- Paper with full data attached
- Open Access
Changes in surface water masses in the northern East China Sea since the Last Glacial Maximum based on diatom assemblages
Progress in Earth and Planetary Science volume 8, Article number: 66 (2021)
We investigated diatom assemblages for the last 19 ka in a piston core KY07-04 PC01 collected from the northern Okinawa Trough, East China Sea. Most of the diatom taxa in the Core KY07-04 PC01 were subtropical to temperate marine species throughout the core. Pronounced turnover of major diatom groups from periphytic to planktonic taxa occurred during deglaciation between 17 and 14 ka ago. During the Last Glacial Maximum (LGM) to early deglaciation, the representative taxa were Paralia spp., a periphytic diatom abundant in continental shelves of the modern East China Sea covering the Chinese Coastal Water. Relative abundances of Paralia spp. rapidly decreased during 15–14 ka ago, corresponding to sea-level rise, displaced by planktonic taxa such as Thalassionema. Thalassionema nitzschioides varieties living in subtropical water increased since 12 ka and have reached the present level at 8 ka ago, suggesting strengthening the influences of Kuroshio water in the northern East China Sea during the early to middle Holocene. Warm planktonic diatom taxa such as Nitzschia bicapitata also gradually increased from 12 to 8 ka ago. Near the core top, a sudden increase in N. bicapitata might relate to the intensifying Kuroshio during the latest Holocene.
The East China Sea is a marginal sea of the western North Pacific bordered by the Kyushu, the Ryukyu Islands, and Taiwan. The East China Sea connects with the Japan Sea via the Tsushima Strait (~ 130 m sill depth) and the South China Sea via the Taiwan Strait (less than 100 m in depths). The East China Sea is composed of two areas: continental shelves (< 200 m water depth) in the northwest, including the Yellow Sea, and the Okinawa Trough (1000–2200 m water depth) in the southeast (Fig. 1). The Yellow River (Huanghe) and the Yangtze River (Changjiang) discharge into the East China Sea, providing much fresh water and suspended particles. The Yellow River is the second largest river globally in suspended sediment load (Milliman and Meade 1983). The Yangtze River supplies about 80% of the total discharge of freshwater from rivers flowing into the East China Sea, playing a critical role in sea-surface salinity distribution of the continental shelves of the East China Sea (Ichikawa and Beardsley 2002).
Bathymetry constrains the distribution of surface water masses and oceanic fronts in the East China Sea (Ichikawa and Beardsley 2002). The Kuroshio is a western boundary current of the North Pacific, playing an essential role in poleward heat transport (Qiu 2019). The Kuroshio flows northward and enters the East China Sea through the channel between Taiwan and Yonaguni-Jima. In the East China Sea, the Kuroshio path follows closely along the steep continental slope and changes the direction to the east around ~ 30°N, flowing out to the Philippine Sea through the Tokara Strait. As a result, warm, saline, and nutrient-depleted Kuroshio water occupies the southern and central Okinawa Trough. The Tsushima Warm Current flows northward and enters the Japan Sea through the Tsushima Strait. The Taiwan Warm Current flowing northward through the Taiwan Strait and onshore Kuroshio intrusion across the East China Sea shelf break is the source of the Tsushima Warm Current (Isobe 2008). This warm water prevails in the northern Okinawa Trough. The Chinese Coastal Current flows southward along the Chinese coast on the continental shelves of the western East China Sea, mixing the Yangtze River discharge (Ichikawa and Beardsley 2002). Thus, cold, less saline, and nutrient-rich Chinese Coastal water distributes in the continental shelf regions of the East China Sea.
The East China Sea has experienced marked geographic changes with the sea-level rise since the LGM. During the LGM between 21 and 17 ka ago, sea-level was estimated to be − 125 to − 130 m (Yokoyama et al. 2018), leading to aerial exposure of most East China Sea continental shelves, closure of the Taiwan Strait, and constriction of the Tsushima Strait. Such major geographic changes must have led to changes in the distribution and circulation of surface water in the East China Sea. There is a line of evidence for low sea-surface temperature (SST) widely observed over the glacial East China Sea (Ijiri et al. 2005; Sun et al. 2005; Chang et al. 2009a; Yu et al. 2009; Chen et al. 2010; Kubota et al. 2010, 2015b; Xu et al. 2013; Ujiié et al. 2016; Matsuzaki et al. 2019), expansion of the Chinese Coastal Water (Xu and Oda 1999), advancement of river mouths of the Yellow River (Xu et al. 2014; Zheng et al. 2016; Zhao et al. 2017, 2018; Beny et al. 2018) and the Yangtze River (Dou et al. 2010a, b, 2012). Most previous studies indicated weakened the Kuroshio Current during the LGM. At the same time, Kawahata and Ohshima (2004) suggested an intrusion of the Kuroshio Current into the northern East China Sea during the LGM based on the occurrence of pollen Phyllocladus, celery pines originated in New Guinea and Southeast Asia. The glacial path is controversial as reviewed by Gallagher et al. (2015) whether the southward migration occurred (Ujiié et al. 2003; Su and Wei 2005; Kao et al. 2006; Dou et al. 2010a, b, 2012, 2016; Lim et al. 2017; Li et al. 2018; Ma et al. 2021) or the path remained similar to the modern position (Lee et al. 2013; Zheng et al. 2016; Vogt‐Vincent and Mitarai 2020).
Diatoms are unicellular photosynthetic eukaryotes producing biogenic opal frustules found in nearly all marine and freshwater habitats. They are one of the most major primary producers playing essential roles in the carbon and silicon cycles of the ocean (Smol and Stoermer 2010). A great diversity of species is living by sensitively responding to the aquatic environmental changes. In the modern East China Sea, characteristic diatom assemblages are dwelling in response to the water masses changes and the with pronounced seasonality (Asaoka 1975, 1980; Oh and Koh 1995; Furuya et al. 1996; Chiang et al. 1999; Ishikawa and Furuya 2004; Guo et al. 2014; Li et al. 2014; Chen et al. 2019b). Although the East China Sea is befitting for reconstructing changes in surface water masses, a few paleoceanographic studies employing diatom assemblages are available. Chang et al. (2009b) presented a diatom assemblage record in Core MD01-2404 from the central part of the Okinawa Trough for the past 100 ka at millennial timescales. The diatom record in Core MD01-2404 seemed to be synchronous with the millennial-scale climate changes in the high-latitude Northern Hemisphere during the glacial-deglacial periods. Tanimura et al. (2002) employed a periphytic diatom, Paralia sulcata, in Core KH82-4 St-14 from the northern Okinawa Trough to discuss the expansion and retreat of the Chinese Coastal Water since the LGM with centennial timescales. They found abundant Paralia sulcata during the LGM to early glacial termination, which suggested significant expansion of the Chinese Coastal Water during then. Li et al. (2012, 2015) investigated diatom assemblages in Core MD05-2908 from the southern Okinawa Trough at decadal resolutions for the past six ka. These studies have revealed that diatom assemblages are helpful to reconstruct past surface environmental changes of the East China Sea. However, a high-resolution whole assemblage record since the LGM has not yet been available in the East China Sea. Unfortunately, these previous studies (both modern and paleo) presented minimal taxonomic information and photos using a light microscope (LM). Only Li et al. (2014) presented scanning electron microscope (SEM) images for several Thalassiosira taxa.
We present the whole diatom assemblages record and their LM and SEM images in Core KY07-04 PC01 from the northern Okinawa Trough since the LGM at centennial timescales. Available high-resolution geochemical proxy records such as oxygen isotopes and Mg/Ca SST in Core KY07-04 PC01 allow us to directly compare the diatom assemblage and the geochemical dataset (Kubota et al. 2010, 2015b). The purpose of this study is to clarify changes in surface water masses such as the Kuroshio Current and the Chinese Coastal Water from the semi-closed LGM to the present via deglacial sea-level rise.
Materials and methods
Core KY07-04 PC01 and its age model
A piston core sample KY07-04 PC01 was obtained from a water depth of 758 m on the northern slope of the Okinawa Trough, East China Sea (31° 38.35ʹ N, 128° 56.64ʹ E) during the R/V Kaiyo KY07-04 cruise in February 2007 (Fig. 1). Core KY07-04 PC01 consists of homogeneous olive to gray silty clay with two ash layers (Kubota et al. 2010). The widespread tephra identified the upper ash layer between 408.5 and 488.5 cm in core depth as the Kikai‐Akahoya (K-Ah; erupted at 7.3 ka ago).
