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Low-high latitude forcing on the East Asian winter monsoon evolution since the last glacial maximum

Published online by Cambridge University Press:  23 September 2024

Debo Zhao Open the ORCID record for Debo Zhao [Opens in a new window] ,
Shiming Wan Open the ORCID record for Shiming Wan [Opens in a new window] ,
Xinquan Zhou ,
Shoushu Jiang  and
Anchun Li
Debo Zhao*
Affiliation:
Key Laboratory of Marine Geology and Environment, Institute of Oceanology, Chinese Academy of Sciences, Qingdao, China
Shiming Wan
Affiliation:
Key Laboratory of Marine Geology and Environment, Institute of Oceanology, Chinese Academy of Sciences, Qingdao, China CAS Center for Excellence in Quaternary Science and Global Change, Xi’an, China
Xinquan Zhou
Affiliation:
State Key Laboratory of Marine Geology, Tongji University, Shanghai, China
Shoushu Jiang
Affiliation:
Key Laboratory of Marine Geology and Environment, Institute of Oceanology, Chinese Academy of Sciences, Qingdao, China College of Marine Sciences, University of Chinese Academy of Sciences, Beijing, China
Anchun Li
Affiliation:
Key Laboratory of Marine Geology and Environment, Institute of Oceanology, Chinese Academy of Sciences, Qingdao, China
*
Corresponding author: Debo Zhao; Email: [email protected]
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Abstract

The East Asian winter monsoon (EAWM) has a profound effect on the winter climate in East Asia. The modern EAWM variability is tightly linked to the high-latitude Northern Hemisphere climate change through the Siberian High and can also be regulated by the low-latitude El Niño-Southern Oscillation through oceanic or atmospheric teleconnections. However, the Quaternary EAWM evolution has long been only attributed to the high-latitude climate change, resulting in the uncertainty in interpreting the out-of-phased EAWM variation recording in the East Asian continent and marginal seas. Here we presented a sediment record at Integrated Ocean Drilling Program Site U1427 in the southern Japan Sea to reconstruct the EAWM evolution since the last glacial maximum. By combining our record with previous reconstructions and simulations, we found the synchronous relationship between winter monsoon in northern and southern regions of East Asia from ∼24 to 8 ka, but anti-correlated relationship since ∼8 ka. We proposed the winter insolation and Atlantic meridional overturning circulation were the main drivers from last glacial to early Holocene, and then ENSO became a dominant factor in controlling the regional heterogeneity of EAWM evolution in the middle and late Holocene. This research explains much of the controversy in the Quaternary EAWM records and highlights the low-high latitude interaction in East Asian winter climate change.

Keywords

EAWMgrain sizeSr-Nd isotopesediment provenanceENSOJapan Sea
Type
Original Article
Information
Geological Magazine , Volume 161 , 2024 , e3
Creative Commons
Creative Common License - CCCreative Common License - BY
This is an Open Access article, distributed under the terms of the Creative Commons Attribution licence (https://creativecommons.org/licenses/by/4.0/), which permits unrestricted re-use, distribution and reproduction, provided the original article is properly cited.
Copyright
© The Author(s), 2024. Published by Cambridge University Press

1. Introduction

The East Asian winter monsoon (EAWM) characterized by cold and dry northwesterlies over northern East Asia and marginal seas and northeasterlies above southern East Asia and South China Sea is a specific feature that could cause extreme frigid/warm winter weather or climate events, which give profound economical, biological and societal influences on this densely populated region (Chang et al. Reference Chang, Wang, Hendon and Wang2006; Gao et al. Reference Gao, Chen, Jia, Ke, Han, Zhang, Wang, Sun, Zhu, Li, Sun, Ren, Wang and Gao2008; Wang et al. Reference Wang, Yu and Song2011). The modern EAWM variability is tightly linked to variations in northern high-latitude climate via the Siberian High (Chang & Lu, Reference Chang and Lu2012; Zhang & Wang, Reference Zhang and Wang2020). On the other hand, low-latitude El Niño-Southern Oscillation (ENSO) can also regulate EAWM by modifying the atmospheric circulation over the western North Pacific (Geng et al. Reference Geng, Noh, Kim and Kug2023; Son et al. Reference Son, Park, Kug, Yoo and Kim2014; Zhang et al. Reference Zhang, Li, Stuecker, Jin and Turner2016).

The Quaternary EAWM intensity has been reconstructed extensively based on Chinese loess, lake and marine sediments (Hao et al. Reference Hao, Wang, Oldfield, Peng, Qin, Song, Xu, Qiao, Bloemendal and Guo2012; Huang et al. Reference Huang, Wang, Wei, Yuan and Tian2023; Jia et al. Reference Jia, Bai, Yang, Xie, Wei, Ouyang, Chu, Liu and Peng2015; Kang et al. Reference Kang, Du, Wang, Dong, Wang, Wang, Qiang and Song2020; Li et al. Reference Li, Zhao and Tian2017; Liu & Ding, Reference Liu and Ding1998; Sun et al. Reference Sun, Clemens, Morrill, Lin, Wang and An2012; Zhao et al. Reference Zhao, Wan, Song, Gong, Zhai, Shi and Li2019; Zheng et al. Reference Zheng, Li, Wan, Jiang, Kao and Johnson2014). However, these reconstructed monsoon variabilities and proposed forcing mechanisms remain under debate at multi-time scales. Especially, records have suggested inconsistent EAWM patterns between the northern and southern East Asia and its marginal seas (Hao et al. Reference Hao, Liu, Ogg, Liang, Xiang, Zhang, Zhang, Zhang, Liu and Li2017; Huang, Reference Huang2015; Huang et al. Reference Huang, Tian and Steinke2011; Huang et al. Reference Huang, Wang, Wei, Yuan and Tian2023; Liu et al. Reference Liu, Sun, Vandenberghe, Cheng, Zhang, Gowan, Lohmann and An2020; Steinke et al. Reference Steinke, Glatz, Mohtadi, Groeneveld, Li and Jian2011; Zheng et al. Reference Zheng, Li, Wan, Jiang, Kao and Johnson2014), probably indicating the regional heterogeneity of EAWM evolution (Zhao et al. Reference Zhao, Wan, Song, Gong, Zhai, Shi and Li2019). Studies have linked the winter solar insolation and the resultant variations in atmospheric circulation over East Asian continent and Pacific to the EAWM variation (Huang et al. Reference Huang, Wang, Wei, Yuan and Tian2023; Kutzbach, Reference Kutzbach1981; Wen et al. Reference Wen, Liu, Wang, Cheng and Zhu2016). Changes in Northern Hemisphere ice volume and hemispheric temperature gradient have also been adopted as dominant factors (Hao et al. Reference Hao, Wang, Oldfield, Peng, Qin, Song, Xu, Qiao, Bloemendal and Guo2012; Kang et al. Reference Kang, Du, Wang, Dong, Wang, Wang, Qiang and Song2020). Besides, millennial scale of abrupt changes in EAWM during the last glaciation has been attributed to the Atlantic meridional overturning circulation (AMOC) reorganization (Liu et al. Reference Liu, Sun, Vandenberghe, Cheng, Zhang, Gowan, Lohmann and An2020; Sun et al. Reference Sun, Clemens, Morrill, Lin, Wang and An2012). Nevertheless, all these proposed forcings cannot fully explain the observed regional heterogeneity of EAWM evolution.

