Orbital and Millennial Variations in Sea Ice in the Southwestern Okhotsk Sea Since the Last Interglacial Period and Their Implications
Anqi Wang1 
Zhengquan Yao1,2* 
Xuefa Shi1,2* 
Kunshan Wang1,2 
Jianjun Zou1,2 
Yanguang Liu1,2 
Yonghua Wu1,2 
Sergey A. Gorbarenko3- 1Key Laboratory of Marine Geology and Metallogeny, First Institute of Oceanography, Ministry of Natural Resources, Qingdao, China
- 2Laboratory for Marine Geology, Pilot National Laboratory for Marine Science and Technology, Qingdao, China
- 3V.I. Il’ichev Pacific Oceanological Institute, Far East Branch of Russian Academy of Science, (FEB of RAS), Vladivostok, Russia
Sea ice in the Okhotsk Sea plays a significant role in global climate change. However, the history and mechanism of changes in sea ice spanning the last glacial cycle remain controversial. In this study, an 8.8 m core (LV55-40-1) was recovered from the southwestern Okhotsk Sea that contains a continuous sea ice record over the past ∼110 kyr. The sand fraction and dropstones were used as ice-rafted debris proxies to reconstruct the history of sea ice variations over the last ∼110 kyr and to determine the underlying causes on orbital and millennial timescales. Sea ice expansions occurred during MIS 5b, MIS 4, mid-MIS 3, and early MIS 1, which were controlled mainly by decreased autumn insolation on an orbital timescale. Superimposed on the orbital-scale changes, millennial-scale variations in sea ice were also observed, with 19 expansion events that coincided with cold Dansgaard-Oeschger stadials. Millennial scale sea ice variations were most likely controlled by both the Arctic oscillation and the East Asian summer monsoon. During periods of negative Arctic oscillation patterns, decreased air temperatures over the Okhotsk Sea caused more active sea ice formation. Such conditions could have been reinforced, by a reduced influence of warm advection at the surface of the Okhotsk Sea caused by decreased discharge from the Amur River that resulted from a weakened East Asian summer monsoon during cold stadials.
Introduction
Sea ice is widespread in the subarctic North Pacific, and its expansion and retreat impact local and global climate changes by modulating the sea ice-induced albedo and energy budgets at both high and low latitudes (Turner et al., 2015; Serreze et al., 2016). Variations in sea ice influence the primary productivity in the Okhotsk Sea (Seki et al., 2004; Iwasaki et al., 2012; Jimenez-Espejo et al., 2018), as well as global ocean circulation and ventilation (Itaki, 2004). Consequently, sea ice variations on geologic timescales have played a significant role in paleoclimatic changes (Harada et al., 2012).
The Okhotsk Sea is located at the southernmost boundary of the region influenced by sea ice, and approximately two-thirds of the sea are covered by sea ice during the winter (Sakamoto et al., 2006). Therefore, sea ice coverage in the Okhotsk Sea is very sensitive to local and global changes in oceanography and climate (Nürnberg and Tiedemann, 2004; Seki et al., 2004; Sakamoto et al., 2005, Sakamoto et al., 2006; Nürnberg et al., 2011; Vasilenko et al., 2017; Vasilenko et al., 2019). The history of sea ice variations and their underlying causes have attracted attention from the paleoceanography research community (e.g., Nürnberg and Tiedemann, 2004; Sakamoto et al., 2006; Nürnberg et al., 2011; Vasilenko et al., 2017; Vasilenko et al., 2019; Lo et al., 2018). However, sea ice variations and their driving mechanisms over the last glacial cycle remain controversial. Some studies have suggested that the entire Okhotsk Sea has been influenced by seasonal/annual sea ice since the last interglacial period (Gorbarenko et al., 2003; Seki et al., 2004; Sakamoto et al., 2005; Sakamoto et al., 2006; Vasilenko et al., 2019; Gorbarenko et al., 2020), while other studies have demonstrated that perennial sea ice was present during severe cold stages, such as MIS 4, MIS 2 (Wang and Wang, 2008; Vasilenko et al., 2019), and at ∼30 ka (Lo et al., 2018). Moreover, the mechanisms driving sea ice variations on orbital and millennial timescales are still debated. Previous studies have suggested that sea ice variations on orbital scales are controlled largely by glacial–interglacial cycles (Gorbarenko et al., 2002; Gorbarenko et al., 2003; Nürnberg and Tiedemann, 2004; Sakamoto et al., 2005). However, C25 highly branched isoprenoid (IP25)-derived sea ice records suggest that variations in sea ice in the central Okhotsk Sea were controlled by both insolation and atmospheric CO2 concentrations (Lo et al., 2018). In contrast, sea ice variations on millennial scales are more complex. Vasilenko et al. (2017) demonstrated that millennial-scale sea ice expansion was controlled by the velocity of geostrophic winds that dominated over the Okhotsk Sea, as the direction of ice drift coincided with the wind direction. The Arctic Oscillation (AO) is a dynamic atmospheric process in which the associated pressure changes over the Arctic influence atmospheric circulation over the Eurasian continent and adjacent areas (Thompson, 1998). It has been suggested that polar atmospheric circulation in the northern hemisphere is a key process that affects sea ice expansion on millennial scales (Sakamoto et al., 2006). Sakamoto et al. (2006) also inferred that discharge from the Amur River and polar atmospheric dynamics were potential factors that control sea ice expansion on millennial scales. Based on sea ice extents and inter-annual variations in Amur River discharge, Ogi et al. (2001) found a strong correlation between sea ice extent in the Okhotsk Sea and monsoon-induced fluvial discharge. However, there is no evidence suggesting that such a mechanism operates on geologic timescales. In addition, most of the sedimentary records related to sea ice changes during the last glacial cycle were from the central and eastern parts of the Okhotsk Sea, records from the southwestern Okhotsk Sea that are sensitive to fluvial effects are scarce. The southwestern Okhotsk Sea is subject to the influence of fluvial discharge via the East Sakhalin Current (Zhabin et al., 2010). Therefore, this is an ideal region for studying the history of sea ice cover and its potential connections with fluvial discharge. In this study, we analyzed an 8.8 m long core (LV55-40-1) collected from the southwestern Okhotsk Sea to determine the history of sea ice variations since ∼110 ka. Combined with previous results, we attempted to determine the dominant factors that control sea ice variations at orbital and -millennial timescales during the last glacial cycle.
Regional Setting
The Okhotsk Sea is the second largest marginal sea in the Pacific Ocean. It is surrounded by the Asian continent, Sakhalin Island, the Kamchatka Peninsula, the Kuril Islands and the island of Hokkaido. The Okhotsk Sea is connected to the North Pacific and the Japan Sea by the Straits of the Kuril Islands and by the Tatar and Soya straits, respectively (Figure 1).
FIGURE 1. Map of the Okhotsk Sea showing the locations of the core used in this study (LV55-40-1, red star) and other cores (blue dots) mentioned in the text (Sakamoto et al., 2006; Harada et al., 2008; Lo et al., 2018). Blue arrows indicate the East Sakhalin Current (ESC), West Kamchatka Current (WKC), and Soya Warm Current (SWC). The dashed line represents the average sea ice boundary from November to June according to Lo et al. (2018). Map generated using Ocean Data View version 4 (Schlitzer, 2021).
Surface circulation in the Okhotsk Sea is characterized by a cyclonic gyre composed of the West Kamchatka Current (WKC), East Sakhalin Current (ESC), and the salty Soya Warm Current (SWC). The ESC flows along Sakhalin Island southward toward the Kuril Islands, and finally leaves the Okhotsk Sea through the Bussol Strait (Lapko and Radchenko, 2000). The water mass at 300–800 m depth in the Okhotsk Sea is called the Okhotsk Sea Intermediate Water (OSIW) and is characterized by low-density (26.7–27σθ), low-salinity (33.8‰), and oxygen-rich water (Morley and Hays, 1983; Talley, 1993; Yang and Honjo, 1996). The OSIW has similar characteristics to the North Pacific Intermediate Water (NPIW) and is regarded as the present source of NPIW (Talley, 1991; Yasuda, 1997; Freeland et al., 1998; Martin and Kawase, 1998; Wong et al., 1998). Below the OSIW, ancient deep Pacific water masses enriched in CO2 flow into the Okhotsk Sea through the Krusenstherna Strait and flow out through the Bussol Strait (Nürnberg and Tiedemann, 2004).
