Table 1 presents the results of AMS ¹⁴C dating for the five layers. Results from acid-insoluble organic matter dating in sediments using the AMS¹⁴C method are usually affected by old carbon and therefore need to be calibrated. After calibration with the Calib 8.2.0 program (Stiver and Reimer, 1993) using the Marine20 dataset (Heaton et al., 2020) and adopting an ΔR value of 1120 for carbon-reservoir correction, the top age of the core was determined to be 2118 cal a BP, and the bottom age as 28,116 cal a BP (Yoshida and Moriwaki, 1979; Takano et al., 2012). In line with previous studies (Pudsey et al., 2006; Andrews et al., 2017; Hu et al., 2022), we generally performed age correction by subtracting the age at the top of the core. Owing to the proximity of the core ANT37-C5/6-07 sediments to the study location of Hu et al. (2022), we also treated the surface deposits as modern, resulting in an age of 0 cal a BP at the core’s top and an old carbon age of 2118 a. Corrections involved subtracting the old carbon age and making appropriate adjustments to derive the final calendar age. The sediment-age framework for core ANT37-C5/6-07 referenced the work of Hu et al. (2023) ( Figure 2 ).

Figure 3 illustrates the contents and variations of clay minerals from core ANT37-C5/6-07. Among the clay minerals, illite exhibits the highest content, ranging from 29% to 61%, with an average of 45.98%. Illite content exhibits significant fluctuations between 40 and 60 cm, with minor changes from 0 to 40 cm. The overall variation in smectite content is relatively insignificant, ranging from 12% to 35%, averaging at 21%. Observable peaks and valleys are present in the curves to depict its content change, predominantly occurring at depths between 40 and 60 cm. Kaolinite content ranges from 15% to 30%, averaging at 22%. Below 60 cm, its content is relatively lower; however, above 60 cm, it increases and exhibits fluctuations. Chlorite content ranges from 7% to 16%, averaging at 11%. It is lower and more stable compared with the others. Overall, the fluctuation is minimal below 60 cm, with slight fluctuations observed above 60 cm. The highest content is situated at approximately 40 cm. Illite crystallinity varies from 0.31°Δ2θ to 0.53°Δ2θ. Small variations are observed below 60 cm and above 40 cm, all below 0.4°Δ2θ, indicating better crystallization. Larger variations are noted from 40 to 60 cm, exceeding 0.4°Δ2θ and indicating worse overall crystallization. The chemical index of illite ranges from 0.02 to 0.21, with a mean value of 0.06. Overall, all values are less than 0.1, with a peak around 45 cm, indicating enhanced chemical weathering. However, the overall trend suggests weathering predominantly dominated by physical weathering and controlled by cold and dry climatic conditions in the Antarctica.

Figure 4 illustrates the vertical variation of grain size characteristic parameters in core ANT37-C5/6-07. By using the Udden-Wentworth grain-size classification method (Gladstone et al., 2001), we selected three grain-size parameters: the percentage content of grain-size fractions less than 4 μm, 4–63 μm, and greater than 63 μm. These parameters represent the percentage content of the clay, silt, and sand fractions in the samples. Silt dominated the sediments in this core, with the average percentage of clay-component contents at 21.0% (7.1–32.2%), the average percentage of silt component contents at 58.0% (34.3–67.2%), and the average percentage of sand-component contents at 21.0% (2.4–51.9%). The variations in silt- and clay-component contents were similar but were opposite to those of sand-component contents. The mean grain size (Mz) ranged from 7.2 μm to 90.5 μm, experiencing more frequent fluctuations between 45 cm and 91 cm and then stabilizing and increasing above 45 cm. In addition, the grain size characteristics of sediments can reflect hydrodynamic conditions and ice-rafted debris content variations (Bischof et al., 1996; Chen et al., 2014). However, using grain size data to infer depositional environments introduces some uncertainty. To mitigate this, a statistical approach—grain size-standard deviation—is often applied to enhance the interpretation of grain size data (Chen et al., 2013). This method’s analysis ( Figure 5 ) reveals three significant deviation peaks at 14.6 µm, 58.3 µm, and 1230 µm, along with three minor peaks at 0.22 µm, 25.4 µm, and 406.1 µm in the sediment of core ANT37-C5/6-07. Thus, the sediment can be classified into three environmentally sensitive grain size groups: 0.22–25.4 µm (component A), 25.4–406.1 µm (component B), and 406.1–1866.1 µm (component C). Among these, component C is minor and exhibits a standard deviation near zero, rendering its discussion irrelevant.