The age model of KY07-04 PC01 was established based on 18 radiocarbon dating of planktic foraminiferal shells and tephrochronology by Kubota et al. (2010). This study revised the Core KY07-04 PC01 age model with 26 radiocarbon dating of planktic foraminiferal shells (Table 1). New radiocarbon dates for eight samples during the middle to late Holocene interval were measured by the National Electrostatics Corporation 250 kV single-stage accelerator mass spectrometry at Atmosphere and Ocean Research Institute, The University of Tokyo (Yokoyama et al. 2019). We conducted radiocarbon calibration to convert radiocarbon age to calendar age using CALIB 8.2 (Stuiver et al. 2021) with the Marine20 calibration curve (Heaton et al. 2020). Local marine reservoir age (ΔR) was estimated as − 200 ± 100 yr from 33 data from the East China Sea coast (Konishi et al. 1982; Kong and Lee 2005; Hideshima et al. 2001; Southon et al. 2002; Yoneda et al. 2007; Hirabayashi et al. 2017)) in 14CHRONO Marine20 reservoir correction database. The K-Ah tephra age was 7252 ± 56 yr, estimated from Lake Suigetsu varve sediment (McLean et al. 2018). Based on the radiocarbon and K-Ah tephra dates, the revised age model of Core KY07-04 PC01 was established (Table 1; Fig. 2). The revised age model is consistent with the previous one by Kubota et al. (2010). Its continuous sedimentation with a high sedimentation rate of ~ 80 cm kyr−1 ensures Core KY07-04 PC01 for centennial to millennial scales paleoceanographic study.
Microscopic observation for diatoms
Core KY07-04 PC01 samples were sliced at 2.5 cm intervals and stored in a refrigerator. A total of 72 subsamples taken at ~ 20 cm intervals were taken for diatom assemblage work and freeze-dried with an EYELA FDU-1200 freeze-dryer. Approximately 1 mg of the freeze-dried sample was treated with 25 mL of 30% hydrogen peroxide at hydrogen peroxide on a hot plate with top plate temperature set to 100 °C for about 1 h to digest organic matter. After the reaction was complete, Millipore-Elix water was added to a total volume of 200 mL and allowed to stand for 8 h. The removal of supernatant was removed, and Millipore-Elix water was added again. The following is a procedure of slides for LM observation. The pretreated suspended solution of each sediment sample was drawn by 2 mL plastic pipette, dropped on cover glass (24 × 40 mm), and dried on a hot plate with top plate temperature set to 40–50 °C. Pleurax (Mount Media, Wako Pure Chemical Industries, Tokyo, Japan) was dropped on the cover glass and mounted on the glass slide at 120 °C. LM observations were performed at magnifications of × 1000 using Olympus BX53 and BX50 bright-field microscopes to identify and count diatoms in Core KY07-04 PC01 samples. Counting of diatom valves was performed as follows: (1) for centric diatoms, a valve with a central part was counted as one valve; and (2) for pennate diatoms, a valve with an apical part was counted as 0.5 valves. More than 200 diatom valves were counted for diatom assemblage analyses of Core KY07-04 PC01 samples (Additional file 1: Tables S1 and S2).
Sample preparation for SEM observation is described as follows. The pretreated suspended solution of each sediment sample was filtered through an Advantec membrane filter (0.45 µm pore size, 47 mm diameter), rinsed with Millipore-Elix water, and dried. The filter samples were cut into 6 mm × 6 mm squares, mounted onto brass stubs with carbon tape, and coated with OsO4 using an osmium coater (Neoc-STB; Meiwafosis Co. Ltd., Tokyo, Japan). A field-emission scanning electron microscope (FE-SEM, JMS-7001F; JEOL Ltd., Akishima, Japan) was used for detailed taxonomic work of the diatoms. The acceleration voltage was set at 5 kV.
Identification and counting were conducted at the species level as much as possible. Images of observed major diatom taxa are shown in Additional file 2: Plates 1–6 in the supplement. We counted specimens belonging to the genus Paralia as Paralia spp. Paralia spp. include several species such as P. sulcata, P. fenestrata, P. longispina, P. allisonii, P. crawfordii, P. ehrmanii, and P. obscura (Hasle and Syvertsen 1997; Sawai et al. 2005; Konno and Jordan 2008; MacGillivary and Kaczmarska 2012, 2013). The morphology of encountered Paralia specimens in Core KY07-04 PC01 often had intermediate features between the species and was hard to identify by LM observation. Genus Thalassionema was one of the most abundant diatoms in Core KY07-04 PC01 samples. This study classified Thalassionema into six species, four varieties, and two morphological types (Table 2; Additional file 2: Plate 4–6) following to Hasle and Syvertsen (1997), Tanimura (1999), Hasle (2001), Tanimura et al. (2007) and Akiba et al. (2014). The diatom taxa were grouped by their lifestyle (periphytic, planktonic), habitats (freshwater, brackish, marine), and geographic distributions (coastal, cold, warm) based on Round et al. (1990), Hasle and Syvertsen (1997), and Koizumi (2008) (Table 2).
One hundred twenty-five diatom taxa were observed in Core KY07-04 PC01 samples (Table 2). Paralia, Thalassionema, and Nitzschia were the most abundant diatom genus in Core KY07-04 PC01 samples (Fig. 3). Paralia (periphytic) was the dominant genus before 14 ka ago, whereas Thalassionema and Nitzschia (planktonic) were abundant after 14 ka ago.
At the species level, downcore profiles of diatom taxa with greater than 4% at least in a sample were shown (Fig. 3). Paralia spp., periphytic coastal diatom taxa, was representative in Core KY07-04 PC01 samples before 14 ka ago, exceeding 30% during the LGM and early deglaciation from 19 to 15 ka ago (Fig. 3). Another periphytic coastal diatom species, Delphineis surirella, showed a similar pattern with Paralia spp., with high relative abundances before 16 ka ago (Fig. 3). Relative abundances of Nitzschia bicapitata, a major planktonic warm species, were high from the deglacial period to middle Holocene and the core top of Core KY07-04 PC01 (Fig. 3). Thalassionema species and varieties presented various downcore profile patterns in Core KY07-04 PC01 (Fig. 3). Morphological varieties of Thalassionema nitzschioides were persistently high percentages throughout the core. Among the T. nitzschioides varieties, three varieties (var. incurvatum, var. inflatum, and var. parvum) increased during the middle-late Holocene. On the other hand, Thalassionema frauenfeldii sensu stricto (s.s.) and Thalassionema synedriforme were relatively high during the deglacial period.
Figure 4 shows diatom groups by habitats (freshwater and brackish) and geographic distributions (coastal, cold, warm) in Core KY07-04 PC01. During the LGM, periphytic diatoms, mostly Paralia spp., were predominant, whereas planktonic diatoms were the minority. During the deglacial pronounced turnover between 18 and 14 ka ago, Planktonic diatoms became the majority in Core KY07-04 PC01. With the turnover, coastal diatoms decreased significantly. Note that contributions of freshwater and brackish water diatoms have been small in total assemblage even during the LGM and early deglaciation (Fig. 4). Marine diatoms were the majority in the diatom assemblages in Core KY07-04 PC01 since the LGM. Planktonic warm water diatom group gradually increased from 18 to 12 ka ago, occupying ~ 40% for the last 12 ka.