The Amur River is the largest river in East Siberia and is adjacent to the northwestern continental shelf of the Okhotsk Sea. The drainage area of the Amur River is ∼1.85 × 106 km2 (Mclennan, 2013). The river delivers ∼14 t km−2 of sediment to the northern Okhotsk Sea annually, which is two to three times higher than that of other Siberian rivers, including those that drain into the Arctic Ocean (Anikiev et al., 2001). Freshwater input from the Amur River is approximately 310 km3 per year (Vörösmarty et al., 1996) and is mainly affected by the East Asian Summer Monsoon (EASM). Due to EASM precipitation and melting snow at high altitudes, the Amur River discharge is the highest during August–October, also producing the warmest water in the Okhotsk Sea (∼20°C) during the same period (Ogi et al., 2001). The formation of a low-salinity layer in the Okhotsk Sea is mainly due to inflow from the Amur River (Freeland et al., 1998).
Sea ice in the Okhotsk Sea initially forms in November, starting in the northwestern part of the basin and repeatedly expanding southward (Sakamoto et al., 2005) due to transport by the northerly winds and the southward flow of the Okhotsk Sea (Ohshima et al., 2001; Wang et al., 2021). This creates a polynya along the coast and forms new sea ice (Sakamoto et al., 2005; Sakamoto et al., 2006). Sea ice in the Okhotsk Sea reaches its maximum extent during March, with a maximum thickness of ∼1 m (Rycroft, 1995). The sea ice disappears entirely in June, with ice-free conditions from July to October (Parkinson et al., 1987). The expansion and retreat of sea ice are influenced not only by ocean–atmosphere interactions, but also by the density of the surface water that influences ocean circulation (Ohtani and Nagata, 1990). Intense sea ice formation causes brine rejection and forms Dense Shelf Water on the northern Okhotsk Sea shelves (Martin and Kawase, 1998; Gladyshev, 2003) and contributes to the formation and ventilation of the NPIW (Ohtani and Nagata, 1990; Talley, 1991; Wong et al., 1998).
Materials and Methods
Core Description
Core LV55-40-1 (48.12°N, 147.15°E) was recovered from the northern Kuril Basin in the southwestern Okhotsk Sea at a water depth of 1,730 m (Figure 1). The 8.8 m thick deposits were composed of homogeneous olive gray (5Y 4/2) silty clay with distinctive layers dominated by coarse-grained sand and gravel at 340–345 cm and 385–388 cm depths. These layers were also characterized by extremely high magnetic susceptibility, and abundant volcanic glass (Figure 2).
FIGURE 2. Variations in (A) Magnetic Susceptibility, (B) Numbers of dropstones, and (C) Grain-size compositions with depth in core LV55-40-1.
Accelerator Mass Spectrometer 14C Dating
Mixed samples of the planktonic foraminifera Neogloboquadrina pachyderma (sinistral) and Globigerina bulloides larger than 145 μm were collected from the core for accelerator mass spectrometer (AMS) 14C dating (Table 1). The AMS 14C analyses were performed by Beta Analytic Laboratory. Calibrated calendar ages were converted using CALIB 8.20 (Stuiver and Reimer, 1993) with the MARINE20 database (Heaton, 2020) and a calculated weighted mean △R = 450 ± 90 a (Lo et al., 2018).
TABLE 1. AMS14C ages and calendar ages obtained from core LV55-40-1.
X-Ray Fluorescence Scanning Analyses
X-ray fluorescence (XRF) scanning was performed at 0.5 cm intervals using an Itrax XRF core scanner with a 20 s count time, an X-ray voltage of 30 kV, and an X-ray current of 40–55 mA, which allowed for rapid, non-destructive, high-resolution elemental analyses of the sedimentary cores (Jansen et al., 1998).
Biogenic Silica Analyses
Biogenic silica (opal) analyses were performed on 440 samples using molybdate blue with modified pretreatments (Mortlock and Froelich, 1989). Opal was extracted using 40.0 ml of 0.2 mol/L NaCO3 solution at 85°C for 6 h. During the analyses, 2 ml of C₂H₂O₄ was added to avoid interference by P and As. The opal contents were quantified using a Mettler UV5 spectrophotometer. The relative standard deviation (RSD) was less than 3%.
Chlorin Analyses
A total of 440 samples were analyzed to determine the chlorin concentrations with modified pretreatments (Harris and Maxwell, 1995). Briefly, ∼1 g of each sample was extracted using 20 ml of 90% acetone and stored at 4°C for 24 h in the dark. The extracted liquor was centrifuged and filtered through GF/F membranes. The chlorin concentrations were determined using a TD-700 fluorometer. The RSD was less than 2%.