Table 2 presents the results of elemental analyses for the sediments in core ANT37-C5/6-07. The contents of Al₂O₃ and Fe₂O₃ are the highest. Aluminum is commonly considered an element enriched by terrestrial-source debris. Its coefficient of variation is very small (0.06), making it suitable as a standardized element to mitigate the influence of terrestrial-source debris on elemental content. The results reveal a high coefficient of variation for the redox-sensitive element Mo and an elevated content of Ba among the trace elements in core ANT37-C5/6-07. The average concentrations are 231.73 ppm for total rare-earth elements (REE), 213.09 ppm for light rare-earth elements (LREE), and 18.64 ppm for heavy rare-earth elements (HREE). The trends reflect a remarkable accumulation of LREE. The alterations in the characteristics of certain elements in the sediment samples from core ANT37-C5/6-07 are illustrated in Figure 6 . The variations in the characteristics of elements in the sediments manifested in two distinct phases: the last glacial period and the Holocene, exhibiting significant cyclic fluctuations. Notably, except for the elements Ba and Mn, a sudden change occurred in the other elements at around 46 cm. The characteristics of terrestrial enrichment elements depicted in Figure 6 , including Ti, Al, Fe, K, P, and Mg, exhibit a similarity to the trend of changes in other elemental characteristics and show a positive correlation. Conversely, Si and Ba display a negative correlation.

Sediments in high-latitude marine environments are frequently transported by glaciers and ocean currents, encapsulating valuable insights into alterations in source areas and depositional processes. As highlighted earlier, the clay-mineral composition and characteristics of impeccably preserved sediments bear information regarding depositional sources and climatic changes. However, discussions regarding the sediment source based solely on clay-mineral characteristics may be prone to bias owing to the influence of multiple mechanisms (Singer, 1984; Yemane et al., 1996). And REEs have been widely used as useful and reliable provenance proxy for terrigenous sediments from different regions (Taylor and McLennan, 1985; Xu et al., 2021). Therefore, based on the analysis of the characteristics of the clay-mineral assemblage, combined with the REE characteristics of the sediments, and compared with the characteristics in the sediments of the neighboring seas, we could identify the origin of sediments in core ANT37-C5/6-07.

