Low content of highly reactive iron in sediments from Prydz Bay and the adjacent Southern Ocean: Controlling factors and implications for sedimentary organic carbon preservation

1 Introduction

The role of iron (Fe) speciation, rather than its total amount, is critical in Fe biogeochemical processes such as activity, migration, and bioavailability in marine sediments (Tagliabue et al., 2017). Due to its diverse mineralogy, crystallography, morphology, and chemical composition, Fe exhibits significant oxidation-reduction and adsorption reactivities (Kostka and Iii, 1994; Thamdrup, 2000). The sequential separation of different Fe species from the reaction phase is the foundation of Fe biogeochemistry (Poulton and Raiswell, 2005). Marine sediments serve as both a crucial Fe sink and source (Wadley et al., 2014; Homoky et al., 2016). The characteristics of Fe speciation in sediments are influenced by multiple factors, including the mixing of source materials with varying intensities of chemical weathering, bedrock type, redox conditions, pH values, chemical properties of organic matter, and diagenesis (Canfield, 1989; Poulton and Raiswell, 2005; Konhauser et al., 2011; Wehrmann et al., 2014; Thomasarrigo et al., 2019; Wei et al., 2021; Pasquier et al., 2022). Furthermore, highly reactive Fe (Fe_HR, operationally defined as Fe (oxyhydr)oxides and carbonates that readily react with sulfide to form sulfide minerals and eventually pyrite [Canfield, 1989]) in sediments has a significant impact on the biogeochemical cycling and fate of carbon (C) and other trace elements (Tagliabue et al., 2017). Therefore, the analysis of Fe speciation in sediments and the identification of controlling factors are crucial in studying Fe and C biogeochemical cycles.

Early studies demonstrated that Antarctic glacial sediments, which contain poorly chemically weathered material, exhibit significantly lower Fe_HR content and Fe_HR/total Fe (Fe_T) ratios compared to terrestrial riverine particulates (Poulton and Raiswell, 2002; Raiswell et al., 2006). Recent studies on polar regions have revealed that glacial runoff meltwater contributes additional Fe_HR to coastal Antarctic waters (Bhatia et al., 2013; Hawkings et al., 2014; Wehrmann et al., 2014; Lyons et al., 2015; Dinniman et al., 2020), presenting a promising opportunity to enhance primary productivity in the Southern Ocean and accelerate carbon dioxide consumption from the atmosphere in this region (Blain et al., 2007). Correspondingly, the Fe_HR content and Fe_HR/Fe_T ratio in Antarctic marine sediments may rise (Henkel et al., 2018). Given the increasing melting rate of Antarctic glaciers in recent decades (Shepherd et al., 2018), these impacts may become more significant. However, limited data on Fe species in Antarctic sediments pose challenges in assessing the impact of glacial melting on the biogeochemical cycles of Fe and C in polar regions under the context of global warming.

The natural process of “Fe fertilization”, which involves the transport of more Fe_HR to the ocean due to increased glacial melting, not only enhances the transport of organic carbon (OC) to the deep sea (Pollard et al., 2009), but also has the potential to promote sedimentary OC burial. OC-Fe_HR complexes formed by the combination of Fe_HR and OC exhibit long-term preservation potential (Lalonde et al., 2012; Faust et al., 2021), and their formation is therefore significant for improving the burial efficiency of marine sedimentary OC and mitigating global warming (Salvadó et al., 2015). However, the proportion of OC in OC-Fe_HR complexes to total OC (TOC) (f_OC-Fe) in global marine surface sediments varies widely (0.5% – 80%) (Lalonde et al., 2012; Longman et al., 2021; Longman et al., 2022). Fe speciation and Fe_HR content in different sedimentary environments are significantly differ, which may be a crucial factor influencing the degree of OC-Fe_HR complexing (Ma et al., 2018; Faust et al., 2021). Therefore, investigating the species composition of Fe_HR in Antarctic marine sediments and its potential relationship with OC preservation is of great significance for comprehending the OC-Fe_HR coupling mechanism and evaluating the response of the Antarctic C cycle to climate change.

Prydz Bay is the largest bay in the Indian Ocean sector of Antarctica. Its seaward perimeter is delineated by two shallower water depth banks, namely Fram Bank to the northwest and Four Ladies Bank to the northeast. The continental shelf region in Prydz Bay is comparable to that of the Weddell Sea and the Ross Sea, which are the two major Antarctic coastal seas and have the most productive coastal polynyas (Arrigo et al., 2015). However, Prydz Bay has fewer ice-free zones (Campbell et al., 1993) and less ice shelf melting (Shepherd et al., 2018; The IMBIE team, 2018), leading to weak chemical weathering and low Fe_HR inputs. The accumulation of marine materials in the surface sediments of Prydz Bay is primarily driven by primary production, as indicated by the distribution of chlorophyll a in surface waters and sedimentary TOC and total nitrogen (TN) (Vaz and Lennon, 1996; Liu et al., 2014). Therefore, Prydz Bay and the adjacent Southern Ocean provide an ideal area for studying Fe speciation and its relationship with OC, given the specific geographical environment and material source conditions.

