The Asian-Australian monsoon is an important component of the Earth's climate system that influences the societal and economic activity of roughly half the world's population. The past strength of the rain-bearing East Asian summer monsoon can be reconstructed with archives such as cave deposits 1, 2, 3 , but the winter monsoon has no such signature in the hydrological cycle and has thus proved difficult to reconstruct. Here we present high-resolution records of the magnetic properties and the titanium content of the sediments of Lake Huguang Maar in coastal southeast China over the past 16,000 years, which we use as proxies for the strength of the winter monsoon winds. We find evidence for stronger winter monsoon winds before the Bølling-Allerød warming, during the Younger Dryas episode and during the middle and late Holocene, when cave stalagmites suggest weaker summer monsoons 1, 2, 3 . We conclude that this anticorrelation is best explained by migrations in the intertropical convergence zone. Similar migrations of the intertropical convergence zone have been observed in Central America for the period ad 700 to 900 (refs 4-6), suggesting global climatic changes at that time. From the coincidence in timing, we suggest that these migrations in the tropical rain belt could have contributed to the declines of both the Tang dynasty in China and the Classic Maya in Central America.
Oxygen-isotope records from Greenland ice cores 1,2 indicate numerous rapid climate¯uctuations during the last glacial period. North Atlantic marine sediment cores show comparable variability in sea surface temperature and the deposition of icerafted debris 3±5 . In contrast, very few continental records of this time period provide the temporal resolution and environmental sensitivity necessary to reveal the extent and effects of these environmental¯uctuations on the continents. Here we present high-resolution geochemical, physical and pollen data from lake sediments in Italy and from a Mediterranean sediment core, linked by a common tephrochronology. Our lacustrine sequence extends to the past 102,000 years. Many of its features correlate well with the Greenland ice-core records, demonstrating that the closely coupled ocean±atmosphere system of the Northern Hemisphere during the last glacial 4 extended its in¯uence at least as far as the central Mediterranean region. Numerous vegetation changes were rapid, frequently occurring in less than 200 years, showing that the terrestrial biosphere participated fully in lastglacial climate variability. Earlier than 65,000 years ago, our record shows more climate¯uctuations than are apparent in the Greenland ice cores. Together, the multi-proxy data from the continental and marine records reveal differences in the seasonal character of climate during successive interstadials, and provide a step towards determining the underlying mechanisms of the centennial±millennial-scale variability.A series of four sediment cores (B, D, J and L) obtained from Lago Grande di Monticchio (408 569 N, 158 359 E, 656 m above sea level), a maar lake in Basilicata, southern Italy, extends to a depth of 72.5 m. Sedimentation rates, estimated from annually laminated sections of a composite of these cores, provide a chronology 6,7 that gives a date of 101.7 kyr ago for the base of the record (Fig. 1). This calendaryear chronology, based solely upon Monticchio sedimentation rates, is independent of palynostratigraphic (that is, pollen-based), marine d 18 O event or ice-core interstadial correlations. It is complemented by a tephrochronology and a series of radioisotopic ages.
Establishing phase relationships between earth-system components during periods of rapid global change is vital to understanding the underlying processes. It requires records of each component with independent and accurate chronologies. Until now, no continental record extending from the present to the penultimate glacial had such a chronology to our knowledge. Here, we present such a record from the annually laminated sediments of Lago Grande di Monticchio, southern Italy. Using this record we determine the duration (17.70 ؎ 0.20 ka) and age of onset (127.20 ؎ 1.60 ka B.P.) of the last interglacial, as reflected by terrestrial ecosystems. This record also reveals that the transitions at the beginning and end of the interglacial spanned only Ϸ100 and 150 years, respectively. Comparison with records of other earthsystem components reveals complex leads and lags. During the penultimate deglaciation phase relationships are similar to those during the most recent deglaciation, peaks in Antarctic warming and atmospheric methane both leading Northern Hemisphere terrestrial warming. It is notable, however, that there is no evidence at Monticchio of a Younger Dryas-like oscillation during the penultimate deglaciation. Warming into the first major interstadial event after the last interglacial is characterized by markedly different phase relationships to those of the deglaciations, warming at Monticchio coinciding with Antarctic warming and leading the atmospheric methane increase. Diachroneity is seen at the end of the interglacial; several global proxies indicate progressive cooling after Ϸ115 ka B.P., whereas the main terrestrial response in the Mediterranean region is abrupt and occurs at 109.50 ؎ 1.40 ka B.P.Eemian ͉ phase relationships ͉ pollen ͉ varves R econstructing the phase relationships between major earthsystem components relies on precise, accurate, and independent chronologies. However, absolute dating of geological records beyond the range of radiocarbon (more than Ϸ50 ka B.P.) is problematic, and age estimates for records of the last interglacial (LI) commonly rely on indirect dating approaches (1-4), often either by tuning to the time scale of orbital variations (2) or ''wiggle-matching'' to another record and applying its chronology (3, 4). Until now no continuous continental record extending from the present through the LI to the penultimate glacial had its own internal chronology to our knowledge. Thus timing and duration of the LI, as reflected in continental, marine, and ice-core records, and the phase relationships between these major earth-system components during marine oxygen isotope stage (MIS) 6-4, have been the subject of much debate (1, 5-9). Shackleton (9) first proposed correspondence between the LI and MIS 5e, whereas Woillard (10) subsequently demonstrated such apparent correspondence in a continental record. More recently, however, pollen, alkenone, and ␦ 18 O analyses of marine cores from locations close to the Iberian peninsula have shown asynchrony between changes in terrestrial veg...
