Abstract
Understanding the causes of abrupt hydrologic declines in the Asian summer monsoon region may help limit the adverse effects of such events on the region’s economy and ecology. Here, we provide a high-resolution record of hydrological evolution in the East Asian monsoon margin region since the last deglaciation. Our synthesis of hydrological records in the East Asian monsoon region reveals that northern and southern China were generally wet during the early Holocene, while two significant drought events occurred in northern China under the suppressive effect of Northern Hemisphere ice sheets. The hydrological pattern of “southern drought–northern floods” developed during the middle Holocene, and the southward withdrawal of the Intertropical Convergence Zone, which was controlled by the inter-hemispheric temperature gradient, along with the enhanced suppression of the East Asian monsoon by the Hadley Circulation, combined to cause synchronous extreme droughts during the mid- to late-Holocene.
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Introduction
The welfare of the large human population of East Asia is inextricably linked with the East Asian monsoon precipitation. The ecosystems, economy, and human civilizations in the East Asian monsoon region have depended heavily on the intensity and distribution of monsoon precipitation1,2. For example, Neolithic populations migrated across the Hu Line to the wetter west in response to changes in precipitation3, and the collapse of civilizations has been linked extreme drought events4,5,6. Therefore, an improved understanding of the hydrological evolution of the East Asian monsoon region, especially the spatiotemporal pattern of drought events and their origin, is important for ecosystem maintenance and socioeconomic development in this region.
The hydrological evolution of the Asian summer monsoon (ASM) region on several timescales and at different times has been comprehensively addressed in several studies. This research has revealed that bipolar and tri-polar patterns of hydrological evolution developed in the middle Holocene7; that similar hydrological modes occurring during the Little Ice Age (LIA) and the last deglaciation8,9; and that the Qinling Mountains were the boundary between the northern and southern hydrological regimes in eastern China during the LIA10. However, it is unclear whether antiphase hydrological modes existed during the early Holocene; and even the hydrological evolution of northern China during the early Holocene remains controversial, since research has tended to focus on determining whether the wettest interval in northern China occurred during the middle Holocene2,11,12, or the early Holocene13,14,15. However, a δ13C record from Diaojiaohaizi Lake in the Daqing Mountains has identified a prolonged dry period in the early Holocene16, This finding agrees with a paleohydrological record from Daihai Lake, which revealed low precipitation in the early Holocene, and abundant precipitation in the middle Holocene17. On orbital timescales, the variation of the Asian summer monsoon (ASM) intensity is consistent with that of insolation at 65°N18. Various mechanisms have been proposed to explain extreme hydrological events in the East Asian monsoon region, including the sapping of groundwater from Hunshandake Sandy Land by the Xilamulun River, which led to irreversible drought conditions and the disruption of the Hongshan culture4. Additionally, precipitation anomalies induced by the high-frequency variability of the ASM, modulated by centennial- to interannual-scale mechanisms such as the Pacific Interdecadal Oscillation and the El Niño-Southern Oscillation (ENSO), are proposed to have contributed to the collapse of Neolithic culture5. While the impact of extreme drought events on ancient societies and civilizations in China has attracted much research attention, this has imposed temporal and spatial limitations on the interpretation of extreme drought events, resulting in uncertainty regarding the influence of the climate system on regional drought events.
Precipitation is the most important hydrological recharge mechanism of closed lakes, and thus the levels of such lakes are closely related to precipitation, while closed alpine lakes in particular act as rain gauges10; however, in some lakes the effects of surface runoff and evapotranspiration can bias the precipitation estimates. With chronological controls, the elevation of former lake shorelines can be used as a proxy to quantify paleo-lake levels13,19,20; however, such records are often fragmentary due to factors like hydrodynamic perturbations or the failure of lake shorelines to develop21. Recently, modern process studies have validated the biomarkers of %OH-GDGTs and %Cren as a paleo-lake-level proxy10,22,23, making it possible to quantitatively reconstruct paleolake levels at a high resolution10,24. In this study, we used sedimentary records of GDGTs (%OH-GDGTs) and δ2H to reconstruct lake level changes in Daihai Lake (Fig. 1), in northern China, since the last deglaciation. Combined with other records from this region, we use the results from Dahai Lake to characterize the hydrological evolution of northern China, including abrupt drought events, with the aim of providing new insights into the climatic evolution of the ASM region and its driving mechanisms.