In this study, we conducted the sequential extraction of Fe species and measured TOC, Fe_T, grain size and specific surface area (SSA) in 20 surface sediments from Prydz Bay and the adjacent Southern Ocean. The aim was to characterize the distribution of Fe species, particularly Fe_HR, and speculate on its controlling factors. Additionally, we preliminarily discussed the relationship between TOC and Fe speciation in the research region and the implications from a global perspective.

2 Materials and methods

2.1 Sampling procedure

During the 24^th to 29^th Chinese National Antarctic Research Expeditions (CHINARE-24 to -29, 2007 – 2013), a total of 20 surface sediment samples were collected from Prydz Bay and the adjacent Southern Ocean (Figure 1; Table 1). The box sampler was used to collect the sediment samples, and the topmost 0 – 1 cm layer was considered as the surface sample. The samples were immediately frozen at –20°C and transported to the laboratory where they were stored at the same temperature until analysis.

FIGURE 1

Figure 1 Surface sediment sampling stations in Prydz Bay and the adjacent Southern Ocean during the 24^th to 29^th Chinese National Antarctic Research Expeditions (CHINARE-24 to -29). The circumfluence map is modified after Williams et al. (2016). PBG, Prydz Bay Gyre; mCDW, modified Circumpolar Deep Water; DSW, Dense Shelf Water; ISW, Ice Shelf Water.

TABLE 1

Table 1 Sampling information, sand, clay, silt and categories of surface sediment from Prydz Bay and the adjacent Southern Ocean.

2.2 Grain size and specific surface area analysis

The sediment grain size was analyzed using a laser particle size analyzer (Malven Mastersizer 3000, UK) with an analysis range of 0.01 – 3500 μm and a precision better than 1%. Approximately 1 g of wet sediment was placed into pure water and mixed well with ultrasonication. The bulk sediment samples were then separated into 3 standard size fractions: sand (> 63 μm), silt (4 – 63 μm), and clay (< 4 μm). The freeze-dried sediments were heated in a muffle oven at 350°C for 12 h to remove organic matter. The SSA of the sediments was measured by the static volumetric method using an automatic analyzer (Bessed 3H-2000 PS1, China) with an analysis range of > 0.005 m²/g and a precision better than 1%.

2.3 TOC analysis

The TOC content in the sediments was determined using an elemental analyzer–isotope ratio mass spectrometer (EA–IRMS) (Thermo Delta V advantage, US). The freeze-dried sediment samples were analyzed after removing carbonates by acid fumigation and oven drying at 60°C for 24 h (Harris et al., 2001). The precision of the reference material (Acetanilide) was ± 0.23% (n = 5). One sample was selected to run as replicates in parallel (P7-16), and the relative standard deviation (RSD) of TOC measurements was < 16% (n = 2, Table S2).

2.4 Total Fe and Al determination

The Fe_T and Al content were analyzed using an inductively coupled plasma–atomic emission spectrometer (ICP–AES) (Thermo Fisher IRIS Intrepid II XSP, US). The freeze-dried sediment samples were placed in a polytetrafluoroethylene inner tank, which was immersed in nitric acid and leached with deionized water. The samples were then digested with mixed HF–HClO₄–HNO₃ acids (guaranteed reagent) in a microwave digestion instrument. The acid was expelled, and the volume was calibrated by adding Rhodium. The Fe_T and Al content in the digestion fluid were determined by subtracting blanks. Reference materials (GBW07314 [offshore marine sediments, The State Bureau of Quality and Technical Supervision of China], GBW07103 [granite rock composition analysis reference materials, The State Bureau of Quality and Technical Supervision of China] and GSP-2 [granodiorite powdered reference materials, USGS]) were also digested using the same method for quality control. The recovery efficiencies of Fe_T and Al for the reference materials were 100.2% – 101.9% and 100.1% – 100.4%, respectively. Replicates were analyzed for two samples (P4-07, P7-07), and the RSDs were ≤ 5.3% (n = 2, Table S2).

