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• W1845141885 abstract "Helium mobility in geologic materials is a fundamental constraint onthe petrogenetic origins of helium isotopic variability and on the applicationof radiogenic and cosmogenic helium geochronology.3He and 4He volume diffusivities determined at 25-600°C in basalticglasses by incremental-heating and powder storage experiments (using adiffusion model incorporating grain size and shape information to obtainhigh precision) are three to four orders of magnitude greater than forcommon cations. Diffusion in tholeiitic glass can be described by anArrhenius relation with activation energy = 16.85±.13 Kcal/mole and log Do= -2.37±.06, although low temperature data are better described by a distribution of activation energies model . The best estimate for D at 0°C intholeiitic glass is 5±2 x 10-16 cm2/s, an order of magnitude higher thanthe results of Kurz and Jenkins (1981) but lower than suggested by Jambon,Weber and Begemann (1985). Measurements in an alkali basalt show thathelium diffusion is composition dependent (Ea = 14.4±.5 Kcal/mole; log Do = 3.24±.2), and roughly five times faster than in tholeiites at seafloortemperatures. The corresponding timescales for 50% helium loss or exchangewith seawater (1 cm spheres) are about one million years for mid-ocean-ridge-basalts, and about 100,000 years in seamount alkali basalts. Radiogenic4He diffusion has a higher activation energy (27±2 Kcal/mole; log Do = +2.4±1.0) than inherited (magmatic) helium, suggesting very low mobility (D= 3xl0-19 cm2/s at 0°C; factor of 5 uncertainty) and that U+Th/4He geochronologyof fresh seafloor basalt glasses is unlikely to be hampered byhelium loss.Measured isotopic diffusivity ratios, D3He/D4He, are not compositiondependent, average 1.08±.02, and vary slightly with temperature, consistentwith an activation energy difference of 60±20 cal/mole. This result differsfrom the inverse-square-root of mass prediction of 1.15, and may beexplained by quantization of helium vibrational energies. These resultssuggest preferential loss of 3He will be minimal at low temperature(D3He/D4He = 1.02± .03 at 0°C). Therefore, alteration of magmatic 3He/4Heratios in basaltic glasses on the seafloor will occur only by heliumexchange with seawater, and be important only for samples with low heliumcontents (<10-8 ccSTP/g), such as those found in island arc environments.Extrapolating the glass results to magmatic temperatures yields diffusivitiessimilar to melt values, and suggests D3He/D4He approaches 1.15 atthese and higher temperatures.Helium diffusivities in olivine and pyroxene at magmatic and mantletemperatures (900-1400°C) are higher than for cations, (E = 100±5 Kcal/mole, log Do = +5.1±.7; and 70±10 Kcal/mole, log Do = +2.1±1.2, respectively),but are still too low to transport or homogenize helium in the mantleor even in magma chambers. However, diffusion equilibrates melts and mantleminerals within decades, and interaction with wall-rocks may be enhancedfor helium in comparison…" @default.
• W1845141885 created "2016-06-24" @default.
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• W1845141885 date "1989-01-01" @default.
• W1845141885 modified "2023-09-27" @default.
• W1845141885 title "Diffusion of helium isotopes in silicate glasses and minerals : implications for petrogenesis and geochronology" @default.
• W1845141885 doi "https://doi.org/10.1575/1912/5399" @default.
• W1845141885 hasPublicationYear "1989" @default.
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