Results and discussion
Interpretation and validation of OH-GDGTs as a paleohydrological proxy
Group I.1a Thaumarchaeota inhabit subsurface waters in order to reduce ammonia-oxygen competition25,26,27, and during the rainy season, Thaumarchaeota are more active in surface waters compared to other archaea28. Soil Thaumarchaeota are dominated by Group 1.1b, which can produce abundant crenarchaeol (Cren) and crenarchaeol regioisomer (Cren’)29,30; whereas aquatic Group 1.1a Thaumarchaeota, in addition to the production of Cren and Cren’, can also produce OH-GDGTs. These observations indicate that OH-GDGTs are produced in situ in lakes31. The distribution patterns of isoGDGTs in soils and surface sediments are similar, but OH-GDGTs were only detected in the surface sediments (Supplementary Fig. 1), which is consistent with results from the Lugu Lake basin32. Therefore, the contribution of soil-derived Cren and Cren’ from inputs of terrestrial source Group 1.1b Thaumarchaeota may influence the assessment of the source of Cren and Cren’ in sediments, which may lead to errors in paleohydrological reconstructions22. Habitat selection in subsurface water bodies is such that aquatic Group I.1a Thaumarchaeota produce OH-GDGTs in response to changes in water level30,33. This finding has been verified by abundant data, which confirm the relationship between %OH-GDGTs and water depth22,24 and it enables the reconstruction of past lake levels22,23.
We combined the previous lake shoreline data from Daihai Lake19 with %OH-GDGTs data in the corresponding dated core-sediments to establish a calibration function for water depth vs. GDGTs. This revealed a good positive correlation between water depth and GDGTs (Supplementary Fig. 2), showing the potential of %OH-GDGTs for quantitatively reconstructing paleo-water depths. However, this calibration function lacks control data from shallow water-depths (<25 m), and thus it may be subject to a large bias in the reconstruction of low water-levels.
Hydrological patterns and synchronous drought events in the EASM region since the last deglaciation
An inverse hydrological pattern (i.e., “southern floods (drought)–northern drought (floods)” occurred between northern and southern China during the last deglaciation9, the middle Holocene7,34, and the Little Ice Age8. In northern China a wetness maximum in the middle Holocene has been proposed, which is supported by pollen-based precipitation reconstructions from Gonghai Lake2 and Daihai Lake17, and by the increased frequency of paleosol development on the Chinese Loess Plateau, which also indicate a middle Holocene wetness maximum11. Lake level changes, indicating changes in environmental humidity, are the integrated effects of precipitation, evaporation, and surface runoff recharge. High lake-levels in the early Holocene are demonstrated by studies of lake shorelines at several lakes, including Dali Lake13, Daihai Lake19, and Angulinao Lake15, and these high levels were maintained from the early through middle Holocene. Additionally, Hunshandake Sandy Land was an extremely wet environment during the early Holocene14. A nutrient-poor freshwater environment at this time also indicated a maximum in lake volume31,35. An early Holocene lake level maximum was also determined from the lakeshore embankments of Chagan Nuur21 and Angulinao Lake15. This interpretation of a wet early Holocene in northern China is controversial and two alternative hypotheses have been proposed to explain it: strong monsoon precipitation13,14, and increased snow/ice melt runoff recharge12,36,37
The timing of the reconstructed precipitation maximum (the upper limit of estimates), based on pollen assemblages, falls consistently within the early–middle Holocene38, which indicates that we cannot exclude the role of extreme precipitation in contributing to the observed high lake-levels. Depleted δ2H29 values in the sediments of Daihai Lake during the early–middle Holocene suggest the gradual enhancement of the Asian summer monsoon (Fig. 2). However, this averaged-state enhancement cannot fully explain the overall high water-level in the early–middle Holocene based on the water depth responses indicated by %OH-GDGTs, despite the good positive correlation between %OH-GDGTs and δ2H29 (Supplementary Fig. 3). This indicates that the hydrological evolution of Daihai Lake on a long timescale is modulated by the Asian summer monsoon, and that the early Holocene high water-levels may be related to recharge by non-monsoon precipitation.
a %OH-GDGTs (blue circles) and δ2H (cyan crosses) from Daihai Lake. b Lakeshore elevation (orange squares19) and a pollen-based annual precipitation reconstruction from Daihai Lake (blue line17). c RIK37-based lake salinity record from Dali Lake (green circles and line35), and a precipitation record (the upper limit of estimates) from Bayanchagan Lake (dark blue circles and lines38). d Pollen-based annual precipitation reconstruction from Gonghai Lake (blue line2), and a synthesis of palaeosol development in the Chinese Loess Plateau (red open squares11). e Hydroclimatic record of water-table depth from the Dajiuhu Peat based on hopanoid flux (orange circle39) and CIA from Nanyi Lake (red line34): f tropical + subtropical arboreal taxa (blue line60) and TOM (green line67) from Huguangyan Maar Lake.