Diatom assemblages as paleoenvironmental indicators
Throughout the core, marine diatoms were dominant, suggesting that the northern Okinawa Trough has been a marine environment and limited fresh/brackish water influences even during the LGM. This is consistent with the previous study reporting the continuous occurrences of planktic foraminifera (Xu and Oda 1999; Ijiri et al. 2005) and radiolarians (Matsuzaki et al. 2019) during the LGM in the northern East China Sea. Periphytic diatom Paralia spp. were dominant in the Core KY0704 PC01 during the LGM. Previous studies in the modern and past East China Sea referred to as Paralia sulcata, equivalent to Paralia spp. in the present study (Asaoka 1980; Oh and Koh 1995; Furuya et al. 1996; Tanimura et al. 2002; Chang et al. 2009b; Ishikawa and Furuya 2004; Guo et al. 2014; Yuan et al. 2014; Chen et al. 2019b). Paralia spp. distributes on muddy sediments of the Japanese coast with salinity ranging from 11 to 34 (Sawai et al. 2005). In the modern East China Sea and the Yellow Sea, Paralia spp. dwells on the continental shelves as a representative coastal water indicator throughout the year (Asaoka 1980; Furuya et al. 1996; Ishikawa and Furuya 2004; Guo et al. 2014; Yuan et al. 2014; Chen et al. 2019b), including the eutrophic coastal area of the Yellow Sea (Di et al. 2013; Liu et al. 2013). Asaoka (1980) revealed that Paralia spp. distributions in summer were almost synchronous with suspended mud deposited on the central part of East China Sea continental shelves. Furuya et al. (1996) and Ishikawa and Furuya (2004) reported dominant Paralia spp. in the inner shelf area (< 70 m water depth) by active vertical mixing in winter and spring, respectively. Guo et al. (2014) presented the seasonality of diatom assemblages and the abundances in the continental shelf area of the East China Sea. Based on their study, Paralia spp. was one of the most abundant diatom taxa in spring, fall, and winter. On the other hand, the occurrence of Paralia spp. was low in summer. These modern observations have clarified that abundant Paralia spp. occurrences in the nutrient-rich shelf water of the East China Sea with temperatures ranging from 11 to 20 °C and salinity from 33.5 to 34.5. This water-mass property corresponds to the water mass properties of Chinese coastal water (Ichikawa and Beardsley 2002). Paralia spp. is transported with suspended mud from the coastal area/continental shelves to the northeastern East China Sea.
Tanimura et al. (2002) investigated Paralia spp. abundances in KH82-4 St-14 piston core (31° 44.4ʹ N, 129° 02.1ʹ E, 740 m water depth) adjacent to KY07-04 PC01. They found abundant Paralia spp. occurrences from 19 to 13 cal ka BP (16–10 ka BP in 14C age shown in Tanimura et al. (2002), suggesting a significant expansion of Chinese coastal water sea-level drop during the LGM to early deglaciation. A similar but much smaller (up to 20%) abundance peak during the LGM to early deglaciation was observed at Core MD01-2404 in the southwestern Okinawa Trough (Chang et al. 2009b). Delphineis surirella, a periphytic coastal diatom species that dwell in the subtidal zone (Zong and Horton 1999; Sawai et al. 2009), showed relatively high abundances during 19–14 ka ago, presenting a similar pattern with Paralia spp. (Fig. 3). These consistently support the expansion of Chinese coastal water during the LGM to early deglaciation.
In Core KY-07-04 PC01, planktonic diatom Thalassionema was the dominant diatom genus since 14 ka ago (Fig. 3). This study classified Thalassionema into six species, four varieties, and two morphological types (Table 2; Fig. 3) following the previous studies (Hasle and Syvertsen 1997; Tanimura 1999; Hasle 2001; Tanimura et al. 2007; Akiba et al. 2014). Thalassionema nitzschioides is known as a cosmopolitan planktonic species (Hasle 2001). In the East China Sea, occurrences of Thalassionema nitzschioides have been reported from the Yellow Sea, the continental shelves, and the Okinawa Trough (Asaoka 1975, 1980; Oh and Koh 1995; Furuya et al. 1996; Chiang et al. 1999; Ishikawa and Furuya 2004; Guo et al. 2014). In particular, Thalassionema nitzschioides was abundant near the shelf break (Furuya et al., 1996; Chiang et al., 1999; Ishikawa and Furuya, 2004; Guo et al., 2014).
Tanimura et al. (2007) indicated that each Thalassionema nitzschioides species and varieties showed specific geographical distributions in the North Pacific: T. nitzschioides var. nitzschioides and T. pseudonitzschioides in the Subarctic Gyre; T. nitzschioides var. incurvatum, var. inflatum, and var. parvum in the Subtropical Gyre. Tanimura (1999) proposed a ratio of three T. nitzschioides varieties (var. incurvatum, var. inflatum, and var. Parvum) in Thalassionema nitzschioides complex (hereafter refers as T-ratio) as an index for Kuroshio intensity based on sediment trap experiments in the Kuroshio path, western North Pacific. Tanimura (1999) exhibited temporal changes in T-ratio and distance from the Kuroshio (the shortest distance from the trap station to the Kuroshio path). When Kuroshio migrated to the north, the sediment trap station was covered with subtropical water where the three T. nitzschioides varieties were abundant. In Core KY-07-04 PC01, T-ratio has increased since 12 ka ago and has reached its present level since 8 ka ago (Fig. 5), which is consistent with the timings of northward migration of Kuroshio in the western North Pacific (Takemoto and Oda 1997; Tanimura 1999; Yamamoto et al. 2005) and intensification of Tsushima Warm Current flowing into the Japan Sea (Gallagher et al. 2015; Yokoyama et al. 2006), respectively. A typical dark color layer in many deep-sea sediment cores from the Japan Sea with high organic carbon contents, called TL1, is seen when the Tsushima Warm Current intrusion was re-established since the LGM (Oba et al. 1991; Tada et al. 1999; Yokoyama et al. 2006). Thus, the T-ratio increase suggests strengthening the influence of Kuroshio Current water in the northern East China Sea.
Tanimura et al. (2007) recognized nine species, varieties, and morphological types of Thalassionema nitzschioides. Akiba et al. (2014) described the Nd morphological type of Thalassionema nitzschioides sensu lato (s.l.) as a new species Thalassionema umitakae. The distribution of T. umitakae in the North Pacific is mainly in the subarctic region but a few occurrences in the subarctic boundary of the western North Pacific (Tanimura et al. 2007). Abundant occurrences of T. umitakae were reported in the glacial Japan Sea (Akiba et al. 2014). In Core KY07-04 PC01, T. umitakae occurred throughout the core since the LGM with no pronounced trend (Fig. 3), implying no significantly cold surface water covered in the northern Okinawa Trough even during the LGM.
Thalassionema frauenfeldii was relatively abundant in the western margin of the North Pacific (Tanimura et al. 2007). In this study, we counted T. frauenfeldii as separated the two morphological types T. frauenfeldii s.l. and T. frauenfeldii s.s. Simonsen (1974) described Thalassiothrix frauenfeldii (= Thalassionema frauenfeldii s.l.), T. frauenfeldii s.l. is reported from the open ocean of the western North Pacific (Hasle 2001; Tanimura et al. 2007). On the other hand, Thalassionema frauenfeldii s.s. is likely to be a coastal species because Hallegraeff (1986) and Sar et al. (2007) collected this from the Argentine and Korean coasts. In Core KY07-04 PC01, T. frauenfeldii s.l. gradually increased since the LGM, whereas T. frauenfeldii s.s. was relatively high abundances during the LGM to the deglacial period with a gentle peak centered at ~ 12 ka ago (Fig. 3). The overall trend suggests a transition from semi-closed to open ocean environments during the deglacial period.
Warm water taxa dwelling in the open ocean gradually increased since the LGM and reached ~ 30% at 8 ka ago (Fig. 3). Among them, Nitzschia bicapitata is the major open-ocean species abundant in tropical to temperate oceans (Fryxell 2000), including in the western Pacific warm pool in the western equatorial Pacific with > 28 °C sea-surface temperature (Kobayashi and Takahashi 2002) and Kuroshio region (Tanimura 1992). In Core KY07-04 PC01, relative abundances of N. bicapitata were high between 12 and 5 ka ago, with a rapid increase near the core top (Fig. 3). Li et al. (2012, 2015) also reported a high percentage of N. bicapitata for the last 400 ka in Core MD05-2908 from the southern Okinawa Trough off northeast of Taiwan. Because of the restricted N. bicapitata distribution in the open ocean, abundant N. bicapitata suggests strengthening Kuroshio inflow into the East China Sea. During the early to middle Holocene, Kuroshio intensified due to strengthening the Subtropical Gyre by precessional forcing (Isono et al. 2009; Yamamoto 2009).