2.5 Fe speciation

Fe species analyses, including carbonate associated ferrous Fe (Fe_carb), easily reducible amorphous/poorly crystalline Fe oxides (Fe_ox1), reducible crystalline Fe oxides (Fe_ox2), magnetite (Fe_mag), and poorly reactive sheet silicate Fe (Fe_PRS), were conducted following the methods of Poulton and Canfield (2005) and März et al. (2012) as shown in Table S1. Briefly, the surface sediments were homogenized after freeze-drying, weighed accurately to 0.1 g, and then sequentially extracted by adding the respective reagents necessary for each Fe species to the centrifuge tube containing the sediments. The tubes were centrifuged at 4800 rpm for 10 min and the supernatants were transferred into PET bottles for Fe species analysis. The sediment residuals from the previous step were then washed twice with distilled water, which was added to the extracted supernatants. The Fe content in the supernatants was determined on a flame atomic absorption spectrophotometer (ZEE nit 700P, Germany). The RSDs for 10 samples were < 6.5% for Fe_carb, < 8.2% for Fe_ox1, < 4.9% for Fe_ox2, < 13% for Fe_mag (n = 3); and the RSDs for 2 samples was < 5.5% for Fe_PRS (n = 2) (Table S2). The sediments exhibited no observable indications of Fe sulfides (black mottles), leading to the assumption that pyrite-bound Fe was insignificant (März et al., 2012) and was not subject to analysis in this study. Here, we established Fe_HR = Fe_carb + Fe_ox1 + Fe_ox2 + Fe_mag as per Poulton and Canfield (2005). Consequently, the equation for unreactive silicate Fe (Fe_U) was: Fe_U = Fe_T – (Fe_HR + Fe_PRS).

2.6 Statistical analyses

To establish relationships between the measured parameters, a Pearson correlation analysis and a two-tailed test of significance were conducted using the statistical software SPSS (Version 25). Additionally, a cluster analysis was performed using the same software. One-way analysis of variance with a 95% confidence interval (p < 0.05) was used to identify statistically significant differences.

3 Results

3.1 Grain size and grouping

The sediment composition in the study area is analyzed in terms of the content of clay (5.12% – 40.0%), sand (2.75% – 72.7%), and silt (22.1% – 81.9%). Silt is found to be the dominant component, accounting for an average of 57.4% of the sediment volume (Table S3). Sandy silt is identified as the main sediment type in the study area (Figure 2) according to the sediment classification method of Folk (1980). Cluster analysis of grain size results in the division of sediment samples into 4 categories: “Coarse”, “Medium”, “Fine” and “Ultra-fine”, as shown in Figure 2. The “Coarse” category includes 2 stations from Fram Bank, the “Medium” category includes 5 stations from the Amery Ice Shelf front, Four Ladies Bank and Prydz Channel, the “Fine” category includes 8 stations from the Cape Darnley polynya and Amery Basin, and the “Ultra-fine” category includes 5 stations from the deep Southern Ocean and Four Ladies Bank (Table 1).

FIGURE 2

Figure 2 Classification of surface sediments in Prydz Bay and the adjacent Southern Ocean. Samples are classified into 4 categories based on a cluster analysis: “Coarse” (red squares), “Medium” (blue triangles), “Fine” (green dots) and “Ultra-fine” (yellow diamonds).

3.2 SSA, TOC and OC loading

The SSA of the sediment samples ranges from 1.78 to 41.2 m²/g. The highest SSA is found in the “Ultra-fine” sediment category (33.9 ± 8.13 m²/g), followed by “Fine” (17.7 ± 4.86 m²/g) and “Medium” (8.57 ± 4.06 m²/g) sediments. The “Coarse” sediment category has the lowest SSA (1.87 ± 0.128 m²/g) (Table S3).

The TOC content ranges from 0.13% to 1.65%, similar to values (0.14% – 1.20%) in Liu et al. (2014). The “Fine” sediment category has significantly (p < 0.005) higher TOC content (1.02% ± 0.35%) than the other 3 categories (0.19% ± 0.02%, 0.32% ± 0.28%, 0.34% ± 0.19% for “Coarse”, “Medium” and “Ultra-fine”, respectively) (Table S3).

The OC loading (i.e., the TOC/SSA ratio) ranges from 0.04 to 1.29 mg/m². The “Coarse” sediment category has the highest OC loading (0.99 ± 0.18 mg/m²), followed by “Fine” (0.62 ± 0.33 mg/m²), “Medium” (0.38 ± 0.21 mg/m²), and “Ultra-fine” (0.12 ± 0.11 mg/m²) sediments (Table S3).

3.3 Total Fe and Fe speciation

The Fe_T content ranges from 1.22% to 5.19% (2.72% ± 0.993%), and is significantly (p < 0.01) higher in the “Ultra-fine” category sediments (3.99% ± 0.950%) than “Fine” (2.01% ± 0.387%) and “Medium” (2.37% ± 0.430%) sediments, with the middle value in “Coarse” category (3.25% ± 0.348%) (Table S3).

The characteristics of Fe speciation are reported in Table S3. A comparison of the average yields of various Fe pools and their ratios to Fe_T in the 4 grain size categories are shown in Figure 3. Fe_U is the largest Fe pool (290 ± 125 μmol/g), followed by Fe_PRS (134 ± 105 μmol/g) and Fe_HR (64.0 ± 43.7 μmol/g) (Figure 3B). Within Fe_HR, the content of Fe_ox2 (24.7 ± 19.4 μmol/g) and Fe_ox1 (21.0 ± 15.9 μmol/g) is significantly (p < 0.001) higher than Fe_carb (3.70 ± 1.31 μmol/g), with Fe_mag in the mid-range of these values (14.7 ± 9.99 μmol/g) (Figure 3A).