Due to the influence of the Meiyu belt and ENSO, the hydrological pattern of southern China is the opposite to that in northern China9,34, except during the early Holocene when a common pattern of hydrological evolution occurred—a gradual increase in precipitation and high environmental humidity. The high concentration of hopanoids in Dajiuhu peatland in the middle Holocene suggests an arid environment39, which agrees with the trend of δ2H40. In these two records, extreme drought events can be clearly recognized, and in addition, pollen records from the middle and lower reaches of the Yangtze River indicate abrupt decreases in precipitation at ~7–6 cal kyr BP, 7.7–7 cal kyr BP, and ~4.9–4.2 cal kyr BP41,42 Similarly, in central China, low values of the environmental magnetic parameter IRMsoft-flux, which was linked to ENSO-related storms, suggest an arid environment during the middle Holocene43.
Although the dipolar hydrological pattern between northern and southern China developed in the middle Holocene, rapid drought events occurred almost synchronously throughout the regional influenced by the ASM. This is demonstrated by low precipitation, low environmental humidity, and the salinization of lakes due to falling water levels. (Fig. 2). Here, we identify at least seven well-defined drought events: during 11.7–11.3 cal kyr BP, 10.6–10.2 cal kyr BP, 9.6–9 cal kyr BP, 7.6–7.3 cal kyr BP, 7–6 cal kyr BP, 4.7–4.2 cal kyr BP, and 3.9–3.4 cal kyr BP.
Freshwater forcing led to independent early Holocene drought events in northern China
The variability of the ASM and its precipitation has been explained by regional-scale differences in ocean–land thermal gradients, influenced on orbital timescales by insolation and high-latitude Northern Hemisphere cryospheric forcing, and these variations show pronounced precession and obliquity cycles18,44,45. Ice-sheet forcing impeded the northward extension of the early Holocene ASM precipitation, which was proposed as the cause of the mismatch between monsoon precipitation and monsoon circulation2. Meltwater inputs from melting ice sheets or glaciers weakened the thermohaline circulation in the North Atlantic, and subsequently the summer monsoon precipitation decreased, most notably during the early Holocene intervals of 11.7–11.3 cal kyr BP and 9.6–9.0 cal kyr BP46,47. The Pre-Boreal Oscillation (PBO) has occasionally been detected outside the Atlantic region48,49. This event is documented in sedimentary records from mid-latitude East Asia, including Jeju Island in Korea, and in Hunshandake Sandy Land and Daihai Lake13,14,50. However, a weakening of monsoon activity during the PBO is not evident in the oxygen isotope record of Hulu cave51, and precipitation in southern China does not appear to have been affected by meltwater forcing in the early Holocene (Fig. 3)
a %OH-GDGTs (blue circles) and δ2H (light blue cross) from Daihai Lake. b δ18O record from Dongge cave (blue line68) and integrated ISM proxy based on four cave δ18O records (green line69). c Global sea-level70. d Ti concentration from the Cariaco Basin71. e ENSO variability (1.5–2.7 years)72. f ΔSST of the western73 and eastern74 tropical Pacific Ocean. g ΔT of the Northern and Southern Hemispheres (ΔT = TNH − TSH, solid line75, dashed line76).
Linkages between abrupt drought events and the weakening of inter-hemispheric temperature gradients
A “Jet transition hypothesis” of seasonal monsoon change has been proposed, which suggests that East Asian summer monsoon precipitation variability is influenced by the timing and duration of the transition to the Meiyu season52,53. Additionally, at ~6 cal kyr BP, the rapid increase in the meridional temperature gradient caused by the rapid expansion of Atlantic sea ice delayed the northward advance of the seasonal ASM, leading to the rapid shift to drought conditions in lakes and the ending of the Holocene humid period in the Indo–East Asian monsoon region19. Although a precipitation decrease or drought during 5.9–5.5 cal kyr BP has also been observed in the East Asian summer monsoon region (Fig. 2), it does not appear to have been an extreme event. A more extreme drought event occurred in the East Asian monsoon region during 7–6 cal kyr BP, which appears to have been spatially discontinuous based on a summary of lake shoreline studies19, possibly related to very low water levels resulting from a megadrought. Therefore, the limited high-latitude sea-ice extension events cannot fully explain the extreme drought events that occurred in the East Asian monsoon region during the middle and late Holocene, especially when the sea level was relatively close to the present-day level.