The EAWM brings dry air-mass across the Asian continent but carries moisture when it flows across the warm Japan Sea. This moisturized wind brings much more snowfall and rainfall to the Japan Sea side of the Japanese Islands during winter than other seasons (Sone et al. Reference Sone, Kano, Okumura, Kashiwagi, Hori, Jiang and Shen2013). Such hydroclimate condition favours more sediment eroded from the island’s input to the southern Japan Sea during winter than other seasons (Otosaka et al. Reference Otosaka, Togawa, Baba, Karasev, Volkov, Omata and Noriki2004). Thus, the sediment records in this region could be the ideal candidates to reconstruct EAWM evolution. Here we present a high-resolution sediment record at Integrated Ocean Drilling Program (IODP) Site U1427 in the southern Japan Sea (Figure 1a). Grain-size analysis and Sr-Nd isotopic sediment source tracing have been used to trace the sediment supply from the island to Japan Sea and further reconstruct the EAWM evolution since the last glacial maximum (LGM). By comparing the EAWM in the northern and southern regions of East Asia and its marginal seas, we proposed that ENSO overwhelmed winter insolation and became the dominant factor in controlling the regional heterogeneity of long-term EAWM evolution through ocean-atmosphere interactions in the middle and late Holocene.

Figure 1. (a) Map showing the location of the IODP Site U1427 (red dots), bathymetry of the Japan Sea and the flow of surface currents (yellow arrow lines). The referenced ocean sites and lake pollen and speleothem records are shown with orange dots and purple squares, respectively. EAWM, EASM and Northern Hemisphere subtropical westerlies are shown with blue, red and purple arrows, respectively. White lines show rivers on the Japanese Islands. Abbreviations of East Asian monsoon, ocean currents and straits are also shown. (b) Monthly rainfall at the Hiraiwa Precipitation Observatory and temperature at Itoigawa (Sone et al. Reference Sone, Kano, Okumura, Kashiwagi, Hori, Jiang and Shen2013) in the Japan Sea side of the Japanese Islands are shown with purple triangles in (a). (c) Mean annual dust flux in the Eurasia and North Pacific (Kok et al. Reference Kok, Adebiyi, Albani, Balkanski, Checa-Garcia, Chin, Colarco, Hamilton, Huang, Ito, Klose, Leung, Li, Mahowald, Miller, Obiso, Pérez García-Pando, Rocha-Lima, Wan and Whicker2021). Numbers show the deserts in the northern China, which were divided into three regions: Deserts A, B and C (Chen et al. Reference Chen, Li, Yang, Rao, Lu, Balsam, Sun and Ji2007).

2. Study area

The Japan Sea is a back-arc basin in the northwestern Pacific bounded by the Eurasian continent, the Japanese Islands and Sakhalin Island, and connects to the East China Sea, Sea of Okhotsk and North Pacific by shallow straits (Figure 1a). It has an average depth of 1350 m and a maximum depth of ∼3700 m. Climatologically, the Japan Sea is influenced by the prevalent East Asian monsoon, consisting of the East Asian summer monsoon (EASM), characterized by warm and moist winds from the Pacific in boreal summer, and the EAWM, characterized by cold and dry air winds from the Siberian High in boreal winter (Tada et al. Reference Tada, Murray, Zarikian, Lofi, Bassetti, Brace, Clemens, Dickens, Dunlea and Gallagher2014).

Given the Tsushima Warm Current (TWC), a branch of the Kuroshio Current, flow into the Japan Sea through the Tsushima Strait (Figure 1a), the cold and dry northwesterly winter winds can be moistened and heated. Thus, the EAWM and the carried water vapour and heat over the Japan Sea are the major factors contributing to variations in snowfall and rainfall on the Japan Sea side of the Japanese Islands (Inoue et al. Reference Inoue, Kibe, Ueda and Mika2015; Takahashi, Reference Takahashi2021; Takano et al. Reference Takano, Tachibana and Iwamoto2008). Instrumental record at Hiraiwa Precipitation Observatory near our study site suggest the rainfall during the EAWM months (from November to March) accounts for 59% of the annual precipitation (Sone et al. Reference Sone, Kano, Okumura, Kashiwagi, Hori, Jiang and Shen2013) (Figure 1b). Such hydroclimate condition enhanced sediment erosion on the islands and thus results in higher sediment flux in Yamato Basin in the eastern Japan Sea during winter than summer (Otosaka et al. Reference Otosaka, Togawa, Baba, Karasev, Volkov, Omata and Noriki2004).

