Sea ice in the Southern Ocean is one of the most seasonal and variable features of the Earth’s surface, and has a significant influence on key oceanic and atmospheric processes, which, in turn, have major impacts on global climate1. Although Antarctic sea ice extent has undergone a slight overall increase in recent decades, this is not the case for all regions, with dramatic reductions in the Bellingshausen and Amundsen Seas, being of particular note2. Reconstruction of sea ice conditions over longer timeframes is, therefore, critical for contextualizing recent changes, and for the broader interpretation of past climate conditions and the prediction of future climate states3. Some models, for example, suggest that Antarctic sea ice extent will reduce by 24% and more than a third in terms of total volume by 2100 (refs 3, 4), while others have predicted shorter sea ice seasons5. Currently, however, the general paucity of palaeo sea ice records from the Southern Ocean impacts on modern climate modelling6, and further reconstructions are needed to better inform, and test, current modelling efforts. From a methodological perspective, analysis of fossil diatoms archived in marine sediments forms the basis of established approaches for the determination of Antarctic winter and summer sea ice extent, although these become less reliable beyond the late Quaternary as extinct taxa with uncertain ecological affiliations become more prevalent7. Further, confidence in the reconstruction of past Antarctic summer sea ice extent is weaker than for winter sea ice due to fewer reference or analogue samples, although its determination represents an essential parameter with respect to evaluating seasonal sea ice cycles and net changes8,9.

In recent years, the analysis of an organic geochemical lipid biomarker—a so-called highly branched isoprenoid (HBI) diene (until now referred to as diene II; Fig. 1)—has been proposed as a possible proxy measure of Antarctic sea ice10,11,12,13,14,15,16,17,18. Diene II is a close structural analogue of the mono-unsaturated HBI lipid IP25, which has become a well-established proxy for seasonal sea ice in the Arctic19,20. In fact, diene II—hereafter referred to as IPSO25: Ice Proxy for the Southern Ocean with 25 carbon atoms, by analogy with IP25 for the Arctic19—co-occurs with IP25 in certain Arctic sea ice diatoms21 and its distribution in Arctic sediments exhibits a close parallel to that of IP25 (ref. 20). However, IP25 has not been reported in the Antarctic, likely due to the absence of the specific diatoms that biosynthesize this biomarker in the Southern Ocean. In contrast, IPSO25 has been reported in Antarctic sea ice and near-surface sediments, albeit in a relatively small number of studies12,22,23,24, with a stable isotopic composition (δ13C=ca. −5 to −18‰) indicative of a sea ice diatom origin12,24. Importantly though, unlike IP25, for which the source21, seasonal production25 and distribution pattern across the Arctic have been determined following analysis of sea ice and several hundred surface sediments from different Arctic regions20,26, no source has been identified for IPSO25. As such, although a number of sea ice reconstructions based on IPSO25 have been reported, spanning recent decades, the Holocene10,11,12,13,14,16,17 and the last glacial (ca. 60 kyr BP (ref. 15)), the lack of knowledge of its source, has almost certainly had an impact on the interpretation of its sedimentary occurrence and abundance characteristics.

Figure 1: Distribution of Berkeleya adeliensis and IPSO25 in previous studies.
figure 1

Summary map of Antarctica showing locations where Berkeleya adeliensis and HBI diene II (IPSO25) have been identified in sea ice, surface sediments and palaeo records (note: B. spp designates studies where diatom identification was not conducted beyond the genus level). The black and white stippled lines refer to the median winter and summer sea ice margins for the interval 1979–2010 (National Snow and Ice Data Center), respectively. Abbreviated location names are as follows: AP, Antarctic Peninsula; BS, Bellingshausen Sea; AS, Amundsen Sea; AL, Adélie Land; WI, Windmill Islands; PB/EF, Prydz Bay/Ellis Fjord; LB, Lützow-Holm Bay. The structure of the di-unsaturated HBI lipid biomarker diene II (IPSO25) is also shown.