The inter-hemispheric temperature gradient is important in regulating the latitudinal position of the planetary atmospheric circulation54; and changes in this gradient are driven by insolation, which controls the position of the Hadley circulation terminus, the Hadley circulation, and the ITCZ55,56,57. The ITCZ, as an important feature of the global climate system, regulates the global monsoon, and its position is regulated by the inter-hemispheric temperature gradient (ΔTN-S)58,59. When the inter-hemispheric temperature gradient decreases, the ITCZ moves southward and the rainbelt is unable to penetrate deeper into the interior of East Asia, thus weakening the intensity of the monsoon rainfall. The role of the ITCZ together with sea level may explain why a marine sedimentary phytolith record failed to track the variations in the tropical Pacific meridional land-ocean climate system during the Holocene60. Warming of the tropical western Pacific strengthens the Hadley circulation61, and thus the enhancement of the lower tropospheric low-latitude return flow (northeasterly winds) reduces the ability of the EASM to move northward62. During abrupt drought events, changes in the latitudinal climate system can lead to the onset of weakened monsoon precipitation (Figs. 3 and 4).
Seasonal drought events in tropical East Asia are controlled by changes in the zonal SST gradient in the tropical Pacific Ocean, and by the westward shift of the Western Pacific sub-tropical high (WPSH), due to changes in the Hadley circulation60. At the onset of drought events in the middle and late Holocene, the Walker circulation strengthened due to the intensified zonal SST gradient (ΔTW-E) in the tropical Pacific Ocean, in response to warming SSTs in the western Pacific (Fig. 3). At the same time, the westward advance of the WPSH expanded its region of influence in East Asia, leading to zonal synoptic drought in the ASM region. This phenomenon cannot be explained by the movement of the rainbelt controlled by north–south shifts of the WPSH, which may be due to the blocking effect of the enhanced Hadley circulation on the transport of water vapor to middle and high latitudes62. Our conclusions indicate that extreme hydrological events in the EASM region during the middle and late Holocene were caused by changes in latitudinal and zonal SST gradients in the tropical Pacific. This is based on the rise of sea level to a relatively stable level, as a falling sea level would expand the land area and thus reduce the role of water vapor as a recharge mechanism for inland lakes; this would be coupled with a weakening of the East Asian monsoon precipitation caused by changes in latitudinal or zonal climatic regimes.
Methods
Regional setting and sample collection
Daihai Lake (40°29′–40°37′N, 112°33′–112°46′E, 1218 m a.s.l) is a hydrologically closed lake in the arid–semiarid region of northern China, located in Liangcheng County, Inner Mongolia, China. Daihai Lake has an area of 68.67 km2 and maximum water depth of ~7 m. The lake is mainly recharged by precipitation and by six rivers (the Gongba, Wuhao, Buliang, Tiancheng, Muhua, and Suodai rivers). The area has a typical East Asian summer monsoon, with summer temperature and precipitation maxima. The average annual temperature is 5.9 °C and the average annual precipitation is 406.4 mm, of which 80% occurs in summer; however, the average annual evaporation exceeds 1100 mm, which is almost three times the annual precipitation63,64.
In October 2020 we collected a 1235-cm-long continuous sediment core (DH20B, 40.57858°N, 112.672831°E) at the water depth of 6 m, using a UWITEC piston corer. This core was subsampled at 1-cm intervals in the laboratory and the samples were then freeze-dried prior to lipids extraction.
Chronology
Sixteen samples from core DH20B were used for AMS 14C dating and assessment of the carbon reservoir. They included four samples of plant remains, eight bulk sediment samples, and four samples of pollen concentrates. The radiocarbon ages of the plant remains and bulk samples were determined by Beta Analytic (Florida, USA), and those of the pollen concentrates were determined in the Key Laboratory of Western China’s Environmental Systems, Lanzhou University. An age-depth model for core DH20B was constructed using the Bacon program implemented in “R” software with the IntCal 20 calibration curve65, and the basal age of the core was estimated by extrapolation (Supplementary Fig. 4).
Lipids extraction and GDGTs analysis
A total of 211 samples from core DH20B, 5 soil samples and 4 surface sediment samples were used for lipids extraction and GDGTs analysis. The samples were homogenized and ultrasonically agitated four times using dichloromethane: methanol (v:v = 9:1), and then concentrated to dryness with N2 gas. The total lipid extracts were redissolved with hexane, analyzed using silica gel column chromatography, and then sequentially eluted with hexane, dichloromethane, and methanol. The polar fraction (containing GDGTs) was eluted with methanol and then filtered using 0.22 μm PTFE filters prior to LC–MS/MS analysis.