3. Material and methods

3.a. Core descriptions and chronological framework

IODP Site U1427 (35°57.92’ N, 134°26.06’ E, 330 m water depth) is located in the south-central part of the Japan Sea on the outer margin of the southeast-northwest trending continental shelf, ∼35 km from the northern coast of Honshu Island (Tada et al. Reference Tada, Murray, Zarikian, Lofi, Bassetti, Brace, Clemens, Dickens, Dunlea and Gallagher2014) (Figure 1a). The lithologic composition of sediments is dominated by clayey silt and nannofossil- or biosiliceous-rich clayey silt. Centimetre-thick tephra layers occur frequently throughout the succession. The hole A of Site U1427 was cored to 548.6 m depth below seafloor, with a recovery of 542.59 m (98.9%). Here we focused on the top 7.75 m of the Hole A. No obvious tephra layers appear in this interval (Tada et al. Reference Tada, Murray, Zarikian, Lofi, Bassetti, Brace, Clemens, Dickens, Dunlea and Gallagher2014).

Chronological framework was established based on 5 accelerator mass spectrometry (AMS) 14C dates measured by Beta Analytic Inc, in conjunction with correlations between reflectance b* (Tada et al. Reference Tada, Murray, Zarikian, Lofi, Bassetti, Brace, Clemens, Dickens, Dunlea and Gallagher2014) and NGRIP δ18O record (Andersen et al. Reference Andersen, Azuma, Barnola, Bigler, Biscaye, Caillon, Chappellaz, Clausen, Dahljensen and Fischer2004). Radiocarbon dates were performed on mixed planktonic foraminifera from 5 fine-grained sediment layers (Table 1). All radiocarbon ages were calibrated using software CALIB based on the marine calibration dataset Marine 20 (Reimer & Stuiver, Reference Reimer and Stuiver2016) with an adjustment for a regional 14C reservoir age (ΔR = −21 ± 76) (Yoneda et al. Reference Yoneda, Uno, Shibata, Suzuki, Kumamoto, Yoshida, Sasaki, Suzuki and Kawahata2007). The reflectance b* of Site U1427 has been interpreted to reflect the ratio of biogenic to terrigenous input, and thus used to correlate with the benthic foraminiferal δ18O to build the age model (Sagawa et al. Reference Sagawa, Nagahashi, Satoguchi, Holbourn, Itaki, Gallagher, Saavedra-Pellitero, Ikehara, Irino and Tada2018). The trend of sediment colour reflectance b* data of the study interval at Site U1427 closely follows the NGRIP δ18O record (Figure 2). Here 9 horizons were correlated between sediment reflectance b* and NGRIP δ18O (Figure 2, Table 1). Between age control points, ages were linearly interpolated assuming constant sedimentation rates. The established age model reveals that the sediments extend to approximately 23.81 ka BP, with an average sedimentation rate of about 32.5 cm/ka. This is similar to the sedimentation rate of a nearby piston core obtained during the pre-expedition site survey cruise, which suggests an average sedimentation rate of ∼30 cm/ka (Tada et al. Reference Tada, Murray, Zarikian, Lofi, Bassetti, Brace, Clemens, Dickens, Dunlea and Gallagher2014).

Table 1. Radiocarbon dating and correlation points between reflectance b* and NGRIP δ18O

Figure 2. Age model of the top 7.75 m of the Hole A sediments at IODP Site U1427. The layers and their corresponding AMS 14C dates are shown with yellow squares and red diamonds with black error bars, respectively, connected by red dotted lines. The blue dotted lines show the correlations between (a) NGRIP δ18O and (b) sediment reflectance b*.

3.b. Analytical methods

A total of 266 samples from IODP Site U1427 were taken for the grain-size analysis. Samples were measured after removal of organic matter, carbonate and biogenic silica by hydrogen peroxide (15%), hydrochloric acid (0.5 mol/L) and sodium carbonate (2 mol/L), respectively (Zhao et al. Reference Zhao, Wan, Clift, Tada, Huang, Yin, Liao, Shen, Shi and Li2018; Zhao et al. Reference Zhao, Wan, Lu, Zhai and Li2020). Grain-size measurements were carried out on a Cilas 1190 L apparatus in the laboratory of Institute of Oceanology, Chinese Academy of Sciences (IOCAS). The analytical range is from 0.04 to 2500 μm. The measurement repeatability of the instrument is 0.5%, and the reproducibility is better than 2%. Then unmixing of the yielded raw grain-size distributions into unimodal parametric end-members was performed by parametric end-member analysis (EMA) with skewed generalized Gaussian (SGG) distribution using the Matlab-based software package AnalySize (Paterson & Heslop, Reference Paterson and Heslop2015; Zhao et al. Reference Zhao, Wan, Lu, Zhai and Li2020).

The bulk fine fractions of the samples (n = 9) were pretreated using the same procedure with grain-size analysis to remove the organic matter, carbonate and biogenic silica. Then, the 2–32 μm and 32–63 μm fractions were separated by wet-sieve and centrifugation. Further, the Sr-Nd isotope compositions of these two separated fractions were determined. The Sr-Nd isotope compositions were measured by Thermo Fisher Scientific Triton TIMS instrument at the laboratory of Tianjin Center, China Geological Survey, following the method described by (Tang et al. Reference Tang, Wan, Clift, Zhao, Xu, Zhang, Song, Jin, Li, Shi and Li2022). The standard Sr solution (NBS987) showed an average 87Sr/86Sr value of 0.710250 ± 4 (2σ) (n = 11, recommended value of 0.710250), and the standard Nd solution (JNdi-1) yielded an average 143Nd/144Nd value of 0.512111 ± 4 (2σ) (n = 11, recommend value of 0.512115). All measured 143Nd/144Nd and 87Sr/86Sr values were normalized to 146Nd/144Nd = 0.7219 and 88Sr/86Sr = 0.1194, respectively. Nd isotopic results are presented as εNd = [((143Nd/144Nd)sample)/0.512638)-1] × 10000 (Jacobsen & Wasserburg, Reference Jacobsen and Wasserburg1980).

