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Copyright © 2013 by The Geochemical Society of Japan. et al., 2002, 2006). The hotspots produce oceanic island basalts (OIBs) with an enriched mantle signature (e.g., Hart, 1984), spanning a wider range of radiogenic isotope compositions than basalts in other regions (e.g., Vidal et al., 1984). Seismological studies have commonly shown large areas of pronounced low seismic velocity in the lower mantle beneath the South Pacific Ocean and the African continent (e.g., Lay, 2007). All these observations suggest the presence of mantle upwelling beneath the South Pacific region. Morgan (1971) proposed that hotspot volcanism is generated by mantle plumes, involving the rapid ascent of unusually hot and buoyant mantle materials from deep thermal boundary layers in the lower mantle. In the present study, the boundary between the upper and lower mantle is assumed to be at a depth of 660 km, with the mantle delineated by the Moho discontinuity and the core mantle boundary (CMB). The mantle transition zone (MTZ) comprises the lower third of the upper mantle (410–660 km depth). Several models, modified from the classicalplume model, have been proposed to explain the South Pacific and African hotspots (e.g., Davaille, 1999; Torsvik et al., 2006; Suetsugu et al., 2009); such models are commonly based on the notion that the South Pacific hotspots Origin of hotspots in the South Pacific: Recent advances in seismological and geochemical models