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Temporal controls on silicic acid utilisation along the West Antarctic Peninsula

  • Nature Communications 8, Article number: 14645 (2017)
  • doi:10.1038/ncomms14645
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The impact of climatic change along the Antarctica Peninsula has been widely debated in light of atmospheric/oceanic warming and increases in glacial melt over the past half century. Particular concern exists over the impact of these changes on marine ecosystems, not only on primary producers but also on higher trophic levels. Here we present a record detailing of the historical controls on the biogeochemical cycling of silicic acid [Si(OH)4] on the west Antarctica Peninsula margin, a region in which the modern phytoplankton environment is constrained by seasonal sea ice. We demonstrate that Si(OH)4 cycling through the Holocene alternates between being primarily regulated by sea ice or glacial discharge from the surrounding grounded ice sheet. With further climate-driven change and melting forecast for the twenty-first century, our findings document the potential for biogeochemical cycling and multi-trophic interactions along the peninsula to be increasingly regulated by glacial discharge, altering food-web interactions.


The west Antarctic Peninsula (WAP) is the most northerly part of Antarctica (Fig. 1) and has experienced the greatest increase in surface atmospheric temperature of anywhere in the Southern Hemisphere during the second half of the twentieth century1,2. Although there has been an absence of such warming since the late 1990s3, the region has continued to experience increases in coastal summer sea surface temperature4,5 and glacier retreat6. These changes have had an impact on both the oceanography7 of the regional water column as well as phytoplankton communities and higher trophic levels in the marine ecosystem8,9. Central to this biological response are diatoms, unicellular siliceous algae, which dominate primary productivity along the WAP with peak abundance focused around spring months10. Although diatom productivity is ultimately regulated by light availability, blooms are sustained by intrusions of nutrient rich Upper Circumpolar Deep Water (UCDW) onto the shelf that are mixed into the surface layer via a number of processes, the most significant of which includes brine-induced destabilization of the winter water column following seasonal sea-ice growth10,11,12.

Figure 1: Location of ODP site 1098 at Palmer Deep off the West Antarctic Peninsula.
Figure 1

Coloured surface waters indicate silicate concentrations from the World Ocean Atlas 2013 ( Map created using Ocean Data View (

Silicon, in the form of silicic acid [Si(OH)4], represents a key nutrient for diatom growth/uptake13. During the biomineralization of silicic acid into particulate hydrous silica, lighter 28Si is preferentially incorporated into the frustule over the heavier 29Si and 30Si with an enrichment factor (ɛ) in marine systems of −1.1‰ to −1.2‰ that is independent of temperature, pCO2(aq), iron availability and other vital effects14,15,16,17. With the progressive uptake of Si(OH)4 increasing δ30Si (30Si/28Si) in both the dissolved and particulate phases, records of diatom silicon isotopes (δ30Sidiatom) can be used to examine temporal/spatial changes in photic zone Si(OH)4 utilization, controlled by the biological demand/uptake of Si(OH)4 and the rate at which nutrients are supplied to the photic zone18,19,20.

Using the silicon isotope composition of diatom frustules (δ30Sidiatom) in a region that is not iron limited21,22, we document the long-term controls on photic zone Si(OH)4 utilization along the WAP from 12.6 to 0.2 kyr, to assess whether future cycling may be dominated by processes other than sea ice. For example, studies have advocated a role for glacial discharge, wind and solar irradiance in regulating macro-nutrient availability in Antarctic surface waters along the WAP8,23,24. In contrast to the modern day, we demonstrate that rates of Si(OH)4 utilization are not closely aligned to changes in sea ice, except from 12.6 to 9.1 kyr and 5.3 to 2.6 kyr. In particular, we show that changes in biogeochemical cycles are highly related to glacial discharge into the photic zone over the last 5.4 kyr, indicating the capability for the system to be driven by different processes as the climate system evolves.


