The Li isotopic composition of Oldoinyo Lengai: Nature of the mantle sources and lack of isotopic fractionation during carbonatite petrogenesis

Details The Li isotopic composition of Oldoinyo Lengai: Nature of the mantle sources and lack of isotopic fractionation during carbonatite petrogenesis The Li isotopic composition of Oldoinyo Lengai: Nature of the mantle sources and lack of isotopic fractionation during carbonatite petrogenesis

Feb 2007

adsabs.harvard.edu/cgi-bin/nph-data_query?bibcode=2007e%26psl.254...77h&link_type=abstract

Earth and Planetary Science Letters, Volume 254, Issue 1-2, p. 77-89.

Computer Science

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Scientific paper

Lithium concentrations and Li isotope compositions are reported for natrocarbonatites and silicate lavas from Oldoinyo Lengai, Tanzania. Natrocarbonatites are characterized by very high Li contents (211 294 ppm) and a narrow range of δ7Li values between + 3.3 and + 5.1. These Li isotope compositions overlap with those reported for MORB and OIB and suggest that the natrocarbonatites reflect the Li isotopic composition of their mantle source. Co-genetic silicate lavas, covering a wide compositional spectrum, show no obvious isotopic fractionation as a function of igneous differentiation or liquid immiscibility. Primitive olivine melilitites (Mg# = 58 70), considered to be parental magmas, contain 14 23 ppm Li and have δ7Li values of + 2.4 to + 4.4. A highly differentiated, peralkaline nephelinite (Mg# = 12), likely to be related to the natrocarbonatites by liquid immiscibility, has about twice as much Li as the melilitite (57 ppm), but a similar isotopic composition (δ7Li = + 3). In contrast, a phonolite with 15 ppm Li has a lighter Li isotope composition (δ7Li = - 0.4), which may reflect assimilation of isotopically light lower crustal mafic granulites, a conclusion supported by radiogenic isotope data. Clinopyroxene and olivine separates from the silicate lavas have uniformly lower Li concentrations (3 15 ppm) and lower δ7Li values (δ7Li = - 2.9 to - 0.5) than the respective whole-rocks, with Δ7Liwhole-rock-mineral between 1.4 and 6.3. This difference between whole-rock and mineral data is interpreted to reflect diffusion-driven isotopic fractionation.

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