# Sourcing the iron in the naturally fertilised bloom around the Kerguelen Plateau: particulate trace metal dynamics

P. van Der Merwe, A. R. Bowie, F. Quéroué, L. Armand, S. Blain, Fanny Chever, D. Davies, F. Dehairs, Frédéric Planchon, Géraldine Sarthou, et al.

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## To cite this version:

P. van Der Merwe, A. R. Bowie, F. Quéroué, L. Armand, S. Blain, et al., Sourcing the iron in the naturally fertilised bloom around the Kerguelen Plateau: particulate trace metal dynamics. Biogeo-sciences, 2015, 12 (3), pp.739-755. 10.5194/bg-12-739-2015. hal-01207931

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# Sourcing the iron in the naturally fertilised bloom around the Kerguelen Plateau: particulate trace metal dynamics

P. van der Merwe<fnref n="1" />, A. R. Bowie<fnref n="1" />,<fnref n="2" />, F. Quéroué<fnref n="1" />,<fnref n="2" />,<fnref n="3" />, L. Armand<fnref n="4" />, S. Blain<fnref n="5" />,<fnref n="6" />, F. Chever<fnref n="3" />,<fnref n="7" />, D. Davies<fnref n="1" />, F. Dehairs<fnref n="8" />, F. Planchon<fnref n="3" />, G. Sarthou<fnref n="9" />, A. T. Townsend<fnref n="10" />, and T. W. Trull<fnref n="1" />,<fnref n="11" />

*Correspondence to:* P. van der Merwe (pvander@utas.edu.au)

Received: 26 August 2014 – Published in Biogeosciences Discuss.: 18 September 2014

Revised: 15 December 2014 – Accepted: 8 January 2015 – Published: 6 February 2015

**Abstract.** The KEOPS2 project aims to elucidate the role of natural Fe fertilisation on biogeochemical cycles and ecosystem functioning, including quantifying the sources and processes by which iron is delivered in the vicinity of the Kerguelen Archipelago, Southern Ocean. The KEOPS2 process study used an upstream high-nutrient, low-chlorophyll (HNLC), deep water (2500 m), reference station to compare with a shallow (500 m), strongly fertilised plateau station and continued the observations to a downstream, bathymetrically trapped recirculation of the Polar Front where eddies commonly form and persist for hundreds of kilometres into the Southern Ocean. Over the Kerguelen Plateau, mean particulate (1–53 µm) Fe and Al concentrations (pFe = 13.4 nM, pAl = 25.2 nM) were more than 20-fold higher than at an offshore (lower-productivity) reference station (pFe = 0.53 nM, pAl = 0.83 nM). In comparison, over the plateau dissolved

Fe levels were only elevated by a factor of ~2. Over the Kerguelen Plateau, ratios of pMn / pAl and pFe / pAl resemble basalt, likely originating from glacial/fluvial inputs into shallow coastal waters. In downstream, offshore deep-waters, higher pFe / pAl, and pMn / pAl ratios were observed, suggesting loss of lithogenic material accompanied by retention of pFe and pMn. Biological uptake of dissolved Fe and Mn and conversion into the biogenic particulate fraction or aggregation of particulate metals onto bioaggregates also increased these ratios further in surface waters as the bloom developed within the recirculation structure. While resuspension of shelf sediments is likely to be one of the important mechanisms of Fe fertilisation over the plateau, fluvial and glacial sources appear to be important to areas downstream of the island. Vertical profiles within an offshore recirculation feature associated with the Polar Front show pFe

<footnote n="1">¹Antarctic Climate and Ecosystems CRC, University of Tasmania, TAS 7004, Australia</footnote>

<footnote n="2">²Institute for Marine and Antarctic Studies, University of Tasmania, Battery Point, TAS 7004, Australia</footnote>

<footnote n="3">³Laboratoire des Sciences de l'Environnement Marin (LEMAR), Université de Bretagne Occidentale, CNRS, IRD, UMR6539, IUEM, Technopole Brest Iroise, Place Nicolas Copernic, 29280 Plouzané, France</footnote>

<footnote n="4">⁴Department of Biological Sciences and Climate Futures, Macquarie University, North Ryde, NSW 2109, Australia</footnote>

<footnote n="5">⁵Sorbonne Universités, UPMC Univ Paris 06, UMR7621, Laboratoire d'Océanographie Microbienne, Observatoire Océanologique, 66650 Banyuls/mer, France</footnote>

<footnote n="6">⁶CNRS, UMR7621, Laboratoire d'Océanographie Microbienne, Observatoire Océanologique, 66650 Banyuls/mer, France</footnote>

<footnote n="7">⁷IFREMER/Centre de Brest, Département REM/EEP/Laboratoire Environnement Profond, CS 10070, 29280 Plouzané, France</footnote>

<footnote n="8">⁸Vrije Universiteit Brussel, Analytical, Environmental and Geo-Chemistry & Earth System Sciences research group, Brussels, Belgium</footnote>