4. Results

4.a. Grain-size end-member analysis

The goodness of fit statistics (coefficient of determination r2 > 90%, degree of angle < 5 for 3 end-members) shows that the three end-member model is the optimization (Figure 3a and b). These three end-member model contains grain-size modes of ∼12 μm, ∼32 μm and ∼56 μm for end-members EM1, EM2 and EM3, respectively (Figure 3c). The end-member abundances for each end-member since LGM have been shown in Figure 3d. The EM1 suggests overall increased trends during ∼24–17 ka and ∼15–8 ka, and decreased trends during ∼17–15 ka and since ∼8 ka. Generally, the EM3 shows almost reverse relationship with EM1, but with low abundances during ∼21–17 ka and ∼10–7.5 ka. The EM2 also shows a reverse trend compared with EM1, except for several millennial scale of fluctuations during ∼17.5–15 ka, ∼12–10 ka and ∼7.5–6.5 ka.

Figure 3. End-member modelling results of Site U1427 grain-size data. (a) Coefficients of determination (R2) for each size class of models with 1–5 end-members. (b) Angular differences (in degrees) between the reconstructed and observed datasets as a function of the number of end-members. (c) Modelled three end-members of the terrigenous sediment fractions from Site U1427. (d) Variations of end-member abundances of EM1–EM3 during the last ∼24 ka.

4.b. Sr-Nd isotopic composition

The Sr-Nd isotopic compositions are shown in Table 2. The 2–32 μm fraction has higher 87Sr/86Sr values (average 0.710883) than the 32–63 μm fraction (average 0.7079383), suggesting the grain-size effect on the Sr isotopic composition. This is mainly due to the coarse fractions are dominated by quartz and feldspar, with low 87Sr/86Sr values, whereas the fine fraction mainly contains clay minerals and micas, which are characterized by high 87Sr/86Sr ratios (Innocent et al. Reference Innocent, Fagel and Hillaire-Marcel2000; Meyer et al. Reference Meyer, Davies and Stuut2011). Such grain-sized effect has also been observed in the previous studies of East Asian marginal sea sediments (Shen et al. Reference Shen, Wan, France-Lanord, Clift, Tada, Révillon, Shi, Zhao, Liu, Yin, Song and Li2017; Zhao et al. Reference Zhao, Wan, Toucanne, Clift, Tada, Révillon, Kubota, Zheng, Yu and Huang2017). In contrast, Nd isotopes in sediments are not significantly influenced by erosion and transport compared to the original bedrock values (Zhao et al. Reference Zhao, Wan, Toucanne, Clift, Tada, Révillon, Kubota, Zheng, Yu and Huang2017). The εNd(0) of the 2–32 μm fraction shows more negative values (average −6.4) than the 32–63 μm fraction (average −3.6), indicating their distinct sediment sources.

Table 2. Sr-Nd isotopic composition of 2–32 μm and 32–63 μm fractions in IODP Site U1427 sediments

5. Discussion

5.a. Sediment provenance

A prerequisite for interpretation of mineralogical or geochemical trends in marine sediments is ascertaining their source areas (Colin et al. Reference Colin, Turpin, Blamart, Frank, Kissel and Duchamp2006; Wan et al. Reference Wan, Toucanne, Clift, Zhao, Bayon, Yu, Cai, Yin, Révillon and Wang2015). IODP Site U1427 has multiple potential sediment sources including the deserts in central and eastern Asia, nearby islands and mainland Asia. Modern observation and modelling results suggest the Japan Sea is a region that is significantly affected by the eolian dust released from the Asian arid regions (Kok et al. Reference Kok, Adebiyi, Albani, Balkanski, Checa-Garcia, Chin, Colarco, Hamilton, Huang, Ito, Klose, Leung, Li, Mahowald, Miller, Obiso, Pérez García-Pando, Rocha-Lima, Wan and Whicker2021) (Figure 1c). Sediment source tracing studies also suggested that eolian dust from these regions transported by the westerlies and/or the EAWM is the most important source of sediments in the Japan Sea (Irino & Tada, Reference Irino and Tada2003; Nagashima et al. Reference Nagashima, Tada, Matsui, Irino, Tani and Toyoda2007a; Nagashima et al. Reference Nagashima, Tada, Tani, Toyoda, Sun and Isozaki2007b; Nagashima et al. Reference Nagashima, Tada and Toyoda2013; Shen et al. Reference Shen, Wan, France-Lanord, Clift, Tada, Révillon, Shi, Zhao, Liu, Yin, Song and Li2017).

Surrounding rivers in Japan Arc, Korean Peninsula and Russian coast are other possible sources of sediments in the Japan Sea. Rivers in the Japan Sea side of the Japanese Islands (Figure 1a) deliver a total of about 10 million tons/year (Mt/yr) of suspended sediments to the study region (Milliman & Farnsworth, Reference Milliman and Farnsworth2013). Nakdong and Seumjin Rivers in Korean Peninsula deliver 8 Mt/yr and 2 Mt/yr sediments to the Tsushima Strait, respectively (Milliman & Farnsworth, Reference Milliman and Farnsworth2013), are also possible sources of the southern Japan Sea sediments. Sediment contribution from the Russian Tumnin and Zheltaya Rivers should be very minor because of their very low sediment discharge (<0.5 Mt/yr) (Milliman & Farnsworth, Reference Milliman and Farnsworth2013) and the blocking effect of the northeastward current system in the Japan Sea (Figure 1a). Besides, fine-grained suspended sediments derived from the Chinese large rivers including Yangtze and Yellow River can also be transported to the southern part of the Japan Sea by the TWC (Nagashima et al. Reference Nagashima, Tada, Tani, Toyoda, Sun and Isozaki2007b).

To identify the provenance of sediments at IODP Site U1427, 87Sr/86Sr versus εNd(0) diagrams of 2–32 μm and 32–63 μm fractions were plotted with fine- (Figure 4a) and coarse-grained (Figure 4b) data, respectively, from potential sources including Japanese rocks and river sediments, Asian deserts, Chinese Loess Plateau, Yangtze and Yellow Rivers in East Asia and Korean river. All the samples of 32–63 μm fraction plot within the range of Japanese end-member, indicating the dominant contribution of terrigenous materials eroded from Japan to this coarse fraction. This is reasonable because the nearshore location (∼35 km from the coast) and higher sedimentation rate (∼32.5 cm/ka) of IODP Site U1427 are compared with other offshore sites (e.g. IODP Site U1430 (Figure 1a), with an average sedimentation rate of ∼3.9 cm/ka during the late Pleistocene (Shen et al. Reference Shen, Wan, France-Lanord, Clift, Tada, Révillon, Shi, Zhao, Liu, Yin, Song and Li2017)).

