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Hydroclimate of the Western Indo-Pacific Warm Pool During the Past 24,000 Years

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Hydroclimate of the Western Indo-Pacific Warm Pool During the Past 24,000 Years Hydroclimate of the western Indo-Pacific Warm Pool during the past 24,000 years Eva M. Niedermeyera,b,1, Alex L. Sessionsa, Sarah J. Feakinsc, and Mahyar Mohtadid aDivision of Geological and Planetary Sciences, California Institute of Technology, Pasadena, CA 91125; bBiodiversity and Climate Research Centre (BiK-F) and Senckenberg Gesellschaft für Naturforschung, D-60325 Frankfurt, Germany; cDepartment of Earth Sciences, University of Southern California, Los Angeles, CA 90089; and dMARUM–Center for Marine Environmental Sciences, University of Bremen, D-28359 Bremen, Germany Edited by Thure E. Cerling, University of Utah, Salt Lake City, UT, and approved May 6, 2014 (received for review January 13, 2014) The Indo-Pacific Warm Pool (IPWP) is a key site for the global Ocean precipitation gradient. A recent proxy data-modeling hydrologic cycle, and modern observations indicate that both the approach combining a set of relative moisture reconstructions Indian Ocean Zonal Mode (IOZM) and the El Niño Southern Oscil- from East Africa and simulations from coupled climate models lation exert strong influence on its regional hydrologic character- suggests an IOZM-like relationship between eastern Indian istics. Detailed insight into the natural range of IPWP dynamics and Ocean cooling and positive rainfall anomalies in East Africa on underlying climate mechanisms is, however, limited by the spatial decadal timescales during the past millennium (4). Coral-based and temporal coverage of climate data. In particular, long-term reconstructions of sea surface temperature (SST) anomalies in (multimillennial) precipitation patterns of the western IPWP, a the eastern tropical Indian Ocean (off the coast of West Sumatra) key location for IOZM dynamics, are poorly understood. To help indicate distinct periods of IOZM variability throughout the rectify this, we have reconstructed rainfall changes over North- past 7,000 y (5, 6). However, despite the pronounced impact west Sumatra (western IPWP, Indian Ocean) throughout the past of the IOZM on present-day hydrology of Indian Ocean rim 24,000 y based on the stable hydrogen and carbon isotopic com- δ δ13 countries (e.g., refs. 7 and 8), the importance of the Indian Ocean positions ( D and C, respectively) of terrestrial plant waxes. As for past rainfall variability over the western IPWP has not yet a general feature of western IPWP hydrology, our data suggest been demonstrated. similar rainfall amounts during the Last Glacial Maximum and the To help fill this gap, we explored precipitation changes in NW Holocene, contradicting previous claims that precipitation in- Sumatra during the past 24,000 y recorded in a marine sediment creased across the IPWP in response to deglacial changes in sea core from the Nias basin (yellow star in Fig. 1; eastern Indian level and/or the position of the Intertropical Convergence Zone. We attribute this discrepancy to regional differences in topogra- Ocean). The study site is under the influence of modern sea phy and different responses to glacioeustatically forced changes surface anomalies associated with IOZM variability, making it in coastline position within the continental IPWP. During the Holo- an ideal location to study past variability of the Indian Ocean cene, our data indicate considerable variations in rainfall amount. precipitation gradient. Comparison of our isotope time series to paleoclimate records At present, the study site receives abundant rainfall carried by from the Indian Ocean realm reveals previously unrecognized fluc- tropical maritime trade winds throughout the year with no dry tuations of the Indian Ocean precipitation dipole during the Holo- season (9). Local rainfall amounts are largely independent of cene, indicating that oscillations of the IOZM mean state have the seasonal migration of the ITCZ as the site remains within been a constituent of western IPWP rainfall over the past ten the tropical rain belt year-round (for a detailed description of thousand years. moisture supply over the Maritime Continent, see SI Text and Figs. S1 and S2). Present-day rainfall anomalies are modulated plant wax δD | plant wax δ13C | Indonesia by SST anomalies relating to the IOZM (1). There appears to be he Maritime Continent (∼10°S–20°N and 90°E–130°E) is Significance Tsituated within the Indo-Pacific Warm Pool (IPWP). Here, intense atmospheric convection and rainfall provide a major The Indo-Pacific Warm Pool (IPWP) is the largest source of driving force for global atmospheric circulation. On a seasonal atmospheric water vapor, and region of highest rainfall, on basis, regional hydrology is governed by migration of the In- Earth. At irregular intervals, this high-rainfall regime weakens, tertropical Convergence Zone (ITCZ) and associated changes of causing severe droughts with massive consequences for the the monsoonal wind flow. In addition, IPWP hydrology under- local population. Research