Evidence from giant-clam δ18O of intense El Ninõ–Southern Oscillation-related variability but reduced frequency 3700 years ago

Giant clams (Tridacna) are the largest marine bivalves, and their carbonate shells can be used for highresolution paleoclimate reconstructions. In this contribution, δOshell was used to estimate climatic variation in the Xisha Islands of the South China Sea. We first evaluate sea surface temperature (SST) and sea surface salinity (SSS) influence on the modern resampled monthly (r-monthly) resolution of Tridacna gigas δOshell. The results obtained reveal that δOshell seasonal variation is mainly controlled by SST and appears to be insensitive to local SSS change. Thus, the δ18O of Tridacna shells can be roughly used as a proxy of local SST: a 1 ‰ δOshell change is roughly equal to 4.41 C of SST. The r-monthly δ18O of a 40-year-old Tridacna squamosa (3673± 28 BP) from the North Reef of the Xisha Islands was analyzed and compared with the modern specimen. The difference between the average δ18O of the fossil Tridacna shell (δ18O =−1.34 ‰) and the modern Tridacna specimen (δ18O =−1.15 ‰) probably implies a warm climate, roughly 0.84 C, 3700 years ago. The seasonal variation 3700 years ago was slightly lower than that suggested by modern instrumental data, and the transition between warm and cold seasons was rapid. Higher amplitudes of reconstructed r-monthly and r-annual SST anomalies imply an enhanced climate variability during this warm period. Investigation of the El Ninõ–Southern Oscillation (ENSO) variation (based on the reconstructed SST series) indicates reduced ENSO frequency but increased ENSO-related variability and extreme El Ninõ winter events 3700 years ago.

Abstract. Giant clams (Tridacna) are the largest marine bivalves, and their carbonate shells can be used for highresolution paleoclimate reconstructions. In this contribution, δ 18 O shell was used to estimate climatic variation in the Xisha Islands of the South China Sea. We first evaluate sea surface temperature (SST) and sea surface salinity (SSS) influence on the modern resampled monthly (r-monthly) resolution of Tridacna gigas δ 18 O shell . The results obtained reveal that δ 18 O shell seasonal variation is mainly controlled by SST and appears to be insensitive to local SSS change. Thus, the δ 18 O of Tridacna shells can be roughly used as a proxy of local SST: a 1 ‰ δ 18 O shell change is roughly equal to 4.41 • C of SST. The r-monthly δ 18 O of a 40-year-old Tridacna squamosa (3673 ± 28 BP) from the North Reef of the Xisha Islands was analyzed and compared with the modern specimen. The difference between the average δ 18 O of the fossil Tridacna shell (δ 18 O = −1.34 ‰) and the modern Tridacna specimen (δ 18 O = −1.15 ‰) probably implies a warm climate, roughly 0.84 • C, 3700 years ago. The seasonal variation 3700 years ago was slightly lower than that suggested by modern instrumental data, and the transition between warm and cold seasons was rapid. Higher amplitudes of reconstructed r-monthly and r-annual SST anomalies imply an enhanced climate variability during this warm period. Investigation of the El Ninõ-Southern Oscillation (ENSO) variation (based on the reconstructed SST series) indicates reduced ENSO frequency but increased ENSO-related variability and extreme El Ninõ winter events 3700 years ago.  (Pätzold et al., 1991;Watanabe et al., 1999Watanabe et al., , 2004Elliot et al., 2009;Ayling et al., 2015;Agbaje et al., 2017). This is because their shells have many favorable properties for recording local environmental changes: they have dense and well-preserved aragonite shells, fast growth rates (up to 1 cm yr −1 ) with clear annual growth lines, and a longevity of several decades to about 100 years. These characteristics allow Tridacna to provide ideal material for highresolution reconstruction of interannual, seasonal, or even subseasonal climatic variations.