GDGTs analyses were performed using an Agilent 1290 II series ultra-performance liquid chromatography-atmospheric pressure chemical ionization-6465B triple quadruple mass spectrometer (UPLC-APCI-MS/MS). A flow rate of 0.3 ml/min was used, and an aliquot of 10 μl was injected and separated using two Hypersil Gold Silica columns in sequence (each 150 mm × 2.1 mm × 1.9 μm; Thermo Fisher Scientific; Lithuania), maintained at 40 °C. GDGTs were eluted isostatically with 84% A and 16% B for the first 5 min, where A = n-hexane and B = Ethyl acetate, followed by a linear gradient change to 82% A and 18% B from 5 min to 65 min, changed linearly to 100% B for 10 min to separate OH-GDGTs (including OH-GDGT-0, OH-GDGT-1, and OH-GDGT-2), then with 100% B maintained for 5 min to wash the system, and then back to 84% A and 16% B to equilibrate the pressure. Analyses were performed with the selective ion monitoring (SIM) mode to track m/z 1302, 1300, 1298, 1296, 1292, 1050, 1048, 1046, 1036, 1034, 1032, 1022, 1020, 1018, 744 (C46). The extraction and analysis of OH-GDGTs and brGDGTs from core DH20B used the same set of experiments and analytical systems. GDGTs were extracted and analyzed at the Key Laboratory of West China’s Environmental System (Ministry of Education), Lanzhou University.
Compound-specific hydrogen isotopes analysis
The GC injector was set at 280 °C, and the oven heating program was as follows: hold at 50 °C for 1 min, heat to 210 °C at 10 °C/min (hold 2 min), ramp (heat) to 300 °C at 4 °C/min, and finally to 310 °C at the rate of 10 °C/min. The internal standard (Squalane, δ2H = −167‰) was used to calibrate the compound-specific δ2H values. Results are reported in the delta notation (‰) relative to the Vienna Standard Mean Ocean Water standard66. δ2Hwax was determined using a Trace GC coupled with a Delta V advantage isotope ratio mass spectrometer in the State Key Laboratory of Biogeology and Environmental Geology, China University of Geosciences, Wuhan.
Data availability
The hydrologic reconstruction data from Daihai Lake generated in this study are freely available online (https://doi.org/10.6084/m9.figshare.25107689). The previously published record/data used in this study can be obtained from the original publications, including precipitation data17 and lakeshore data19 for Daihai Lake; RIK37 from Dali Lake35; precipitation reconstruction data from Bayanchagan Lake38 and Gonghai Lake2; a synthesis of palaeosol development data11; humidity reconstruction data for southern China from Dajiuhu Peat39 and Nanyi Lake34; pollen data60 and TOM67 from Huguangyan Lake; stalagmite δ18O data from Dongge cave68; integrated ISM proxy data based on four cave δ18O records69; global sea-level reconstruction data70; Ti concentration – ITCZ data71; ENSO variability data available through72; SST data for the western73 and eastern tropical Pacific Ocean74; and temperature differences between the Northern75 and Southern Hemispheres76.
References
Zhang, P. Z. et al. A test of climate, sun, and culture relationships from an 1810-year Chinese cave record. Science 322, 940–942 (2008).
Chen, F. H. et al. East Asian summer monsoon precipitation variability since the last deglaciation. Sci. Rep. 5, 11186 (2015).
Zhang, J. P. et al. Crossing of the Hu line by Neolithic population in response to seesaw precipitation. Sci. Bull. 67, 844–852 (2022).
Yang, X. P. et al. Groundwater sapping as the cause of irreversible desertification of Hunshandake Sandy Lands, Inner Mongolia, northern China. Proc. Natl Acad. Sci. USA 112, 702 (2015).
Sun, Q. L. et al. Climate as a factor for Neolithic cultural collapses approximately 4000 years BP in China. Earth 197, 102915 (2019).
Kennett, A. J. et al. Drought-induced civil conflict among the ancient maya. Nat. Commun. 13, 1–10 (2022).
Rao, Z. G. et al. Investigating the long-term palaeoclimatic controls on the δD and δ18Oof precipitation during the Holocene in the Indian and East Asian monsoonal regions. Earth 159, 292–305 (2016).
Chen, J. H. et al. Hydroclimatic changes in China and surroundings during the Medieval Climate Anomaly and Little Ice Age: spatial patterns and possible mechanisms. Quat. Sci. Rev. 107, 157–158 (2015).
Zhang, H. B. et al. East Asian hydroclimate modulated by the position of the westerlies during Termination I. Science 362, 580–583 (2018).
Chen, L. et al. GDGTs-based quantitative reconstruction of water level changes and precipitation at Daye Lake, Qinling Mountains, over for the past 2000 years. Quat. Sci. Rev. 267, 107099 (2021).