FIGURE 3

Figure 3 The average content of (A) Fe_carb, Fe_ox1, Fe_ox2, Fe_mag and (B) Fe_HR, Fe_PRS, Fe_U, Fe_T in “Coarse”, “Medium”, “Fine” and “Ultra-fine” categories of sediments from Prydz Bay and the adjacent Southern Ocean. Note: Fe_HR = Fe_carb + Fe_ox1 + Fe_ox2 + Fe_mag.

Regarding different grain size categories, Fe_ox1, Fe_ox2, Fe_mag, Fe_HR and Fe_PRS content is all significantly (p < 0.01) higher in “Ultra-fine” sediments (44.6 ± 11.7, 53.7 ± 8.02, 27.8 ± 6.87, 129 ± 26.0, 285 ± 83.6 μmol/g, respectively) than “Coarse” (4.37 ± 0.0778, 3.59 ± 0.601, 4.42 ± 2.16, 15.1 ± 3.37, 29.5 ± 13.5 μmol/g, respectively), “Medium” (11.1 ± 3.04, 16.0 ± 8.44, 14.1 ± 8.82, 44.4 ± 17.7, 80.0 ± 43.9 μmol/g, respectively) and “Fine” (16.5 ± 5.73, 17.2 ± 9.82, 9.43 ± 3.79, 47.7 ± 17.9, 98.0 ± 39.1 μmol/g, respectively) categories. Fe_U is significantly (p < 0.01) higher in “Coarse” sediments (538 ± 45.5 μmol/g) than in “Medium” (300 ± 68.6 μmol/g), “Fine” (215 ± 67.4 μmol/g) and “Ultra-fine” (300 ± 135 μmol/g) sediments, while there is no significant difference (p > 0.05) in Fe_carb (2.72 ± 1.90, 3.20 ± 0.830, 4.59 ± 1.41 and 3.16 ± 0.605 μmol/g for “Coarse”, “Medium”, “Fine” and “Ultra-fine” categories, respectively) (Figure 3).

4 Discussion

4.1 Fe_HR characteristics and controlling factors

4.1.1 Control of weak weathering and slow glacier melting on low Fe_HR/Fe_T ratio

In the sediments from Prydz Bay and the adjacent Southern Ocean, there is a significant positive correlation between Fe_HR and Fe_T, as well as between Fe_HR and Al (R² = 0.55, p < 0.001; R² = 0.31, p < 0.05; Figure S1). This finding is consistent with the global riverine and glacial particulates, implying that Fe_HR are closely associated with Fe-bearing aluminosilicate minerals (Poulton and Raiswell, 2002; Poulton and Raiswell, 2005). The Fe_HR/Fe_T ratios in the research region (0.13 ± 0.06) are similar to those in Antarctic glacial particulates (0.11 ± 0.05), and lower than those in global river particulates (0.43 ± 0.03) and modern marine sediments (0.26 ± 0.08) (Figure 4) (Poulton and Raiswell, 2002). This result suggests that the sediments in our study area are mainly influenced by weak chemical weathering. Generally, during chemical weathering, the easily solubilized major elements (such as Na, K, Ca, etc.) in rock minerals are leached, while the insoluble elements, such as Al and Fe, are enriched. As a result, Fe forms insoluble mineral phases (mainly Fe oxides) that continuously adsorb on the surface of parent rock minerals (Martin and Meybeck, 1979; Canfield, 1997). Therefore, the degree of chemical weathering can determine the Fe_HR content as well as the Fe_HR/Fe_T ratio (Poulton and Raiswell, 2002; Wei et al., 2021).

FIGURE 4

Figure 4 Comparison of Fe_HR/Fe_T and Fe_T in “Coarse”, “Medium”, “Fine” and “Ultra-fine” categories of sediments from Prydz Bay and the adjacent Southern Ocean with global riverine particulates and modern marine sediments, Antarctic glaciers (Raiswell and Canfield, 1998; Poulton and Raiswell, 2002), off the western Antarctic Peninsula (Burdige and Christensen, 2022), off King George Island (Henkel et al., 2018), South Yellow Sea (Ma et al., 2018), East China Sea (Zhu et al., 2012), Barents Sea (Faust et al., 2021), Umpqua (Roy et al., 2013) and the Jiaozhou Bay (Zhu et al., 2015). Data are averages of surface sediments (0 – 2 cm) by recalculation of Henkel et al. (2018) and Burdige and Christensen (2022).