Previous studies indicate that Tridacna species grow their shells in oxygen isotopic (δ 18 O) equilibrium with the surrounding seawater (Aharon, 1991;Aharon and Chappell, 1986;Pätzold et al., 1991;Romanek and Grossman, 1989;Watanabe et al., 1999). The reliability of reconstructing temperature and seawater δ 18 O variability is not reduced and does not show obvious increasing or decreasing trends due to Tridacna's ontogenetic growth (Welsh et al., 2011). These studies imply that δ 18 O shell can be used to reconstruct Late Quaternary sea-level and climatic changes. Indeed, the δ 18 O of marine biogenic carbonates is influenced not only by sea surface temperature (SST) but also by surrounding seawater δ 18 O. Meanwhile, seawater δ 18 O has a close correlation with sea surface salinity (SSS), which is affected by tropical evaporation and the precipitation balance. Nonetheless, the influence of SST and SSS on δ 18 O shell is unclear due to the distinct variation of temperature and salinity in different areas. For example, the δ 18 O shell of Tridacna from southwestern Japan can be directly used as a proxy of SST (Yamanashi et al., 2016), while the δ 18 O shell of Indonesian Tridacna has been interpreted to be a contribution of 71.4 % from SST and 28.6 % from SSS (Arias-Ruiz et al., 2017). Thus, local calibration from modern Tridacna is important in determining the relationship of δ 18 O shell , SST, and SSS.
Climatic variation in the Meghalayan (which began 4200 BP in the Late Holocene) has significant impacts on human society and ecosystem development. However, early Meghalayan climatic conditions in SE Asia around the South China Sea still remain poorly understood. Shi (1994) reviewed data from various sources (such as ice cores, inland lakes, paleosols in loess and eolian sands, sea-level fluctuations, palynological and botanical studies) in China and found that the early Meghalayan is a part of the Holocene megathermal period (8 to 3 kyr BP). Sediments in the South China Sea also imply that the temperature might have been relatively higher in the early Meghalayan than in the present (Ouyang et al., 2016). However, these studies are lowresolution, and high-resolution records under interannual climate variation are rare. With global warming and numerous climatic disasters happening in recent decades, climatic conditions in the early Meghalayan could serve as an analogue to modern problems and have received increasing scientific attention (Schirrmacher et al., 2019;Scuderi et al., 2019;Toth and Aronson, 2019;Zhang et al., 2018). Recent studies of bi-valve mollusk specimen (Arctica islandica) oxygen isotopes show high-resolution data with seasonal signals Wanamaker et al., 2011). High-resolution isotopic geochemical data from Tridacna may also provide detailed insight into climatic variations in the early Meghalayan.
Furthermore, El Ninõ-Southern Oscillation (ENSO) is widely accepted as the main source of interannual climatic variability in the Pacific Ocean. Previous studies suggest that the impacts of ENSO activity are not limited to tropical areas but might also apply to global atmospheric circulation through the heating-up of the tropical atmosphere (Cane, 2005). Thus, reconstructing ENSO is very important for understanding its dynamics and predicting future change. Many early studies on ENSO behaviors were constructed with lowresolution proxy data using deposition events (Rodbell et al., 1999;Koutavas and Joanides, 2012) or ice cores (Thompson et al., 1995) in order to reveal ENSO variance over thousands of years. However, the periodicity of ENSO is short, making it difficult to use these low-resolution data to precisely determine the strength and variability of ENSO activity. Recent studies focus on seasonal or monthly data to examine precise variation of ENSO activity (Arias-Ruiz et al., 2017;Ayling et al., 2015;McGregor et al., 2013;Welsh et al., 2011;Yan et al., 2017), but those fragmental data cannot fully explain the Holocene ENSO dynamics. Therefore, fragments from different times according to different high-resolution samples are needed and can provide an integrated framework for examining ENSO theory and models of the Holocene. In addition, studies on the Middle to Late Holocene ENSO evolution yield controversial findings: coral records show a reduced ENSO variability around the early Meghalayan (Tudhope et al., 2001;McGregor et al., 2013;Cobb et al., 2014;Woodroffe et al., 2003). Other carbonate species like fossil mollusk shells suggest that ENSO variance was severely damped ∼ 4000 years ago (Carré et al., 2014). Yet other studies indicate strengthening ENSO activity at 4 to 3 ka (Duprey et al., 2014;Yang et al., 2019). Thus, this further points to the importance of high-resolution isotopic geochemical data such as from Tridacna in unraveling the dynamics of ENSO.