Figure 4. Provenance of 2–32 μm and 32–63 μm fractions from Site U1427 sediments based on the Sr-Nd isotopic composition. (a) Comparison with fine-grained end-members of potential source areas. (b) Comparison with coarse-grained end-members of potential source areas. Data sources: Japanese rivers (Goldstein & Jacobsen, Reference Goldstein and Jacobsen1988; Shen et al. Reference Shen, Wan, France-Lanord, Clift, Tada, Révillon, Shi, Zhao, Liu, Yin, Song and Li2017), Japanese rocks (Kagami et al. Reference Kagami, Iizumi, Tainosho and Owada1992), Deserts A, B and C (Chen et al. Reference Chen, Li, Yang, Rao, Lu, Balsam, Sun and Ji2007), Gobi Desert (Biscaye et al. Reference Biscaye, Grousset, Revel, Gaast, Zielinski, Vaars and Kukla1997; Zhao et al. Reference Zhao, Sun, Balsam, Zeng, Lu, Otgonbayar and Ji2015), Chinese loess (Chen et al. Reference Chen, Li, Yang, Rao, Lu, Balsam, Sun and Ji2007; Zhao et al. Reference Zhao, Wan, Toucanne, Clift, Tada, Révillon, Kubota, Zheng, Yu and Huang2017), Yangtze River (Meng et al. Reference Meng, Liu, Shi and Dewen2008; Yang et al. Reference Yang, Jiang, Ling, Xia, Sun and Wang2007; Zhao et al. Reference Zhao, Wan, Toucanne, Clift, Tada, Révillon, Kubota, Zheng, Yu and Huang2017), Yellow River (Hu et al. Reference Hu, Li, Li, Bi, Zhao and Bu2012; Meng et al. Reference Meng, Liu, Shi and Dewen2008; Zhao et al. Reference Zhao, Wan, Toucanne, Clift, Tada, Révillon, Kubota, Zheng, Yu and Huang2017), Korean river (Lee et al. Reference Lee, Kim, Yang and Kim2008; Lim et al. Reference Lim, Jung, Xu, Jeong and Li2015).

Almost all the samples of 2–32 μm fraction deviate from the Japanese end-member, but close to the Asian desert end-member, especially the Desert A group including Gurbantunggut Desert, Onqin Daga Sandy Land, Horqin Sandy Land and Hunlun Buir Sandy Land in relatively higher latitude (Figure 1a). This suggests the Desert A region probably contributes a large part of the sediments in the study region. An alternative explanation is that such Sr-Nd isotopic composition of 2–32 μm fraction can be caused by the mixing between Japanese end-member and Asian deserts, Chinese Loess Plateau, Yangtze and Yellow Rivers and Korean river. Observation during the Asian dust period at a Korean site suggests the eolian grain-size distribution is dominated by the mean diameter of 8.5 μm (Park & Kim, Reference Park and Kim2006), close to our 2–32 μm fraction. It has been proposed that the silt (>4 μm) population of Japan Sea sediments have been mostly supplied from the Asian arid regions by eolian dust transport (Nagashima et al. Reference Nagashima, Tada, Tani, Toyoda, Sun and Isozaki2007b). Besides, grain-size end-member with the median grain size of 9.5 μm in the southwestern Japan Sea sediments has also been interpreted as the Asian dust source in a recent research (Bahk et al. Reference Bahk, Um and Jang2021). Therefore, we tend to interpret the 2–32 μm fraction as an eolian dust end-member, but probably can be disturbed by other source regions including Yangtze and Yellow Rivers and Korean river by the TWC intrusion (Nagashima et al. Reference Nagashima, Tada, Tani, Toyoda, Sun and Isozaki2007b; Zou et al. Reference Zou, Shi, Zhu, He, Kandasamy, Tiedemann, Lembke-Jene, Shi, Gong, Liu, Ikehara and Yu2021).

5.b. EAWM evolution in the northern East Asia and its marginal seas

Based on the source tracing results, variation of the 32–63 μm fraction in sediments at IODP Site U1427 can be regarded as the indicator of sediment supply from the Japanese Islands. It can be represented approximately with changes in the combined abundance of EM2 (median grain size of 32 μm) and EM3 (median grain size of 56 μm). To constrain the control mechanism of sediment supply from the Japanese Islands, we compared the abundances of EM2 and EM3 with the potential forcings including southwestern Japan rainfall, EAWM, EASM, sea surface temperature (SST) of the Japan Sea and sea level change (Figure 5).

Figure 5. Comparison between (a) Japanese sediment input index established with EM1 and EM2 abundances with speleothem δ18O record from the Maboroshi Cave (Kato et al. Reference Kato, Amekawa, Hori, Shen, Kuwahara, Senda and Kano2021) and winter rainfall record in Lake Biwa (Kigoshi et al. Reference Kigoshi, Kumon, Hayashi, Kuriyama, Yamada and Takemura2014), and (b) EAWM (Hao et al. Reference Hao, Liu, Ogg, Liang, Xiang, Zhang, Zhang, Zhang, Liu and Li2017; Kang et al. Reference Kang, Du, Wang, Dong, Wang, Wang, Qiang and Song2020; Liu et al. Reference Liu, Sun, Vandenberghe, Cheng, Zhang, Gowan, Lohmann and An2020; Zhao et al. Reference Zhao, Wan, Song, Gong, Zhai, Shi and Li2019; Zheng et al. Reference Zheng, Li, Wan, Jiang, Kao and Johnson2014), (c) Japan Sea SST (Fujine et al. Reference Fujine, Tada and Yamamoto2009; Liu et al. Reference Liu, Chen, Chen, Xing, Zou and Yao2014a), (d) EASM (Cheng et al. Reference Cheng, Edwards, Sinha, Spötl, Liang, Chen, Kelly, Kathayat, Wang and Li2016) and (e) sea level change (Saito et al. Reference Saito, Katayama, Ikehara, Kato, Matsumoto, Oguri, Oda and Yumoto1998). The blue bars show the intervals of YD and H1.