Wang, H. P. et al. Palaeosol development in the Chinese Loess Plateau as an indicator of the strength of the East Asian summer monsoon: Evidence for a mid-Holocene maximum. Quat. Int. 334, 155–164 (2014).
Wen, R. L. et al. Pollen evidence for a mid-Holocene East Asian summer monsoon maximum in northern China. Quat. Sci. Rev. 176, 29–35 (2017).
Goldsmith, Y. et al. Northward extent of East Asian monsoon covaries with intensity on orbital and millennial timescales. Proc. Natl Acad. Sci. USA 114, 1817–1821 (2017).
Ming, G. D. et al. Moisture variations in Lacustrine-eolian sequence from the Monsoon changes since the late Pleistocene. Quat. Sci. Rev. 233, 106210 (2022).
Wang, Y. C. et al. A quantitative reconstruction of Holocene annual precipitation in the marginal zone of the East Asian summer monsoon. Palaeogeogr. Palaeoclimatol. Palaeoecol. 596, 110968 (2022).
Dong, H. W. et al. Plant-wax carbon isotopic evidence of Late glacial and Holocene climate change from lake sediments in the Yin Mountains, inner Mongolia. Quat. Int. 622, 10–20 (2022).
Xiao, J. L. et al. Holocene vegetation variation in the Daihai Lake region of north–central China: a direct indica tion of the Asian monsoon climatic history. Quat. Sci. Rev. 23, 1629–1679 (2004).
Cheng, H. et al. The Asian monsoon over the past 640,000 years and ice age terminations. Nature 534, 640–646 (2016).
Goldsmith, Y. et al. Abrupt contraction of the Indo-East Asian monsoons ended the holocene humid period. Geophys. Res. Lett. 49, e2022GL100137 (2022).
Zhang, Z. P. et al. Lake level evidence for a mid-Holocene East Asian summer monsoon maximum and the impact of an abrupt late-Holocene drought event on prehistoric cultures in north-central China. Holocene 33, 382–399 (2022).
Li, G. Q. et al. Quantitative precipitation reconstructions from Chagan Nur revealed lag response of East Asian summer monsoon precipitation to summer insolation during the Holocene in arid northern China. Quat. Sci. Rev. 239, 106365 (2020).
Wang, H. Y. et al. Lake water depth controlling archaeal tetraether distributions in midlatitude Asia: implications for paleo lake-level reconstruction. Geophys. Res. Lett. 46, 5274–5283 (2019).
Wu, D. et al. Temperature-induced dry climate in basins in the northeastern Tibetan Plateau during the early to middle Holocene. Quat. Sci. Rev. 237, 106311 (2020).
Kou, Q. Q. et al. Distribution, potential sources, and response to water depth of archaeal tetraethers in Tibetan Plateau lake sediments. Chem. Geol. 610, 120825 (2022).
Woltering, M. et al. Vertical and temporal variability in concentration and distribution of thaumarchaeotal tetraether lipids in Lake Superior and the implications for the application of the TEX86 temperature proxy. Geochim. Cosmochim. Acta 87, 136–153 (2012).
Buckles, L. K. et al. Linking isoprenoidal GDGT membrane lipid distributions with gene abundances of ammonia-oxidizing Thaumarchaeota and uncultured crenarchaeotal groups in the water column of a tropical lake (Lake Challa, East Africa). Environ. Microbiol. 15, 2445–2462 (2013).
Sinninghe Damsté, J. S. et al. Intact polar and core glycerol dibiphytanyl glycerol tetraether lipids of group I.1a and I.1b Thaumarchaeota in soil. Appl Environ. Microbiol. 78, 6866–6874 (2012).
Baxter, A. J. et al. Seasonal and multi-annual variation in the abundance of isoprenoid GDGT membrane lipids and their producers in the water column of a meromictic equatorial crater lake (Lake Chala, East Africa). Quat. Sci. Rev. 273, 107263 (2021).
Auguet, J. C. et al. Global ecological patterns in uncultured Archaea. ISME J. 4, 182–190 (2010).
Elling, F. J. et al. Chemotaxonomic characterisation of the thaumarchaeal lipidome. Environ. Microbiol. 19, 2681–2700 (2017).
Chen, L. et al. Lake eutrophication in northeast China induced by the recession of the East Asian summer monsoon. Quat. Sci. Rev. 281, 107448 (2022).
Li, J. J. et al. Depth related variation of isoprenoid and hydroxylated tetraether lipids in Lake Lugu, Southwest China: Implications for palaeoenvironmental reconstructions. Chem. Geol. 619, 121313 (2023).