Species composition

Diatoms were extracted from sediments deposited between 12.6 and 0.2 kyr at Palmer Deep, WAP (ODP Site 1098A, 64°51.72′ S, 64°12.47′ W; Fig. 1)25 and analysed for δ30Si using a fluorination procedure26. Bulk species samples analysed in this study, dominated by Hyalochaete chaetoceros spp resting spores (average relative abundance=c. 60%), primarily represent the spring bloom with populations continuing into the summer months27. Although H. chaetoceros resting spores in their vegetative form are associated with sea ice, they bloom and grow rapidly in well-stratified sea-ice melt water adjacent to the melting ice edge28. Although evidence from cultures has pointed towards inter-specific variation in the fractionation factor (ɛ) for δ30Si29, questions remain over the extent to which this can be extrapolated to the natural environment20 with, for example, no evidence of a variable ɛ in a core-top study from the Southern Ocean and Antarctic Peninsula19. Although no investigation into ɛ has been carried out along the surface waters of the WAP, the nearest study to date on a transect from across the Atlantic and Indian sectors of the Southern Ocean south of the Antarctic Circumpolar Current reveals a tightly constrained fractionation factor of −1.2±0.1‰ (ref. 30).

Of relevance to this study are diatoms reproducing in sea-ice brine channels, which have a heavier isotopic composition due to their growth in semi-closed systems31 and so have the potential to distort sediment records of δ30Sidiatom. An important distinction, however, is needed between cryophilic diatoms that predominantly live within or attached to sea-ice and diatoms, which are associated with the sea-ice environment but are not obligate to within or attached to sea ice. Cryophilic diatoms (such as Amphiprora kjellmanii, Nitzschia stellata, Nitzschia lecointei, Pinnularia quadratarea, Pleurosigma sp. and Berkleya sp.) are thinly silicified and are rarely preserved in the sediment record, instead being dissolved within the water column or surface sediments. Within samples analysed here, cryophilic diatoms constitute on average c. 0.6% of the relative abundance of taxa (max=c. 2%) with the remainder not being cryophilic taxa.

Fragilariopsis curta and Fragilariopsis cylindrus are often called sea-ice diatoms, because they are intimately related to the sea-ice environment and may be found within sea ice32, so it is apposite to consider these taxa here (average relative abundance=c. 10%). Observations suggest that valves within sea ice are thin33 and, as such, have low preservation potential. In Antarctic waters, F. curta and F. cylindrus have been observed as being more prominent in assemblages in open water rather than in ice-covered water34,35,36 and, in a series of sediment traps in the Weddell Sea, highest fluxes were found to be associated with ice-free summer phytoplankton blooms following the seasonal retreat of sea ice32. As such, sea-ice signals transferred to the sea floor are produced during summer from F. curta and F. cylindrus blooms that have been seeded from sea ice to the open water32, hence have been growing and reproducing outside of the sea ice environment. Further, studies have also shown that F. cylindrus has very high growth rates (0.7 doublings per day) in the marginal ice zone adjacent to the melting sea-ice edge28,37. In summary, the bulk of the fossil diatom record analysed in this study for δ30Sidiatom comprises silica that was synthesized in spring waters of the marginal ice zone adjacent to the melting sea ice edge with blooms continuing into the summer months27. Accounting for the potentially higher δ30Sidiatom value of cryophilic diatoms (mean=c. 0.6%; max=c. 2%) with a simple mass-balance model has a negligible impact (within analytical error) on our δ30Sidiatom data. Our record therefore providing a unique opportunity to examine the factors regulating Holocene nutrient dynamics along the WAP and an indication of how twenty-first century atmospheric/ocean warming and ice-sheet melt might drive further changes in the system.

Temporal changes in silicon cycling

At the end of the last glacial through the early Holocene (12.6–8.1 kyr), measurements of δ30Sidiatom are remarkably constant at +0.63 to +0.82‰, with the exception of a notable decrease and increase in δ30Sidiatom at 10.7 and 9.0 kyr, respectively (Fig. 2 and Supplementary Table 1). Following 9.0 kyr, δ30Sidiatom ranges from +1.03 to +0.24‰ with a long-term decline in values from c. +0.9‰ to c. +0.4‰ (P<0.001). Results from the only other δ30Sidiatom record along the coastal Antarctic margin at Adélie Land (East Antarctica)38 show little similarity to those from the WAP, reflecting differences in source waters, prevailing atmospheric/oceanic conditions and the habitat of diatom taxa (see Supplementary Discussion and Supplementary Fig. 1).

