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“The Indonesian seaway is one of the critical zonal tropical seaways which largely influenced the global ocean circulation in the late Mesozoic, Paleogene and Neogene. The

opening and closing of various seaways due to the drifting of continents significantly influenced climatic systems during most of the Cenozoic (Kennett et al. 1985). The long-term Cenozoic cooling trend is thought to have been initially stimulated by changes in the atmospheric circulation pattern resulting from the uplift of the Tibetan Plateau (Ruddiman et al., 1989 and Raymo and Ruddiman, 1992, Cerling et al. 1997). The change in the ocean circulation pattern following the opening of a continuous seaway around Antarctica at ∼ 30 Ma was responsible HSP inhibitor for a fall in temperature in high latitudes (Toggweiler and Samuels, 1995 and Zachos et al., 2001). Significant changes in the circulation during the Pliocene as a result of several tectonic rearrangements in the tropics are believed to be the major causal mechanism for plunging the world into an ice age during the late Pliocene. The closure of the Indonesian seaway (Srinivasan and Sinha, 1998, Cane and Molnar, 2001 and Gourlan et al., 2008) and the Panama seaway (Stehli & Webb (eds.) Stehli and Webb, 1985, Burton

et al., 1997 and Bartoli et al., 2005) during the Pliocene affected the oceanic circulation, probably the deep thermohaline circulation. Deep sea records also provide ample evidence of changes in the thermohaline circulation (Burton Mitomycin C et al. 1997). Rai & Singh (2001) have already published some of the data on faunal diversity and abundance to discuss the broad palaeoceanographic changes in this region. In the present paper several other faunal parameters are added for a better understanding of the response of the benthic foraminiferal distribution to the Indonesian seaway closure. In the course of the northward drift of Australia and Tasmania away from Antarctica, the Indonesian seaway between the Pacific and the Indian Ocean narrowed. Earlier studies

suggested these that the palaeoceanographic changes in the Indian Ocean, equatorial Pacific, South China Sea and Caribbean Sea were linked to the closure of the Indonesian and central American seaways during the Miocene and Pliocene (e.g. Keller, 1985, Kennett et al., 1985, Haug and Tiedemann, 1998, Srinivasan and Sinha, 1998, Chaisson and Ravelo, 2000, Haug et al., 2001 and Jian et al., 2006). Through geological time, the position of the Indonesian seaway changed, as did the geometry of the inflow passages in relation to the tropical Pacific front, which significantly modified the climatic role of the tropical Indian and Pacific Oceans, resulting in reduced atmospheric heat transport from the tropics to high latitudes (Nishimura 1992).