Pouliot, J. et al. Vertical structure of archaeal communities and the distribution of ammonia monooxygenase A gene variants in two meromictic High Arctic lakes. Appl. Environ. Microbiol. 11, 687–699 (2009).
Liu, J. B. et al. Dipolar mode of precipitation changes between north China and the Yangtze River Valley existed over the entire Holocene: Evidence from the sediment record of Nanyi Lake. Int. J. Climatol. 41, 1667–1681 (2021).
Zhao, J. J. et al. Coupling of the ecosystems in North China with the East Asian summer monsoon rainfall during the Holocene. Quat. Sci. Rev. 300, 107885 (2023).
Xiao, J. L. et al. Hydrology of Dali Lake in central-eastern Inner Mongolia and Holocene East Asian monsoon variability. J. Paleolimnol. 40, 519–528 (2008).
Jiang, J. W. et al. Meltwater Contribution to Lake Water Budget in Mid-Latitude Asia During the Deglaciation and Early Holocene. Geophys. Res. Lett. 49, e2022GL100229 (2022).
Jiang, W. Y. et al. Reconstruction of climate and vegetation changes of Lake Bayanchagan (Inner Mongolia): Holocene variability of the East Asian monsoon. Quat. Res. 65, 411–420 (2006).
Xie, S. C. et al. Concordant monsoon-driven postglacial hydrological changes in peat and stalagmite records and their impacts on prehistoric cultures in central China. Geology 41, 827–830 (2013).
Huang, X. Y. et al. Response of carbon cycle to drier conditions in the mid-Holocene in central China. Nat. Commun. 9, 1–9 (2018).
Lu, F. Z. et al. Variability of East Asian summer monsoon precipitation during the Holocene and possible forcing mechanisms. Clim. Dyn. 52, 969–989 (2019).
Li, J. Y. et al. Quantitative Holocene climatic reconstructions for the lower Yangtze region of China. Clim. Dyn. 50, 1101–1113 (2017).
Zhu, Z. M. et al. Holocene ENSO-related cyclic storms recorded by magnetic minerals in speleothems of central China. Proc. Natl Acad. Sci. USA 114, 852–857 (2017).
Biasutti, M. et al. Global energetics and local physics as drivers of past, present and future monsoons. Nat. Geosci. 11, 392–400 (2018).
Mohtadi, M., Prange, M. & Steinke, S. Palaeoclimatic insights into forcing and response of monsoon rainfall. Nature 533, 191–199 (2016).
Fleitmann, D. et al. Evidence for a widespread climatic anomaly at around 9.2 ka before present. Paleoceanography 23, PA1102 (2008).
Yu, S. Y. et al. Freshwater outburst from lake superior as a trigger for the cold event 9300 years ago. Science 328, 1262–1266 (2010).
Bos, J. A. A. et al. Preboreal climate oscillations in Europe: wiggle-match dating and synthesis of Dutch high-resolution multi-proxy records. Q. Sci. Rev. 1927e1950 (2007).
Weldeab, S. et al. Centennial scale climate instabilities in a wet early Holocene West African monsoon. Geophys. Res. Lett. L24702 (2007).
Park, J. et al. High-resolution multi-proxy evidence for millennial- and centennial- scale climate oscillations during the last deglaciation in Jeju Island, South Korea. Quat. Sci. Rev. 105, 112–125 (2014).
Wang, Y. J. et al. A high-resolution absolute-dated late Pleistocene Monsoon record from Hulu Cave, China. Science 294, 2345–2348 (2001).
Chaing, J. C. H. et al. Role of seasonal transitions and westerly jets in East Asian paleoclimate. Quat. Sci. Rev. 108, 111–129 (2015).
Kong, Q. Q., Swenson, L. M. & Chaing, J. C. H. Seasonal transitions and the westerly jet in the holocene East Asian Summer Monsoon. J. Clim. 30, 3343–3365 (2017).
McGee, D. et al. Changes in ITCZ location and cross-equatorial heat transport at the Last Glacial Maximum, Heinrich Stadial 1, and the mid-Holocene. Earth Planet. Sci. Lett. 390, 69–79 (2014).
D’Agostino, R. et al. Factors controlling Hadley circulation changes from the last glacial maximum to the end of the 21st century. Geophys. Res. Lett. 44, 8585–8591 (2017).
Chiang, J. C. H. & Friedman, A. R. Extratropical cooling, interhemispheric thermal gradients, and tropical climate change. Annu. Rev. Earth Planet. Sci. 40, 383–412 (2012).