Ice-Rafted Debris Analyses
In the Okhotsk Sea, coarse sediment fractions with grain sizes larger than 63 μm in the Okhotsk Sea have been defined as ice-rafted debris (IRD) according to previous studies based on samples from sediment traps, surface sediments, and sediment cores from the region (Sakamoto et al., 2005). Laser diffraction and sieving of the IRD were performed, both of which were used to describe the grain size fractions in the core (Sakamoto et al., 2005, Sakamoto et al., 2006). Both of these methods were used in order to make the results more credible.
Laser Diffraction Grain-Size Analysis
Grain-size analyses were performed on 442 samples at ∼1–2 cm intervals to characterize the sediment texture using a Malvern Master size laser particle sizer (Malvern 3000) with a range of ∼0.02–2,000 μm. Carbonates, organic material, and diatoms were removed before analysis following the procedure introduced by Vasilenko et al. (2017). Briefly, ∼0.1 g of sediment was pre-treated with excess 15% H2O2 to remove organic matter, and with excess 10% HCl to remove CaCO3. The liquid was centrifuged three times at pH = 7, then 20 ml of 2 mol/L Na2CO3 was added and water-bathed at 85°C for 8 h to remove diatoms. Representative samples were observed under a microscope to ensure that the diatoms were completely removed. The accuracy of the measurements was 99% and the repeatability error was less than 0.1%.
Sieve Analysis
Approximately 3–10 g of dry samples were weighed before sieving and washed with water passing through a 63 μm mesh sieve. The residual samples on the sieve were dried at 60°C and passed through a 2,000 μm mesh sieve, and every fraction was weighed (Sakamoto et al., 2006; Nürnberg et al., 2011). The >2,000 μm grains (dropstones) were collected during core description, sampling and sieving, and were counted.
Time-Series Analysis
The IRD (vol%) time series analysis was performed using the wavelet transform in Acycle (Li et al., 2019) and a 95% confidence level was chosen. Cross-wavelet analysis visualizes the continuous variations in power and coherence in the time-frequency domain (Asahi et al., 2016). Prior to spectral analysis, all of the analyzed data were resampled at 0.2 kyr for wavelet transform and cross-wavelet analysis, which was the mean resolution of the sequence based on linear interpolation.
Results
Chronology
The age model for core LV55-40-1 was constructed based on AMS 14C dating of planktonic foraminifera and on correlation of the productivity proxies, such as Ba/Ti, chlorin and opal contents with marine and Greenland ice sheet oxygen isotopic records (Figure 3; Andersen et al., 2004; Lisiecki and Raymo, 2005). The Ba/Ti ratio was assumed to indicate the relative contribution of biological and terrestrial inputs into the Okhotsk Sea, which co-vary with glacial–interglacial cycles with higher Ba/Ti values during the interglacial periods (Figure 3C,F; Lo et al., 2018). Similarly, opal contents exhibited cyclic variations, with high abundances during interglacial periods and low abundances during glacial periods (Figure 3D). The correlation between opal contents and marine oxygen isotopes has been widely used to construct age models for deposits in the Okhotsk Sea (Narita et al., 2002; Sakamoto et al., 2006). In addition, magnetic susceptibility correlated with LR04 (Lisiecki and Raymo, 2005) and exhibited good correlations with log (Ba/Ti) and opal contents (Figure 3C-E).
FIGURE 3. Age model for core LV55-40-1. (A) Linear sedimentation rate, (B) Age-depth plot, (C) XRF-scanning log (Ba/Ti) ratio (blue line) with a 3-point running average (red line), (D) Opal content, (E) Magnetic susceptibility, (F) Chlorin concentration, (G) Oxygen isotopes from the NGRIP ice core (Andersen et al., 2004), and (H) LR04 δ18O stack (Lisiecki and Raymo, 2005). Purple triangles represent age model tie point using AMS 14C, orange and green dashed lines represent age control points obtained using correlations between the log (Ba/Ti) ratio, opal content, magnetic susceptibility, and LR04 δ18O, and using correlations between chlorin concentrations and oxygen isotopes from the NGRIP ice core. Pink shadows represent glacial periods.
