Basalts noble gases

Zhang Y. and Stolper E.M. (1991) Water diffusion in basaltic melts. Nature 351, 306-309. Zhang Y. and Xu Z. (1995) Atomic radii of noble gas elements in condensed phases. Am. Mineral. 80, 670-675. 

Hiyagon and Ozima (1986) employed a laboratory approach of measuring crystal-melt partition coefficients. They measured noble gas concentration in olivine crystals and basalt melts, which were synthesized at 1370-1300°C under an atmospheric pressure, and also at 1360-1050°C under high pressure (0.2-1.5 GPa), of noble gas mixture. From these experimental results, they obtained ranges for noble gas partition coefficients XHe = 0.07, XNe = 0.006-0.08, KM = 0.05-0.15, KXe = 0.3. These partition coefficients are much larger than the values obtained by Marty and Lussiez (1993) and also these of common incompatible elements such as U (-0.002) or K (0.0002 - 0.008) between olivine and basalt melt (e.g. Henderson, 1982). 

Mechanical shock applied in ambient noble gas atmospere also emplaces substantial amount of noble gases into target material. Wiens and Pepin (1988) studied the effects of mechanical shock (20-60 GPa) applied to rock specimens (basalt disk and powder 63-125 pm in size) in ambient air. They found that emplacement efficiencies (number densities in shocked samples/number densities in ambient gases)... 

There is now a large amount of noble gas diffusion data obtained for rocks or minerals. However, very few studies have been done on noble gas diffusion in silicate melts. The latter bears a central importance in understanding the noble gas evolution in the mantle. Figure 2.11 shows one such scarce example (Lux, 1987), where the diffusion coefficients obtained for a tholeiite basalt melt at 1350°C are plotted as a function of noble gas radius. Diffusion obeys more or less the same linear relationship with r as does the solubility. As Lux (1987) noted, it is remarkable that the... 

The first identification of cosmogenic noble gas in crustal rocks was reported by Kurz (1986). Kurz measured a series of basaltic-drilled core samples from Mauna Loa volcanoes in the Hawaiian Islands. The lava flow (14C age 20,000 a) has retained its surface flow structure and, therefore, was concluded to have experienced little surface erosion. Because the 3He concentration in the surface of the lava flow (10 I2-I0 cm3STPg ) gave reasonable agreement with a theoretical production... 

Dymond, X, Hogan, L. (1973) Noble gas abundance patterns in deep-sea basalts - primordial gases from the mantle. Earth Planet. Sci. Lett., 20, 131-9. 

Fisher, D. E. (1985a) Noble gas data from oceanic island basalts do not require an undepleted mantle source. Nature, 316, 716-18. 

Honda, M., McDougall, I., Patterson, D. B., Doulgeris, A., Clague, D. A. (1991a) Possible solar noble gas component in Hawaiian basalts. Nature, 349, 149-51. 

Marty, B., Ozima, M. (1986) Noble gas distribution in oceanic basalt glasses. Geochim. Cosmochim. Acta, 50, 1093-7. 

Shibata, T., Takahashi, E., Ozima, M. (1994) Noble gas partition between basaltic melt and olivine crystals at high pressure. In Noble Gas Geochemistry and Cosmochemistry, J. Matsuda, Ed., pp. 343-54. Tokyo Terra Scientific Publishing Co. 

A number of noble gas studies have focused on xenoliths from the Pliocene to Recent alkali basalts of the Newer Volcanics in SE Australia... 

Graham D. W. (2002) Noble gas isotope geochemistry of midocean ridge and ocean island basalts characterization of mantle source reservoirs. Rev. Mineral. Geochem. 47, 247-317. 

Hiyagon H. and Ozima M. (1982) Noble gas distribution between basalt melt and crystals. Earth Planet. Sci. Lett. 58, 255-264. 

Kaneoka I., Takaoka N., and Upton B. G. J. (1986) Noble gas systematics in basalts and a dunite nodule from Reunion and Grand Comore Islands, Indian Ocean. Chem. Geol. 59, 35-42. 

There are various terrestrial reservoirs that have distinct volatile characteristics. Data from midocean ridge basalts (MORBs) characterize the underlying convecting upper mantle, and are described here without any assumptions about the depth of this reservoir. Other mantle reservoirs are sampled by ocean island basalts (OIBs) and may represent a significant fraction of the mantle (Chapter 2.06). Note that significant krypton isotopic variations due to radiogenic additions are neither expected nor observed, and there are no isotopic fractionation observed between any terrestrial noble gas reservoirs. Therefore, no constraints on mantle degassing can be obtained from krypton, and so krypton is not discussed further. Comparison between terrestrial and solar system krypton is discussed in Chapter 4.12. 

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