9:45 AM - 10:00 AM
[SMP36-10] Magnesian andesites from the Kibblewhite volcano, Kermadec arc
Keywords:Petrology, Kermadec arc, Kibblewhite volcano
Samples were collected from this volcano by dredging during the RV SONNE Vitiaz (SO255) cruise in March-April 2017. The recovered lavas range from basalt to rhyolite (SiO2 = 49.9-70.9 wt.%; Mg# = 78.2-28.8) and belong to the Low-K to Medium-K series of Gill (1981), consistent with previous observations (Wright et al., 2006). Here, we focus on magnesian andesites (SiO2 = 57.4-58.8 wt.%; MgO = 5.3-5.7 wt.%; Mg# = 56-58) collected from DR25 at the NE base of the Kibblewhite volcano.
The magnesian andesites are aphyric with skeletal olivine and cpx microphenocrysts and sometimes contain olivine phenocrysts. Olivine microphenocrysts in the magnesian andesites have restricted compositions (Fo = 84-85; NiO = 0.13-0.17), which are in equilibrium with host rocks. Olivine phenocrysts in magnesian andesites extend to more forsteritic compositions (Fo = 86-93) and have higher NiO contents (0.19-0.35 wt.%) that can be in equilibrium with residual arc mantle (Fo = ~93; Ishii et al., 1992). The forsteritic olivine phenocrysts have thin rims (Fo = 85) that are in equilibrium with host rocks without reaction rim, which suggests that the olivines are antecrysts, which have grown within the same magmatic system but in a more primitive magma, rather than xenocrysts. The Sr, Nd and Pb isotopic compositions of magnesian andesites (87Sr/86Sr = 0.70356-0.70368; 143Nd/144Nd = 0.51296-0.51297; 206Pb/204Pb = 18.84-18.85; n = 2) are consistent with the range of published data for the Kibblewhite volcano (Timm et al., 2014).
Fractionation of 15% olivine with the same amount of cpx from the primary melts explains the continuous Fo-NiO trends formed by the olivine microphenocrysts and antecrysts. Estimated primary melt of the magnesian andesite is also andesitic (SiO2 = 54.8 wt.%) with 12.7 wt.% MgO, and its normative composition is similar to that of melts generated in melting experiment of hydrous lherzolite at 1 GPa (Hirose and Kawamoto, 1995). This suggests that the primary melt of magnesian andesite is generated by melting of hydrous mantle at <=1 GPa pressure.
Gill, J. B. (1981). Orogenic Andesites and Plate Tectonics. Minerals, Rocks and Mountains (Vol. 16). Springer-Verlag.
Hirose, K., & Kawamoto, T. (1995). Hydrous partial melting of lherzolite at 1 GPa: The effect of H2O on the genesis of basaltic magmas. Earth and Planetary Science Letters, 133(3–4), 463–473.
Ishii, T., Robinson, P. T., Maekawa, H., & Fiske, R. (1992). Petrological studies of peridotites from diapiric serpentinite seamounts in the Izu-Ogasawara-Mariana Forearc, Leg 125. In Proceedings of the Ocean Drilling Program, Scientific Results (Vol. 125, pp. 445–485).
Timm, C., Davy, B., Haase, K., Hoernle, K. A., Graham, I. J., de Ronde, C. E. J., Woodhead, J., Bassett, D., Hauff, F., Mortimer, N., Seebeck, H. C., Wysoczanski, R. J., Caratori-Tontini, F., & Gamble, J. A. (2014). Subduction of the oceanic Hikurangi Plateau and its impact on the Kermadec arc. Nature Communications, 5, 4923.
Wright, I. C., Worthington, T. J., & Gamble, J. A. (2006). New multibeam mapping and geochemistry of the 30°-35° S sector, and overview, of southern Kermadec arc volcanism. Journal of Volcanology and Geothermal Research, 149(3–4), 263–296.