Sediment input from the Japanese Islands was mainly linked to the land erosion controlled by local rainfall and snowfall, as well as sea level change. The abundances of EM2 and EM3 are roughly coherent with the winter rainfall record based on pollen in Biwa Lake and speleothem δ18O record from Maboroshi Cave, suggesting increased sediment supply under enhanced local rainfall (Figure 5a). It should be noted that this pollen record shows weak fluctuations during deglacial cold events, probably due to the long distance of Biwa Lake from Japan Sea. Despite the glacial depletion of Maboroshi Cave δ18O was ascribed to changes in seasonality of precipitation, larger fractionation under lower temperature or a longer vapour trajectory due to exposed sea shelf, the almost anti-phased relationship between Maboroshi and Chinese cave δ18O record, which also received water vapour generated in lower glacial temperature across the wide exposed sea shelf, indicating increased seasonal rainfall (weakened EASM but enhanced EAWM rainfall (Figure 5a and d)) probably was the main reason of δ18O variation in southwestern Japan. Basically, rainfall in the Japan Sea side of the Japanese Islands mainly depends on EAWM and SST of the Japan Sea. Modern observation data suggest that anomalous high SSTs in the Japan Sea can strengthen the upward heat and moisture flux and the air-mass modification, and thus significantly related to the rainfall or snowfall on the island (Sone et al. Reference Sone, Kano, Okumura, Kashiwagi, Hori, Jiang and Shen2013; Takano et al. Reference Takano, Tachibana and Iwamoto2008). However, the distinct relationship between sediment input reconstructed with abundances of EM2 and EM3 and Japan Sea SST record indicates their weak links (Figure 5a and c). Besides, the warming-induced spring melting of winter snow can also cause higher sediment supply. However, our results are not consistent with the Japan Sea SST record, suggesting that the temperature-induced melting is not the first controlling factor of sediment supply (Figure 5a and c). Generally, the EM2 and EM3 abundances suggest a similar trend compared with the EAWM records in the Chinese Loess Plateau, Okinawa Trough and Yellow Sea, as well as the model simulation (Figure 5a and b), indicating the strong control of EAWM on local rainfall and sediment input from the island to Japan Sea.

Almost anti-phased relationship between EM2 and EM3 abundances and EASM suggests the insignificant roles of EASM in sediment supply from the Japanese Islands (Figure 5a and d). The westerlies can also have an impact on local rainfall through the East Asian Meiyu-Baiu fronts. However, our study region is located on the northern edge of the Meiyu-Baiu fronts, which receive its effects in July (Li et al. Reference Li, Deng, Yang and Zhang2018). This only results in a slight increase in local rainfall during summer season (Figure 1b). Therefore, the meridional shifts of westerlies should have less influence on local hydroclimate compared to the EAWM. Besides, the water depth (∼330 m) of our study site is beyond the sea level fluctuation range (∼120 m) during glacial-interglacial cycles. Combined with the narrow shelf of Honshu Island (Figure 1a), the estuary advances and retreats along with sea level changes should have small effects on the terrestrial materials input to the Japan Sea. This can be verified by the absence of negative relationship between sea level change and EM2 and EM3 abundances since the LGM (Figure 5a and e). It should be noted that deglacial rapid sea level rise-induced sediment reworking probably also contributes to increased EM2 and EM3 abundances from ∼15 to 10 ka (Figure 5a and e). Enhanced anthropogenic activities, e.g. agriculture, have also been proposed as a strong force in driving land weathering and erosion (Pei et al. Reference Pei, Wan, Clift, Cai, Zhao, Zhang, Jiao, Ju, Song and Li2023). However, large scale of population increases and agriculture activities in Japan mainly started after 3 ka BP (Crawford, Reference Crawford2011; Mizuno et al. Reference Mizuno, Gojobori, Kumagai, Baba, Taniguchi, Kondo, Matsushita, Matsushita, Matsuda, Higasa, Hayashi, Wang, Kurosaki and Ueda2021) and thus probably contributed only a small part of increasing in sediment supply from Honshu Island to the Japan Sea since the early Holocene.

As a result, the grain-size index of EM2 and EM3 abundance was interpreted as an EAWM proxy in the Japan Sea. Combined with other EAWM records, we found the EAWM in the northern East Asia and its marginal seas suggest weakened long-term trend during ∼24–17.5 ka and ∼11.8–8 ka and strengthened during ∼17.5–15 ka and since ∼8 ka. On the millennial scale, an intensified EAWM was found during the Heinrich 1 (H1) and Younger Dryas (YD) cooling events and weakened during the Bølling-Allerød (B-A) warming event (Figure 5a and b).

5.c. High-low latitude interaction forcing on the EAWM

To investigate the regional heterogeneity of EAWM evolution and its forcing mechanisms since the LGM, the EAWM records in the northern regions of East Asia and marginal seas have been compared with that in the South China Sea, Northern Hemisphere winter insolation, NGRIP δ18O record and low-latitude ENSO records (Figure 6a–d). A striking phenomenon is that the northern and southern EAWM records exhibit the same evolvement both on the long-term trend and millennial scale from the LGM to ∼8 ka, but towards the anti-phased relationship with a strengthened northern EAWM but weakened one in the southern region since ∼8 ka.