In the current study, we identified IPSO25 in a single sea ice endemic (sympagic) diatom species by manual isolation of individual cells from a bulk sample of mixed sea ice diatom assemblage collected from the West Antarctic Peninsula (WAP) in December 2014, and analysis of its lipid composition by gas chromatography–mass spectrometry (GC–MS). We also determined the abundance distribution of IPSO25 in ca. 150 surface sediments covering different regions of (mainly) West Antarctica, including the Weddell Sea, the Antarctic Peninsula (AP), the Bellingshausen Sea and the Ross Sea, together with its stable isotopic composition (δ13C) in three representative surface sediments from some of these locations. The source of IPSO25 in our sea ice samples, Berkeleya adeliensis Medlin27, is a widespread and commonly occurring constituent of Antarctic sea ice; both important attributes for paleo sea ice reconstruction purposes, yet this diatom is rarely evident in fossil assemblages. As a tube-dwelling species, B. adeliensis is particularly well adapted for growth in the relatively open channels of platelet ice, a common feature of landfast ice proximal to coastal Antarctic locations, which probably has important consequences for the interpretation of sedimentary IPSO25.


IPSO25 in sea ice and picked sea ice diatom cells

The diatom assemblage in a bulk sea ice sample collected from the WAP in December 2014 consisted of B. adeliensis as the major diatom species (>50%) (Fig. 2). Further, the lipid biomarker IPSO25 was identified in non-polar extracts obtained from both the bulk sea ice sample and picked cells of B. adeliensis, with an estimated cellular concentration (ca. 6 pg per cell) consistent with that of other HBI-producing diatoms21. No other HBI lipids were identified in the bulk sea ice sample or the picked cells of B. adeliensis.

Figure 2: IPSO25-producing species and lipid extracts containing IPSO25.
figure 2

(a) Light microscopy image of B. adeliensis isolated from a sample of Antarctic sea ice immediately following partial thawing. The strands of cells are particularly characteristic of this tube-dwelling species. The white scale bar represents 100 μm; (b) partial GC–MS chromatograms of IPSO25 in various samples (SIM mode; m/z 348.3). BC492 and BC608 are surface sediments. The structure of IPSO25 is also shown.

IPSO25 in Antarctic surface sediments

Within the surface sediments, IPSO25 could be identified and quantified in 125 out of the 149 samples analysed, with concentrations ranging from 0.22 to 1,830 ng g−1 (Fig. 3; Supplementary Table 1). Highest concentrations (>500 ng g−1) were always associated with samples taken from coastal locations, with a general drop-off in abundance for offshore sites (Fig. 4). In some cases, there were also substantial abundance variations in IPSO25, even for relatively nearby study sites. Finally, the stable isotopic composition (δ13C) of IPSO25 in surface sediments from Marguerite Bay (WAP), the SE Weddell Sea and the northern AP was found to be −15.00±0.03‰, −13.46±0.02‰ and −14.39±0.07‰, respectively (Supplementary Fig. 1).

Figure 3: IPSO25 in surface sediments.
figure 3

(a) Distribution map showing the variable concentration of IPSO25 in Antarctic surface sediments (note: the key refers to this map only and values correspond to concentration ranges of IPSO25 in ng g−1 dry sediment); (b) Locations where IPSO25 was below the limit of detection (that is, <0.2 ng g−1 dry sediment).

Figure 4: IPSO25 distribution in coastal-offshore transects.
figure 4

Regional maps illustrating the gradient drop-off in IPSO25 concentration in surface sediments from coastal to offshore settings. (a) Map of West Antarctica showing two named sub-regions and individual sampling locations for which IPSO25 data are further illustrated in b and c. (b) IPSO25 concentrations in surface sediments from the SE Weddell Sea; (c) IPSO25 concentrations in surface sediments from the Bellingshausen Sea.