Changes in surface water mass in the East China Sea since the LGM
Diatom assemblages dominated by Paralia spp. in Core KY07-04 PC01 indicate intensified Chinese coastal water whereas weak Kuroshio water in the northern East China Sea during the LGM. Planktic foraminiferal assemblage records also suggested enhanced coastal water during the LGM (Xu and Oda 1999; Ijiri et al. 2005). Reconstructed SSTs during the LGM were ranging from 19 to 22 °C in the northern East China Sea based on planktic foraminiferal Mg/Ca (Kubota et al. 2010; Ujiié et al. 2016), alkenone (Ijiri et al. 2005), and radiolarian transfer function (Matsuzaki et al. 2019) (Fig. 5). In the central and southern Okinawa Trough, reconstructed SSTs during the LGM were between 21 and 24 °C (Sun et al. 2005; Chang et al. 2009a; Yu et al. 2009; Chen et al. 2010; Xu et al. 2013) (Fig. 5). These SSTs were 2–5 °C lower than the present ones but still within temperate to subtropical ranges, consistent with continuous occurrences of warm open-water diatom taxa in Core KY07-04 PC01 since the LGM. In addition, the regional high-resolution climate model study by (Vogt‐Vincent and Mitarai 2020) supports scenario-based proxy records. Kuroshio kept flowing into the Okinawa Trough during the LGM but significantly weakened. However, Kuroshio’s path and intensity during the LGM varied depending on the models. During the LGM, the Kuroshio path migrated to the south of the Ryukyu Islands suggested by a model (Kao et al. 2006). On the contrary, a simulation indicates stronger Kuroshio flowing into the Okinawa Trough (Lee et al. 2013).
Expansion of the nutrient-rich Chinese coastal water led to enhanced productivity in the glacial East China Sea (Ijiri et al. 2005; Chang et al. 2009a; Kubota et al. 2017; Matsuzaki et al. 2019). Dominant Paralia spp. in Core KY07-04 PC01 as an indicator of nutrient-rich coastal water (McQuoid and Nordberg 2003; Di et al. 2013; Liu et al. 2013) demonstrated high productivity in the glacial northern East China Sea. The Chinese coastal water prevailing in the northern East China Sea was an advancement of the river mouth of the Yellow River with sea-level drop during the LGM. Clay mineral compositions and Sr-Nd isotopes of the detrital matter revealed an ample detrital supply from the old Yellow River to the northern East China Sea during the LGM (Xu et al. 2014; Zhao et al. 2017, 2018; Beny et al. 2018). Tsushima Warm Current (TSWC) gradually intensified since 16 ka ago, elevated at 11 ka, and fully evolved at ~ 7 ka after the K-Ah eruption in the northern Okinawa Trough (Xu et al. 2014; Zhao et al. 2017). These timings were consistent with the increasing patterns of %warm diatoms and T-ratio (Fig. 5). In the central Okinawa Trough, the Yangtze River played a critical role in detrital supply (Diekmann et al. 2008; Dou et al. 2010a, b, 2012).
Relative abundances of Paralia spp., periphytic diatom taxa, in Core KY07-04 PC01 gradually decreased since the LGM, subsequently rapidly decreased from 15 to 14 ka ago (Fig. 3). One of the most pronounced deglacial events is meltwater pulse 1A (MWP-1A) between 14.6 and 14.3 ka ago when relative sea-level rose at Tahiti, Barbados, and Sunda Shelf about 10–20 m from − 110 to − 90 m (Deschamps et al. 2012). Due to the East China Sea location as categorized as a far-field (i.e., sites far away from past and present ice-covered regions (Yokoyama and Purcell 2021), a similar magnitude of relative sea-level rise is expected. With the rapid sea-level rise during MWP-1A, river mouths of the Yellow River and the Yangtze River must have retreated. The supporting evidence is by records of clay mineral compositions and Sr-Nd isotopes of detrital matter, suggesting switch of the source region from the river to the continental shelves (Dou et al. 2010a, b, 2012; Xu et al. 2014; Zhao et al. 2017; Hu et al. 2020). Gradual increases in warm diatoms, T-ratio, and Mg/Ca SST in Core KY07-04 PC01 indicate a gradual intensification of Kuroshio during the deglacial period. During the Younger Dryas between 12.9 and 11.6 ka ago (Cheng et al. 2020), warm diatoms kept increasing, whereas Mg/Ca SST was relatively low (Fig. 5).
In the northern Okinawa Trough, Kuroshio intensified between 12 and 5 ka ago, reaching its maximum at ~ 8 ka ago based on diatom taxa living in warm, open water (Fig. 5). Multi-proxy records also indicate the intensified Kuroshio during late deglacial to middle Holocene, i.e., SST rise (Ijiri et al. 2005; Kubota et al. 2010, 2015b; Ruan et al. 2015; Zhao et al. 2015), deepening of the thermocline (Li et al. 2020), planktic foraminiferal assemblage (Xu and Oda 1999; Ijiri et al. 2005), floral changes of calcareous nannoplankton assemblage (Su and Wei 2005), sortable silt (Diekmann et al. 2008), terrigenous input from Taiwan (Dou et al. 2010a, b, 2012, 2016; Xu et al. 2014, 2019; Zheng et al. 2016; Zhao et al. 2017; Hu et al. 2020), organic carbon and reactive phosphorus (Shao et al. 2016; Li et al. 2018), mercury concentration (Lim et al. 2017), and redox sensitive metals (Zou et al. 2020). Warm diatoms showed several rapid decreases based on the direct comparison between diatom assemblage and Mg/Ca SST in Core KY07-04 PC01. Some of these events accompany Mg/Ca SST drops during the Holocene (Fig. 5). An event at 7 ka ago was the most prominent. Subsequently, Kuroshio intensity might have weakened during the late Holocene due to its southward migration by precessional forcing controlling the strength of the North Pacific subtropical gyre (Isono et al. 2009; Yamamoto 2009). However, a sudden increase in N. bicapitata, representative diatom species dwelling in the open ocean with high SST, was observed near the core top of KY07-04 PC01 (Fig. 3). High-resolution diatom assemblage record during the late Holocene in the southern Okinawa Trough showed high abundances of N. bicapitata for the last ~ 400 yrs (Li et al. 2015, 2012). Such high abundances of N. bicapitata over the Okinawa Trough is consistent with the finding of intensification of Kuroshio during the latest Holocene (Zhang et al. 2019), implying persistent poleward heat transport regardless of the weakening of the Atlantic Meridional Overturning Circulation (Summerhayes and Zalasiewicz 2018). Alternatively, the high N. bicapitata abundances might be related to the response to the global warming (Chen et al. 2019a) and southward course shift of the Yellow River discharged into the Yellow Sea between 1546 and 1855 A.D. (Saito and Yang 1995).
We conducted microscopic observations for diatom assemblages since the LGM in Core KY07-04 PC01 from the northern Okinawa Trough, East China Sea. The produced diatom assemblage data are the first centennial-scale resolution since the LGM in the East China Sea with SEM and LM photographs of the representative taxa. Most of the diatoms found in Core KY07-04 PC01 were marine taxa throughout the core, with a few freshwater/brackish water taxa. There was a substantial turnover of major diatom groups from periphytic to planktonic taxa during deglaciation between 17 and 14 ka ago. During the LGM and early deglaciation, the representative periphytic taxa were Paralia spp., abundant in the modern continental shelf region of the East China Sea covered by the Chinese coastal water. The advancement of the Yellow River mouth with a sea-level drop during the LGM was the plausible reason for the prevailing Chinese coastal water in the northern East China Sea. Rapid decrease in the relative abundances of Paralia spp. during 15–14 ka ago corresponded to MWP-1A, a major deglacial event with the rapid sea-level rise during 14.6–14.3 ka ago. Planktonic cold diatom taxa were less than 10% throughout the core, suggesting the oceanic environment in the northern Okinawa Trough has been temperate to subtropical even during the LGM. Planktonic diatom Thalassionema was the dominant diatom genus since 14 ka ago. A ratio of three T. nitzschioides varieties (var. incurvatum, var. inflatum, and var. parvum) in Thalassionema nitzschioides complex (T-ratio) increased since 12 ka ago and has reached its present level since 8 ka ago, responding to strengthening and northward migration of Kuroshio during early to middle Holocene by precessional forcing. Warm planktonic diatom taxa also showed a gradual increase from 12 to 8 ka ago. A sudden increase in N. bicapitata, warm open ocean species, was found near the core top, which might be related to the intensifying Kuroshio during the latest Holocene.