Schneider, T., Bischoff, T. & Haug, G. H. Migrations and dynamics of the intertropical convergence zone. Nature 513, 45–53 (2014).
Routson, C. C. et al. Mid-latitude net precipitation decreased with arctic warming during the Holocene. Nature 568, 83–87 (2019).
Guo, Z. T., Zhou, X. & Wu, H. B. Glacial-interglacial water cycle, global monsoon and atmospheric methane changes. Clim. Dyn. 39, 1073–1092 (2012).
Zhang, J. P. et al. Seasonal drought events in tropical East Asia over the last 60000y. Natl Acad. Sci. USA 117, 30988–30992 (2020).
Feng, J., Li, J. & Xie, F. Long-term variation of the principal mode of boreal spring Hadley circulation linked to SST over the Indo-Pacific warm pool. J. Clim. 26, 532–544 (2013).
Zeng, G., Sun, Z., Wang, W. C. & Min, J. Interdecadal variability of the east Asian summer monsoon and associated atmospheric circulations. Adv. Atmos. Sci. 24, 915–926 (2007).
Wang, X., Cui, L. L., Xiao, J. L. & Ding, Z. L. Stable carbon isotope of black carbon in lake sediments as an indicator of terrestrial environmental changes: an evaluation on paleorecord from Daihai Lake, Inner Mongolia, China. Chem. Geol. 347, 123–134 (2013).
Shen, Z. W. et al. Investigation of Modern n -Alkanes in Daihai Lake Basin Northern China: implications for the interpretation of paleoclimate research. Front. Earth Sci. 10, 1–11 (2022).
Reimer, P. J. et al. The IntCal20 Northern Hemisphere radiocarbon age calibration curve (0–55 kcal BP). Radiocarbon 62, 1–33 (2020).
Yang, Y., Zhang, Y. R., Zhang, H. B. & Huang, X. Y. 2023. Quantitative reconstruction of the relative humidity by a coupled d18O-d2H approach during the Younger Dryas in central China. Quat. Sci. Rev. 299, 107879 (2023).
Wang, X. S. et al. Millennial-scale Asian summer monsoon variations in South China since the last deglaciation. Earth Planet. Sci. Lett. 451, 22–30 (2016).
Dykoski, C. A. et al. A high-resolution, absolute-dated Holocene and deglacial Asian monsoon record from Dongge Cave, China. Earth Planet. Sci. Lett. 233, 71–86 (2005).
Liu, X. K. et al. New insights on Chinese cave δ18O records and their paleoclimatic significance. Earth Sci. Rev. 207, 103216 (2020).
Siddall, M. et al. Sea-level fluctuations during the last glacial cycle. Nature 423, 853–858 (2003).
Haug, G. H., Hughen, K. A., Sigman, D. M., Peterson, L. C. & Röhl, U. Southward mi- gration of the intertropical convergence zone through the Holocene. Science 293, 1304–1308 (2001).
Liu, Z. et al. Evo- lution and forcing mechanisms of El Nino over the past 21,000 years. Nature 515, 550e553 (2014).
Stott, L., Poulsen, C., Lund, S. & Thunell, R. Super ENSO and global climate oscillations at millennial time scales. Science 297, 222–226 (2002).
Leduc, G. et al. Moisture transport across Central America as a positive feedback on abrupt climatic changes. Nature 445, 908–911 (2007).
Shakun, J. D. et al. Global warming preceded by increasing carbondioxide concentrations during the last deglaciation. Nature 484, 49–54 (2012).
Marcott, S. A., Shakun, J. D., Clark, P. U. & Mix, A. C. A reconstruction of regional and global temperature for the past 11,300 years. Science 339, 1198–120 (2013).
Acknowledgements
This research was supported by the National Natural Science Foundation of China (42171153) and the Basic Science Center for Tibetan Plateau Earth System (BSCTPES, NSFC project 41988101). We thank Prof. Jianping Zhang for his useful discussions and inspiration and Dr. Jan Bloemendal for improving the English language.
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L.C. proposed the study and led the writing. J.C and M.L. contributed to the chronological analyses. L.C., J.Z. and S.Z. contributed to GDGT analyses. X.H. contributed to compound-specific hydrogen isotopes analysis. S.Z., M.L., X.H., J.L. and A.Z. contributed to the discussion and editing. A.Z. proposed and directed the study.
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Chen, L., Chen, J., Shen, Z. et al. Drought in the Asian summer monsoon region is liked to a weakened inter-hemispheric temperature gradient. Commun Earth Environ 5, 432 (2024). https://doi.org/10.1038/s43247-024-01603-4
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DOI: https://doi.org/10.1038/s43247-024-01603-4
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