The data presented herein establish B. adeliensis as a source of IPSO25 in Antarctic sea ice. Similar HBI alkenes have recently been identified in a different species within the genus Berkeleya (B. rutilans28), including an HBI diene, but this was a different isomer to IPSO25 identified here in Antarctic sea ice and sediments. Determining whether B. adeliensis represents the only source of IPSO25 in Antarctic sea ice will require analysis of samples from other Antarctic regions, and individual diatom species within these. In the meantime, we note that, among the more common and abundant Antarctic sea ice diatom genera, Fragilariopsis, Chaetoceros and Nitzschia, are not producers of HBI lipids29. In fact, of the known HBI-producing diatom genera, only Haslea, Pleurosigma, Navicula and Berkeleya are found in Antarctic sea ice, and only the latter two contain species that are generally considered to be common and abundant (viz. Navicula glaciei and B. adeliensis); however, no HBI lipids (including IPSO25) were identified previously in N. glaciei12. In addition, species within the Pleurosigma genus do not biosynthesize HBIs with a 6–17 double bond30, which is one of the structural characteristics of IPSO25 (Fig. 2). In previous studies of HBI lipids in Antarctic sea ice and sea ice diatoms12,22,23, only IPSO25 has been identified as a common and abundant component, despite analyses having been conducted on mixed diatom assemblages of varying composition. This either means that B. adeliensis is a unique source of IPSO25 in Antarctic sea ice or that other species also only produce this particular HBI, and no others. However, the latter seems unlikely given the large number of HBIs of different structural type made by various diatoms and, unlike all other HBI-producing diatom genera, which have thus far, always been shown to produce a suite of HBIs (typically >3) (for a recent review, see ref. 28 and references therein), the genus Berkeleya appears to biosynthesize predominantly only one isomer. Further, the occurrence of up to seven HBI isomers in Arctic sea ice31 can be attributed to the presence of several HBI-producing diatoms, and not just those that biosynthesize IP25 (refs 19, 21, 25). Therefore, although it is feasible that species other than B. adeliensis may be producers of IPSO25 in Antarctic sea ice, these are likely to be only relatively minor contributors of this biomarker. As such, we believe that B. adeliensis probably represents a major source of IPSO25 in coastal Antarctic sea ice and underlying sediments, and further data support this hypothesis. For example, the identification of IPSO25 in sediments from a large number of coastal locations is consistent with the presence of B. adeliensis as a common and relatively abundant species within Antarctic landfast ice diatom communities27,32,33,34. On a more specific regional basis, IPSO25 has previously been reported in sea ice and/or sediments from locations where B. adeliensis has also been identified in sea ice, including Ellis Fjord24,35, Adélie Land11,12,18,34,36, Lützow-Holm Bay37,38, the WAP13,16 (and this study) and the Ross Sea/McMurdo Sound23,33,39,40 (Fig. 1). For the Windmill Islands, East Antarctica, B. adeliensis has also been identified in sediments from Stephenson Cove41, while IPSO25 has been reported in sea ice from the same location and nearby O’Brien Bay12 (Fig. 1).

B. adeliensis is a constituent species of the tube-dwelling genus Berkeleya Grunow, found frequently in Antarctic coastal waters and sea ice33,34,36,42,43, and is commonly associated with landfast ice, where it can colonize both consolidated bottom ice and platelet ice; in some cases forming elongated strands that extend below the ice surface34,36,42,43. On the other hand, B. adeliensis has not been reported outside of the Antarctic, so cannot be a source of IPSO25 in sediments from the Arctic, for example, despite the common occurrence of this biomarker in sediments from high latitude northern hemisphere settings20. A more specific habitat preference for B. adeliensis in Antarctic sea ice is not entirely clear, since elevated cell numbers have been reported in bottom ice and platelet ice34,36, although some migration to the latter has been noted during ice melt36. Indeed, Riaux-Gobin et al.36 suggested that B. adeliensis may be more tolerant towards the contrasting environments of bottom ice and platelet ice than many other sympagic species, with the more open-channel network of platelet ice possibly more compatible with such tube-dwelling species34. Further, Riaux-Gobin et al.34 identified substantially higher abundances of B. adeliensis in sea ice from coastal locations compared with offshore settings around Adélie Land, East Antarctica, while in the water column, generally low abundances of B. adeliensis, attributed to ice melt release, were restricted to under-ice waters or polynyas proximal to coastal locations34,43.