Availability of data and material
The datasets supporting the conclusions of this article are included within the article and its additional files.
Changjiang River Diluted Water
Last Glacial Maximum
Scanning electron microscope
Tsushima Warm Current
Akiba F, Tanimura Y, Oi T, Ishihama S, Matsumoto R (2014) Diatom biostratigraphy and diatom-derived black grains of the uppermost quaternary cores from the Japan Sea, and their paleoceanographic implications. J Jpn Assoc Pet Technol 79:130–139
Asaoka O (1975) Biological oceanography of the East China Sea. Mar Sci Mon (kaiyokagaku) 7:38–45
Asaoka O (1980) Distribution of Melosira sulcata (Ehrenberg) Kützing, a diatom species, in the seas west of Japan. Oceanogr Mag 31:1–13
Beny F, Toucanne S, Skonieczny C, Bayon G, Ziegler M (2018) Geochemical provenance of sediments from the northern East China Sea document a gradual migration of the Asian Monsoon belt over the past 400,000 years. Quat Sci Rev 190:161–175. https://doi.org/10.1016/j.quascirev.2018.04.032
Chang Y-P, Chen M-T, Yokoyama Y, Matsuzaki H, Thompson WG, Kao S-J, Kawahata H (2009) Monsoon hydrography and productivity changes in the East China Sea during the past 100,000 years: Okinawa Trough evidence (MD012404). Paleoceanography. https://doi.org/10.1029/2007pa001577
Chang YP, Wang WL, Chen MT (2009b) The last 100 000 years’ palaeoenvironmental changes inferred from the diatom assemblages of core MD012404 from the Okinawa Trough, East China Sea. J Quat Sci 24(8):890–901. https://doi.org/10.1002/jqs.1316
Chen MT, Lin XP, Chang YP, Chen YC, Lo L, Shen CC, Yokoyama Y, Oppo DW, Thompson WG, Zhang R (2010) Dynamic millennial-scale climate changes in the northwestern Pacific over the past 40,000 years. Geophys Res Lett. https://doi.org/10.1029/2010gl045202
Chen C, Wang G, Xie S-P, Liu W (2019a) Why does global warming weaken the gulf stream but intensify the Kuroshio? J Clim 32(21):7437–7451. https://doi.org/10.1175/jcli-d-18-0895.1
Chen M, Li Y, Qi H, Wang L, Zhang A, Shen L, Fang Q (2019b) Data of surface sediment diatoms on the inner shelf of the East China Sea from winter 2008 to summer 2009. Data Brief 24:103959. https://doi.org/10.1016/j.dib.2019.103959
Cheng H, Zhang H, Spotl C, Baker J, Sinha A, Li H, Bartolome M, Moreno A, Kathayat G, Zhao J, Dong X, Li Y, Ning Y, Jia X, Zong B, Ait Brahim Y, Perez-Mejias C, Cai Y, Novello VF, Cruz FW, Severinghaus JP, An Z, Edwards RL (2020) Timing and structure of the Younger Dryas event and its underlying climate dynamics. Proc Natl Acad Sci U S A 117(38):23408–23417. https://doi.org/10.1073/pnas.2007869117
Chiang KP, Chen YT, Gong GC (1999) Spring distribution of diatom assemblages in the East China Sea. Mar Ecol Prog Ser 186:75–86. https://doi.org/10.3354/meps186075
Deschamps P, Durand N, Bard E, Hamelin B, Camoin G, Thomas AL, Henderson GM, Okuno J, Yokoyama Y (2012) Ice-sheet collapse and sea-level rise at the Bolling warming 14,600 years ago. Nature 483(7391):559–564. https://doi.org/10.1038/nature10902
Di B, Liu D, Wang Y, Dong Z, Li X, Shi Y (2013) Diatom and silicoflagellate assemblages in modern surface sediments associated with human activity: a case study in Sishili Bay, China. Ecol Ind 24:23–30. https://doi.org/10.1016/j.ecolind.2012.05.020
Diekmann B, Hofmann J, Henrich R, Fütterer DK, Röhl U, Wei K-Y (2008) Detrital sediment supply in the southern Okinawa Trough and its relation to sea-level and Kuroshio dynamics during the late quaternary. Mar Geol 255(1–2):83–95. https://doi.org/10.1016/j.margeo.2008.08.001
Dou Y, Yang S, Liu Z, Clift PD, Shi X, Yu H, Berne S (2010a) Provenance discrimination of siliciclastic sediments in the middle Okinawa Trough since 30ka: constraints from rare earth element compositions. Mar Geol 275(1–4):212–220. https://doi.org/10.1016/j.margeo.2010.06.002
Dou Y, Yang S, Liu Z, Clift PD, Yu H, Berne S, Shi X (2010b) Clay mineral evolution in the central Okinawa Trough since 28ka: Implications for sediment provenance and paleoenvironmental change. Palaeogeogr Palaeoclimatol Palaeoecol 288(1–4):108–117. https://doi.org/10.1016/j.palaeo.2010.01.040
Dou Y, Yang S, Liu Z, Shi X, Li J, Yu H, Berne S (2012) Sr–Nd isotopic constraints on terrigenous sediment provenances and Kuroshio current variability in the Okinawa Trough during the late Quaternary. Palaeogeogr Palaeoclimatol Palaeoecol 365–366:38–47. https://doi.org/10.1016/j.palaeo.2012.09.003
Dou Y, Yang S, Shi X, Clift PD, Liu S, Liu J, Li C, Bi L, Zhao Y (2016) Provenance weathering and erosion records in southern Okinawa Trough sediments since 28 ka: geochemical and Sr–Nd–Pb isotopic evidences. Chem Geol 425:93–109. https://doi.org/10.1016/j.chemgeo.2016.01.029
Fryxell GA (2000) Nitzschia bicapitata (Bacillariophyceae) and related taxa from oceanic aggregations. Diatom Res 15(1):43–73. https://doi.org/10.1080/0269249x.2000.9705486
Furuya K, Kurita K, Odate T (1996) Distribution of phytoplankton in the East China Sea in the winter of 1993. J Oceanogr 52(3):323–333. https://doi.org/10.1007/bf02235927
Gallagher SJ, Kitamura A, Iryu Y, Itaki T, Koizumi I, Hoiles PW (2015) The Pliocene to recent history of the Kuroshio and Tsushima currents: a multi-proxy approach. Prog Earth Planet Sci. https://doi.org/10.1186/s40645-015-0045-6
Guo S, Feng Y, Wang L, Dai M, Liu Z, Bai Y, Sun J (2014) Seasonal variation in the phytoplankton community of a continental-shelf sea: the East China Sea. Mar Ecol Prog Ser 516:103–126. https://doi.org/10.3354/meps10952
Hallegraeff GM (1986) Taxonomy and morphology of the marine plankton Diatoms thalassionema and thalassiothrix. Diatom Res 1(1):57–80. https://doi.org/10.1080/0269249x.1986.9704958
Hasle GR (2001) The marine, planktonic diatom family Thalassionemataceae: morphology. Taxon Distrib Diatom Res 16(1):1–82. https://doi.org/10.1080/0269249x.2001.9705509
Hasle GR, Syvertsen EE (1997) Marine diatoms. In: Tomas CR (ed) Identifying marine phytoplankton. Academic Press, San Diego, pp 5–385. https://doi.org/10.1016/B978-0-12-693018-4.X5000-9
Heaton TJ, Köhler P, Butzin M, Bard E, Reimer RW, Austin WEN, Bronk Ramsey C, Grootes PM, Hughen KA, Kromer B, Reimer PJ, Adkins J, Burke A, Cook MS, Olsen J, Skinner LC (2020) Marine20—the marine radiocarbon age calibration curve (0–55,000 Cal Bp). Radiocarbon. https://doi.org/10.1017/rdc.2020.68
Hideshima S, Matsumoto E, Abe O, Kitagawa H (2001) Northwest Pacific marine reservoir correction estimated from annually banded coral from Ishigaki Island. South Jpn Radiocarb 43(2A):473–476. https://doi.org/10.1017/s0033822200038352
Hirabayashi S, Yokoyama Y, Suzuki A, Miyairi Y, Aze T (2017) Short-term fluctuations in regional radiocarbon reservoir age recorded in coral skeletons from the Ryukyu Islands in the north-western Pacific. J Quat Sci 32(1):1–6. https://doi.org/10.1002/jqs.2923