The analysis of previous experimental results ( Figure 3 ) showed that illite dominated as the clay mineral in core ANT37-C5/6-07. This dominance can be attributed to the terrestrial physical weathering and glacial abrasion processes characteristic of high-latitude regions. Illite primarily originates from the physical weathering of metamorphic and sedimentary rocks in the surrounding land. Experimental results show that the average illite crystallinity is less than 0.4°Δ2θ, indicating superior crystallization. Additionally, the illite chemical-weathering index (<0.2) suggests that the illite is mainly from physical weathering. Notably, Trail and McLeod (1969) observed that the region is predominantly composed of migmatite and gneiss. They further noted that substantial quantities of readily weatherable hydrocarbon source rocks can contribute to the presence of illite and chlorite. Smectite is typically considered a product of seafloor weathering of volcanic material, as observed in sediments from the Ross Sea. This volcanic material originates from the nearby McMurdo volcano (Jung et al., 2021). Smectite has also been identified in some Antarctic soils (Claridge, 1965), suggesting its potential presence in sediments due to the transport of ancient, loosely weathered products and soils into the ocean by glaciers or turbidity currents. Kaolinite typically forms through the chemical weathering of rocks in warm, humid temperate-to-tropical climates. However, in the cold, arid climate of the Antarctic continent, characterized by weak chemical weathering, glaciers likely transported kaolinite from the soils and loose sediments of coastal plains from the Mesozoic to the Tertiary (Hambrey et al., 1991). Ehrmann et al. (1992) identified the presence of high levels of kaolinite in sediments from the Oligocene period, coinciding with the formation of ice sheets in the East Antarctica. After the ice sheet formed, unconsolidated debris was transported away from the continents, leaving glaciers to primarily erode unweathered rock, which resulted in only a small quantity of kaolinite being produced. Additional kaolinite likely resulted from the weathering of preexisting kaolinite-bearing sediments and the erosion of ancient soils (Trail and McLeod, 1969). Moreover, the Lambert Glacier and Emery Ice Shelf in the Prydz Bay were found to be filled with older kaolinite. When the glacier melted, the older kaolinite beneath was exposed, and subsequent weathering and erosion contributed to the kaolinite content.

Sediment provenance is further examined by considering the potential source areas of the four clay minerals and analyzing the clay-mineral assemblages. Given that both illite and chlorite result from physical weathering (Ehrmann et al., 1992), we combined their contents as a composite end member to explore their potential source regions. This analysis involved comparing them with clay mineral characteristics of other marine sediments that may share the same sediment source station (Ehrmann, 1991; Melles, 1991; Dai et al., 2016) and integrating this information with the current characteristics of the study area. The source analysis triangulation for clay minerals is shown in Figure 7 . The comparison of results reveals that the clay mineral assemblages in core ANT37-C5/6-07 exhibit a distinct signature, which only partially matches that of the clay mineral assemblages from core P4-03 in Prydz Bay. This suggests that the primary source of clay minerals in core ANT37-C5/6-07 is likely nearby Enderby Land, with a portion also possibly originating from the coastal land along Prydz Bay. Referring to the core locations and current characteristics illustrated in Figure 1 , both cores fell within the influence of the eastward ASC. The ASC, driven by the horizontal gradient pressure of the Antarctic Slope Peak, exhibits a high flow velocity, reaching a maximum of 25 cm/s and being particularly active at a water depth of 750–1250 m. Below this depth, the flow velocity gradually decreases, facilitating the deposition of detrital material (Hunt et al., 2007; Williams et al., 2010). As both cores are situated at water depths below 2500 m, their clay-mineral assemblages are significantly influenced by the ASC. Consequently, we propose that the sediments in core ANT37-C5/6-07 are partly derived from rocks weathered on the continental shelf of Prydz Bay, transported by the ASC. Additionally, some sediments are believed to originate from coastal Enderby Land. To elucidate the sediment origin further, we selected REE as proxy indicators for compositional analysis. REE is typically associated with source rocks owing to their low reactivity. However, the fractionation of REE during deposition is influenced by multiple factors. Notably, a grain size effect has been observed in REE, often leading to enrichment in fine-grained material (Cullers et al., 1987). Additionally, study results confirm the reactivity of REE during chemical weathering, where the intensity of chemical weathering can affect their composition. Moreover, REE is influenced by mineral adsorption, and research has indicated that the composition of REE is also affected by ferromanganese oxides. Correlation analysis of the REE content of the sediments with Mz, the illite chemical index indicating chemical weathering intensity, and the (Fe₂O₃+MnO)/Al₂O₃ value representing ferromanganese oxide content (Dou et al., 2012) reveals that the REE content in core ANT37-C5/6-07 exhibits a weak correlation with these three factors ( Figure 8 ). This suggests that the variation in REE features is primarily influenced by the source. Therefore, the sediment source can be inferred based on the and considering light and heavy rare-earth fractionation features, such as (La/Sm)_N and (Gd/Yb)_N.