River and glacier particulates are known to represent the high and low end-members of weathering intensity, respectively, and their mixing in varying proportions determines the Fe_HR/Fe_T ratio characteristics of sediments in different marine environments (Poulton and Raiswell, 2005). In the research region, the Fe_HR/Fe_T ratios belong to the lower end-member compared to other polar sediments (Figure 4). For example, in the Arctic Barents Sea, off the Antarctic Peninsula and King George Island, the Fe_HR/Fe_T ratios of surface sediments (shallower than 2 cm) are 0.28 ± 0.07, 0.21 ± 0.05 and 0.35 ± 0.06, respectively (Henkel et al., 2018; Faust et al., 2021; Burdige and Christensen, 2022), all significantly (p < 0.01) higher than our result (0.13 ± 0.06) (Figure 4). This difference can be attributed to the differences in the glacier melting and the bedrock weathering. In our study region, the ice-free area is small and the glacier melting rate is slow (Campbell et al., 1993; The IMBIE team, 2018). However, in the Arctic Barents Sea, off the Antarctic Peninsula and King George Island, there are larger ice-free zones and higher glacier melting rates (Stammerjohn et al., 2008; Screen and Simmonds, 2010; Rueckamp et al., 2011; The IMBIE team, 2018). Therefore, intense weathering process occurs: the runoff formed from ice melting continuously erodes the bedrock, producing soluble Fe²⁺ and secondary nanoparticulates, which are then oxidized and aged into Fe oxides, and transported to the marginal seas along with the runoff (Henkel et al., 2018). This situation is similar to those in rivers of middle and low latitudes, which can continuously transport Fe-containing particulates with high Fe_HR/Fe_T ratio. Besides, the Fe_HR/Fe_T ratios are significantly (p < 0.05) higher off King George Island (Figure 4), probably due to the semi-enclosed bay topography, which is conducive to Fe_HR enrichment, similar to the Jiaozhou Bay and Bohai Sea (Zhu et al., 2015; Wang et al., 2019).

Our findings demonstrate that the Fe_HR/Fe_T ratios vary across the 4 grain size-based sediment categories in the study area. Specifically, the Fe_T content in “Coarse” sediments (3.25% ± 0.348%) is comparable to that of the Earth’s crust (3.5%) (Taylor, 1964), and the Fe_HR/Fe_T ratios are extremely low (0.03 ± <0.005), representing minimal weathering of the input material from the Antarctic continent. In “Medium” and “Fine” sediments, the Fe_T content (2.37% ± 0.430% and 2.01% ± 0.387%, respectively) and Fe_HR/Fe_T ratios (0.10 ± 0.03 and 0.13 ± 0.04, respectively) are comparable to those of the Antarctic glacial particulates (2.10% ± 0.539% and 0.11 ± 0.05) (Poulton and Raiswell, 2002), indicating that sediments along the shelf of Prydz Bay primarily originate from the weak weathering Antarctic continent. While in “Ultra-fine” sediments, mainly from the deep Southern Ocean, the Fe_T content (3.99% ± 0.950%) is comparable to that of global deep sea sediments (4.29% ± 0.98%), and the Fe_HR/Fe_T ratios (0.18 ± 0.03) are slightly lower than those in global deep sea sediments (0.25 ± 0.10) (Poulton and Raiswell, 2002), indicating relatively enhanced weathering in this sediment category.

4.1.2 Indications of the relative content of Fe_carb, Fe_ox1 and Fe_ox2

The Fe_carb/Fe_T ratios of the 4 grain size-based sediment categories in our research region (0.005 ± 0.003, 0.008 ± 0.003, 0.013 ± 0.005 and 0.005 ± 0.001 for “Coarse”, “Medium”, “Fine” and “Ultra-fine” categories, respectively) exhibit similarity (p > 0.05) to values from oxygen-rich sedimentary environments (e.g., 0.013 ± 0.004 and 0.019 ± 0.007 for the South Yellow Sea and off King George Island, respectively) (Henkel et al., 2018; Ma et al., 2018), but are significantly (p < 0.001) lower than those from anoxic or hypoxic sedimentary environments (e.g., 0.11 and 0.06 ± 0.02 for FOAM and the East China Sea, respectively) (Canfield, 1989; Zhu et al., 2012) (Figure 5). Generally, in an Fe-rich and sulfide-free hypoxic or anoxic environment, intense microbially-mediated dissimilatory Fe reduction promotes the transformation of Fe_ox1 and Fe_ox2 to Fe(II) (Canfield, 1989; Mathew et al., 2022). Under neutral pH and oxidizing conditions, Fe(II) can rapidly oxidize to Fe(III) and hydrolyze to Fe (hydrogen)oxides (Konhauser et al., 2011; Ma et al., 2018). Therefore, our results indicate that the formation and accumulation of Fe(II) are restricted in oxygen-rich Antarctic marine environments (Meijers et al., 2010; Katsumata et al., 2015).