<footnote n="9">⁹CNRS, Université de Brest, IRD, Ifremer, UMR6539 LEMAR, IUEM ; Technopôle Brest Iroise, Place Nicolas Copernic, 29280 Plouzané, France</footnote>

<footnote n="10">¹⁰Central Science Laboratory, University of Tasmania, Sandy Bay, TAS 7005, Australia</footnote>

<footnote n="11">¹¹Commonwealth Scientific and Industrial Research Organisation, Oceans and Climate Flagship, GPO Box 1538, Hobart, Tasmania, Australia</footnote>
and pMn levels that were 6-fold and 3.5-fold lower, respectively, than over the plateau in surface waters, though still 3.6-fold and 1.7-fold higher respectively than the reference station. Within the recirculation feature, strong depletions of pFe and pMn were observed in the remnant winter water (temperature-minimum) layer near 175 m, with higher values above and below this depth. The correspondence between the pFe minima and the winter water temperature minima implies a seasonal cycle is involved in the supply of pFe into the fertilised region. This observed association is indicative of reduced supply in winter, which is counterintuitive if sediment resuspension and entrainment within the mixed layer is the primary fertilising mechanism to the downstream recirculation structure. Therefore, we hypothesise that lateral transport of pFe from shallow coastal waters is strong in spring, associated with snow melt and increased runoff due to rainfall, drawdown through summer and reduced supply in winter when snowfall and freezing conditions predominate in the Kerguelen region.

# 1 Introduction

Small scale fertilisation experiments have now clearly established that Southern Ocean primary production is limited by the availability of the micronutrient iron (Fe) (Boyd et al., 2007; de Baar, 2005). This limitation on the biological pump means that the Southern Ocean does not realise its full potential in transferring atmospheric CO₂ into the ocean interior; a result illustrated in Antarctic continental ice records over geological timescales and supported by modelling studies (Barnola et al., 1987; Bopp et al., 2003; Martin, 1990; Watson et al., 2000). Less well understood is the overall system response to the addition of Fe as efficiency estimates (defined here as the amount of carbon exported relative to Fe added above baseline conditions) can vary by an order of magnitude (Blain et al., 2007; Pollard et al., 2009; Savoye et al., 2008). Both the original and subsequent KEOPS missions aimed to resolve not only the efficiency estimate, but also the response of the ecosystem and the overall effect on biogeochemical cycles due to natural Fe fertilisation in the vicinity of the Kerguelen Plateau. The KEOPS natural fertilisation experiment is complementary to artificial Fe enrichment experiments due to the fact that its scale is much larger and its time frame longer than that which is currently feasible in artificial fertilisation experiments. Furthermore, due to the sustained release of Fe into the fertilised region, as opposed to a sudden pulse artificial experiment, the technical challenges of monitoring carbon export are reduced. Furthermore, there is growing evidence that sustained Fe fertilisation favours large, highly silicified, slow growing diatoms that are efficient at exporting carbon into the ocean interior (Quéguiner, 2013). When the results of process studies such as KEOPS are extrapolated over the whole Southern Ocean,

a small change in the efficiency estimate could result in different conclusions as to the efficacy, for instance, of artificial Fe fertilisation as a means of mitigating rising atmospheric concentrations of anthropogenic CO₂.

Dissolved Fe (dFe < 0.2 µm) includes colloidal and nanoparticulate Fe, which may only be partially bioavailable, as well as soluble Fe (sFe < 0.02 µm) which is highly bioavailable (de Baar and de Jong, 2001). As a result, the larger particulate fraction (> 0.2 µm) is often less studied due to the perception that it has low bioavailability. However, the particulate fraction can yield important information for several reasons; firstly the dissolved fraction is constantly in a state of change with uptake, particle scavenging and remineralisation occurring simultaneously and at varying rates depending on many factors including complexation with organic ligands (Johnson et al., 1997) and the biological community present (Sunda, 2001). Thus, interpretation of dFe data is difficult without a rarely obtained perspective on the time varying aspects of the dFe distribution. Secondly, as a fraction of the total Fe, the major sources of Fe into fertilised regions (e.g. weathering products delivered by fluvial and glacial processes, resuspension of sediments and porewaters, atmospheric and extra-terrestrial dust) are small particles (> 0.2 µm), with the concentration being more stable over weeks to months, due to its abundance and relatively slow biological uptake. The particulate fraction is primarily lost from surface waters through sinking, either directly or via adhesion to bioaggregates (Frew et al., 2006). However, there is a constant transfer of dissolved Fe to particulate Fe, either via biological uptake or precipitation and, particulate Fe to dissolved Fe, via dissolution and biologically mediated processes (Moffett, 2001). Thus, the particulate fraction that is small enough to avoid sinking out of the water column rapidly (0.2–5 µm) can be considered as a significant source of dissolved Fe, with the rate of supply into surrounding waters dependent on the dissolution and leaching rate. Furthermore, there is growing evidence that particles in this size fraction are readily produced by mechanical erosion of bedrock due to glacial processes at high latitudes and that this large source may be partially bioavailable (Hawkings et al., 2014; Poulton and Raiswell, 2005; Raiswell et al., 2008a, b, 2006).