REE compositions in chondrite meteorites are believed to be undifferentiated. Analyzing the chondrite-normalized REE partitioning patterns can thus provide a clearer understanding of the differentiation characteristics of the sample’s REE (Boynton, 1984). We compared the REE compositions in the core ANT37-C5/6-07 sediments with those in the potential source area to try to analyze the source of the sediments (Shi et al., 1998; Chen et al., 2015; Li et al., 2017; Xiu et al., 2017). The REE compositions in the core ANT37-C5/6-07 sediments, as shown in the chondrite-normalized partitioning patterns ( Figure 9 ), display a marked enrichment in Light REE (LREE) and a depletion in Heavy REE (HREE). This pattern aligns with terrestrial source characteristics, suggesting a significant terrestrial influence, particularly from nearby Enderby Land. In contrast, the REE abundance in the sediments from the Antarctic Peninsula and Ross Island differs markedly, indicating a distinct geological origin (Shi et al., 1997; Chen et al., 2015). Moreover, the sediments in core ANT37-C5/6-07 show a higher REE content compared to those from the Ross Sea (Xiu et al., 2017). The similarity in LREE levels and the deficit in ΣHREE compared to the Enderby Land metamorphic rocks, along with distinct positive Ce anomalies and negative Eu anomalies, reflect the underlying bedrock composition, primarily ancient metamorphic rocks such as gneisses and mafic rocks (Sheraton et al., 1984; Tingey, 1991; Stagg et al., 2004). These features, supported by the bedrock characteristics in Prydz Bay and Enderby Land, suggest a mixed sediment source for core ANT37-C5/6-07.

The normalized ratios (La/Sm)_N and (Gd/Yb)_N indicate the fractionation levels of light and heavy rare-earth elements, respectively. A higher (La/Sm)_N ratio signifies greater enrichment in LREEs, while a lower (Gd/Yb)_N ratio points to greater HREE enrichment. By comparing the REE ratios in the sediments to those in potential source rocks, we can assess the fractionation between HREEs and LREEs. In core ANT37-C5/6-07 sediments (refer to Figure 10 ), the (La/Sm)_N and (Gd/Yb)_N ranges overlap with those from the Enderby Land Metamorphic Rocks and Prydz Bay sediments. This overlap suggests that these locations are the primary sources, as supported by the REE partitioning patterns observed.

In conclusion, the integrated analysis results of clay-mineral assemblages and REE composition strongly suggest that the predominant source of sediments in the study area is coastal land of Prydz Bay and Enderby Land. We consider that the sediments primarily originate from coastal-land weathering, transported into the ocean through processes like glacial or turbidite deposition, and subsequently carried by the ASC before settling at this specific station.

Clay-mineral assemblages in marine sediments from distinct regions convey varied climatic information. Considering the stability of ASC influencing the deposition of core ANT37-C5/6-07 (Williams et al., 2010), we propose that alterations in the clay-mineral characteristics of the sediments may indirectly indicate paleoclimatic changes. Drawing from prior studies, we propose that the smectite in the study area may have an authigenic origin, potentially affecting the accuracy of the paleoclimate information it contains (Iacoviello et al., 2010). In contrast, kaolinite originates from old kaolinite buried under glaciers or formed through chemical weathering under warm and humid climatic conditions, signifying a warm climate. Illite and chlorite result from physical weathering, typically indicating dry and cold climates. Thus, the (illite + chlorite)/kaolinite value can serve as a proxy indicator of paleoclimatology, reflecting the shift between warm and cold climates in the source area (Yang et al., 2022). Combined with other paleoclimatic proxies, we can further elucidate the reasons for the alteration of clay-mineral assemblages and changes in depositional processes to reconstruct the paleoclimatology of the source region.

