Figure 6. Comparison of the bGDGTs-based MAAT record (this study) with records of ice-volume equivalent sea-level and external climate forcings. (a ) Greenland δ18O ice core (GRIP) record (Vinther et al., 2006); (b ) bGDGTs-based MAAT record from Huguangyan Maar Lake (this study; The data for 10–20 kyr BP is from Chu et al., 2017); (c ) Global ice volume record (relative sea level) from Grant et al. (2012); (d ) Ice-volume equivalent sea-level record (Lambeck et al., 2014); (e ) Dome C, antarctica, ice core CO2 record (Bereiter et al., 2015); (f ) WAIS Divide CH4 concentration (Fudge et al., 2013); (g ) Sulfate record of volcanic forcing from a Greenland ice core (Kobashi et al., 2017); (h ) Sulfate record from the Dome C ice core, Antarctica (Castellano et al., 2004).
The most striking cooling events evident in the brGDGTs-based MAAT record are linked with the abrupt weakening of the tropical summer monsoon (see Supplementary Figure S3). For example, the high-resolution δ18O record from Klang Cave in the Thai-Malay Peninsula (Chawchai et al., 2021) shows a large increase of 1.5 ‰ from 6.4 to 5.8 ka BP; and the δ13C27-35record of leaf wax lipids from the annually laminated sediments of Myanmar Maar Lake Twintaung indicates abrupt failures of the tropical monsoon at ~3.8 and ~5.8 ka BP (Chu et al., 2020).
4 Conclusions
Our brGDGTs-based temperature record shows an increasing MAAT during the last deglaciation and early Holocene and reached a maximum at ~6.6 kyr BP, followed by a decrease in middle and late Holocene. It is noted that our temperature reconstruction is in good agreement with instrumental temperature from 2010 CE to 1951 CE. We contend that the last deglaciation and early Holocene temperature variation is linked with the ice volume and/or ice sheet, while the temperature variations during the middle and late Holocene could be ascribed to several possible factors, such as oceanic and atmospheric circulation, and external drivers in Huguangyan Lake region.
Author contributions
Funding acquisition: G. Q. Chu, Q. Sun
Investigation: G. Q. Chu, Z. Y. Zhu, Q. Z. Zhu
Methodology: Q. Li, M. M. Xie, N. Zhan ,Y. Ling
Writing-Original draft: Q. Li, G. Q. Chu, Q. Sun
Writing-reviewing & editing: Q. Li, G. Q. Chu, Q. Sun, M. M. Xie
Acknowledgments
This work was funded by the National Natural Science Foundation of China (Grant 42030507, 41877301), the National Key Research and Development Program of China (Grant 2017YFA0603400) and the Strategic Priority Research Program of the Chinese Academy of Sciences (Grant XDB26000000).
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