The chlorin content in the Okhotsk Sea increased during Dansgaarde-Oeschger interstadials (DOIs), and have also been used to construct high-resolution age models in the Okhotsk Sea (Gorbarenko et al., 2007; Gorbarenko et al., 2009; Gorbarenko et al., 2010; Gorbarenko et al., 2012; Vasilenko et al., 2017; Gorbarenko et al., 2020). Thus, the resolution of the age model was improved further by correlating the chlorin content to DOIs in Greenland ice cores. In core LV55-40-1, the peaks in chlorin content correlated well with long-lasting DOIs 8, 12, 14, 19, and 21 within established MISs (Figure 2F,G). The 8.8 m core thus revealed orbital and millennial variations with a basal age of 110 kyr (early MIS 5d; Figure 3).
Variations in Ice-Rafted Debris in Core LV55-40-1
The IRD (vol%) content determined by laser diffraction was calculated as the volume percentage of the total terrigenous materials and excludes the influence of biological material. The IRD (wt%) content determined by sieving includes both terrigenous grains and biogenic fractions. However, in the Okhotsk Sea, the biogenic fraction is insignificant (Sakamoto et al., 2006) and can be ignored in the sand fraction. Moreover, the variations in the IRD fraction between these two analytical methods were consistent in core LV55-40-1 (Figures 4C,D), which confirms the above inference, and indicates that both are suitable as proxies.
FIGURE 4. Comparisons between variations in IRD proxies in core LV55-40-1 and other proxies. (A) SON-insolation (48°N; September, October, and November mean insolation), (B) IP25 content in core MD01-2414 from the central Okhotsk Sea, a proxy of sea ice (Lo et al., 2018), (C) IRD (wt%) in core LV55-40-1, (D) IRD (vol%) in core LV55-40-1, (E) Number of dropstones in core LV55-40-1, (F) Opal content in core LV55-40-1, and (G) LR04 δ18O stack (Lisiecki and Raymo, 2005). Blue shadows represent intervals of sea ice expansion.
Variations in IRD (vol%) ranged from 0.36 to 46.7% (Figures 4D, 5D). In general, IRD (vol%) exhibited strong cyclic variations from ∼110 to ∼10 ka (Figure 4D), mostly ranging from ∼5 to ∼15%. High-frequency fluctuations were observed at 105, 94, 87, 80, 78, 74, 70, 62, 58, 48, 40, 37, 34, 31, 29, 27, 22, 17, and 12 ka (Figure 5D,E). Two significant peaks in IRD (vol%), with values of 46.7 and 39.3%, corresponded to ∼31 and ∼27 ka, respectively. The IRD (vol%) was low during the Holocene, with a mean of 4.7%. The variations in IRD (wt%) ranged from ∼2 to ∼52% throughout the core, and exhibited a similar pattern to those of the IRD (vol%) (Figures 4D, 5D).
FIGURE 5. Comparison between millennial-scale changes in IRD proxies in core LV55-40-1 and other proxies. (A) Oxygen isotopes from stalagmites (Cheng et al., 2016), a proxy for the East Asian summer monsoon (EASM), (B) Oxygen isotopes of the NGRIP ice core (Andersen et al., 2004), a proxy for air temperature, (C) Alkenone-derived temperature (°C) (Harada et al., 2008), indicating AO variations, (D) IRD (vol%) and (E) IRD (wt%) in core LV55-40-1. Grey shadows represent DOSs intervals, orange shadows represent intervals potentially affected by volcanic eruptions.
A total of 99 dropstones were collected from the core sequence (Figure 2B), with diameters ranging from 2 to 60 mm. The presence of dropstones verifies the presence of sea ice, as ice rafting is the main transport method for grains larger than 2 mm to hemipelagic regions, especially in areas influenced by seasonal sea ice (Sakamoto et al., 2006). Dropstones mostly occurred in intervals with high IRD contents, and the maximum number of dropstones (17) was observed at ∼27 ka, which may have also been influenced by volcanic eruption as suggested by the extremely high magnetic susceptibility (Figure 2A).