The geochemical elemental characteristics of the sediments bear information about paleoenvironmental changes. The contents of various grain size fractions were analyzed through an R-type factor analysis with the sediment elements at this station ( Table 3 ). The chosen rotation method for factor analysis was the maximum-variance rotation method, leading to the identification of two primary factors, F1 and F2. Examination of Table 3 reveals that the variance factor of F1 was larger than that of F2, signifying that F1 predominantly influenced the composition of sediment elements. The TiO₂, Al₂O₃, Fe₂O₃, MgO, K₂O, P₂O₅, and clay fractions displayed high positive loadings, denoting their typical characteristics as terrigenous inputs. The iron could be correlated with chlorite, illite, and smectite, while potassium was primarily linked to potassium feldspar and illite. The F2 factor has positive high loadings only for MnO and chalk, which may indicate that Mn is more likely to be in the silty sand grain fraction relative to the other elements (Zhang, 2011). The SiO₂ and barium constitute components of marine-derived sediments, and SiO₂ levels could be associated with diatoms. Previous research has demonstrated that climatic variations can influence the timing and extent of sea-ice coverage in the Southern Ocean, subsequently influencing the photosynthesis of surface phytoplankton (Wong et al., 1999; Ducklowa et al., 2008). Therefore, biogenic barium (Ba_bio) and Si/Al were chosen as paleo-productivity indicators to indirectly infer information on climate warming and cooling. The Ba_bio was calculated using the following formula (Bonn et al., 1998):

where (Ba/Al)_ter represents the abundance of barium in the terrestrial crust and has a value of 0.0051 (Taylor, 1964).

Combined with the previous section, the grain size composition and characteristics of marine sediments can indirectly reflect the hydrodynamic strength at the time of deposition, currents and other changes in the depositional environment (Hall et al., 2011). Compared with component A, the content of component B is higher, and the change of the content B shows an obvious positive correlation with the average grain size change of the sediment in the core ANT37-C5/06-07, which indicates that the change of the content B influences the overall change of the grain size of the sediment, and it is more sensitive to the environmental changes. Therefore, this paper suggests that component B can be used as a proxy indicator for changes in the depositional environment, and that the grain size components A and B correspond to the environmentally sensitive clay and silt, which to some extent can be indicative of weak and strong hydrodynamic conditions.

The ebb and flow of glaciers are deeply intertwined with shifts in climate patterns. Studies, including Stammerjohn et al. (2015), have demonstrated that rising temperatures significantly influence ice melt. This melting corresponds with periods of glacial retreat, often associated with warmer climates, which in turn fosters the emergence of open oceanic environments and an increase in surface productivity. In contrast, cooler climates are marked by a reduction in this productivity due to expansive sea-ice coverage. The presence of coarser grain sizes in sediment, like those greater than 63 μm, 125 μm, and 150 μm, is frequently interpreted as an indicator of increased ice-rafted debris (Chen et al., 2006), reflecting such climatic shifts. Within the specific environmental context of the area under study, it is plausible that the kaolinite found originates from the physical weathering and erosion of ancient, glacier-buried deposits, as indicated by its concentration. Notably, this kaolinite content aligns with the >63 μm grain size fraction, providing a sedimentary record that can be used to trace historical glacial movements.

To unravel the history of climate in Antarctica, we turned to ice cores, which are rich archives of past climatic conditions. In this study, the analysis went further, incorporating additional proxies; we delved into the intricate details of sedimentary records from core ANT37-C5/6-07. We scrutinized the variations in the composition of clay minerals, their relative proportions, the Ba_bio, the silicate-to-aluminum ratio (Si/Al), the >63 μm grain size fractions, and the component B. These sedimentary parameters were cross-referenced with the oxygen isotope data (δ¹⁸O) from the EDML ice core, which was obtained near our study site (as illustrated in Figure 1 ; Epica Community Members, 2006). Our comprehensive approach allowed us to piece together a dynamic history of hydrodynamics, paleoproductivity, and ice cover in the region. Through this lens, we discerned four distinct periods alternating between warmer and cooler climates (labeled P1 through P4). Moreover, we pinpointed the timing of these local environmental shifts in relation to broader global climatic events, as depicted in Figure 11 .