FIGURE 5

Figure 5 Fe_carb/Fe_T, Fe_ox1/Fe_T and Fe_ox2/Fe_T ratios in “Coarse”, “Medium”, “Fine” and “Ultra-fine” categories of sediments from Prydz Bay and the adjacent Southern Ocean, as well as in sediments from FOAM (friends of anoxic mud) (Canfield, 1989), the ECS (East China Sea) (Zhu et al., 2012), SYS (South Yellow Sea) (Ma et al., 2018) and KGI (King George Island) (Henkel et al., 2018). Data are averages of surface sediments (0 – 2 cm) by recalculation of Canfield (1989) and Henkel et al. (2018).

Interestingly, the Fe_ox2/Fe_T ratios of the 4 categories in our research region (0.01 ± <0.005, 0.04 ± 0.02, 0.05 ± 0.02 and 0.08 ± 0.01 for “Coarse”, “Medium”, “Fine” and “Ultra-fine” categories, respectively) are significantly (p < 0.001) lower than those in highly weathered marginal seas, such as the East China Sea and off King George Island (0.13 ± 0.03 and 0.16 ± 0.04) (Zhu et al., 2012; Henkel et al., 2018). However, the Fe_ox1/Fe_T ratios (0.03 ± <0.005, 0.05 ± 0.01 and 0.06 ± 0.01 for “Medium”, “Fine” and “Ultra-fine” categories, respectively) are similar (p > 0.05) to those from the East China Sea, South Yellow Sea, and off King George Island (0.05 ± 0.01, 0.04 ± 0.01 and 0.04 ± 0.01) (Zhu et al., 2012; Henkel et al., 2018; Ma et al., 2018) (Figure 5).

There are 3 potential explanations for the observed differences in patterns between Fe_ox1/Fe_T and Fe_ox2/Fe_T. Firstly, the transformation of Fe_ox1 to Fe_ox2 in the sediments of our study area is restricted. Generally, the initial Fe oxides in the redox cycle are highly reactive and amorphous: i.e., Fe_ox1. Over time, Fe_ox1 gradually transforms into more stable and crystalline Fe oxides: i.e., Fe_ox2 (Senn et al., 2017). However, the half-life of Fe oxides aging in low temperature environments (< 0°C) is 4 – 6 times longer than in mid-latitude areas (15°C – 20°C) (Canfield et al., 1992; Raiswell and Canfield, 1998; Schwertmann et al., 2004). Considering the relatively new surface sediment ages in the continental shelf of Prydz Bay (Wu et al., 2017), the insufficient conversion time may be responsible for the low Fe_ox2/Fe_T ratios observed.

Secondly, there may be additional Fe_ox1 sources in the study area. Icebergs are considered to be an important Fe_HR source to the Southern Ocean (Lin et al., 2011; Raiswell et al., 2016; Raiswell et al., 2018). The Fe in icebergs is often isolated by the ice, limiting Fe contact with water and organic matter and preventing Fe from further aging (Raiswell et al., 2016; Raiswell et al., 2018). Therefore, a high content of ferrihydrite exists in icebergs and may rapidly settle into sediments during melting by scavenging. However, due to a lack of systematic studies, it is still impossible to quantitatively assess the importance of iceberg contributions to sedimentary Fe pools, especially Fe_ox1.

Finally, the dynamic equilibrium of the conversion between the transformation from Fe_ox1 to Fe_ox2 promoted by aging and the transformation from Fe_T to Fe_ox1 promoted by chemical weathering (Schwertmann et al., 2004; Poulton and Raiswell, 2005) also explains our Fe_ox1/Fe_T results. In summary, these results demonstrate that the regulation of Fe_HR/Fe_T ratio by weathering is mainly reflected in the control of Fe_ox2/Fe_T ratio rather than Fe_ox1/Fe_T ratio.

4.2 Relationship between Fe_HR and TOC

The correlation between Fe_HR and TOC was investigated in the sediments of Prydz Bay and the adjacent Southern Ocean. Results show a significant negative correlation between TOC and Al, and TOC and Fe_T (R² = 0.53, p < 0.01; R² = 0.35, p < 0.01, Figures S2A, B). The source of Fe in the sediments is mainly from weak-weathered rock of the Antarctic continent (see section 4.1), while TOC is mainly derived from primary production by phytoplankton based on organic biomarkers (Zhao et al., 2014) and TOC/TN ratios (Liu et al., 2014). Therefore, the negative correlations indicate significant differences in the sources of TOC (biogenic) versus Al and Fe_T (lithogenic), and the dilution relationship between each other.

Previous studies have shown that TOC is often positively correlated with Fe_HR in surface sediments from riverine particulates, glaciers and marginal seas (Poulton and Raiswell, 2005; Zhu et al., 2012; Roy et al., 2013; Zhu et al., 2015). However, there is no significant (p > 0.05) correlation between the TOC and Fe_HR, Fe_carb, Fe_ox1 or Fe_ox2 content in the sediments of our study area (Figures S2C–F), possibly due to the complex sedimentary environment. Based on a wide range of samples, we summarize and classify the relationship between TOC and Fe_HR in different sedimentary environments around the world (Figure 6), as follows.