Discussion
Sea Ice Variations in the Okhotsk Sea on Orbital Timescale
Ice rafting is the dominant method of transport for coarse-grained terrigenous material and dropstones to hemipelagic regions in the Okhotsk Sea (Sakamoto et al., 2006; Nürnberg et al., 2011). However, turbidity currents, gravity flows, and volcanic eruptions can also transport coarse materials into the sea (Nürnberg et al., 2011; Wang et al., 2017). Evidence of turbidity currents or gravity flows was not observed in core LV55-40-1, and has not been recorded in cores from nearby regions (Karp, 1996; Biebow, 1999). The extremely high magnetic susceptibility (Figure 2A) and volcanic glass observed at ∼31 and ∼27 ka implies that abundant volcanic materials were brought by either directly volcanic eruption or by sea ice, which was difficult to distinguish and may have affected the IRD content only during early MIS 2 (Figures 4D,G, 5D); however, this disturbance may be negligible because the abundant coarse volcanic material occurred as very thin layers in the core. The obvious effects of volcanic material on the IRD in the rest of the core could also be precluded due to the relatively low magnetic susceptibility values (Figure 2A).
The presence of IRD is generally the result of the expansion of sea ice under cold climatic conditions (Nürnberg and Tiedemann, 2004; Seki et al., 2004; Sakamoto et al., 2005, Sakamoto et al., 2006; Nürnberg et al., 2011). During cold stages, lower sea levels resulted in greater exposure of the surrounding continental shelf; thus, more terrigenous grains were captured and transported by sea ice to the ocean (Sakamoto et al., 2005). It has been suggested that perennial sea ice or ice-free conditions occur when IRD contents are 0% or approximately 0% (Seki et al., 2004; Sakamoto et al., 2005; Sakamoto et al., 2006). Seasonal sea ice is the only method that can transport dropstones to the ocean by ice rafting (Sakamoto et al., 2006), which is supported by the presence of dropstones during both warm and cold stages (Figures 2B, 4E-G). Even in the modern southwestern Okhotsk Sea, there is a small area of seasonal sea ice cover at the study site (Figures 4C,D). IRD was abundant throughout the sequence in core LV55-40-1, suggesting that seasonal sea ice was predominant in the southwestern Okhotsk Sea over the past ∼110 kyr. This is supported by analyses of IRD in cores MD01-2412 (Sakamoto et al., 2006) and XP98-PC4 (Sakamoto et al., 2005) from the southwestern Okhotsk Sea, which demonstrated that seasonal sea ice cover was present during the past ∼100 kyr. However, conditions were different in other regions. The diatom records from the central Okhotsk Sea suggested perennial sea ice conditions during MIS 2 and MIS 4 (Wang and Wang, 2008), whereas IRD records from the eastern Okhotsk Sea indicate a seasonal to perennial sea ice cover (Nürnberg et al., 2011). Other IRD records indicate that during MIS 2 perennial sea ice covered the Okhotsk Sea only near the northwestern and western coasts (Vasilenko et al., 2019). However, perennial sea ice conditions were not present at our study site, even during the Last Glacial Maximum (LGM). Instead, a seasonal sea ice cover was present (Figures 4C,D). This implies that sea ice variations in the Okhotsk Sea are spatially heterogeneous on geologic timescales (Gorbarenko et al., 2014; Bosin et al., 2015; Vasilenko et al., 2019).
Generally, sea ice variations in the Okhotsk Sea exhibit cyclic glacial–interglacial patterns on an orbital scale, with expanding sea ice extents during glacials and retreating sea ice extents during interglacials (Nürnberg and Tiedemann, 2004; Sakamoto et al., 2005; Nürnberg et al., 2011; Zou et al., 2015; Wang et al., 2017; Jimenez-Espejo et al., 2018). Variations in core LV55-40-1 do not strictly follow the glacial-interglacial cycles, and four obvious sea ice expansions were observed during MIS 5b, MIS 4, mid-MIS 3, and early MIS 1, as indicated by high IRD contents (Figure 4D). The reconstructed sea ice variations from this core are mostly consistent with the IP25 record from core MD01-2414 in the central Okhotsk Sea (Lo et al., 2018; Figures 4B,D).
Sea ice formation in the modern Okhotsk Sea mainly occurs during the winter (Parkinson et al., 1987; Rycroft, 1995). Previous studies have demonstrated that air temperature and sea-surface conditions during autumn play an important role in sea ice formation during the subsequent winter (Ogi et al., 2001; Ogi and Tachibana, 2006). Therefore, local autumn insolation may be related to sea ice formation during the winter. This inference is confirmed by a good correlation between the variations in sea ice derived from IRD and autumn insolation in the study area (48°N; September, October, and November mean insolation, SON-insolation). Four sea ice expansions corresponded to either declining or minimum SON-insolation (Figures 4A,D). This suggests that seasonal sea ice variations on an orbital scale in the Okhotsk Sea were controlled by local autumn insolation, which exhibits a strong precession cycle. This inference is further supported by the wavelet transform analysis of IRD (Figure 6A) and a cross-wavelet analysis between IRD and SON-insolation (Figure 6B), which exhibited a strong 20-kyr cycle throughout the sequence (Figure 4D).