The close association of B. adeliensis with landfast ice prompted Riaux-Gobin et al.43 to suggest that the occurrence of the cells of such sympagic species may represent suitable proxies in sedimentary records, adding the caveat that the poor preservation potential of the cells may prevent such an application, in practice. Indeed, B. adeliensis was not identified in sediment assemblage counts from Lützow-Holm Bay, despite being abundant in overlying sea ice and the water column37, and the organism is rarely (if ever) a constituent of diatom inventories used in paleoceanographic reconstructions9,44,45,46. Abundances of B. adeliensis have been shown to exhibit a high-to-low abundance trend for coastal to offshore sites for Adélie Land in both sea ice34 and surface waters soon after ice melt43, and a similar trend in IPSO25 distribution has been observed previously in surface sediments from the same region, with highest concentrations for near-shore settings, lower values offshore, and absence for sites beyond the marginal ice zone12. A similar offshore depletion in abundances of IPSO25 was also identified previously in sediments from Lützow-Holm Bay38, from where B. adeliensis has been reported in coastal landfast ice37 and the generality of this gradient can be readily seen through inspection of the surface sediment data for IPSO25 presented herein, with highest concentrations (up to ca. 1,800 ng g−1) for coastal locations and substantially lower abundances offshore (ca. 0.22–8.51 ng g−1) (Fig. 4). Finally, concentrations of IPSO25 in surface waters from East Antarctica during late spring (that is, during and shortly after ice melt) were recently shown to be strongly dependent on the nature and length of seasonal ice cover, with highest values for coastal locations experiencing at least partial ice cover extending into the summer47.

Collectively, these observations suggest that distributions of IPSO25 in Antarctic sediments are closely related to the ecology of the source diatom, B. adeliensis. If this is the case, the apparently strict association of B. adeliensis to landfast ice might limit the value of IPSO25 as a general Antarctic sea ice proxy. However, instead, the environmental specificity of its source should enable more detailed insights into defining past sea ice conditions to be made with confidence. Thus, since it has been shown previously that B. adeliensis increases in abundance towards the end of the spring bloom and during the onset of ice melt34,40, it follows that the occurrence of sedimentary IPSO25 likely signifies the past presence of landfast ice during late spring/early summer. Such an interpretation parallels, to some extent, that for IP25 in the Arctic, the sedimentary presence of which is interpreted as reflecting spring sea ice cover19,20, although this is not restricted to landfast ice.

Previous palaeo sea ice reconstructions based on IPSO25 have largely been conducted on sediment cores retrieved from near-coastal locations around the Antarctic Peninsula (AP)13,14,16, Adélie Land11,18 and Prydz Bay10, so its occurrence in these is consistent with the source and surface sediment data presented herein. Interestingly, however, B. adeliensis was not reported in the taxonomic inventories of any of these previous studies, which presumably reflects the susceptibility of this species towards dissolution in the water column and in sediments. Indeed, it has been suggested previously that many sea ice diatoms such as B. adeliensis may be under-represented in Antarctic sediments48, likely as a result of their only lightly silicified frustules. However, on the basis of readily detectable quantities of IPSO25 in surface sediments described here, and in previous downcore investigations10,11,12,13,14,15,16,17,18, we infer that there must be at least partial deposition of B. adeliensis from the melting sea ice to underlying sediments, even if subsequent dissolution of its silica frustules is significant. By combining the intracellular concentration of IPSO25 in B. adeliensis determined in the current study with its abundance distribution in surface sediments, we estimate that the corresponding contribution of B. adeliensis falls within the range ca. 102–105 cells per gram, which is lower than typical total diatom cell concentrations in Antarctic sediments (ca. 105–107 cells per gram)49,50 and certainly below the 2–3% threshold generally used in taxonomy-based paleoceanographic reconstructions45,51. On the other hand, the occurrence of IPSO25 likely offers complementary information to taxonomic-based sea ice reconstructions, not least, since a clear distinction can be made between the respective signatures of IPSO25 and commonly employed sea ice diatom taxa in sediments. Thus, IPSO25 is biosynthesized by at least one individual diatom species (B. adeliensis) that resides and blooms within the sea ice matrix itself, and therefore represents a proxy measure of late spring/summer (permanent) sea ice. In contrast, the frequently used diatom taxa for palaeo sea ice reconstruction (for example, Fragilariopsis curta and F. cylindrus45,46,51) bloom within the open waters of the marginal ice zone52,53, and their sedimentary distribution corresponds to seasonal (winter) sea ice cover.

In previous studies, semi-quantitative interpretations of temporal changes to sea ice conditions have been inferred from the variability of IPSO25 in downcore records in much the same way that distributions of IP25 has been interpreted in Arctic sea ice reconstructions20. However, in contrast to IP25, there have been, as yet, no published reports that calibrate sedimentary IPSO25 concentrations with known sea ice conditions, including seasonal sea ice concentration. Further studies are therefore required to place the interpretations of abundance changes of IPSO25 on a firmer footing. In practice, however, the greater heterogeneity of Antarctic sea ice may limit the feasibility of performing such calibrations, especially for coastal locations, owing to the myriad of ice types that exist, the prevalence of polynyas, and the fluctuations that occur within these, both seasonally and annually. In the meantime, we note substantial (orders of magnitude) abundance changes in IPSO25, even for sediments from proximate locations within each of the AP, the Weddell Sea and Ross Sea. For example, the concentration ranges of IPSO25 are 34–750, 150–1,200, 37–1,100 and 8–1,800 ng g−1 in Marguerite Bay (AP), the NW and SE Weddell Sea, and the Ross Sea, respectively.