Figure 2: Palaeoceanographic records from ODP Site 1098.
Figure 2

Records of δ30Sidiatom (this study) plotted alongside F. curta (sea-ice-associated taxa)40, clay/silt ratios from Southern Chile with higher ratios reflecting stronger Southern Hemisphere Westerly Winds43 and δ18Odiatom (glacial discharge)27 alongside TSI for 9.4–0.0 kyr (green line)44 and Greenland GISP2 ice-core 10Be for 12.1–9.4 kyr (dark orange line)45. Bottom panel displays changes in Si(OH)4 utilization under an open system model. Starred Si(OH)4 utilization data points were removed from any ordination analyses (n=6) (see Methods). Shaded/unshaded intervals indicate transitions between zones/subzones as identified by the hierarchical clustering of samples.

Under an ocean open system model marked by continuous supply of silicic acid to the photic zone, records of δ30Sidiatom can be used to calculate temporal changes in the utilization of Si(OH)4 along the WAP (Fig. 2). Rates of Si(OH)4 utilization follow δ30Sidiatom with both displaying notable variability after c. 7.1 kyr (Fig. 2), highlighting the potential for nutrient consumption to alter rapidly on centennial/sub-centennial timescales. Hierarchical cluster analysis of the Si(OH)4 utilization data revealed two significant zones (Zone 1: 5.3–0.2 kyr; Zone 2: 12.6–5.6 kyr) (Fig. 3). Whereas rates of Si(OH)4 utilization are close to 50% in the early/mid Holocene period (Zone 2 Si(OH)4 utilization: x=48.3%, interquartile range=40.3–56.0%) rates are significantly lower (P<0.001) in the late Holocene/neoglacial (Zone 1 Si(OH)4 utilization: x=34.2%, interquartile range=17.5–40.9%).

Figure 3: Numerical zonation of the δ30Sidiatom data at ODP Site 1098A.
Figure 3

Zone 1 and Zone 2 are statistically significant under a Broken-Stick model.

Early Holocene controls on Si(OH)4 utilization

For the modern day39 sea-ice melt plays a key role in regulating spring photic zone productivity and biomineralization by altering water column stability, mixed layer depth, light availability and the suspension of diatoms in the photic zone. However, other mechanisms may have dominated in the past, for example, increases in glacial discharge may have increased the transportation of nutrients, as glacial flour, to the photic zone lowering rates of nutrient usage23. Similarly, changes in wind intensity, in particular the southward migration of Southern Hemisphere Westerly Winds (SWWs), can increase the upwelling of UCDW onto the shelf.

To provide further insights into the controls on Holocene Si(OH)4 cycling, significant zones and primary subzones were explored using principal components analysis, to highlight dominant patterns and the inter-relationships between variables (Table 1). Rates of Si(OH)4 utilization were examined alongside: (1) changes in seasonal sea-ice abundance, based on the relative abundance of F. curta at the same site40, which is closely associated with pack/fast-ice and commonly found near the sea-ice edge34,41 with higher abundances, indicating a reduced growing season due to a denser sea ice cover42; (2) glacial discharge from the continental ice sheet, as indicated by the oxygen isotope composition of diatom silica (δ18Odiatom) measured on the same samples as those analysed here for δ30Sidiatom (ref. 27); (3) changes in the position and intensity of SWWs using clay/silt ratios from the Skyring fjord system of Chile43; and (4) measurements of solar irradiance from a combined total solar irradiance (TSI) record for 9.4–0.0 kyr BP (ref. 44) and from the Greenland GISP2 ice-core 10Be record for 12.1–9.4 kyr BP (ref. 45). TSI has been widely used to constrain how changes in solar activity drive decadal–centennial scale environmental changes through the Holocene46,47 and is employed here to understand how solar activity may regulate biogeochemical cycling over multi-centennial timescales.

Table 1: Matrix documenting how different environmental variables and processes may potentially increase or decrease rates of Si(OH)4 utilization over the analysed interval at ODP Site 1098A.

