A 25 m.y. isotopic record of paleodiet and environmental change from fossil mammals and paleosols from the NE margin of the Tibetan Plateau

Details A 25 m.y. isotopic record of paleodiet and environmental change from fossil mammals and paleosols from the NE margin of the Tibetan Plateau A 25 m.y. isotopic record of paleodiet and environmental change from fossil mammals and paleosols from the NE margin of the Tibetan Plateau

Jul 2005

adsabs.harvard.edu/cgi-bin/nph-data_query?bibcode=2005e%26psl.236..322w&link_type=abstract

Earth and Planetary Science Letters, Volume 236, Issue 1-2, p. 322-338.

Computer Science

9

Scientific paper

We use the carbon and oxygen isotopic compositions of fossil tooth enamel and paleosols to reconstruct the late Cenozoic history of vegetation and environmental change in the Linxia Basin at the northeastern margin of the Tibetan Plateau. The δ13C values of fossil enamel from a diverse group of herbivores and of paleosol carbonate and organic matter indicate that C4 grasses were either absent or insignificant in the Linxia Basin prior to ˜2 3 Ma and only became a significant component of local ecosystems in the Quaternary. This is in striking contrast to what was observed in Pakistan, Nepal, Africa and the Americas where C4 plants expanded rapidly in the late Miocene as indicated by a positive δ13C shift in mammalian tooth enamel and paleosols. The δ18O results from the same herbivore species show several significant shifts in climate in the late Cenozoic. Most notably, a positive δ18O shift after ˜7 Ma indicates a shift to warmer and/or drier conditions and is comparable in timing and direction to the δ18O shift observed in paleosol carbonates in Pakistan and Nepal. This late Miocene climate change observed in the Indian sub-continent and in the Linxia Basin, however, seems to be a regional manifestation of a global climate change. The lack of evidence for C4 plants in the Linxia Basin prior to ˜2 3 Ma suggests that the East Asian summer monsoon, which brings precipitation into northern China during the summer and creates optimal conditions for the growth of C4 grasses, was probably not strong enough to affect this part of China throughout much of the Neogene. This implies that the Himalayan-Tibetan Plateau may not have reached the present-day elevation across its vast extent to support a strong East Asian monsoon system before ˜2 3 Ma. Our data also suggest that regional climatic conditions played an important role in controlling the expansion of C4 plants.

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