The East Asian summer monsoon (EASM) plays a major role in the global climate 63 system (Wang, 2009). In mid-latitude and southern Asia, ecosystems, rain-fed agriculture and 64 economic prosperity critically depend on the amount and distribution of monsoonal 65 precipitation (Yasuda and Shinde, 2004). Therefore, detailed knowledge of the monsoon 66 system variability is essential for understanding global climate processes and is of societal and 67 economic interest, particularly with regard to existing uncertainties in future rainfall 68 projections (Stocker et al., 2013). 69A large number of palaeoenvironmental records have already been generated to better 70 understand the spatio-temporal variability and control mechanisms of the Asian monsoon (e.g. 71 Wang et al., 2010;Cao et al., 2013;Ran and Feng, 2013;An, 2014;Yang et al., 2014). In 72 general, these studies primarily invoke local or regional moisture changes as most indicative 73 of variations in monsoon strength and large-scale circulation patterns. Particularly, oxygen 74 isotope records from speleothems in S/E China have substantially influenced palaeo-monsoon 75 research as they are well dated and widely considered to be high-resolution summer monsoon 76 proxies (e.g., Wang et al., 2005; Liu et al., 2014 suggesting a similar moisture evolution across the monsoon-influenced regions of China 82 (Zhao et al., 2009a; Zhang et al., 2011;Ran and Feng, 2013). 83However, other studies point to much more variability of the summer monsoon in space 84 and time. In particular, towards its northern margin, proxy records reveal region-specific 85 palaeoenvironmental changes, suggesting a complex interplay between the Indian summer 86 monsoon (ISM), the EASM and other major climatic factors, including topography and 87 vegetation (Hu et al., 2003; Maher and Hu, 2006;An et al., 2006;Zhao and Yu, 2012; Ran 88 and Feng, 2013). 89To reveal coherent spatio-temporal patterns of climate evolution in monsoonal Asia and 90 adjacent regions, available proxy data were used for summarizing compilations, over-regional 91 correlations, for constructing 'monsoon/moisture indices' and data-model comparisons (An, 92 2000;Ren and Beug, 2002; Morrill et al., 2003;An et al., 2006;Herzschuh, 2006; Chen et al., 93 2008; Zhao et al., 2009a,b;Cai et al., 2010;Wang et al., 2010; Kleinen et al., 2011; Zhao and 94 Yu, 2012;Cao et al., 2013, Dallmayer et al., 2013 Leipe et al., 2014;Yang et al., 2014). 95However, the regional behaviour of the summer monsoon and its over-regional linkages is far 96 from being well understood. This is reflected in ongoing debates regarding (i) the regional 97 impact of the major atmospheric circulation systems controlling moisture distribution patterns 98 in China (e.g. Clemens et al., 2010;Ran and Feng, 2013), (ii) the phase 99 relationships between these systems (e.g. He et al., 2004;Zhao et al., 2009a; Wang et al., 100 2010;Cai et al., 2010; Clemens et al., 2010; Zhang et al., 2011; Ran and 101 Feng, 2013; Li et al., 2014;Yang et al., 2014),...
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