We suggest that a number of features other than sea ice concentration and/or duration likely have influence over IPSO25 abundances and consideration of the ecology of B. adeliensis may offer particularly useful insights. For example, unlike the source diatoms of IP25 in Arctic sea ice, which have a generally consistent contribution of ca. 1–5% of the total diatom taxa21, the proportion of B. adeliensis in Antarctic sea ice diatom communities is highly variable, both spatially and temporally, with seasonal shifts in composition also having been observed in previous studies34,36. B. adeliensis represented the major taxon in our sea ice samples from the WAP, but much lower percentages (and absences) have been reported from the same54 and other regions35,36,53, and inter-annual variability is also high. As such, sedimentary IPSO25 may be much more strongly influenced by variations in Antarctic sea ice diatom assemblages than is the case for IP25 in the Arctic.

B. adeliensis is also known to flourish in platelet ice, where diatom communities, in general, can proliferate to yield significantly elevated biomass compared with consolidated ice or other sea ice forms55,56,57. In addition, larger and chain-forming sea ice diatoms such as Porosira pseudodenticulata are known to have higher sinking rates compared with solitary pennate species in the Antarctic58, a phenomenon commonly associated with aggregated sea ice diatoms59. The seemingly effective transfer of B. adeliensis from sea ice to the underlying sediments, despite its general fragility towards dissolution may, therefore, reflect its propensity to form elongated strands and mats within platelet ice that have elevated sinking rates. Abundances of B. adeliensis (and thus IPSO25) may thus potentially provide a sensitive proxy indicator of platelet ice, whose occurrence and concentration is commonly associated with the provision of super-cooled low-density sub-surface water derived from nearby ice shelves55,60,61,62. Certainly, the widespread occurrence of B. adeliensis and IPSO25, with elevated abundances of both for coastal locations, is consistent with ice shelves occupying almost half of the Antarctic coastline and enhanced platelet ice formation within the trajectory of super-cooled surface waters62.

The production of IPSO25 by B. adeliensis is not restricted to platelet ice, however, since both have been observed in samples of bottom ice, including those analysed as part of the current study. In fact, production of IPSO25 in both platelet ice and consolidated bottom ice communities may potentially explain some of the differences in one of the frequently cited characteristics of IPSO25 in Antarctic settings, namely, its relatively enriched 13C content (compared with pelagic organic carbon), a feature found previously for other individual lipids and bulk organic matter derived within sea ice57,63,64,65,66,67. Although the causes of the enrichment of sea ice-derived particulate organic matter are still debated, CO2 limitation represents the general consensus view, which effectively partially reverses the photosynthetic preference for 12C assimilation pertinent to CO2-replete, open water environments, resulting in increased (less negative) δ13C values57,63,64,65,66,67. Indeed, consistent with lower CO2 concentrations in the brine channels of sea ice68, it has been shown that Antarctic sea ice particulate organic matter can become increasingly enriched in 13C with greater distance from the ice/water interface65, and with the seasonal transition from late winter (October) to spring (December), concomitant with increasing biomass63, as CO2 potentially becomes depleted. It has also been demonstrated that interstitial CO2 drawdown has a significant impact on δ13C for particulate organic carbon (POC)66, although the precise relationship between δ13C and CO2 supply/demand is probably complicated by variable (and inconsistent) nutrient exchange67, leading to large ranges in δ13C for sea ice-derived POC57,63,64,65,66,67, with only relatively minor 13C enrichment in some cases57,63,67. In accordance with these previous studies, although some δ13C data for IPSO25 are consistent with significant enrichment of 13C within a relatively enclosed (and potentially CO2-limited) sea ice matrix, with δ13C=−5.7 to −8.5‰ in sea ice12 and ca. −9‰ in Ellis Fjord sediments24, a relatively depleted value (δ13C=−17.8‰) was found for IPSO25 in surface sediment material from Adélie land, East Antarctica12. Massé et al.12 suggested that this might be attributed to the formation of IPSO25 at a time of sea ice melt, when the ice matrix would probably have been more permeable to CO2 and nutrient replenishment. However, given our new findings, we suggest that a more likely explanation for the lighter isotopic composition of IPSO25 in Adélie Land sediment is biosynthesis of this biomarker by B. adeliensis in the relatively open channels of platelet ice, with comparably free supplementation of CO2 from surrounding waters. An alternative suggestion, involving production of IPSO25 in CO2-replete open waters following ice melt seems unlikely given the sensitivity of B. adeliensis towards dissolution in the water column. Consistent with our suggestion, Thomas et al.57 found only a small 13C enrichment in POC in the interstitial waters of platelet ice from the eastern Weddell Sea (highest δ13C=−20.9‰) with a mean δ13C value (−24.0‰) only slightly higher than that for the underlying open water (δ13C=−25.6‰). On the other hand, a relative enrichment in 13C for IPSO25 in sediments from Ellis Fjord24, likely reflects its biosynthesis in the semi-enclosed environment of consolidated bottom ice, which B. adeliensis is known to colonize for this region35. Within our own samples, we note that δ13C values for IPSO25 in selected surface sediments from the WAP, the northern AP and the SE Weddell Sea, were in the range ca. −13.5 to −15‰ (that is, intermediate between typical sea ice and open water values), and thus indicative of a semi-enclosed sea ice host. Interestingly, IPSO25 abundances in these samples were also among the highest across all samples, consistent with the higher biomass generally associated with platelet ice55,56,57.