Previous work from the last deglaciation has advocated a key role for sea-ice in regulating biological processes in the region through the stabilization of the water column during seasonal melting of sea ice48,49. Our work advances this by showing that although no single process dominates, sea ice (as indicated by the abundance of sea-ice-associated F. curta) is strongly associated with biogeochemical cycling into the early Holocene (subzone 2b: 12.6–9.1 kyr) with enhanced water column stability during spring sea-ice melt retaining diatoms in the photic zone and increasing rates of Si(OH)4 consumption (Figs 4 and 5a). This link between sea ice and Si(OH)4 utilization disappears after 9.1 kyr and into subzone 2a (8.9–5.6 kyr) with rates of Si(OH)4 utilization instead becoming closely related to TSI44 (adjusted R2=0.91, P<0.01, n=5; Fig. 4); Si(OH)4 and TSI did not display an association before this interval.

Figure 4: Principal component analysis biplots of the Si(OH)4 utilization-defined sub-zones.
Figure 4

Aligned vectors indicate a strong positive correlation between the two variables. Vectors at right angles/opposites indicate no correlation/negative correlation, respectively. Eigenvalues for each axis indicate the variance in the data explained by each axis. SWW, Southern Hemisphere Westerly Winds; TSI, total solar irradiance; %Si(OH)4, percent Si(OH)4 utilization.

Figure 5: Conceptual model of the processes controlling photic zone Si(OH)4 utilization along the WAP.
Figure 5

(a) 12.6–9.1 kyr: sea-ice melt enhances water column stability and enables diatoms to remain in the photic zone for longer, increasing rates of Si(OH)4 consumption. (b) 5.3–2.6 kyr: water column stability continues to be supported by sea-ice melt. At the same time glacial discharge from the Antarctic ice-sheet regulates the supply of UCDW nutrients to the photic zone through brine-induced destabilisation of the winter water column. (c) 2.4–0.2 kyr: glacial discharge from the Antarctic ice-sheet continues to regulate the supply of UCDW-derived nutrients to the photic zone. Dark and light blue indicate UCDW and AASW, respectively, with pale white colour in surface waters reflecting freshwater inputs from sea-ice (a,b) and glacial discharge (b,c).

A link between diatom productivity and solar variability has been proposed for the late Holocene WAP48; however, the mechanisms behind this remain unknown. Although increased TSI can enhance summer stratification of the water column via warming of the surface layer24,39, leading to increased productivity, the negative correlation between Si(OH)4 utilization and TSI observed here requires an alternative set of interactions. With no comparable analogue in the modern day, we are unable to propose a definitive process that links TSI and nutrient utilization during this interval characterized by reduced glacial discharge following the earlier collapse of the George VI Ice Shelf at 9.6 kyr (ref. 27) and sea ice (F. curta) unchanged from before 9.1 kyr.

Mid/Late Holocene controls on Si(OH)4 utilization

The Mid/Late Holocene, encompassing the shift from non-cyclic to cyclic internal forcing of the Antarctic climate system and the neoglacial period27,50, is characterized by a switch away from an association between TSI and rates of Si(OH)4 utilization. Instead, in subzone 1b (5.3–2.6 kyr), a strong positive correlation emerges between Si(OH)4 utilization and both glacial discharge and sea ice (Fig. 4). This switch, advocating a return to sea-ice-driven stabilization of the spring water column in regulating biogeochemical cycling (Fig. 5b), coincides with evidence of reduced winter mixing and UCDW in surface waters at nearby Marguerite Bay51, a process that would lower nutrient concentrations and cause rates of Si(OH)4 utilization to become more sensitive to inter-annual variations in the strength of spring sea-ice-driven stratification when peak diatom production occurs. The simultaneous emergence of an association between Si(OH)4 utilization and glacial discharge coincides with increases in glacial discharge at the start of the neoglacial related to a strengthened El Niño–Southern Oscillation and enhanced La Niña activity27. Rather than glacial discharge regulating water column stability, higher values of δ18Odiatom (less glacial discharge) are linked to increased Si(OH)4 consumption and vice versa (Fig. 4, Table 1).

