Chinese cave records and the East Asia Summer Monsoon

Liu, Zhengyu; Wen, Xiaohao; Brady, Esther C.; Otto‐Bliesner, Bette L.; Yu, Ge; Lu, Huayu; Cheng, Hai; Wang, Yongjin; Zheng, Weipeng; Ding, Yihui; Edwards, R. Lawrence; Cheng, Jun; Liu, Wei; Yang, Hao

doi:10.1016/j.quascirev.2013.10.021

Cited by 504 publications

(453 citation statements)

References 51 publications

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“…At present, however, it is impossible to determine the exact TOE sensitivity of ε LAND because it is modulated by changes in the underlying spatial distribution of δ 18 O precip . For instance, Chinese speleothem calcite records (Cheng et al, 2016;Wang et al, 2008Wang et al, , 2001) as well as isotope-enabled climate model simulations (Battisti et al, 2014;Liu et al, 2014) demonstrate that δ 18 O precip in southeastern China changes with EASM (East Asian summer monsoon) strength, such that local δ 18 O precip decreases during periods of an intense monsoon and increases with a weaker monsoon. Since this region is important for global oxygen production, it follows that a decrease in EASM intensity after a HE would act to increase ε LAND .…”

Section: Discussionmentioning

confidence: 99%

“…We suggest that δ 18 OS is driven by the superposition of these two components, both of which likely operate in the same direction. For a northward migration of the thermal equator and tropical rainfall belts, rainfall over productive northern regions like Southeast Asia becomes more isotopically depleted (Battisti et al, 2014;Cheng et al, 2016;Liu et al, 2014;Wang et al, 2008Wang et al, , 2001 a D-O warming). In the opposite scenario (southward shift of thermal equator) during a HE, for example, the superposition of (1) and (2) would act to increase δ 18 OS because of a strong increase in Northern Hemisphere δ 18 O precip and a southward shift of the TOE.…”

Section: Discussionmentioning

confidence: 99%

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Does δ18O of O2 record meridional shifts in tropical rainfall?

et al. 2017

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Abstract. Marine sediments, speleothems, paleo-lake elevations, and ice core methane and δ 18 O of O 2 (δ 18 O atm ) records provide ample evidence for repeated abrupt meridional shifts in tropical rainfall belts throughout the last glacial cycle. To improve understanding of the impact of abrupt events on the global terrestrial biosphere, we present composite records of δ 18 O atm and inferred changes in fractionation by the global terrestrial biosphere ( ε LAND ) from discrete gas measurements in the WAIS Divide (WD) and Siple Dome (SD) Antarctic ice cores. On the common WD timescale, it is evident that maxima in ε LAND are synchronous with or shortly follow small-amplitude WD CH 4 peaks that occur within Heinrich stadials 1, 2, 4, and 5 -periods of low atmospheric CH 4 concentrations. These local CH 4 maxima have been suggested as markers of abrupt climate responses to Heinrich events. Based on our analysis of the modern seasonal cycle of gross primary productivity (GPP)-weighted δ 18 O of terrestrial precipitation (the source water for atmospheric O 2 production), we propose a simple mechanism by which ε LAND tracks the centroid latitude of terrestrial oxygen production. As intense rainfall and oxygen production migrate northward, ε LAND should decrease due to the underlying meridional gradient in rainfall δ 18 O. A southward shift should increase ε LAND . Monsoon intensity also influences δ 18 O of precipitation, and although we cannot determine the relative contributions of the two mechanisms, both act in the same direction. Therefore, we suggest that abrupt increases in ε LAND unambiguously imply a southward shift of tropical rainfall. The exact magnitude of this shift, however, remains under-constrained by ε LAND .