By further consideration of the environmental sensitivity of B. adeliensis (and thus of IPSO25) towards nearby glacial and ice shelf water inflow, we provide potentially new insights into the impacts of past changes to such processes by re-inspection of some previous palaeo sea ice reconstructions based on IPSO25 (termed diene II in previous reports). For example, we note that enhanced IPSO25 in sediment core JPC24 from Prydz Bay (East Antarctica) between ca. 10.9 and 10.4 cal. kyr BP (Fig. 5d), previously interpreted as reflecting heavier sea ice conditions during the deglaciation at this site, also coincided with an interval where the retreating Amery Ice Shelf was probably in the vicinity of, but not over, the core site10. Interestingly, lower IPSO25 concentrations were observed both before this interval, likely reflecting an ice shelf covering the site, and afterwards, indicative of a more retreated ice shelf edge, as deduced previously, based largely on taxonomic distributions10. Similarly, elevated IPSO25 in a high resolution (sub-decadal) record from the WAP since ca. 1950 AD (core MTC 18A; Fig. 5b), likely reflects enhanced meltwater-induced platelet ice formation during the recent (and abrupt) retreat of ice shelves and glaciers around the WAP69,70, rather than an increase in sea ice per se. Finally, as part of a Holocene palaeoclimate record for the WAP, Etourneau et al.16 interpreted elevated concentrations of IPSO25 in a core from Palmer Deep (core JPC10; Fig. 5e) during the late Holocene (last ca. 3 kyr) as an indication of increased sea ice presence and duration compared with the early and mid-Holocene, stating that glacial ice probably only had a relatively minor influence on IPSO25 abundance. An apparent paradox between increased sea ice and coeval increases to surface temperatures within the same record, and enhanced glacial ice melt derived from a nearby core site (core ODP1098; Fig. 5f)70, was reconciled by proposition of a late Holocene transition towards colder winter/spring seasons and warmer summers. On the other hand, Pike71 questioned the possible influence of other ice sources on the production and distribution of biomarkers such as IPSO25, and we believe that the new data help resolve this. Thus, we suggest that, enhanced IPSO25, observed especially after ca. 3 kyr in Palmer Deep (JPC10; Fig. 5e)16, likely reflects the positive influence of increasing meltwater discharge from neighbouring ice shelves and glaciers (ODP1098; Fig. 5f)70, on platelet sea ice formation, with further (slightly) elevated concentrations of IPSO25 in the earliest part of the JPC10 record (ca. 8–9 kyr BP; Fig. 5e), and also in core JPC38 from the northeastern AP14 (Fig. 5c), coincident with enhanced glacier discharge or accelerated glacier/iceberg melt during the final stages of the deglaciation70,72.