FIGURE 6

Figure 6 Diagram of the relationship between the content of TOC and Fe_HR. Specific ranges of TOC/Fe_HR ratios characterize different sedimentary environments, and reflect the degree of OC-Fe_HR complexing in different environments. Data related to OC/Fe_HR ratios are derived from this study, Wijsman et al. (2001); Roy et al. (2013); Jessen et al. (2017); Ma et al. (2018); Faust et al. (2021) and Zhu et al. (2012); Zhu et al. (2015). The f_OC-Fe data are from Lalonde et al. (2012); Shields et al. (2016); Ma et al. (2018); Faust et al. (2021) and Zhao et al. (2018). OET, oxygen-exposure time; SYS, South Yellow Sea; ECS, East China Sea, JZ Bay, the Jiaozhou Bay. Data are averages of surface sediments (0 – 2 cm) by recalculation of Jessen et al. (2017); Faust et al. (2021) (stations 393, 506 and 448), Shields et al. (2016) and Wijsman et al. (2001) (station 19).

The first scenario pertains to high TOC/Fe_HR ratios (> 2.5), observed in “Fine” sediments with elevated TOC content (1.02% ± 0.35%) and high OC loading (TOC/SSA = 0.62 ± 0.33 mg/m²) in this study (Table S3), as well as in anoxic environments like the Black Sea (Wijsman et al., 2001; Jessen et al., 2017). Usually, the extremely high TOC content and TOC/Fe_HR ratios in anoxic environments are due to the reduced remineralization of TOC (Jessen et al., 2017). In contrast, “Fine” sediments are mainly located in the center of Prydz Bay, with shallow water depths (251 – 748 m), and high primary productivity (412 mmol C m^–2 d^–1), summer particulate deposition fluxes (2515 ± 1828 μmol C m^–2 d^–1) and sedimentation rates (2.9 – 8.7 g C m^–2 a^–1) (Behrenfeld and Falkowski, 1997; Yu et al., 2009; Han, 2018). These conditions favor high OC accumulation rates and OC loading (Blair and Aller, 2012). However, the effect of dilution by marine OC on Fe_HR content is more significant due to the low Fe_HR content caused by inputs of relatively unweathered materials, as described in section 4.1. It should be noted that, unlike in anoxic environments, the situation in our study area is a novel discovery in oxygen-rich polar marine environments and may have significant global implications for the long-term preservation of marine OC (Liu et al., 2014).

The second scenario pertains to low TOC/Fe_HR ratios (< 0.6), observed in suspended particulates of rivers with high discharge rates (the Amazon River and the Yellow River) (Poulton and Raiswell, 2005) and deep-sea sediments (Lalonde et al. (2012) and this study). In the former, there are substantial inputs of terrestrial materials (OC and Fe_HR) to the ocean; however, more than 90% of the OC is remineralized into CO₂ (Aller and Blair, 2006), and most Fe_HR is oxidized and crystallized into hematite, which has relatively poor bioavailability (Zhao et al., 2018, and references therein), due to frequent physical transformations and rapid redox cycling. In the latter, such as “Ultra-fine” sediments in this study, the prolonged oxygen exposure time of OC in deeper waters (> 3000 m) promotes OC remineralization, and the enhanced weathering leads to more Fe_HR development (Poulton and Raiswell, 2002).

The third scenario pertains to sediments with both low TOC and Fe_HR content, such as “Coarse” and “Medium” sediments in this study, and in icebergs (Poulton and Raiswell, 2005). The former are usually located at the front edge of Amery Ice Shelf or in shallow waters where sea ice cover persists for extended periods, resulting in low rates of OC deposition (1.1 – 5.7 g C m^–2 a^–1) (Yu et al., 2009) and limited TOC accumulation in sediments (Mayer, 1994; Blair and Aller, 2012). Additionally, weak weathering hinders the development of Fe_HR.

The final scenario pertains to mid-range TOC/Fe_HR ratios (0.6 – 2.5), including typical riverine particulates and marginal shelf sediments (Poulton and Canfield, 2005; Roy et al., 2013). In this scenario, there is a significant positive correlation between TOC and Fe_HR, as both are derived from terrestrial sources and interact with each other to form OC-Fe_HR complexes through adsorption/coprecipitation. These complexes are then transported to the coastal and shelf sediments and preserved for extended periods (Faust et al., 2021). Therefore, mid-range TOC/Fe_HR ratios represent the characteristics of the residual portion of relatively stable terrestrial OC (Poulton and Raiswell, 2005; Lalonde et al., 2012; Roy et al., 2013; Faust et al., 2021).