During the period from 26,000 to 18,600 cal a BP, the (illite + chlorite)/kaolinite value was relatively high, and the kaolinite content was low. These features suggest a cold climate, weak chemical weathering intensity, and the reburial of older kaolinite due to the re-formation of the ice sheet. And content of component B is consistently low, indicating a less hydrodynamic depositional environment. This may be due to the fact that the exchange between the upper and lower water column was inhibited during that period due to sea ice cover. Concurrently, reduced values of Ba_bio and the Si/Al value point to diminished marine surface productivity, attributable to the sea ice extent. Marked variations in the >63μm grain size fraction, representing ice-rafted debris, were observed throughout this interval. Complementing these findings, the persistently low δ¹⁸O values in the EDML ice core corroborate a colder climate and intensified glacial conditions. The alignment of these conditions with the Last Glacial Maximum (LGM) confirms the chronology posited by Huybrechts (2002). Additionally, the shifts in these indicators denote that the study area commenced the Last Deglaciation around 18,600 cal a BP.

During the interval from 16,800 to 15,000 cal a BP (P1), a notable trend was observed: a decline in the (illite + chlorite)/kaolinite value to a nadir coincided with a significant rise in the δ¹⁸O values of the EDML ice cores. Concurrently, the content of component B showed an upward tendency. These trends collectively suggest a warming climate. In this phase, the >63 μm grain size fraction, initially increased and then declined, mirroring the glacier retreat that first released and later reduced the transport of such debris to the study area. This glacial retreat also facilitated enhanced phytoplankton photosynthesis and wind-stressed upwelling, intensifying surface-layer productivity and hydrodynamic conditions. Additionally, weathering and erosion exposed older kaolinite previously under the ice sheet, resulting in a significant increase in the kaolinite content. However, there was no significant change in Ba_bio, an indicator of productivity. This was attributed to a warming climate. The sudden increase in surface productivity led to the deposition of settled organic matter that consumes large amounts of oxygen, creating an anoxic environment and resulting in low levels of Ba_bio (Hu et al., 2023).

The subsequent period between 14,800 and 13,500 cal a BP (P2) was characterized by an opposite trend: the (illite + chlorite)/kaolinite value ascended, δ¹⁸O values dropped, and the >63 μm grain size fraction markedly escalated, while kaolinite content diminished. Si/Al, Ba_bio, and component B contents were comparatively low, suggesting a cooling climate, a surge in ice-rafted debris due to new ice sheet formation, and the reburial of kaolinite. And the new ice sheet resulted in restricted vertical mixing in the water column, weaker hydrodynamics, and reduced surface productivity.

From 12,800 to 11,400 cal a BP (P3), a warming climate was once again indicated by a decrease in the (illite + chlorite)/kaolinite value, a rise in kaolinite and component B content, a decline in the >63μm fraction, and the increase in δ¹⁸O. Conversely, the Si/Al value and Ba_bio content remained relatively stable, implying lower temperatures during this warm period compared to the previous warm period. Studies by Borchers et al. (2016) in the nearby Burton Basin in East Antarctica also indicated that the ice shelf front started to retreat from the site around 12,800 cal a BP, evidencing warming during this period.