Figure 5: IPSO25 in downcore records.
figure 5

(a) Summary map showing the locations and core names where IPSO25 (diene II) has been reported in previous studies (note: location (f) is a meltwater record only). (be): Abundances of IPSO25 in previously published downcore records covering different timescales. The relationship between enhanced IPSO25 and increased meltwater inflow from nearby ice shelves and glaciers is highlighted in each case with a shaded blue box. (b) WAP13; (c) northeastern AP14; (d) Prydz Bay, East Antarctica10; (e) Palmer Deep (WAP)16. (f) Meltwater record from core ODP1098 (ref. 70), which is at the same site as JPC10. The smoothed lines in e and f were created using a sixth-order polynomial function.

Finally, although most of the previous Antarctic studies incorporating IPSO25 data have been conducted on near-coastal environments10,11,13,14,16,17,18, exceptionally, Collins et al.15 investigated the broader potential of this biomarker for palaeo sea ice reconstruction by determining its distribution in glacial age sediments from three sites in the northern, central and southern sectors of the Scotia Sea, all of which are located further north of the boundary between IPSO25 presence/absence in modern surface sediments (Fig. 3). The occurrence of IPSO25 in sediments from all three core locations, especially during MIS 2 (ca. 12–24 cal. kyr BP), during which time, sea ice diatom indicator species (that is, F. curta and F. cylindrus) were also relatively abundant, either suggests that a different source may be responsible for IPSO25 biosynthesis in such settings, or that B. adeliensis is also able to colonize sea ice for non-coastal marine settings, especially for those under the influence of nearby glacial meltwater.

In conclusion, the identification of the organic geochemical biomarker IPSO25 in the Antarctic sea ice diatom B. adeliensis likely ensures that future interpretations of the sedimentary occurrence of this sea ice proxy can be made with greater confidence and in more detail. Thus, in addition to representing a qualitative measure of the past occurrence of Antarctic landfast ice during late spring/summer, our findings indicate that variability in sedimentary IPSO25 potentially provides further insights into changes to ice shelf and glacial melt processes in long-term records. Further, the determination of the stable isotopic composition (δ13C) may also be particularly enlightening for determining the structural characteristics of the sea ice from which IPSO25 was derived (that is, platelet versus consolidated bottom ice). However, measuring the IPSO25 content in a larger number of sea ice diatoms and in sea ice of different types and from other regions is required before the interpretation of its precise sedimentary signature can be fully deciphered.


Sample description

Two landfast sea ice cores were collected from Ryder Bay, situated close to the British Antarctic Survey Rothera Research Station (Adelaide Island; 67°35'8" S, 68°7'59" W) on 3 December 2014. Bottom sections (ca. 10 cm) of each core were sliced from the main cores and left to melt in the dark at 4 °C. Aliquots of the thawed samples were then filtered (GF/F; 0.7 μm), with the remaining material re-frozen and stored at −20 °C until further use. Surface sediment material from the Antarctic Peninsula, the Bellingshausen Sea, the Amundsen Sea and the Weddell Sea was taken from the upper 0–1 cm of archived box cores, multi-cores and gravity cores held at the British Antarctic Survey, the British Ocean Sediment Core Research Facility (BOSCORF, UK) and the Alfred Wegener Institute for Polar Marine Research (AWI, Germany). Additional sediment samples from the AP and the Ross Sea were collected during several R/V ARAON cruises between 2001 and 2015. All surface sediment material was assumed to represent accumulation during the modern era.

Species identification

The tube-dwelling Berkeleya adeliensis Medlin was identified using scanning electron microscopy (SEM) at the University of Plymouth following the detailed description of Medlin27. Preparation of cells for analysis by SEM was carried out by digestion of organic material (HCl; 30 min; 70 oC) followed by washing of frustules (3 × 4 ml H2O). Cleaned frustules were then dried onto glass and sputter-coated (Cr) prior to observation (JEOL 7001F SEM). Morphometric assessment, including elongated central area, apical and transapical length (36 and 8 μm, respectively), number of parallel striae in 10 μm (50) and asymmetric axial area adopting a distinct urn-shape around the simple helictoglossa, support our identification. Individual diatom cells for isolation were identified using a Nikon TS2000 inverted light microscope ( × 10 and × 40 objectives) in phase contrast and isolated manually using a modified Pasteur pipette21.