Based on the preceding discussion, we have deduced that the TOC/Fe_HR ratios to some extent can reflect the degree of OC-Fe_HR complexing in various environments. This implies that the contribution of Fe_HR to OC preservation may differ across different sedimentary settings. For example, in continental shelf marginal sea sediments with mid-range TOC/Fe_HR ratios, the f_OC-Fe is 16.1% ± 9.5% (n = 73) (Lalonde et al., 2012; Salvadó et al., 2015; Shields et al., 2016; Ma et al., 2018; Faust et al., 2021). In the mobile mud area of the Changjiang Estuary, characterized by low TOC/Fe_HR ratios, the f_OC-Fe is only 8.1% ± 4.2% (n = 26) (Zhao et al., 2018). In the deep-sea sediments with prolonged oxygen exposure, the f_OC-Fe is 13.7% ± 8.7% (n = 13) (Longman et al., 2022). Therefore, we propose that the f_OC-Fe may exhibit significant variation across different sediment categories in Prydz Bay and the adjacent Southern Ocean. However, research on the f_OC-Fe in Antarctic marine sediments is scarce, with only one Antarctic deep sea sediment out of 406 samples worldwide (Lalonde et al., 2012; Longman et al., 2022). Further research on the f_OC-Fe in Antarctic marine sediments is necessary in consideration of the low Fe_HR/Fe_T ratios and complex TOC/Fe_HR ratios.

5 Conclusion

The Fe_HR/Fe_T ratios observed in marine sediments from Prydz Bay and the adjacent Southern Ocean are similar to those in the Antarctic glacial particulates, but lower than those in global riverine particulates and modern marine sediments. This suggests that Fe_HR is mainly derived from the Antarctic bedrock with weak weathering. Our Fe_HR/Fe_T ratios are also lower than those in sediments from the Arctic Barents Sea, off the Antarctic Peninsula and King George Island, likely due to the slower glacier melting. The Fe_ox1/Fe_T ratios in our study area are equivalent to, those in sediments from other continental shelf marginal seas with intense weathering, but the Fe_ox2/Fe_T ratios are lower. This indicates that there is a potential inhibitory effect of low temperatures on aging of iceberg melting Fe_ox1, and the regulation of weathering on Fe_HR/Fe_T ratio is mainly reflected in Fe_ox2/Fe_T ratio. There is no significant correlation between TOC and Fe_HR, Fe_carb, Fe_ox1 or Fe_ox2 content, due to the complex and diverse sedimentary environments in the research region: “Fine” sediments with high TOC/Fe_HR ratios, TOC content, OC loading and low Fe_HR content, “Ultra-fine” sediments with contrary characteristics, and “Medium” and “Coarse” sediments with both low TOC and Fe_HR content.

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 author.

Author contributions

WH and JZ made substantial contributions to draft the manuscript. XG and WH made substantial contributions to the data analysis. DL, JH, HZ, CZ, ZH, WS, YS and JP made substantial contributions to participate the manuscript discussion. All authors contributed to the article and approved the submitted version.

Funding

This research was jointly supported by the National Natural Science Foundation of China (NSFC) (Nos. 41976228, 42276255, 41976227, 42176227), the Scientific Research Fund of the Second Institute of Oceanography, MNR (No. JG1805), National Polar Special Program “Impact and Response of Antarctic Seas to Climate Change” (Nos. IRASCC 01-01-02A and 02-02), and the China Scholarship Council (No. 201704180017).

Acknowledgments

The authors would like to thank Dr. Jihao Zhu for helping in Fe_T determination, and Ms. Huijuan Zhang for grain size measurements. We also extend thanks to the R/V Xuelong crews who devoted their time and effort to sample sediments in the CHINARE-24 to -29.

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.

Publisher’s note

All claims expressed in this article are solely those of the authors and do not necessarily represent those of their affiliated organizations, or those of the publisher, the editors and the reviewers. Any product that may be evaluated in this article, or claim that may be made by its manufacturer, is not guaranteed or endorsed by the publisher.

Supplementary material

The Supplementary Material for this article can be found online at: https://www.frontiersin.org/articles/10.3389/fmars.2023.1142061/full#supplementary-material

Abbreviations

Fe_carb, carbonate associated ferrous Fe; Fe_ox1, easily reducible amorphous/poorly crystalline Fe oxides (ferrihydrite, lepidocrocite); Fe_ox2, reducible crystalline Fe oxides (goethite, akaganéite, hematite); Fe_mag, magnetite; Fe_PRS, poorly reactive sheet silicate Fe; Fe_T, Total Fe; Fe_HR, Highly reactive Fe (Fe_carb + Fe_ox1 + Fe_ox2 + Fe_mag); Fe_U, Unreactive silicate Fe (Fe_T – Fe_HR – Fe_PRS); SSA, Specific surface area; TOC, Total organic carbon; f_OC-Fe, Proportion of OC in OC-Fe_HR complexes to TOC.

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