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Section: Discussionmentioning

confidence: 99%

Section: Discussionmentioning

confidence: 99%

Does δ18O of O2 record meridional shifts in tropical rainfall?

et al. 2017

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“…The model is based on the Community Atmosphere Model version 3 (CAM3) (Collins et al, 2006), and the isotope module was developed by David Noone, University of Colorado. More details of isoCAM3 can be found in Noone and Sturm (2010) The isoCAM3 model has been applied in several studies that investigated the isotopic response to past climate changes (Tharammal et al, 2013;Speelman et al, 2010;Sturm et al, 2010;Pausata et al, 2011;Liu et al, 2012;Sewall and Fricke, 2013;Liu et al, 2014).…”

Section: The Model Isocam3mentioning

confidence: 99%

How does sea ice influence δ18O of Arctic precipitation?

et al. 2017

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Abstract. This study investigates how variations in Arctic sea ice and sea surface conditions influence δ 18 O of presentday Arctic precipitation. This is done using the model iso-CAM3, an isotope-equipped version of the National Center for Atmospheric Research Community Atmosphere Model version 3. Four sensitivity experiments and one control simulation are performed with prescribed sea surface temperature (SST) and sea ice. Each of the four experiments simulates the atmospheric and isotopic response to Arctic oceanic conditions for selected years after the beginning of the satellite era in 1979.Changes in sea ice extent and SSTs have different impacts in Greenland and the rest of the Arctic. The simulated changes in central Arctic sea ice do not influence δ 18 O of Greenland precipitation, only anomalies of Baffin Bay sea ice. However, this does not exclude the fact that simulations based on other sea ice and sea surface temperature distributions might yield changes in the δ 18 O of precipitation in Greenland. For the Arctic, δ 18 O of precipitation and water vapour is sensitive to local changes in sea ice and sea surface temperature and the changes in water vapour are surface based. Reduced sea ice extent yields more enriched isotope values, whereas increased sea ice extent yields more depleted isotope values. The distribution of the sea ice and sea surface conditions is found to be essential for the spatial distribution of the simulated changes in δ 18 O.

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“…ISM precipitation is directly influenced by the intertropical convergence zone, associated with tropical heating and ultimately related to solar radiation (Chao 2000;Fleitmann et al 2007). However, EASM precipitation is mainly caused by a frontal system, which forms when warm and moist air flows brought by the monsoonal southeasterly winds meet the cold air brought by the westerlies (Ding and Chan 2005;Liu et al 2014a). Therefore, a better understanding of the interaction between the EASM and mid-latitude westerlies is important to reveal the nature of moisture changes in East Asia.…”

Section: Introductionmentioning

confidence: 99%

Lagged response of summer precipitation to insolation forcing on the northeastern Tibetan Plateau during the Holocene

et al. 2017

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Chinese cave records and the East Asia Summer Monsoon

Cited by 504 publications

References 51 publications

Does δ<sup>18</sup>O of O<sub>2</sub> record meridional shifts in tropical rainfall?

Does δ<sup>18</sup>O of O<sub>2</sub> record meridional shifts in tropical rainfall?

How does sea ice influence <i>δ</i><sup>18</sup>O of Arctic precipitation?

Lagged response of summer precipitation to insolation forcing on the northeastern Tibetan Plateau during the Holocene

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Chinese cave records and the East Asia Summer Monsoon

Cited by 504 publications

References 51 publications

Does δ&lt;sup&gt;18&lt;/sup&gt;O of O&lt;sub&gt;2&lt;/sub&gt; record meridional shifts in tropical rainfall?

Does δ&lt;sup&gt;18&lt;/sup&gt;O of O&lt;sub&gt;2&lt;/sub&gt; record meridional shifts in tropical rainfall?

How does sea ice influence &lt;i&gt;δ&lt;/i&gt;&lt;sup&gt;18&lt;/sup&gt;O of Arctic precipitation?

Lagged response of summer precipitation to insolation forcing on the northeastern Tibetan Plateau during the Holocene

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Does δ<sup>18</sup>O of O<sub>2</sub> record meridional shifts in tropical rainfall?

Does δ<sup>18</sup>O of O<sub>2</sub> record meridional shifts in tropical rainfall?

How does sea ice influence <i>δ</i><sup>18</sup>O of Arctic precipitation?