This study aims to evaluate seasonality, climate variation, and ENSO activity in the Xisha Islands of the northern South China Sea, based on two high-resolution δ 18 O shell profiles of modern and fossil Tridacna. The study area is situated in the northwest margin of the west Pacific warm pool (WPWP), and the local climate is widely accepted to be directly responsive to ENSO activity (Mitsuguchi et al., 2008;Yan et al., 2010). A modern Tridacna gigas shell was first used to estimate the extent of environmental control (SST and SSS) on δ 18 O shell , and a new SST-δ 18 O shell linear regression was proposed. Subsequently, a fossil Tridacna squamosa (which lived to 40 years) was used to reconstruct seasonality and climatic variation, and the obtained results are compared with the modern species and meteorological observations. Finally, ENSO activity and extreme El Ninõ winter events were discussed, using the re-established SST anomalies.

Regional setting
The South China Sea is located in the northwest of WPWP (Fig. 1a), and its interannual climate is closely related to ENSO activities (Mitsuguchi et al., 2008;Yan et al., 2010). The Xisha Islands in the northern South China Sea are substantially influenced by two contrasting Asian monsoons from opposite directions: the Asian summer monsoon from the southwest and the Asian winter monsoon from the northeast. These two monsoons provide distinct seasonal SST for the Tridacna populating the coral reefs of the Xisha Islands. Our sample (Tridacna squamosa A5) was collected in the North Reef (17 • 05 N, 111 • 30 E), whilst the modern Tridacna gigas sample YX1 (studied previously by  was acquired from Yongxing Island (16 • 50 N, 112 • 50 E), which is about 90 km away from the North Reef (Fig. 1b).
Meteorological observations (atmosphere temperature, AT; SST; SSS; rainfall) were obtained from the Institute of Meteorology of China, which has taken records for the Xisha Islands since 1958. In order to compare geochemical analyses with monthly environmental data, isotopic records and meteorological observations were resampled according to the method suggested by Schöne and Fiebig (2009). They used bivalve shells (Arctica islandica) to reconstruct the climate, examining that seven points per year would minimize the influence of different growth rates throughout the year; meanwhile, only the annual sample number for which more than or equal to seven existed could be used. As the yearly minimum number of δ 18 O Y X1 is seven, 1 year includes 7 resampled months (r months). Figure 1d shows the r-monthly average time series of AT, SST, SSS, and rainfall, and their standard deviations (SDs). The mean SST is 27.77 • C, and AT shows a highly positive correlation with SST (r = 0.98), but it is about 0.7 • C lower. The SST seasonality is 5.33 • C, with the lowest value and highest value occurring in first and fourth r months, respectively. It is excluded that river runoff effects on SSS as the Xisha Islands are about 300 km away from the continent (Hainan Island). SSS varies from 33.25 ‰ to 33.81 ‰, and the change is mainly dominated by rainfall: higher SSS in dry winters and lower SSS in wet summers (Fig. 1e).
The SST data in the North Reef are acquired from NOAA HadISST, a global monthly SST data with a spatial resolution of 1 × 1 • (data grid cell includes both the North Reef and Yongxing Island) from 1982 to 2017. Ninõ 1 + 2 SST data are obtained from NOAA monthly data between 1982 and 2017 (http://www.cpc.ncep.noaa.gov/data/indices/sstoi. indices; last access: 31 December 2017).

Shell descriptions and sample preparation
The original fossil Tridacna was cut from the umbo to the ventral (red line in Fig. 1b), where the thickness of the inner layer is the greatest. From the slice we cut, the fossil Tridacna has three different zones ( Fig. 1c): the inner layer, the outer layer, and the hinge. A recent study investigating the architecture of Tridacna shells shows a crossed lamellar microstructure with a strong fiber texture with optimized mechanical performance (Agbaje et al., 2017), and the mineralization of inner layer and outer layer is independent of each other (Gannon et al., 2017). The inner layer is chosen for the analyses because of its clear growth layer and well-preserved shell. Published data also reveal that inner layer δ 18 O values are unaffected by ontogeny (Welsh et al., 2011) and could better reflect actual δ 18 O than the outer layer or the hinge (Pätzold et al., 1991;Elliot et al., 2009).