Glacial discharge can transport glacially derived nutrients to the photic zone along the WAP23,52, potentially regulating biogeochemical cycling through this interval alongside sea ice. Although there are few direct measurements of macro-nutrients in Antarctic glacial discharge, records from both Greenland and elsewhere demonstrate the abundance of nutrients including iron in glacial melt53,54. Changes in the supply of glacially derived iron are unlikely to induce iron limitation/alter nutrient utilisation along the WAP due to the deep water replenishment of photic zone iron concentrations via winter mixing52. Similarly, elevated levels of dissolved silica in meltwater from the Greenland ice-sheet are only observable in fjords and in waters immediately proximal to the ice-sheet with Si(OH)4 rapidly mixed and diluted with marine waters beyond the mouth of individual fjords55. Although no comparable data exists for Antarctica, results from northern Marguerite Bay along the WAP indicate that the majority of dissolved silica in the photic zone is supplied from upwelled deep waters56. On this evidence, we argue that the link between glacial discharge and biogeochemical cycling through subzone 1b (5.3–2.6 kyr) is not related to the supply of glacially derived nutrients. Instead, we highlight work demonstrating that increased glacial discharge increases subsequent austral autumn and winter sea-ice formation57, a process that would increase UCDW flow on the shelf through brine-induced destabilization of the winter water column10,11,12 and lower nutrient utilization in the following spring bloom. Using this, we argue that periods of high (low) Si(OH)4 utilization in subzone 1b (5.3–2.6 kyr) are associated with increased (reduced) sea-ice-driven water column stability in spring months and reduced (increased) glacial discharge, which reduces (increases) the flow of nutrient-rich UCDW onto the shelf in winter months (Fig. 5b).

In subzone 1a (2.4–0.2 kyr), the association between sea ice and Si(OH)4 utilization significantly weakens (Fig. 4), a transition that may be related to increased wind strength over the last two millennia40, which would have limited sea-ice-driven stratification of the water column and lowered diatom concentrations58,59 (Fig. 2). Instead, in contrast to the modern day, nutrient dynamics over this interval become predominantly associated solely with changes in glacial discharge (Fig. 4) with increased (reduced) Si(OH)4 consumption strongly associated with reduced (increased) glacial discharge. Similar to subzone 1b (5.3–2.6 kyr), a link between rates of Si(OH)4 utilization and the transportation of glacially derived nutrients to ODP Site 1098 is ruled out due to the distance from the grounded ice sheets. Although Si(OH)4 utilization through this period is therefore most likely to be controlled by the aforementioned process in which glacial discharge increases austral autumn/winter sea ice57 and the flow of nutrient-rich UCDW onto the shelf (Fig. 5c), this argument is seemingly weakened by the absence of a link between sea ice and either glacial discharge or Si(OH)4 utilization in the ordination results (Fig. 4). However, we argue that the absence of any link to sea ice is an artefact driven by the reduction in spring sea-ice-driven stratification over the last two millennia and does not reflect the combined glacial-discharge/sea-ice/UCDW mechanism proposed here in which nutrient flow onto the shelf is aided by brine-induced destabilisation of the winter water column.

Future implications

Modern day studies have advocated the role of sea ice in regulating intra-annual to decadal variations in phytoplankton biomass and community structure along the WAP, compounded by changes in cloud cover, wind-driven mixing and glacial melt8,23,24,39,60. Our work extends this to demonstrate that the dominant control on biogeochemical cycling varies over time with Si(OH)4 utilization strongly associated to sea ice, glacial discharge and solar forcing at different intervals through the Holocene. Of particular note is evidence that with the exception of the modern day, changes in rates of Si(OH)4 utilization and sea ice are only concordant from 12.6 to 9.1 kyr and 5.3 to 2.6 kyr. With projections indicating further warming and glacial discharge61 during the twenty-first century, our results suggest that Si(OH)4 utilization may again become increasingly regulated by glacial discharge and the associated transport of UCDW-derived nutrients to the photic zone.

With primary production along the coastal margin dominated by siliceous organisms, any change in nutrient dynamics has the potential to alter the ecosystem structure and food web interactions. For example, recent reductions in the marginal sea-ice zone in the northern subregion of the WAP have reduced both phytoplankton cell size/net productivity and altered the algal community through relative reductions in the abundance of diatoms, having an impact on both zooplankton and higher trophic levels8,9. Increased regulation of biogeochemical cycling through glacial discharge and associated water column stratification may compensate for this by increasing diatom populations and photic zone Si(OH)4 supply, but will not offset ecosystem changes linked to warmer sea surface temperature or loss of sea-ice habitats8,9. In addition, further inputs of glacial discharge are likely to exacerbate declines in krill populations linked to lithogenic particles in the water column62.

