between H 2 and H 2 O (a H2O-H2(eq)) is a sensitive indicator of temperature, and has been used as a geothermometer for natural springs and gas discharges. However, dD H2 measured in spring waters may underestimate subsurface temperatures of origin due to partial isotopic re-equilibration during ascent and cooling. We present new experimental data on the kinetics of D-H exchange for H 2 dissolved in liquid water at temperatures below 100°C. Comparing these results with published exchange rates obtained from gas phase experiments (100-400°C), we derive a consistent activation energy of 52 kJ/mol, and the following rate expressions; ln k ¼ 9:186 À 6298=T and k 1 ¼ 9764:61 ½H 2 O e À6298=T where T is absolute temperature (K), k is the universal rate constant ([L/mol]/hr), and k 1 is a pseudo-first-order constant (hr À1) applicable to water-dominated terrestrial systems by constraining [H 2 O] as the density of H 2 O (in mol/L) at the P-T of interest. The density-dependent rate constant accounts for the kinetic disparity of D-H exchange with H 2 when dissolved in liquid H 2 O relative to a gas/steam phase, exemplifed by 1/k 1 at 100°C of $2 days in liquid, versus $7 yrs in saturated steam. This difference may explain the high variability of dD H2 observed in fumarolic gases. Fluids convecting in the crust frequently reach T > 225°C, where isotopic equilibrium is rapidly attained (<1 hr). We compare fractionation factors measured in natural fluids (a OBS) with values expected for equilibrium at the T of acquisition. Where these values differ, we use kinetic models to estimate cooling rates during upward advection that account for the observed disequilibrium. Models fit to fluids from Yellowstone Park and the Lost City (deep-sea) vent field, both recovered at $90°C, require respective transit times of $7 hrs and $11 days between higher temperature reaction zones and the surface. Using estimates of subsurface depths of origin, however, suggests similar mean fluid flow rates (10 s of meters/hr). Additional complications must be considered when interpreting the dD H2 of lower-temperature effluent. When applied to data from deep-sea hydrothermal systems, our kinetic models indicate microbial catalysis accelerates D-H exchange once fluids cool below $60°C. The H 2 measured in both continental alkaline springs and fracture fluids from Precambrian shield rock is likely produced at T < 100°C, through processes such as serpentinization. In these settings, dD H2 values appear closer to equilibrium with H 2 O than those from geothermal systems. Considering kinetic isotope effects may yield H 2 that is out of equilibrium when generated at lower temperatures, we calculate maximum (isothermal) times to apparent isotopic equilibrium of 1.3 yrs at 50°C, 9 yrs at 25°C, and 35 yrs at 10°C. A similar calculation applied to Antarctic brines (À13°C), where measured dD H2 is far from equilibrium, yields $350 yrs. This time is shorter than the fluids have been isolated (2.8 ka), suggesting...

show abstract

Section: Continental Volcanic and Geothermal Systemsmentioning

confidence: 99%

Kinetics of D/H isotope fractionation between molecular hydrogen and water

Pester

Conrad

Knauss

et al. 2018

Geochimica et Cosmochimica Acta

View full text Add to dashboard Cite

show abstract

“…In particular, for the hydrogen isotope exchange reaction between H 2 O and H 2 in fumaroles at outlet temperatures greater than 400°C, the calculated isotope temperatures (assuming hydrogen isotope exchange equilibrium between H 2 O and H 2 ; see Section 3.3 for the details of the calculation) were close to the actual outlet temperatures (e.g. Bottinga, 1969;Mizutani, 1983;Kiyosu and Okamoto, 1998;Taran et al, 2010).…”

Section: Introductionmentioning

confidence: 59%

“…Symonds et al, 1994), typical variation range of dD values in fumarolic H 2 O are much narrower than that of fumarolic H 2 (e.g. Bottinga, 1969;Mizutani, 1983;Giggenbach, 1992;Taran et al, 1995Taran et al, , 2010Kiyosu and Okamoto, 1998;Goff and McMurtry, 2000). As a result, we can approximate the dD values of fumarolic H 2 O to be uniform irrespective of variations in the temperature of fumaroles.…”

Section: Application To Remote Temperature Sensing On Volcanic Fumaromentioning

confidence: 95%

Hydrogen isotopes in volcanic plumes: Tracers for remote temperature sensing of fumaroles

Tsunogai

Kamimura

Anzai

et al. 2011

Geochimica et Cosmochimica Acta

View full text Add to dashboard Cite

In high-temperature volcanic fumaroles (>400°C), the isotopic composition of molecular hydrogen (H 2 ) reaches equilibrium with that of the fumarolic H 2 O. In this study, we used this hydrogen isotope exchange equilibrium of fumarolic H 2 as a tracer for the remote temperature at volcanic fumaroles. In this remote sensing, we deduced the hydrogen isotopic composition (dD value) of fumarolic H 2 from those in the volcanic plume. To ascertain that we can estimate the dD value of fumarolic H 2 from those in a volcanic plume, we estimated the values in three fumaroles with outlet temperatures of 630°C (Tarumae), 203°C (Kuju), and 107°C (E-san). For this we measured the concentration and dD value of H 2 in each volcanic plume, along with those determined directly at each fumarole. The average and maximum mixing ratios of fumarolic H 2 within a plume's total H 2 were 97% and 99% (at Tarumae), 89% and 96% (at Kuju), and 97% and 99% (at E-san). We found a linear relationship between the depletion in the dD values of H 2 , with the reciprocal of H 2 concentration. Furthermore, the estimated end-member dD value for each H 2 -enriched component (À260 ± 30& vs. VSMOW in Tarumae, À509 ± 23& in Kuju, and À437 ± 14& in E-san) coincided well with those observed at each fumarole (À247.0 ± 0.6& in Tarumae, À527.7 ± 10.1& in Kuju, and À432.1 ± 2.5& in E-san). Moreover, the calculated isotopic temperatures at the fumaroles agreed to within 20°C with the observed outlet temperature at Tarumae and Kuju. We deduced that the dD value of the fumarolic H 2 was quenched within the volcanic plume. This enabled us to remotely estimate these in the fumarole, and thus the outlet temperature of fumaroles, at least for those having the outlet temperatures more than 400°C. By applying this methodology to the volcanic plume emitted from the Crater 1 of Mt. Naka-dake (the volcano Aso) where direct measurement on fumaroles was impractical, we estimated that the dD value of the fumarolic H 2 to be À172 ± 16& and the outlet temperature to be 868 ± 97°C. The remote temperature sensing using hydrogen isotopes developed in this study is widely applicable to many volcanic systems.

show abstract

The Geochemistry of Hot Springs

Erfurt¹

2021

The Geoheritage of Hot Springs

View full text Add to dashboard Cite

Variation in fumarolic H2 gas and volcanic activity at Nasudake in Japan

Cited by 7 publications

References 24 publications

Kinetics of D/H isotope fractionation between molecular hydrogen and water

Kinetics of D/H isotope fractionation between molecular hydrogen and water

Hydrogen isotopes in volcanic plumes: Tracers for remote temperature sensing of fumaroles

The Geochemistry of Hot Springs

Contact Info

Product

Resources

About