Figure 6. Comparison between EAWM with its potential forcing mechanisms. (a) NGRIP δ18O record (Andersen et al. Reference Andersen, Azuma, Barnola, Bigler, Biscaye, Caillon, Chappellaz, Clausen, Dahljensen and Fischer2004) and winter insolation in 35°N (Laskar et al. Reference Laskar, Robutel, Joutel, Gastineau, Correia, Correia and Levrard2004). (b) EAWM reconstructions and simulation in the northern East Asia and its marginal seas. (c) EAWM reconstructions and simulation in the southern China and South China Sea (Huang et al. Reference Huang, Tian and Steinke2011; Huang et al. Reference Huang, Wang, Wei, Yuan and Tian2023; Wen et al. Reference Wen, Liu, Wang, Cheng and Zhu2016; Zhao et al. Reference Zhao, Wan, Song, Gong, Zhai, Shi and Li2019). (d) ENSO reconstructions and simulation (Clement et al. Reference Clement, Seager and Cane2000; Conroy et al. Reference Conroy, Overpeck, Cole, Shanahan and Steinitz-Kannan2008; Liu et al. Reference Liu, Lu, Wen, Otto-Bliesner, Timmermann and Cobb2014b; Moy et al. Reference Moy, Seltzer, Rodbell and Anderson2002). (e) Regression coefficients of the 850-hPa wind (vectors in m/s) and rainfall anomalies (shadings in mm/day) with respect to the December, January and February (DJF) mean Niño-3.4 index for the midwinter (Geng et al. Reference Geng, Noh, Kim and Kug2023). The EAWM records in the northern and southern regions are shown with dots and squares, respectively. Orange, red and blue boxes show the regions of model simulation. (f) Regression coefficients of the 850-hPa wind (vectors in m/s) and 500-hPa geopotential height anomalies (shadings in m) with respect to the DJF mean Niño-3.4 index for the midwinter (Geng et al. Reference Geng, Noh, Kim and Kug2023).

The long-term trend evolution of EAWM can be linked to the winter solar insolation (Huang et al. Reference Huang, Tian and Steinke2011; Huang et al. Reference Huang, Wang, Wei, Yuan and Tian2023; Wen et al. Reference Wen, Liu, Wang, Cheng and Zhu2016). As perihelion shifts from boreal summer to winter, the insolation is reduced in the Northern Hemisphere in winter. This leads to a cooling and higher pressure over the East Asian continent relative to the surrounding oceans and thus a stronger northerly wind. Both the northern and southern EAWMs are generally anti-correlated with the winter insolation before ∼8 ka (Figure 6a–c). After ∼8 ka, the increased winter insolation probably also plays a role in controlling the weakened southern EAWM but cannot explain the strengthened northern EAWM (Figure 6a–c). Such strengthened northern EAWM since the early Holocene has been recently interpreted with the increased meridional temperature gradient between the Siberian High and Equatorial Low (Kang et al. Reference Kang, Du, Wang, Dong, Wang, Wang, Qiang and Song2020).

On the millennial scale, the intensified Northern and southern EAWMs during cold H1 and YD events were coeval with the shutdown or a reduction in strength of the AMOC (Figure 6a–c), indicating a strong linkage between the AMOC and the EAWM through changes in the meridional temperature gradient and Northern Hemisphere westerlies (Huang et al. Reference Huang, Tian and Steinke2011; Sun et al. Reference Sun, Clemens, Morrill, Lin, Wang and An2012). However, the northern and southern EAWMs were all not strong enough as expected during the LGM but went for a maximum until the deglacial (Figure 6b and c). Actually, such relatively weak EAWM during LGM compared to deglacial has also been found in the Gulang (Sun et al. Reference Sun, Clemens, Morrill, Lin, Wang and An2012) and Luochuan (Hao et al. Reference Hao, Wang, Oldfield, Peng, Qin, Song, Xu, Qiao, Bloemendal and Guo2012) loess section in Chinese Loess Plateau within dating uncertainties. The relatively stronger AMOC strength during LGM compared to that during H1 and YD events (Huang et al. Reference Huang, Tian and Steinke2011), combined with the high winter insolation during this period probably accounted for such weak EAWM condition.

However, the anti-phased relationship between the northern and southern EAWM can hardly be explained by the insolation and/or northern high-latitude climate forcing (Figure 6b and c). Here we introduced the low-latitude ENSO processes to explain such regional heterogeneity. A modern climate modelling with CCSM3 suggested that a mature phase of El Niño in winter would lead to a strengthened EAWM over the northern East Asia but a weakened one over the south, through the reversed anomalous geopotential height and wind anomalies between the northeastern regions of East Asia and South China Sea, respectively (Sun & Yang, Reference Sun and Yang2005). Recently, such modes among ENSO, cyclone/anticyclones and EAWM system have also been found during the midwinter based on observational and reanalysis datasets (Geng et al. Reference Geng, Noh, Kim and Kug2023) (Figure 6e and f). During the El Niño midwinter, the abrupt North Atlantic Oscillation (NAO) phase transition from positive to negative leads to a rapid adjustment of the mid-latitude atmospheric circulation via wave eastward propagation along the mid-latitude jet. This leads to a strengthened Siberian high, combined with the anomalously negative geopotential height centred over the northeastern part of East Asian marginal seas, producing northwesterly wind anomalies and thus strong EAWM over northern East Asia (Figure 6f), which bring enhanced rainfall and snowfall in the Japan Sea and the Japan Sea side of the Japanese Islands (Figure 6e). In contrast, the anomalous Philippine Sea anticyclone shifts southward and results in the anomalous southwesterlies, and thus a weakened EAWM in the South China Sea.

Such ENSO-EAWM mode can well explain the observed anti-phased relationship between northern and southern EAWMs since ∼8 ka. Enhanced El Niño amplitude since ∼8 ka resulted in a strengthened northern EAWM but a weakened southern EAWM (Figure 6b–d). This low-latitude ENSO forcing on the regional heterogeneity of EAWM evolution has also been proposed in a previous study in the northern Okinawa Trough (Zhao et al. Reference Zhao, Wan, Song, Gong, Zhai, Shi and Li2019). Even the El Niño amplitude also enhanced during the LGM, H1 and YD periods, we proposed that the North Atlantic climate signals were strong enough in dominating the EAWM system, and thus produced the coherent variations of EAWMs in the entire regions of East Asia and marginal seas (Figure 6b–d). In the context of global warming, increased frequency of extreme El Niño and La Niña events will very likely enlarge the spatial discrepancies of EAWM intensities (Cai et al. Reference Cai, Borlace, Lengaigne, Rensch, Collins, Vecchi, Timmermann, Santoso, Mcphaden and Wu2014; Cai et al. Reference Cai, Wang, Santoso, Mcphaden, Wu, Jin, Timmermann, Collins, Vecchi and Lengaigne2015) and lead to higher frequencies of extremely cold/warm winter in this region. Our findings highlight the role of tropical forcing in East Asian climate change through ocean-atmosphere interactions and have important implications for future projections of winter climate in this densely populated region.