FIGURE 6. (A) Continuous wavelet transform analysis of IRD (vol%) in core LV55-40-1 and (B) Cross-wavelet analysis of IRD (vol%) in core LV55-40-1 and SON-insolation. Blue dashed lines represent main orbital cycle of 20-kyr.
Sea Ice Variations in the Okhotsk Sea on Millennial Timescale
High-resolution variations in IRD revealed millennial-scale sea ice fluctuations over the past ∼110 ka, which are superimposed on the variability at the orbital scale. In total, 19 IRD peaks were observed throughout the sequence, which correspond with cold Dansgaarde-Oeschger stadials (DOS) recorded by the Greenland ice sheet (Andersen et al., 2004; Figures 5B,D). Previous studies have reported that millennial-scale sea ice variations can be correlated with millennial climatic changes, such as DO cycles (Gorbarenko et al., 2003; Sakamoto et al., 2005; Sakamoto et al., 2006; Nürnberg et al., 2011; Vasilenko et al., 2017). A recent study suggested that the velocity of geostrophic winds over the Okhotsk Sea dominated sea ice drift, thereby causing the expansion of sea ice on millennial scales (Vasilenko et al., 2017). Mayewski et al. (1994) attributed rapid climatic changes to significant reorganization of atmospheric circulation, which stimulated changes in sea ice cover in the ocean. A study of the history of sea ice variations derived from IRD analyses also highlighted the importance of millennial-scale variations in polar atmospheric circulation for driving sea ice changes in the Okhotsk Sea (Sakamoto et al., 2005). Therefore, atmospheric circulation in the polar region and its correlation with pressure in the mid-latitudes might be related to sea ice changes in the Okhotsk Sea on a millennial scale (Sakamoto et al., 2005; Sakamoto et al., 2006; Harada et al., 2008).
The AO is a dynamic atmospheric process, and the associated pressure changes over the Arctic are opposite to those over the mid-latitude region in the Northern Hemisphere (Thompson, 1998). The AO exerts a strong influence on atmospheric circulation over the Eurasian continent and adjacent areas. Modern data suggests that sea ice cover in winter is strongly affected by the annual integrated AO in the Okhotsk Sea (Ogi and Tachibana, 2006). An IRD record from the central Okhotsk Sea also indicated that sea ice expansions in DOSs during the past ∼100 kyr were the result of variations in polar atmospheric circulation in the Northern Hemisphere (Sakamoto et al., 2005). Therefore, the Arctic atmospheric processes must contribute to sea ice variations in the study area on a millennial scale. It has been suggested that the alkenone-derived ocean surface temperatures corresponded with AO on geologic timescales (Harada et al., 2008) and were coupled with temperature changes in the Arctic, with low temperatures indicating a negative AO, and vice versa. Therefore, negative AO during stadials plays a dominant role in sea ice expansion in the Okhotsk Sea, as negative AO patterns are closely correlated with cold DOSs (Harada et al., 2008; Figures 5C,D). During these sea ice expansion intervals, cold air masses could have easily penetrated through the Arctic region during periods with negative AO pattern, lowering the air temperatures over the Okhotsk Sea and causing more active sea ice formation (Thompson and Wallace, 1998; Harada et al., 2008).