The determination of radiocarbon age was performed at the Institute of Earth Environment of Chinese Academy of Sciences. The 14 C accelerator mass spectrometry data revealed that the fossil Tridacna gigas age is 3437 ± 28 yr BP. Due to the lack of an obvious "reservoir effect" in the dating results of modern Tridacna shells, the atmospheric 4 C yield model is used for calibration . The calibrated date (2σ ) ranges from 3733 to 3613 cal BP, with the median date is 3691 cal BP by using the IntCal13 of Radiocarbon Calibration Program CALIB 7.10 (http://calib.org, last access: 31 December 2018). Both X-ray diffraction (XRD) and laser Raman spectrometers results show aragonite, and no other substances are found.

Stable isotopes
Each stable isotope sample was micromilled parallel to the growth layer with 1 mm long and 100 µm deep under a microdrill automated system (Micro-Drill New Wave Research, Olympus SZ 61) in the Isotope Laboratory of Xi'an Jiaotong University, China. Four intervals were used according to the growth rates: 100 µm (n = 1 to 268), 150 µm (n = 269 to 481), 200 µm (n = 482 to 657), and 300 µm (n = 658 to 765) in a transect from adult to ontogenetically younger shell, respectively (Fig. 2a).
The δ 18 O of the Tridacna was analyzed in the Isotope Laboratory of Xi'an Jiaotong University, using the Thermo Finnigan MAT-253 mass spectrometer fitted with the Kiel IV Carbonate Device. All results were reported in per mil (‰), relative to the Vienna Pee Dee Belemnite (VPDB) standard. The standard GBW04405, which has been compared with international standard NBS-19, was added to the analyses every 10 to 20 samples to check reproducibility. The average value of standard powder in δ 18 O is −8.49 ± 0.14 ‰. Duplicate measurements of GBW04405 standards and samples showed long-term reproducibilities (1σ ) of less than 0.14 ‰ and 0.05 ‰, respectively. Published data of the modern Tridacna gigas shell YX1 were used to investigate the relationship between Tridacna δ 18 O and the local climate . YX1 was collected from Yongxing Island, 90 km ESE of the North Reef (Fig. 1b). The internal carbonate standard of modern Tridacna YX1 δ 18 O (VPDB) was also GBW04405; the standards and samples had reproducibilities (1σ ) of better than 0.08 ‰ and 0.06 ‰, respectively.

Data processing and analyses
PearsonT3 (Version 2.2, January 2017) was used to test the correlation coefficient. Successive sets of 100 years' length were calculated to estimate monthly insolation using the software AnalySeries 2.0.8 (Laskar et al., 2004), which contained the probable life span of Tridacna (A5) considering 2σ confidence intervals of corrected age. The timescale of modern insolation ranges from 1918 to 2017, while the past ranges from 3722 to 3623 BP. Statistical analyses were per-formed with the software Origin 2018 and PAST (Paleontological Statistics) 3.18. The isotopic records, meteorological observations, and insolation data were resampled for seven points per year using the software AnalySeries 2.0.8, as used for other studies in sclerochronology (Schöne and Fiebig, 2009;Wanamaker et al., 2011).

δ 18 O A5 record
Seasonal cycles are distinct in the δ 18 O A5 profile (Fig. 2

Sclerochronology
From the shell section, dark-bright line couples (each couple represents 1 year) can be seen clearly (Fig. 3a). Following the δ 18 O A5 profiles, these short, dark lines (transparent) correspond to higher δ 18 O A5 values, which means that Tridacna grew in lower temperature (cold seasons such as December to February). In contrast, lower δ 18 O A5 values lie in the long bright lines (opaque), corresponding to the higher temperatures (warm seasons such as March to November). Annual growth rates can be calculated with the δ 18 O A5 seasonal cycles and interval distance (Fig. 3c). The results show that growth rates were higher when Tridacna A5 was young, reaching 5 mm yr −1 . The growth then slowed down and stabilized to 1-2 mm yr −1 after the Tridacna had matured (Fig. 3c). Furthermore, daily increments visible as pairs of dark and bright increments can be seen under the microscope (Fig. 3b). A fragment was chosen where δ 18 O values were nearly the highest in a particular year. This period fell during the cold season, when the daily growth increment was about 4.5 µm. When the temperature rose as warm season began, Tridacna grew faster, with daily growth increment reaching up to 8 µm. This situation occurred throughout the Tridacna's life (Yan et al., 2020). In general, Tridacna A5 grew faster in warm seasons and slower in cold seasons.