Hu N, Huang P, Zhang H, Zhang Y, Shi X, Liu J, Fan X (2020) Sr–Nd isotopes indicating the provenance of siliciclastic sediments and paleoenvironmental changes in the middle Okinawa Trough during the last deglaciation. Cont Shelf Res. https://doi.org/10.1016/j.csr.2020.104277
Ichikawa H, Beardsley RC (2002) The current system in the Yellow and East China Seas. J Oceanogr 58(1):77–92. https://doi.org/10.1023/a:1015876701363
Ijiri A, Wang L, Oba T, Kawahata H, Huang C-Y, Huang C-Y (2005) Paleoenvironmental changes in the northern area of the East China Sea during the past 42,000 years. Palaeogeogr Palaeoclimatol Palaeoecol 219(3–4):239–261. https://doi.org/10.1016/j.palaeo.2004.12.028
Ishikawa A, Furuya K (2004) The role of diatom resting stages in the onset of the spring bloom in the East China Sea. Mar Biol 145(3):633–639. https://doi.org/10.1007/s00227-004-1331-9
Isobe A (2008) Recent advances in ocean-circulation research on the Yellow Sea and East China Sea shelves. J Oceanogr 64(4):569–584. https://doi.org/10.1007/s10872-008-0048-7
Isono D, Yamamoto M, Irino T, Oba T, Murayama M, Nakamura T, Kawahata H (2009) The 1500-year climate oscillation in the midlatitude North Pacific during the Holocene. Geology 37(7):591–594. https://doi.org/10.1130/g25667a.1
Kao SJ, Wu C-R, Hsin Y-C, Dai M (2006) Effects of sea level change on the upstream Kuroshio Current through the Okinawa Trough. Geophys Res Lett. https://doi.org/10.1029/2006gl026822
Kawahata H, Ohshima H (2004) Vegetation and environmental record in the northern East China Sea during the late Pleistocene. Glob Planet Change 41(3–4):251–273. https://doi.org/10.1016/j.gloplacha.2004.01.011
Kobayashi F, Takahashi K (2002) Distribution of diatoms along the equatorial transect in the western and central Pacific during the 1999 La Niña conditions. Deep Sea Res Part II Top Stud Oceanogr 49(13–14):2801–2821. https://doi.org/10.1016/s0967-0645(02)00059-0
Koizumi I (2008) Diatom-derived SSTs (Td’ ratio) indicate warm seas off Japan during the middle Holocene (8.2–3.3 kyr BP). Mar Micropaleontol 69(3–4):263–281. https://doi.org/10.1016/j.marmicro.2008.08.004
Kong GS, Lee CW (2005) Marine reservoir corrections (ΔR) for southern coastal waters of Korea. Sea (J Korean Soc Oceanog) 10:124–128
Konishi K, Tanaka T, Sakanoue M (1982) Secular variation of radiocarbon concentrations in seawater: sclerochronological approach. Proc Fourth Int Coral Reef Symp 1:181–185
Konno S, Jordan RW (2008) Paralia longispina sp. nov., an extant species from Palau and Haha-jima, western North Pacific. In: Proceedings of the nineteenth international diatom symposium, pp 55–69
Kubota Y, Kimoto K, Tada R, Oda H, Yokoyama Y, Matsuzaki H (2010) Variations of East Asian summer monsoon since the last deglaciation based on Mg/Ca and oxygen isotope of planktic foraminifera in the northern East China Sea. Paleoceanography. https://doi.org/10.1029/2009pa001891
Kubota Y, Kimoto K, Itaki T, Yokoyama Y, Miyairi Y, Matsuzaki H (2015a) Bottom water variability in the subtropical northwestern Pacific from 26 kyr BP to present based on Mg/Ca and stable carbon and oxygen isotopes of benthic foraminifera. Clim Past 11(6):803–824. https://doi.org/10.5194/cp-11-803-2015
Kubota Y, Tada R, Kimoto K (2015b) Changes in East Asian summer monsoon precipitation during the Holocene deduced from a freshwater flux reconstruction of the Changjiang (Yangtze River) based on the oxygen isotope mass balance in the northern East China Sea. Clim Past 11(2):265–281. https://doi.org/10.5194/cp-11-265-2015
Kubota Y, Suzuki N, Kimoto K, Uchida M, Itaki T, Ikehara K, Kim RA, Lee KE (2017) Variation in subsurface water temperature and its link to the Kuroshio current in the Okinawa Trough during the last 38.5 kyr. Quat Int 452:1–11. https://doi.org/10.1016/j.quaint.2017.06.021
Kubota Y, Kimoto K, Tada R, Uchida M, Ikehara K (2019) Millennial-scale variability of East Asian summer monsoon inferred from sea surface salinity in the northern East China Sea (ECS) and its impact on the Japan Sea during Marine Isotope Stage (MIS) 3. Prog Earth Planet Sci. https://doi.org/10.1186/s40645-019-0283-0
Lee KE, Lee HJ, Park J-H, Chang Y-P, Ikehara K, Itaki T, Kwon HK (2013) Stability of the Kuroshio path with respect to glacial sea level lowering. Geophys Res Lett. https://doi.org/10.1002/grl.50102
Li D, Knudsen MF, Jiang H, Olsen J, Zhao M, Li T, Knudsen KL, Seidenkrantz M-S, Sha L (2012) A diatom-based reconstruction of summer sea-surface salinity in the Southern Okinawa Trough, East China Sea, over the last millennium. J Quat Sci 27(8):771–779. https://doi.org/10.1002/jqs.2562
Li Y, Zhao QL, Lü SH (2014) Taxonomy and species diversity of the diatom genus Thalassiosira (Bacillariophyceae) in Zhejiang coastal waters, the East China Sea. Nova Hedwig 99(3–4):373–402. https://doi.org/10.1127/0029-5035/2014/0170
Li D, Jiang HUI, Knudsen KL, BjÖRck S, Olsen J, Zhao M, Li T, Li J (2015) A diatom record of mid- to late Holocene palaeoenvironmental changes in the southern Okinawa Trough. J Quat Sci 30(1):32–43. https://doi.org/10.1002/jqs.2756
Li D-W, Chang Y-P, Li Q, Zheng L, Ding X, Kao S-J (2018) Effect of sea-level on organic carbon preservation in the Okinawa Trough over the last 91 kyr. Mar Geol 399:148–157. https://doi.org/10.1016/j.margeo.2018.02.013
Li Q, Li G, Chen MT, Xu J, Liu S, Chen M (2020) New insights into kuroshio current evolution since the last deglaciation based on paired organic paleothermometers from the Middle Okinawa Trough. Paleoceanogr Paleoclimatol. https://doi.org/10.1029/2020pa004140
Lim D, Kim J, Xu Z, Jeong K, Jung H (2017) New evidence for Kuroshio inflow and deepwater circulation in the Okinawa Trough, East China Sea: Sedimentary mercury variations over the last 20 kyr. Paleoceanography 32(6):571–579. https://doi.org/10.1002/2017pa003116
Liu D, Shen X, Di B, Shi Y, Keesing JK, Wang Y, Wang Y (2013) Palaeoecological analysis of phytoplankton regime shifts in response to coastal eutrophication. Mar Ecol Prog Ser 475:1–14. https://doi.org/10.3354/meps10234
Locarnini RA, Mishonov AV, Baranova OK, Boyer TP, Zweng MM, Garcia HE, Reagan JR, Seidov D, Weathers K, Paver CR, Smolyar I (2018) World Ocean Atlas 2018, Volume 1: Temperature. A. Mishonov Technical Ed.; NOAA Atlas NESDIS 81, 52 pp
Ma K, Sun Z-L, Zhu M-X, Zhang X-R, Ding K-Y, Li T, Zhang X-L, Zhai B, Cao H, Geng W, Xu C-L (2021) Characterizing geochemistry of organic carbon, sulfur, and iron in sediments of the middle Okinawa Trough since the last glacial maximum. Deep Sea Res Part I Oceanogr Res Pap. https://doi.org/10.1016/j.dsr.2020.103452