In addition to the effects of AO, thermal anomalies at the ocean surface may have also influenced the sea ice formation in the Okhotsk Sea (Ogi et al., 2001; Sakamoto et al., 2005; Sakamoto et al., 2006; Harada et al., 2008). Such thermal anomalies are closely related to the discharge of warm freshwater (Ogi et al., 2001; Harada et al., 2008). In the modern Okhotsk Sea, the Amur River discharge brings warm water advection to the surface seawater, thereby reducing the sea ice formation during the subsequent winter (Ogi et al., 2001). On geologic timescales, the Amur River discharge is a potential factor that controlled sea ice variations during warm periods (Sakamoto et al., 2006). Core LV55-40-1 is located in an area east of the Sakhalin Islands, which is influenced by freshwater discharge from the Amur River that is transported by the ESC (Itoh and Ohshima, 2000; Sakamoto et al., 2005; Figure 1). Therefore, the discharge from the Amur River may have also contributed to sea ice variations during interglacial periods in the study area by modulating the sea-surface thermal conditions. As fluctuations in the Amur River discharge were controlled by the intensity of the EASM (Harada et al., 2008), the reconstructed variations in sea ice also corresponded well with the EASM variability on the millennial scale, with decreased sea ice formation during warm stages (Cheng et al., 2016; Figures 5A,D). During periods of enhanced EASM, increased monsoon precipitation would increase the discharge from the Amur River. The advection of this warm freshwater to the southwestern Okhotsk Sea caused thermal anomalies at the ocean surface (Ogi et al., 2001), thereby suppressing subsequent sea ice formation. In contrast, less warm freshwater input during cold stadials in the interglacials due to weak monsoonal conditions would allow more sea ice formation in the study area.
Conclusion
We reconstructed the history of sea ice variations in the southwestern Okhotsk Sea over the last ∼110 kyr and investigated the factors controlling sea ice changes on orbital and -millennial timescales based on the IRD proxy. Seasonal sea ice was predominant in the southwestern Okhotsk Sea during the past ∼110 kyr. Sea ice expansion occurred during MIS 5b, MIS 4, mid-MIS 3, and early MIS 1, which corresponded to period of less SON-insolation. Combined with the strong 20-kyr cycles in the IRD proxy, we suggest that orbital-scale sea ice variations in the southwestern Okhotsk Sea were controlled primarily by local autumn insolation. The millennial-scale sea ice variations are related to DO cycles, with sea ice expansion corresponding to cold DOSs. We suggest that sea ice variations were impacted by both the AO and the EASM. During intervals of sea ice expansion, cold air masses could have easily penetrated through the Arctic region during periods of negative AO pattern, thereby lowering the air temperature in the Okhotsk Sea latitudes and causing more active sea ice formation. In addition, the high discharges of warm freshwater transported by the Amur River to the southwestern Okhotsk Sea during warm interstadials caused thermal anomalies at the ocean surface, thereby suppressing the subsequent sea ice formation. In contrast, lower warm freshwater input during cold stadials would allow more sea ice formation in the study area.
Data Availability Statement
The original contributions presented in the study are included in the article/supplementary material, further inquiries can be directed to the corresponding authors.
Author Contributions
AW, ZY, and XS designed the study, synthesized and analyzed the data, and wrote the manuscript with contributions from all authors. KW and YW analyzed the data related to sedimentology. YL, JZ, and SG helped collect the core. All authors contributed to the manuscript and approved its submission.
Funding
This work was jointly supported by the National Key Research and Development Program of China (No: 2016YFA0601903), NSFC-Shandong Joint Fund for Marine Science Research Centers (U1606401), the National Program on Global Change and Air-Sea Interaction (Grant No. GASI-GEOGE-03), the Taishan Scholar Program of Shandong (XS), the Russian Science Foundation, Russia (Grant N_19-05-00663A), and the Russian state budget 121021700342-9 of the Pacific Oceanological Institute, Far East Branch of the Russian Academy of Sciences.
Conflict of Interest
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
Acknowledgments
We thank the Editor and two reviewers for their valuable suggestions.
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Keywords: sea ice, ice-rafted debris, orbital scale, millennial scale, the Okhotsk Sea, the Amur River
Citation: Wang A, Yao Z, Shi X, Wang K, Zou J, Liu Y, Wu Y and Gorbarenko SA (2021) Orbital and Millennial Variations in Sea Ice in the Southwestern Okhotsk Sea Since the Last Interglacial Period and Their Implications. Front. Earth Sci. 9:710797. doi: 10.3389/feart.2021.710797
Received: 17 May 2021; Accepted: 24 June 2021;
Published: 07 July 2021.
Edited by:
Min-Te Chen, National Taiwan Ocean University, TaiwanReviewed by:
Fengming Chang, Institute of Oceanology (CAS), ChinaJianguo Liu, South China Sea Institute of Oceanology (CAS), China
Copyright © 2021 Wang, Yao, Shi, Wang, Zou, Liu, Wu and Gorbarenko. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Zhengquan Yao, yaozq@fio.org.cn; Xuefa Shi, xfshi@fio.org.cn