Extraction and analysis of lipids

At the University of Plymouth, HBI lipids were extracted from thawed and filtered sea ice samples, picked cells of B. adeliensis and freeze-dried sediments, using previously published methods21,25,73. For sea ice samples, lipids were extracted from freeze-dried filters by saponification (20% KOH; 80 °C; 60 min) and then re-extracted with hexane21. For isolated cells of B. adeliensis, a total hexane extract only was obtained (hexane; 3 × 1 ml, ultrasonication; 3 × 5 min). In each case, the resulting total hexane extract suspensions were filtered through pre-extracted (dichloromethane/methanol) cotton wool to remove cells before being partially dried (N2 stream) and fractionated into non-polar lipids by column chromatography (hexane (3 ml)/SiO2). For sediments, ca. 1 g of freeze-dried sediment material was extracted by sonication (dichloromethane/methanol; 2:1 v/v, 3 × 3 ml) to obtain a total organic extract. Each total organic extract was partially purified to remove polar components, elemental sulphur and saturated non-polar components using silver-ion chromatography73. For all sample types, an internal standard (9-octylheptadec-8-ene; 0.01–0.1 μg) was added prior to extraction, to enable subsequent quantification of HBIs by GC–MS methods. Analysis of partially purified non-polar lipids was carried out using GC–MS73 with identification of IPSO25 achieved by comparison of its retention index and mass spectrum with those obtained from a purified standard23. Quantification of IPSO25 was achieved by integrating individual ion (m/z 348.3) responses in single-ion monitoring mode, and normalizing these to the corresponding peak area of the internal standard and an instrumental response factor derived from a purified standard23. GC–MS-derived masses of IPSO25 were converted to sedimentary concentrations using the mass of sediment extracted, while a cellular concentration of IPSO25 in B. adeliensis was obtained by dividing the normalized GC–MS response obtained from picked cells by the number of cells extracted.

Stable isotope determinations

The stable (carbon) isotopic composition (δ13C) of IPSO25 was determined using gas chromatography–isotope ratio mass spectrometry (GC–IRMS) at Isoprime Ltd, Cheadle Hulme, UK. All GC–IRMS measurements were performed using an IsoPrime100 IRMS with GC5 interface and Agilent 7890B GC installed with an Agilent HP-5MS column (30 m × 0.2 mm internal diameter, film thickness 0.25 μm). All samples were dissolved in hexane (10–150 μl) and injected into splitless mode with the following inlet conditions: 250 °C, purge flow 25 ml min−1, purge time 0.75 min. GC carrier gas (He) flow rate was 1 ml min−1, oven program as follows: 1 min hold at 50 °C, ramp to 310 °C at 10 °C min−1, then 13 min hold. The combustion furnace consisted of a 0.7 mm inner diameter quartz tube packed with CuO pellets, held at 850 °C. GC–IRMS results were calibrated using the certified Indiana alkane standard mix A5 (Indiana University, Bloomington, IN, USA) and all results are thus reported in delta notation (δ13C) relative to VPDB. IPSO25 was identified in GC–IRMS chromatograms by retention time comparison with corresponding GC–MS analyses. IonOS software (Isoprime Ltd) was used to process GC–IRMS data; ‘peak mapping’ functionality was used to systematically designate specific compound identifications across multiple injections for robust data collation. The A5 alkane mix was analysed between every six sample injections in at least duplicate, with calibrations constructed from at least three interspersed measurements of the A5 mix. Reproducibility of individual alkanes was always ≤0.35‰. Root mean standard error (RMSE) of each of the calibrations was usually≤0.25‰, with an overall RMSE for all calibrations combined of ≤0.21‰, reflecting both the reliability of each calibration, and the long-term stability of the system. Samples containing IPSO25 were run in triplicate.

Data presentation

Distributions of IPSO25 concentrations and study locations referred to in the text are displayed in Figs 1 and 3, 4, 5 using Ocean Data View (ODV) software74.

Data availability

The data that support the findings of this study are available from the corresponding author (S.T.B.) and within the article and its Supplementary Information files.

Additional information

How to cite this article: Belt, S. T. et al. Source identification and distribution reveals the potential of the geochemical Antarctic sea ice proxy IPSO25. Nat. Commun. 7:12655 doi: 10.1038/ncomms12655 (2016).