MacGillivary ML, Kaczmarska I (2012) Genetic differentiation within the Paralia longispina (Bacillariophyta) species complex. Botany 90(3):205–222. https://doi.org/10.1139/B11-101
MacGillivary ML, Kaczmarska I (2013) Lectotypification ofParalia sulcataand description of P. obscura sp. nov. (Bacillariophyta) from the Ehrenberg Collection. Diatom Res 28(3):221–235. https://doi.org/10.1080/0269249x.2013.791646
Matsuzaki KM, Itaki T, Tada R (2019) Paleoceanographic changes in the Northern East China Sea during the last 400 kyr as inferred from radiolarian assemblages (IODP Site U1429). Prog Earth Planet Sci. https://doi.org/10.1186/s40645-019-0256-3
McLean D, Albert PG, Nakagawa T, Suzuki T, Staff RA, Yamada K, Kitaba I, Haraguchi T, Kitagawa J, Smith VC (2018) Integrating the Holocene tephrostratigraphy for East Asia using a high-resolution cryptotephra study from Lake Suigetsu (SG14 core), central Japan. Quat Sci Rev 183:36–58. https://doi.org/10.1016/j.quascirev.2017.12.013
McQuoid MR, Nordberg K (2003) The diatom Paralia sulcata as an environmental indicator species in coastal sediments. Estuar Coast Shelf Sci 56(2):339–354. https://doi.org/10.1016/s0272-7714(02)00187-7
Milliman JD, Meade RH (1983) World-wide delivery of river sediment to the oceans. J Geol 91(1):1–21. https://doi.org/10.1086/628741
Oba T, Kato M, Kitazato H, Koizumi I, Omura A, Sakai T, Takayama T (1991) Paleoenvironmental changes in the Japan sea during the last 85,000 years. Paleoceanography 6(4):499–518. https://doi.org/10.1029/91pa00560
Oh SH, Koh CH (1995) Distribution of diatoms in the surficial sediments of the Mangyung–Dongjin tidal flat, west coast of Korea (Eastern Yellow Sea). Mar Biol 122(3):487–496. https://doi.org/10.1007/bf00350883
Qiu B (2019) Kuroshio and Oyashio currents. Encycl Ocean Sci. https://doi.org/10.1016/b978-0-12-409548-9.11295-3
Round FE, Crawford RM, Mann DG (1990) The diatoms, biology and morphology of the Genera. Cambridge University Press, Cambridge
Ruan J, Xu Y, Ding S, Wang Y, Zhang X (2015) A high resolution record of sea surface temperature in southern Okinawa Trough for the past 15,000 years. Palaeogeogr Palaeoclimatol Palaeoecol 426:209–215. https://doi.org/10.1016/j.palaeo.2015.03.007
Saito Y, Yang Z (1995) Historical change of the Huanghe (Yellow River) and its impact on the sediment budget of the East China Sea. In: Global fluxes of carbon and its realted substances in the coastal sea-ocean-atmosphere system, pp 7–12
Sar EA, Sunesen I, Fernandez PV (2007) Marine diatoms from Buenos Aires Coastal waters (Argentina). II. Thalassionemataceae and Rhaphoneidaceae. Rev Chil Hist Nat 80:63–79
Sawai Y, Nagumo T, Toyoda K (2005) Three extant species of Paralia (Bacillariophyceae) along the coast of Japan. Phycologia 44(5):517–529. https://doi.org/10.2216/0031-8884(2005)44[517:TESOPB]2.0.CO;2
Sawai Y, Jankaew K, Martin ME, Prendergast A, Choowong M, Charoentitirat T (2009) Diatom assemblages in tsunami deposits associated with the 2004 Indian Ocean tsunami at Phra Thong Island, Thailand. Mar Micropaleontol 73(1–2):70–79. https://doi.org/10.1016/j.marmicro.2009.07.003
Shao H, Yang S, Cai F, Li C, Liang J, Li Q, Hyun S, Kao S-J, Dou Y, Hu B, Dong G, Wang F (2016) Sources and burial of organic carbon in the middle Okinawa Trough during late Quaternary paleoenvironmental change. Deep Sea Res Part I Oceanogr Res Pap 118:46–56. https://doi.org/10.1016/j.dsr.2016.10.005
Simonsen R (1974) The diatom plankton of the Indian ocean expedition of RV “Meteor” 1964–1965. Meteor Forschungsergebnisse, vol 19. Gebrüder Borntraeger, Berlin
Smol JP, Stoermer EF (2010) The diatoms: applications for the environmental and earth sciences, 2nd edn. Cambridge University Press, Cambridge
Southon J, Kashgarian M, Fontugne M, Metivier B, Yim W-S (2002) Marine reservoir corrections for the Indian Ocean and Southeast Asia. Radiocarbon 44(1):167–180. https://doi.org/10.1017/s0033822200064778
Stuiver M, Reimer PJ, Reimer RW (2021) CALIB 8.2 [WWW program] http://calib.org. Accessed 20 May 2021
Su X, Wei K-Y (2005) Calcareous nannofossils and variation of the Kuroshio current in the Okinawa Tro ugh during the last 14000 years. Terr Atmos Ocean Sci. https://doi.org/10.3319/tao.2005.16.1.95(ot)
Summerhayes CP, Zalasiewicz J (2018) Global warming and the anthropocene. Geol Today 34:194–200. https://doi.org/10.1111/gto.12247
Sun Y, Oppo DW, Xiang R, Liu W, Gao S (2005) Last deglaciation in the Okinawa Trough: subtropical northwest Pacific link to Northern Hemisphere and tropical climate. Paleoceanography. https://doi.org/10.1029/2004pa001061
Tada R, Irino T, Koizumi I (1999) Land-ocean linkages over orbital and millennial timescales recorded in late quaternary sediments of the Japan Sea. Paleoceanography 14(2):236–247. https://doi.org/10.1029/1998pa900016
Takemoto A, Oda M (1997) New planktic foraminiferal transfer functions for the Kuroshio–Oyashio current region off Japan. Paleontol Res 1:291–310. https://doi.org/10.2517/prpsj.1.291
Tanimura Y (1992) Seasonal changes in flux and species composition of diatoms: sediment trap results from the northwest Pacific, August 1986–November 1988. Bull Natl Sci Mus Ser C (Geol Paleontol) 18:121–154
Tanimura Y (1999) Varieties of a single cosmopolitan diatom species associated with surface water masses in the North Pacific. Mar Micropaleontol 37(2):199–218. https://doi.org/10.1016/s0377-8398(99)00029-8
Tanimura Y, Shimada C, Haga M (2002) Migration of continental mixed-waters preserved in abundance of a diatom species Paralia sulcata: paleoceanography of the northeastern East China Sea from the last glacial through the postglacial. Quat Res (Daiyonki-Kenkyu) 41(2):85–93
Tanimura Y, Shimada C, Iwai M (2007) Modern Distribution of Thalassionema species (Bacillariophyceae) in the Pacific Ocean. Bull Natl Mus Nat Sci Ser C (Geol Paleontol) 33:27–51
Thirumalai K, Quinn TM, Marino G (2016) Constraining past seawater δ18O and temperature records developed from foraminiferal geochemistry. Paleoceanography 31(10):1409–1422. https://doi.org/10.1002/2016pa002970
Ujiié Y, Ujiié H, Taira A, Nakamura T, Oguri K (2003) Spatial and temporal variability of surface water in the Kuroshio source region, Pacific Ocean, over the past 21,000 years: evidence from planktonic foraminifera. Mar Micropaleontol 49(4):335–364. https://doi.org/10.1016/s0377-8398(03)00062-8
Ujiié Y, Asahi H, Sagawa T, Bassinot F (2016) Evolution of the North Pacific Subtropical Gyre during the past 190 kyr through the interaction of the Kuroshio Current with the surface and intermediate waters. Paleoceanography 31(11):1498–1513. https://doi.org/10.1002/2015pa002914