The SST observation in the Xisha Islands suggested that the first r month nearly corresponds to the lowest SST. Thus, the highest δ 18 O of each cycle was chosen as the beginning of a year. Previous studies have demonstrated that Tridacna is in oxygen isotopic equilibrium with the surrounding seawater (Aharon, 1983;Watanabe et al., 1999), which also holds true for Tridacna in the South China Sea . Biogenic carbonate δ 18 O values show linear correlations with SST and seawater δ 18 O water (Aharon and Chappell, 1986;Pätzold et al., 1991;Romanek and Grossman, 1989). The δ 18 O shell -SST-δ 18 O water Eq. (1) of Grossman and Ku (1986) is adopted, as it is widely used in calculations for tropical aragonite mollusk species. Meanwhile, δ 18 O water has a positive relationship with SSS, and Eq. (2), which was established using seawater in the northern South China Sea (Hong et al., 1997), is chosen for the calculation. We merge Eqs. (1) and (2)  (1) The δ 18 O shell reflects a combination of SST and SSS variation. In order to quantify more precisely the relation between those factors and δ 18 O shell , two δ 18 O profiles are calculated (Fig. 4a) (Table S1 in the Supplement). The δ 18 O Y X1 and δ 18 O predicted profiles have nearly the same mean value (1.15 ‰ and 1.14 ‰, respectively), and their positive correlation (r = 0.81, n = 77) indicates that the local Tridacna precipitates its shell in oxygen isotopic equilibrium. Moreover, the comparison of predicted SST (under constant SSS and actual SSS with δ 18 O Y X1 ) further confirms that the SSS variation has no significant effect on the local reconstructed SST (Fig. 4f). The two predicted SST values were highly similar (r = 0.93), and they are well correlated with the actual SST (r vary = 0.79, r constant = 0.78). Thus, we can use δ 18 O shell to roughly estimate the seasonal local SST variation and to establish a new SST-δ 18 O shell linear regression: SST ( • C) = 22.69 − 4.41 × δ 18 O shell (or δ 18 O shell (‰) = −0.136 × SST + 2.634). A 1 ‰ change of δ 18 O shell is roughly equal to 4.41 • C of SST. Yu et al. (2005b) summarized many published δ 18 O-SST slopes for another marine carbonate species, Porites lutea coral, and suggested that the slopes could range from −0.134 to −0.189. Corals from Hainan Island revealed good δ 18 O vs. SST correlation, with a linear regression slope of −0.137 (Su et al., 2006), very similar to our result (−0.136). Consequently, use of the new linear regression for reconstructing the past SST with the fossil δ 18 O shell is a valid approach.

Indication of seasonal variation in modern Tridacna
According to δ 18 O Y X1 (−0.60 ‰ to −1.52 ‰) and δ 18 O predicted (−0.47 ‰ to −1.57 ‰) profiles (Fig. 4b), seasonality is shown with the lowest value occurring in the first r month (cold season) and the highest value in the fourth r month (warm season). The difference in seasonality between δ 18 O Y X1 and δ 18 O predicted is 0.18 ‰, which accounts for 19 % of δ 18 O Y X1 . This situation may be due to the different growth rates and equidistance sampling mode. In each year, the analyzed Tridacna grew faster in warmer seasons than in colder seasons; thus, specimens under equidistance sampling mode have more samples in the warm seasons. Fewer points in the cold seasons decrease the values and lead to a lower δ 18 O shell in the first r month, but the higher number of points makes δ 18 O shell close to δ 18 O predicted in the warm seasons (nearly identical in the fourth r month). Moreover, throughout the life of the analyzed Tridacna, the δ 18 O shell yearly amplitude increasingly approaches the actual δ 18 O predicted when using a greater number of points (fast growth rate) before reaching maturity. After the Tridacna reached maturity, the fewer points obtained under equidistance mode in a year yielded a lower amplitude. This can explain the minor discrepancy between δ 18 O shell and δ 18 O predicted . As a result, δ 18 O shell slightly reduced the actual seasonal variation. However, the correlation between them is high (r = 0.81, n = 77), and the mean δ 18 O Y X1 (−1.15 ‰) and mean δ 18 O predicted (−1.14 ‰) values are similar. Therefore, δ 18 O shell can also be used to estimate the actual seasonal variation, with caution regarding the slightly reduced variation.