The sedimentary record in core ANT37-C5/6-07 provides a detailed account of the Antarctic climate transition from colder to warmer conditions following the Last Glacial Maximum (LGM). This transition in Antarctica was distinct from that in the Northern Hemisphere, largely because the extensive landmass of the Northern Hemisphere experienced more rapid warming during the initial phase of the last deglaciation. This led to increased ice meltwater influx into the North Pacific, causing a weakening of the Atlantic Meridional Overturning Current and consequent heat accumulation in the Southern Ocean. This heat accumulation, in turn, warmed the Antarctic climate, establishing a temperature gradient between the North and South Poles, an effect known as the Bipolar Seesaw (Broecker, 1998; Wang et al., 2015). Compared to previous studies in the East Antarctic (Borchers et al., 2016; Yang et al., 2021), the geochemical proxies in the Cosmonaut Sea, particularly the shifts in (illite + chlorite)/kaolinite values, Ba_bio content, Si/Al, and the content of component B in core ANT37-C5/6-07, provide a clear timeline for the Antarctic ice sheet’s response to these climatic shifts. Notably, the warming in Antarctica from 16,800 cal a BP to 15,000 cal a BP (P1) occurred concurrently with the Heinrich Stadial 1 (HS1) in the Northern Hemisphere, whereas the cooler phase from 14,800 cal a BP to 13,500 cal a BP (P2) aligns with the Antarctic Cold Reversal (ACR). This latter period saw significant glacial expansion in the Ross Sea, further evidencing the frigid conditions in Antarctica (Huang et al., 2016). Following this, the period from 12,800 to 11,400 cal a BP (P3) signifies a warming phase post-ACR, which overlaps with the Younger Dryas (YD) cooling event in the Northern Hemisphere (Alley et al., 2003).

From 11,400 cal a BP to 5,000 cal a BP, the climate data from core ANT37-C5/6-07 show a phase of relative climatic stability and warming in Antarctica. The ratio of (illite + chlorite) to kaolinite was consistently low, reflecting stable conditions, while the δ¹⁸O values showed minimal fluctuations, indicating steady climatic conditions. The low content of >63μm particles, representing ice-rafted debris, along with stable kaolinite content, suggests a constant source and reduced glacial activity. This period saw significant increases in Si/Al values, Ba_bio, and component B content, pointing to diminished sea ice, enhanced water column exchange, and heightened surface plankton photosynthesis, culminating in increased productivity. These conditions mark the gradual climatic shift into the Holocene, characterized by overall warming (Bentley et al., 2009). Post-ACR, the climate witnessed a warming trend, with only minor fluctuations. However, between 5,000 cal a BP and 4,000 cal a BP (P4), a slight cooling is observed, as the (illite + chlorite)/kaolinite value increased, and kaolinite content decreased, which is in line with the δ¹⁸O records. Despite this cooling signal, the sedimentary record from the Antarctic Peninsula by Shevenell et al. (1996) confirms a warmer paleoclimate overall for this period. Notably, Si/Al and Ba_bio levels remained high, indicating sustained productivity, a phenomenon attributed to the reduced influence of sea ice and increased significance of solar irradiance in the post-Holocene warm climate (Hu et al., 2023). After this colder climatic phase, the (illite + chlorite)/kaolinite value remained low and stable, while the value of Si/Al, the content of Ba_bio and component B were high. This indicates that the Antarctica has generally been characterized by warmer conditions and the hydrodynamic is strong, surface productivity is high in the study area, collectively, these indicators suggest the initiation of a climatically suitable period in the Antarctica.

In summary, the variations in clay mineral assemblages, grain size distributions, and elemental compositions within core ANT37-C5/6-07 from the Cosmonaut Sea have proven to be effective indicators of the historical dynamics of the ice sheet since the Last Glacial Maximum (LGM). Comparative analysis with prior studies in West Antarctica (Long et al., 2024) and East Antarctica, including future projections (Borchers et al., 2016; Yang et al., 2021), reveals that the ice sheet in our study area exhibits heightened sensitivity to climatic shifts. This sensitivity allows for more precise dating of climatic events in East Antarctica. Our findings challenge the notion of stability in the East Antarctic ice sheet as proposed by Rignot et al. (2019), suggesting that there remains a considerable risk of ice-shelf collapse under ongoing global warming.