Vogt-Vincent NS, Mitarai S (2020) A persistent Kuroshio in the glacial East China Sea and Implications for coral paleobiogeography. Paleoceanogr Paleoclimatol. https://doi.org/10.1029/2020pa003902
Xu X, Oda M (1999) Surface-water evolution of the eastern East China Sea during the last 36,000 years. Mar Geol 156(1–4):285–304. https://doi.org/10.1016/s0025-3227(98)00183-2
Xu D, Lu H, Wu N, Liu Z, Li T, Shen C, Wang L (2013) Asynchronous marine-terrestrial signals of the last deglacial warming in East Asia associated with low- and high-latitude climate changes. Proc Natl Acad Sci U S A 110(24):9657–9662. https://doi.org/10.1073/pnas.1300025110
Xu Z, Li T, Chang F, Wan S, Choi J, Lim D (2014) Clay-sized sediment provenance change in the northern Okinawa Trough since 22kyrBP and its paleoenvironmental implication. Palaeogeogr Palaeoclimatol Palaeoecol 399:236–245. https://doi.org/10.1016/j.palaeo.2014.01.016
Xu Z, Lim D, Li T, Kim S, Jung H, Wan S, Chang F, Cai M (2019) REEs and Sr–Nd isotope variations in a 20 ky-sediment core from the middle Okinawa Trough, East China Sea: An in-depth provenance analysis of siliciclastic components. Mar Geol. https://doi.org/10.1016/j.margeo.2019.105970
Yamamoto M (2009) Response of mid-latitude North Pacific surface temperatures to orbital forcing and linkage to the East Asian summer monsoon and tropical ocean–atmosphere interactions. J Quat Sci 24(8):836–847. https://doi.org/10.1002/jqs.1255
Yamamoto M, Suemune R, Oba T (2005) Equatorward shift of the subarctic boundary in the northwestern Pacific during the last deglaciation. Geophys Res Lett. https://doi.org/10.1029/2004gl021903
Yokoyama Y, Purcell A (2021) On the geophysical processes impacting palaeo-sea-level observations. Geosci Lett. https://doi.org/10.1186/s40562-021-00184-w
Yokoyama Y, Naruse T, Ogawa NO, Tada R, Kitazato H, Ohkouchi N (2006) Dust influx reconstruction during the last 26,000 years inferred from a sedimentary leaf wax record from the Japan Sea. Glob Planet Change 54(3–4):239–250. https://doi.org/10.1016/j.gloplacha.2006.06.022
Yokoyama Y, Esat TM, Thompson WG, Thomas AL, Webster JM, Miyairi Y, Sawada C, Aze T, Matsuzaki H, Okuno J, Fallon S, Braga JC, Humblet M, Iryu Y, Potts DC, Fujita K, Suzuki A, Kan H (2018) Rapid glaciation and a two-step sea level plunge into the last glacial maximum. Nature 559(7715):603–607. https://doi.org/10.1038/s41586-018-0335-4
Yokoyama Y, Miyairi Y, Aze T, Yamane M, Sawada C, Ando Y, de Natris M, Hirabayashi S, Ishiwa T, Sato N, Fukuyo N (2019) A single stage accelerator mass spectrometry at the Atmosphere and Ocean Research Institute, The University of Tokyo. Nucl Instrum Methods Phys Res Sect B 455:311–316. https://doi.org/10.1016/j.nimb.2019.01.055
Yoneda M, Uno H, Shibata Y, Suzuki R, Kumamoto Y, Yoshida K, Sasaki T, Suzuki A, Kawahata H (2007) Radiocarbon marine reservoir ages in the western Pacific estimated by pre-bomb molluscan shells. Nucl Instrum Methods Phys Res Sect B 259(1):432–437. https://doi.org/10.1016/j.nimb.2007.01.184
Yu H, Liu Z, Berné S, Jia G, Xiong Y, Dickens GR, Wei G, Shi X, Liu JP, Chen F (2009) Variations in temperature and salinity of the surface water above the middle Okinawa Trough during the past 37kyr. Palaeogeogr Palaeoclimatol Palaeoecol 281(1–2):154–164. https://doi.org/10.1016/j.palaeo.2009.08.002
Yuan M, Sun J, Zhai W (2014) Phytoplankton community in Bohai Sea and the North Yellow Sea in autumn 2012. J Tianjin Univ Sci Technol 29:56–64. https://doi.org/10.13364/j.issn.1672-6510.2014.06.012
Zhang Y, Zhou X, He Y, Jiang Y, Liu Y, Xie Z, Sun L, Liu Z (2019) Persistent intensification of the Kuroshio Current during late Holocene cool intervals. Earth Planet Sci Lett 506:15–22. https://doi.org/10.1016/j.epsl.2018.10.018
Zhao J, Li J, Cai F, Wei H, Hu B, Dou Y, Wang L, Xiang R, Cheng H, Dong L, Zhang CL (2015) Sea surface temperature variation during the last deglaciation in the southern Okinawa Trough: modulation of high latitude teleconnections and the Kuroshio Current. Prog Oceanogr 138:238–248. https://doi.org/10.1016/j.pocean.2015.06.008
Zhao D, Wan S, Toucanne S, Clift PD, Tada R, Révillon S, Kubota Y, Zheng X, Yu Z, Huang J, Jiang H, Xu Z, Shi X, Li A (2017) Distinct control mechanism of fine-grained sediments from Yellow River and Kyushu supply in the northern Okinawa Trough since the last glacial. Geochem Geophys Geosyst 18(8):2949–2969. https://doi.org/10.1002/2016gc006764
Zhao D, Wan S, Clift PD, Tada R, Huang J, Yin X, Liao R, Shen X, Shi X, Li A (2018) Provenance, sea-level and monsoon climate controls on silicate weathering of Yellow River sediment in the northern Okinawa Trough during late last glaciation. Palaeogeogr Palaeoclimatol Palaeoecol 490:227–239. https://doi.org/10.1016/j.palaeo.2017.11.002
Zheng X, Li A, Kao S, Gong X, Frank M, Kuhn G, Cai W, Yan H, Wan S, Zhang H, Jiang F, Hathorne E, Chen Z, Hu B (2016) Synchronicity of Kuroshio Current and climate system variability since the last glacial maximum. Earth Planet Sci Lett 452:247–257. https://doi.org/10.1016/j.epsl.2016.07.028
Zong Y, Horton BP (1999) Diatom-based tidal-level transfer functions as an aid in reconstructing quaternary history of sea-level movements in the UK. J Quat Sci 14(2):153–167. https://doi.org/10.1002/(sici)1099-1417(199903)14:2%3c153::Aid-jqs425%3e3.0.Co;2-6
Zou J, Shi X, Zhu A, Kandasamy S, Gong X, Lembke-Jene L, Chen M-T, Wu Y, Ge S, Liu Y, Xue X, Lohmann G, Tiedemann R (2020) Millennial-scale variations in sedimentary oxygenation in the western subtropical North Pacific and its links to North Atlantic climate. Clim Past 16(1):387–407. https://doi.org/10.5194/cp-16-387-2020
Zweng MM, Reagan JR, Seidov D, Boyer TP, Locarnini RA, Garcia HE, Mishonov AV, Baranova OK, Weathers K, Paver CR, Smolyar I (2018) World Ocean Atlas 2018, vol 2: Salinity. A. Mishonov Technical Ed.; NOAA Atlas NESDIS 82
We sincerely thank the scientists, technicians, captain, and crew of the KY07-04 Cruise by R/V Kaiyo, Japan Agency for Marine-Earth Science and Technology, for their efforts in obtaining sediment samples. Mr. Kazuhiko Shimada of Kyushu University supported the FE-SEM operation. We also thank Dr. Fumio Akiba of Diatom Minilab Akiba, Co. Ltd. for his helpful suggestions on diatom taxonomy.
This work was supported by JSPS KAKENHI Grant Numbers 15K13585, 16H04832, 16H04069, 21K12222 to YO, and 20H00193 to YY.
The authors declare that they have no competing interest.
About this article
Cite this article
Shirota, K., Okazaki, Y., Konno, S. et al. Changes in surface water masses in the northern East China Sea since the Last Glacial Maximum based on diatom assemblages. Prog Earth Planet Sci 8, 66 (2021). https://doi.org/10.1186/s40645-021-00456-1
- East China Sea
- Sediment core
- Last Glacial Maximum
- Water mass
- Chinese coastal water