Reconstructed climate with fossil
The fossil Tridacna lived 3700 years ago during the early Meghalayan. The 40 δ 18 O A5 cycles reveal that Tridacna A5 had probably lived for at least 40 years. After calculating data into r-monthly average profiles, the extreme seasonal variation effects were minimized. The mean δ 18 O A5 is −1.34 ‰, with a minimum and maximum of −1.66 ‰ and 0.66 ‰, respectively (Fig. 4c). Contrasting with the mean value of YX1 (−1.15 ‰), the lower δ 18 O A5 mean value may have reflected the higher temperature that Tridacna A5 experienced during the warmer season. To translate into SST (without consider- ing the SSS changes), the temperature was estimated to be roughly 0.84 • C higher than the present. This agrees with other lines of evidence that suggest a higher temperature during that period (Ouyang et al., 2016), considered to be part of the Holocene megathermal in China (Shi et al., 1994).
The average r-monthly seasonal range of this period (1 ‰) is similar to that yielded from YX1 (0.92 ‰). The SDs of δ 18 O A5 (0.38 ‰, n = 281) and δ 18 O Y X1 (0.35 ‰, n = 77) are also similar. These results show similar climate change 3700 years ago and in the present. However, the life of Tridacna YX1 (11 years) was much shorter than the fossil Tridacna (which lived for at least 40 years), and YX1's location is in the south of A5's location; thus modern observation data from the North Reef were used to do the climatic comparison. After translating δ 18 O A5 into SST (Fig. 5), the reconstructed SST shows an average maximum and minimum of 30 and 25.61 • C, respectively, with a seasonal variation of 4.39 • C (Fig. 4e). Comparatively, the r-monthly average range of modern observation is 29.33 to 23.99 • C (from 1982 to 2017), with a seasonal variation of 5.34 • C (Fig. 4e). The warmer climate in the past, associated with seasonality variance, is about 0.95 • C lower. Considering the seasonality discrepancy between δ 18 O shell and δ 18 O predicted , the δ 18 O shell has a 19 % lower seasonal variation than δ 18 O predicted . Therefore, the actual seasonal variation of A5 (roughly 5.23 • C) is still below present seasonality.
In addition, the discrepancy between mean δ 18 O A5 and mean δ 18 O Y X1 is 0.19 ‰; the lower mean δ 18 O A5 is because of more r months in lower values. This reveals a possible prolonged high-temperature period 3700 years ago: warm seasons may have been longer, while cold seasons may have been shorter. This agrees with a comparison between 3700 years ago (3722 to 3623 BP) and the past century (1918 to 2017), which indicates Tridacna A5 lived in more insolation. This occurs from the second to fifth r month (warm seasons); however, less insolation occurs in the rest of the months (Fig. 4d). Thus, the prolonged high temperature in the past might be attributed to more insolation. In www.clim-past.net/16/597/2020/ Clim. Past, 16, 597-610, 2020 addition, although a higher sampling density obtained in the warm seasons enlarges the high-temperature period (from the second to sixth r month), a cold-to-warm transition could still be recognized in A5 and YX1 δ 18 O profiles (Fig. 4c).
Comparison of each r-monthly value with the average value shows that between the first and second r month, there was a larger deviation with a greater slope 3700 years ago. This illustrates a fast transition between cold and warm seasons 3700 years ago. As δ 18 O predicted has stronger seasonal variation than δ 18 O shell , the slope should be sharper, which means more significant actual seasonal transition. Overall, the climate around 3700 years ago had slightly lower seasonality than the present, and the transition between cold and warm seasons was starker.