Increased transportation of UCDW-derived nutrients to the photic zone and associated reductions in Si(OH)4 utilization will also modify the export of organic carbon both along the WAP8 and in the open ocean. At locations in the Southern Ocean with negligible sea-ice cover, the availability of Si(OH)4 regulates opal export and so ocean-atmospheric exchanges of CO2 (ref. 63). Although we do not comment on whether our findings advocate a role for the biological pump in regulating Holocene pCO2 changes, our records show that rates of silicic acid utilization have reduced through the neoglacial and have the potential to do so again with future increases in glacial discharge. Such changes, if replicated at other coastal sites around West Antarctica and the WAP, would suggest the creation of a pool of under-utilized silicic acid that could alter the local biological carbon pump and stimulate further changes in the open ocean away from the continental margin20.


Age model

The age model for ODP Site 1098 follows that published in Pike et al.27 in which previously published down core magnetic susceptibility records25 and lamina-to-lamina correlations were used to re-evaluate the metres composite depth (mcd) scale for the A and C holes. These were then used against the published particulate organic carbon acccelerator mass spectrometry (AMS) radiocarbon ages for ODP Site 1098 (ref. 64) that were re-calibrated to calendar years using Calib 6.0.2, the Marine09 calibration curve and a 1,230 year reservoir correction.

Diatom extraction

Diatoms were extracted and cleaned for isotope analysis using techniques modified for use on coastal Antarctic diatoms65 with sub-samples previously analysed for δ18Odiatom (ref. 27). Samples were placed in c. 1 ml of 30% H2O2 at room temperature for 4 h to disaggregate before being centrifuged in sodium polytungstate three times with progressively lower specific gravities: 2.25, 2.20 and 2.10 g ml−1 at 2,500 r.p.m. Extracted material was re-immersed in H2O2 at 75 °C to remove all organic material adhering to the diatom frustules and left overnight in 5% HCl to dissolve any remaining carbonates.

All samples were checked for purity using scanning electron microscope and × 1,000 magnification light microscopy with these visual analyses, confirming that frustules are exceptionally well preserved and have not been subject to dissolution or other processes that may alter their isotopic composition (Fig. 6). Although we cannot conclusively rule out that dissolution may have affected micro-features on individual frustules, results from sediment traps in Lake Baikal (Russia) demonstrate that such dissolution does not alter δ30Sidiatom (ref. 66). With Lake Baikal experiencing depths of >1,500 m and rates of diatom preservation similar to marine systems (c. 1% of diatoms in Lake Baikal become incorporated into the sediment record67), we extend these results to δ30Sidiatom measurements at ODP Site 1098A. Analyses of core-tops in the Southern Ocean have also found little to no effect of dissolution on δ30Sidiatom (ref. 19).

Figure 6: Diatom isotope sample at 10.49 kyr.
Figure 6

Scanning electron microscope image of the analysed diatom isotope sample at 10.49 kyr (35.45 mcd), showing the excellent preservation and lack of contamination.

δ30Sidiatom analyses were conducted using a fluorination technique26 verified through an inter-laboratory calibration exercise68. Samples were loaded into nickel reaction vessels and outgassed for 2 h at 250 °C to remove superficial water before reaction with BrF5 for 6 min at 250 °C to remove all –OH bonds. Silicon from the -Si-O-Si layer were then dissociated overnight using an excess of reagent at 550 °C and collected as SiF4. Yield measurements for δ30Sidiatom indicated 100% collection of all silicon. Isotope measurements were made on a Finnigan MAT 253 with values were converted to the NBS28 scale using the NIGL within-run laboratory diatom standard (BFCmod) calibrated against NBS28. Replicate analyses of sample material indicate a mean analytical reproducibility (1σ) of 0.03‰ (range=0.00–0.07‰, n=7).