into the underlying mechanisms is goes strong and abrupt variations on an interannual scale that limited by the temporal coverage of climate data. We produced have been linked to the El Niño Southern Oscillation (ENSO), a record of rainfall over the western IPWP covering the past and more recently to the coupled atmosphere-ocean system over 24,000 years. Our data indicate that topography and coastline the Indian Ocean (Indian Ocean Zonal Mode, IOZM) (1, 2). position govern regional IPWP hydrology on glacial−intergla- Whereas ENSO has a significant impact on rainfall patterns cial timescales. During the Holocene, western IPWP rainfall is across the eastern and southern areas of the Maritime Continent, linked to that of East Africa through a precipitation dipole. there appears to be no direct impact of ENSO on rainfall pat- Fluctuations of this dipole identified in our study serve as an terns of Northwest (NW) Sumatra (3). Instead, fluctuations impetus for future studies to advance our understanding of of the IOZM may exert substantial control on NW Sumatran IPWP dynamics. rainfall variability (1). At present, annual mean rainfall received > Author contributions: E.M.N., A.L.S., and M.M. designed research; E.M.N. performed re- in the western IPWP ( 3,000 mm) is higher than that in equato- search; A.L.S., S.J.F., and M.M. contributed new reagents/analytic tools; E.M.N. analyzed rial East Africa (about 500–700 mm; www.worldclim.org/), data; E.M.N. wrote the paper. resulting in a precipitation dipole across the Indian Ocean. The authors declare no conflict of interest. During years of so-called IOZM events, anomalous cooling This article is a PNAS Direct Submission. (warming) off Sumatra (East Africa) corresponds to negative 1To whom correspondence should be addressed. E-mail: [email protected]. (positive) rainfall anomalies along western Sumatra (East This article contains supporting information online at www.pnas.org/lookup/suppl/doi:10. Africa), resulting in a weakening or even reversal of the Indian 1073/pnas.1323585111/-/DCSupplemental. 9402–9406 | PNAS | July 1, 2014 | vol. 111 | no. 26 www.pnas.org/cgi/doi/10.1073/pnas.1323585111 Downloaded by guest on September 23, 2021 no direct influence of ENSO on precipitation in NW Sumatra amounts in NW Sumatra were of about the same order of (3); however, an indirect impact of ENSO is observed during magnitude or slightly elevated during the LGM compared with periods of ENSO and IOZM event interactions (10). the Holocene, depending on the true impact of temperature We measured the stable hydrogen (δD) and stable carbon change on the δD values of our record. This observation is in (δ13C) isotopic composition of terrestrial plant waxes, specifically agreement with reconstructions of seawater δ18OoffWest n n the -C30 and -C32 alkanoic acids, to deduce changes of hy- Sumatra (19) displaying similar values during the LGM and the drology and vegetation on land. We infer that higher plant waxes Holocene, and is further supported by palynological evidence deposited at the study site predominantly derive from the adja- from central West Sumatra indicating cooler but not drier con- cent hinterland of NW Sumatra, as the mineralogy and radio- ditions during the LGM (summarized in ref. 23). genic composition of clay minerals deposited offshore from the The lack of drying in West Sumatra during the LGM contrasts North Sumatran Shelf indicate rocks of North and central with evidence for concurrent drying across the central IPWP. Sumatra as the dominant source of terrestrial material (11, 12) Reconstructions of glacial−interglacial changes in terrestrial pre- SI Text δ 18 ( ). Plant wax D values have been shown to correlate with cipitation based on speleothem calcite δ O records from Borneo those of precipitation (13), which, in the tropics, relate to the (24) and Flores (25), and a plant wax δD record from Sulawesi SI Text amount of rainfall (14) ( ). (26), indicate drier than present conditions during the LGM Since there is debate about whether photosynthetic pathway [Borneo (24)] followed by an increase of precipitation during de- δ and plant morphology has an influence on the D value of plant glaciation [Flores, Sulawesi (25, 26)] (Fig. 2 E−G). waxes (13), we also measured their δ13C values during periods of δ We suggest that these distinctive differences between the pronounced changes in plant wax D. eastern and western Maritime Continent result from exposure of Results the Sunda Shelf during the LGM and resulting changes in re- δ n A gional ocean and atmosphere circulation. During the LGM, when The Dvaluesofthe -C30 alkanoic acids (Fig. 2 )range the Sunda Shelf was exposed (27), the study sites of Borneo, from −148‰ to −175‰. We identify two periods of D depletion Flores, and Sulawesi were connected to a more continental around 14 ka and 11.5 ka during the last glacial period as well as geography, whereas NW Sumatra experienced only a minor two pronounced periods of D depletion during the Holocene change in coastline position (Fig. 1A). According to Griffiths from about 8 ka to 6.5 ka and from 2 ka to 1 ka, and an interval et al.
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