Climate variation comparison between 3700 years ago and present
A comparison was performed between the modern instrumental observations (from 1982 to 2017) in the North Reef and the reconstructed SST anomalies of Tridacna A5. The r-monthly resolution data were first compared, obtained by subtracting the r-monthly SST with the mean value of each r month. In terms of long-term climatic variation, the SST anomalies are markedly different between the 36-year modern instrumental data and the 40-year reconstructed data (Fig. 6a). The SST anomalies (3700 years ago) have sharper peaks and a greater amplitude than in those of recent years, and the SD in the past is much larger (0.68 • C) than in the present (0.42 • C), suggesting more severe climate conditions in the past. However, the deviation should be noted alongside the different growth rates during Tridacna's life span and in equidistant sampling mode. For example, Tridacna may have different annual growth rates; hence an r-monthly value may not represent the corresponding actual r-monthly value under equidistant sampling mode. In this respect, the r-annual SST anomalies are estimated to reduce the deviation (Fig. 6b). The SD of modern observation SST anomalies is 0.30 • C, and the SD of reconstructed SST anomalies is 0.41 • C. This illustrates that the modern-to-past ratios of the r-monthly resolutions or r-annual resolutions are almost the same (0.65 and 0.73, respectively); thus the SD of r-monthly SST anomalies of Tridacna is likely a reliable measure. As a result, the enhanced climate variability 3700 years ago probably indicates increased ENSO-related variability in this region. This conclusion contradicts data from samples (deepsea sediments and fossil mollusk shells) collected in the eastern tropical Pacific at the same time period (Koutavas et al., 2012, Carré et al., 2014. More data should be analyzed from long, successive time periods to understand more about the dynamics of ENSO on a large scale.

ENSO activity recorded by Tridacna δ 18 O
As ENSO is the strongest contributor to global interannual climate variation, a better understanding of its fundamental properties will allow us to better unravel past climate change episodes and to make more accurate predictions for the future. Interannual climate changes in the Xisha Islands were likely dominated by ENSO activity. The local accumulated positive percentage of monthly SST anomaly threshold responds to 76.47 % El Ninõ and 79.41 % La Niña events in the Ninõ 3.4 region (Liu et al., 2016). Previous studies demonstrate that marine biogenic carbonate-based SST reconstructions in the northern South China Sea likely responded to ENSO activity (Sun et al., 2005;Yan et al., 2017). Warm (cold) SST anomalies are related to El Ninõ (La Niña) events. Coral has one of the earliest records revealing ENSO events (Peng et al., 2003;Sun et al., 2005;Wei et al., 2007), yet there are still some technical limitations in using coral, such as those concerning post-depositional diagenetic alteration between aragonite and calcite (McGregor and Gagan, 2003). Analyses of Tridacna species are performed to overcome this limitation by taking advantage of their denser shells, lack of diagenetic alteration, and oxygen isotopic equilibrium with seawater. Recently, Yan et al. (2014) proved that Tridacna species in the Xisha Islands respond to ENSO activity, and then they used fossil Tridacna δ 18 O on Dongdao Island (part of the Xisha Islands) to reconstruct the ENSO variability around 2000 years ago (Yan et al., 2017).
To acquire more precise ENSO reconstructions, modern observation data were analyzed and compared with the SST in Ninõ 1 + 2 region. The SST anomaly series were calculated by subtracting the r-monthly mean values. The spectral analyses were performed to test periodicity among all SST anomalies (Fig. 7), which indicate a spectral peak of 3 to 7 years. According to the SST series, the North Reef SST has a 3-r-month time lag behind the Ninõ 1+2 SST (Fig. 8a), and thus 3 r months of the North Reef SST were brought forward to eliminate the lag. To reconstruct the occurrence of ENSO in the North Reef, 3-7 years of bandpass filtering was performed on the SST anomalies, which yielded North Reef ENSO activity mostly consistent with the Ninõ 1 + 2 SST anomalies (Fig. 8c). A threshold value was calculated under 1σ SST anomalies for moderate El Ninõ-La Niña events. A total of 7 El Ninõ and 10 La Niña events occurred in the past 36 years. In other words, El Ninõ-La Niña events occurred successively at a 5.14-year frequency in the North Reef.