Si(OH)4 utilization

Using an ocean open system model marked by continuous supply of silicic acid to the photic zone, records of δ30Sidiatom can be expressed as a function of the isotope composition of dissolved silicic acid [δ30Si(OH)4] supplied to the photic zone, the fraction of Si(OH)4 remaining in the water (f) and the enrichment factor between diatoms and dissolved silicic acid (ɛ):

The use of an open model along the WAP is based upon evidence that a closed system model is not appropriate for most oceanic regions30, including the Southern Ocean69. For the region close to the WAP in the Southern Ocean values of δ30Si(OH)4 and ɛ have been constrained at +1.4‰ and −1.2‰, respectively30, allowing the calculation of photic zone Si(OH)4 utilization along the WAP:

Owing to an absence of glacial melt samples/end members, we are unable to account for inputs of glacially derived silicic acid, although contribution of such sources are argued to be minimal at ODP Site 1098 relative to inputs from UCDW due to the distance from the grounded ice sheets.

Statistical analyses

To investigate long-term temporal changes in silicon cycling, stratigraphical zones in the Si(OH)4 utilization data set were identified using a hierarchical clustering of a square root-transformed euclidean distance matrix using a Constrained Incremental Sum of Squares agglomeration method70 using the rioja package within R71,72. The significance of individual zones was checked using a Broken-Stick model73, which assesses whether the amount of variation is greater than that expected for a model with the same number of segments where Pr is the expected proportion of variance for the kth zone out of n zones:

All ordinations were conducted using the ‘stats’ and ‘vegan’ packages in R71,74. Diatom counts at ODP Site 1098 were conducted on Core 1098B40 with dates recalculated based on the age model used in this paper. Linear interpolation of the F. curta, SWW and solar irradiance data was then used to obtain values that are comparable to the δ30Sidiatom sample depth/ages. To limit errors, depths where the age difference between the δ30Sidiatom and F. curta/solar irradiance data was >50 years were removed from any ordination analyses (n=6). Although the resolution of the clay/silt SWW data required interpolations between samples with greater age differences, the ordinations and subsequent interpretations in this manuscript are similar whether or not the SWW clay/silt ratio data is included. Detrended correspondence analysis with down-weighting was used to determine whether the data exhibited a linear or unimodal response to the latent variables. All zones and subzones produced a first axis gradient length of <1.5, indicating a linear response, and were further explored using principal components analysis with scaling for all variables.

Data availability

All δ30Sidiatom and Si(OH)4 utilization data from this manuscript are provided in Supplementary Table 1.

Additional information

How to cite this article: Swann, G. E. A. et al. Temporal controls on silicic acid utilisation along the West Antarctic Peninsula. Nat. Commun. 8, 14645 doi: 10.1038/ncomms14645 (2017).

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This work was supported by the Natural Environment Research Council (grant numbers IP-1234-0511, NE/G004137/1, NE/G004811/1). We thank the staff at the IODP Gulf Coast Core Repository for providing samples and assistance with sampling ODP Site 1098, and three anonymous reviewers who provided valuable and constructive comments on the manuscript. This research was supported by a NERC Isotope Geosciences Facilities Steering Committee (NIGFSC) grant (IP-1234-0511) in addition to Natural Environment Research Council (NERC) grants NE/G004137/1 to M.J.L. and G.E.A.S., and NE/G004811/1 to J.P.

Author information


  1. Centre for Environmental Geochemistry, School of Geography, University of Nottingham, University Park, Nottingham NG7 2RD, UK

    • George E. A. Swann
    •  & Melanie J. Leng
  2. Centre for Environmental Geochemistry, British Geological Survey, Nottingham NG12 5GG, UK

    • George E. A. Swann
    • , Melanie J. Leng
    •  & Hilary J. Sloane
  3. School of Earth and Ocean Sciences, Cardiff University, Main Building, Park Place, Cardiff CF10 3AT, UK

    • Jennifer Pike
  4. NERC Isotope Geosciences Facilities, British Geological Survey, Keyworth, Nottingham NG12 5GG, UK

    • Melanie J. Leng
    • , Hilary J. Sloane
    •  & Andrea M. Snelling


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G.E.A.S., J.P. and M.J.L. conceived the project. H.J.S. and A.M.S. performed the δ30Sidiatom analyses. All authors contributed to interpretations and commented on the manuscript.

Competing interests

The authors declare no competing financial interests.

Corresponding author

Correspondence to George E. A. Swann.

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