6. Conclusion

Based on the sediment input from the Japanese Islands to the southern Japan Sea, we reconstruct the history of the EAWM in the northern East Asian marginal sea since the LGM. We found a synchronous relationship between winter monsoons in northern and southern regions of East Asia from ∼24 to 8 ka, but anti-correlated relationship since ∼8 ka. We proposed the winter insolation and AMOC were the main drivers for the long-term and millennial scale of variations from last glacial to early Holocene, and then ENSO became a dominant factor in controlling the regional heterogeneity of EAWM evolution through ocean-atmosphere interactions in the middle and late Holocene.

Supplementary material

To view supplementary material for this article, please visit https://doi.org/10.1017/S0016756824000190

Acknowledgements

We acknowledge the Integrated Ocean Drilling Program and the scientific party and technicians of IODP Expedition 346 for obtaining the samples. We also thank editor Peter D. Clift and two anonymous reviewers for their help and constructive comments to improve this manuscript. This research was funded by National Key Research and Development Program of China (2022YFF0800504), National Natural Science Foundation of China (42176063) and Strategic Priority Research Program of the Chinese Academy of Sciences, China (XDB40010100).

Competing interests

The authors declare none.

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Figure 0

Figure 1. (a) Map showing the location of the IODP Site U1427 (red dots), bathymetry of the Japan Sea and the flow of surface currents (yellow arrow lines). The referenced ocean sites and lake pollen and speleothem records are shown with orange dots and purple squares, respectively. EAWM, EASM and Northern Hemisphere subtropical westerlies are shown with blue, red and purple arrows, respectively. White lines show rivers on the Japanese Islands. Abbreviations of East Asian monsoon, ocean currents and straits are also shown. (b) Monthly rainfall at the Hiraiwa Precipitation Observatory and temperature at Itoigawa (Sone et al.2013) in the Japan Sea side of the Japanese Islands are shown with purple triangles in (a). (c) Mean annual dust flux in the Eurasia and North Pacific (Kok et al.2021). Numbers show the deserts in the northern China, which were divided into three regions: Deserts A, B and C (Chen et al.2007).

Figure 1

Table 1. Radiocarbon dating and correlation points between reflectance b* and NGRIP δ18O

Figure 2

Figure 2. Age model of the top 7.75 m of the Hole A sediments at IODP Site U1427. The layers and their corresponding AMS 14C dates are shown with yellow squares and red diamonds with black error bars, respectively, connected by red dotted lines. The blue dotted lines show the correlations between (a) NGRIP δ18O and (b) sediment reflectance b*.

Figure 3

Figure 3. End-member modelling results of Site U1427 grain-size data. (a) Coefficients of determination (R2) for each size class of models with 1–5 end-members. (b) Angular differences (in degrees) between the reconstructed and observed datasets as a function of the number of end-members. (c) Modelled three end-members of the terrigenous sediment fractions from Site U1427. (d) Variations of end-member abundances of EM1–EM3 during the last ∼24 ka.

Figure 4

Table 2. Sr-Nd isotopic composition of 2–32 μm and 32–63 μm fractions in IODP Site U1427 sediments

Figure 5

Figure 4. Provenance of 2–32 μm and 32–63 μm fractions from Site U1427 sediments based on the Sr-Nd isotopic composition. (a) Comparison with fine-grained end-members of potential source areas. (b) Comparison with coarse-grained end-members of potential source areas. Data sources: Japanese rivers (Goldstein & Jacobsen, 1988; Shen et al.2017), Japanese rocks (Kagami et al.1992), Deserts A, B and C (Chen et al.2007), Gobi Desert (Biscaye et al.1997; Zhao et al.2015), Chinese loess (Chen et al.2007; Zhao et al.2017), Yangtze River (Meng et al.2008; Yang et al.2007; Zhao et al.2017), Yellow River (Hu et al.2012; Meng et al.2008; Zhao et al.2017), Korean river (Lee et al.2008; Lim et al.2015).

Figure 6

Figure 5. Comparison between (a) Japanese sediment input index established with EM1 and EM2 abundances with speleothem δ18O record from the Maboroshi Cave (Kato et al.2021) and winter rainfall record in Lake Biwa (Kigoshi et al.2014), and (b) EAWM (Hao et al.2017; Kang et al.2020; Liu et al.2020; Zhao et al.2019; Zheng et al.2014), (c) Japan Sea SST (Fujine et al.2009; Liu et al.2014a), (d) EASM (Cheng et al.2016) and (e) sea level change (Saito et al.1998). The blue bars show the intervals of YD and H1.

Figure 7

Figure 6. Comparison between EAWM with its potential forcing mechanisms. (a) NGRIP δ18O record (Andersen et al.2004) and winter insolation in 35°N (Laskar et al.2004). (b) EAWM reconstructions and simulation in the northern East Asia and its marginal seas. (c) EAWM reconstructions and simulation in the southern China and South China Sea (Huang et al.2011; Huang et al.2023; Wen et al.2016; Zhao et al.2019). (d) ENSO reconstructions and simulation (Clement et al.2000; Conroy et al.2008; Liu et al.2014b; Moy et al.2002). (e) Regression coefficients of the 850-hPa wind (vectors in m/s) and rainfall anomalies (shadings in mm/day) with respect to the December, January and February (DJF) mean Niño-3.4 index for the midwinter (Geng et al.2023). The EAWM records in the northern and southern regions are shown with dots and squares, respectively. Orange, red and blue boxes show the regions of model simulation. (f) Regression coefficients of the 850-hPa wind (vectors in m/s) and 500-hPa geopotential height anomalies (shadings in m) with respect to the DJF mean Niño-3.4 index for the midwinter (Geng et al.2023).

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