Spectral analysis revealed that δ 18 O A5 anomalies also have a 3-7-year period (Fig. 7c). As discussed above, the Tridacna δ 18 O values are mainly dominated by SST in the Xisha Islands, and 1 ‰ δ 18 O shell is roughly equal to 4.41 • C of SST. δ 18 O A5 anomalies were transformed into the North Reef SST A5 anomalies (Fig. 9b). After the 3-7 years of bandpass filtering of the North Reef SST A5 anomalies, six El Ninõ and five La Niña events were estimated to occur over 40 years with a 1σ SST A5 anomaly threshold (Fig. 9c), giving a 6.67and 8-year frequency, respectively. The ENSO frequency is reduced when compared with modern observation data. The lower frequency is supported in ENSO reconstructions back to 7 ka, which suggest a notable reduction of ENSO between 5 and 3 ka (Liu et al., 2013;McGregor et al., 2013;Tudhope et al., 2001;Emile-Geay et al., 2016). However, implications drawn from a mere 40-year-long Tridacna δ 18 O record are likely inconclusive. A collection of more similar-aged Tridacna is needed to develop a more continuous climate and ENSO activity record in Holocene.

Extreme winter El Ninõ records in fossil Tridacna δ 18 O values
In recent decades, extreme El Ninõ has brought about many climatic disasters, such as catastrophic flooding, bushfire and drought (Ramírez and Briones, 2017;Staupe-Delgado et al., 2018;Yu et al., 2018Yu et al., , 2019. With global warming persisting, the question of whether high temperatures are related to extreme El Ninõ events is still controversial. Therefore, records of extreme El Ninõ events in past warm periods are important. Here, the winter SST is used to estimate extreme El Ninõ events. Winters in the northern South China Sea are very dry, and the SSS variation caused by rainfall is small.  Thus, the SST determined from δ 18 O shell should be close to the actual value. The SST calculated by δ 18 O Y X1 reveals a warmer winter in 1998, corresponding to a stronger El Ninõ that year. A comparison between the reconstructed SST (calculated with δ 18 O A5 ) and modern observation data from the North Reef (Fig. 5) suggested that the average winter SST 3700 years ago was 25.62 • C. There are six distinctly high SSTs within the 40 years (gray fields in Fig. 5), with anomalies ranging from 0.73 to 2.00 • C. As for the SST of modern observations (from 1982 to 2017), the average of winter SST is 23.99 • C, and three anomalously warm temperatures vary from 0.60 to 1.38 • C. It seems that extreme El Ninõ winter events were very frequent in this past warm period. However, this analysis still provides low confidence in answering this controversial question about the relationship between El Ninõ events and warm climate; more Tridacna in the past warm period should be analyzed in future work. Nevertheless, our results still put forward high-resolution data that make a contribution to future work on how El Ninõ events occur in warm periods.

Conclusions
The δ 18 O values derived from Tridacna provide highresolution data, useful to unravel climatic variability and ENSO activity. In the Xisha Islands of the northern South China Sea, the δ 18 O shell of modern Tridacna gigas can serve as a proxy for SST, while SSS has a minor effect on the δ 18 O shell . Thus, a rough δ 18 O-SST linear regression is established: SST ( • C) = 22.69 − 4.41 × δ 18 O shell . Another Tridacna squamosa A5, which lived 3700 years ago, reveals 40 clearly dark-bright line couples consistent with δ 18 O shell profiles. Reconstructed SST implies a warmer climate 3700 years ago, 0.84 • C higher than the present. The seasonal variation slightly decreased, and the transition among cold to warm seasons was faster. The combinations of SST anomalies reconstructed at r-monthly-r-annual resolution suggest enhanced ENSO-related variability during this past warm period. In addition, the frequency of ENSO activity was less 3700 years ago than during the recent 36 years of modern observations. El Ninõ-La Niña events occurred alternatively at a frequency of every 6.67 and 8 years in the past, compared to every 5.14 years in recent decades. Extreme El Ninõ winters have been recorded by a fossil Tridacna with increased numbers and intense variations. Our results imply an unstable climate 3700 years ago, although more data are still needed to support this hypothesis.