The first KEOPS process study was conducted in 2005 and specifically focused on processes affecting the demise of the spring bloom over the Kerguelen Plateau (Blain et al., 2007). Blain et al. (2007) and Chever et al. (2010) demonstrated that dFe fertilisation from the plateau increased primary production in the area. From the data gathered it was proposed that resuspension of plateau-derived sediments and entrainment into the mixed layer during increased wind mixing that deepened the mixed layer, was the primary source of particulate and subsequently, dissolved Fe to the downstream blooms. Resolution of the Fe budget (accounting for all sources and sinks of Fe in the system), from observations made during the first mission, found that the vertical supply of dissolved
<figure><img src="image_4.png" /></figure>

**Figure 1.** SeaWiFS surface chlorophyll on 11 November 2011, approximately half way through the KEOPS2 sampling program. Kerguelen and Heard Island are visible in grey. Stations that were sampled for suspended particles are indicated with black circles. Distinct regimes of interest for the KEOPS2 program are indicated in red.

SeaWiFS files courtesy of CLS (with support from CNES)

Fe was not sufficient to supply phytoplankton demand. Blain et al. (2007) closed the KEOPS Fe budget by assuming that dissolution of a small fraction of the unconstrained particulate Fe pool must occur. The KEOPS2 mission aimed to improve on the successes of the first process study by accounting for the missing Fe in the budget, namely particulate Fe (pFe). Thus, we aim to test the KEOPS1 hypothesis that unconstrained particulate Fe is the missing Fe of the KEOPS Fe budget by documenting the particulate metal enrichment around the Kerguelen Plateau. Our goal is to determine the sources of Fe enrichment within areas of interest (i.e. reference, plateau and the recirculation structure; see Fig. 1). Trace metal analysis of suspended particles, underlying sediment and settling particulate material will elucidate the source to sink progression of the particulate Fe pool. Following on from this work, and together with dissolved Fe measurements (Quéroué et al., 2015), a focused Fe budget will be constructed (Bowie et al., 2014).

# 2 Methods

## 2.1 In situ pumps (ISPs)

All sample handling, processing and preparation was performed in accordance with general GEOTRACES protocols (http://www.geotraces.org/) and specific methodologies outlined in Bowie et al. (2010). Briefly, suspended particles were collected using up to 11 in situ pumps (ISPs) (McLane WTS and Challenger) suspended simultaneously at varying

depths throughout the water column. Depths were chosen after viewing conductivity, temperature and depth (CTD) data to sample within oceanographic features of interest as well as obtaining a representative full water column profile. The ISPs were fitted with 142 mm quartz micro fibre (QMA) (Sartorius) filters with 53 µm Petex pre-filters and 350 µm polyester supports. QMA filters were pre-combusted to remove particulate organic carbon and then acid-washed with Seastar Baseline™ HCl and rinsed with copious amounts of ultra-pure water according to the methods outlined in the GEOTRACES sample handling protocols handbook (Cutter et al., 2010). The pre-filters and supports were carefully acid washed and rinsed with copious amounts of ultra-pure water before use. Both the Petex pre-filter and QMA filter were analysed for every pump giving two size fractions at each sampling location. Therefore, all particles greater than 53 µm were collected on the pre-filter and all particles within the 1–53 µm size range were collected on the underlying QMA filter. Lithogenics sourced from bedrock or sediments in the larger size range (> 53 µm) would have a high sinking velocity (> 500 m day⁻¹) according to Stokes’ law and as such would be expected to make up a relatively small fraction of the total particles in this size range. In comparison, the 1–53 µm size class can potentially capture both small biogenic and lithogenic particles. This is due to the prediction that small lithogenic particles (1–5 µm) have significantly slower sinking rates (0.1–10 m day⁻¹) than large lithogenic particles according to Stokes’ law.

The ISPs were programmed to pump for up to four hours, allowing up to 2000 L of seawater to be filtered. After retrieval, the filters were bagged and processed within an ISO class 5, containerised clean room. Replicate 14 mm punches were taken using an acid-washed polycarbonate punch and stored frozen at -18°C until analysis at the home laboratory. The 14 mm punches were then used for particulate metal analysis, particulate organic carbon and particulate organic nitrogen analysis.

## 2.2 Sediment traps (Technicap PPS3)

For a full description of the sediment trap data during KEOPS2 see Laurenceau et al. (2014) and Bowie et al. (2014). Two Technicap PPS3 free-floating sediment traps were deployed below the mixed layer at a depth of 200 m. The two sediment traps were deployed twice, giving a total of four deployments. The traps were prepared with acid-cleaned sampling cups containing low-trace-metal brine solution (salinity ~ 60). The trap was programmed to sample for 1.5–5.5 days, whilst the 12 individual sampling containers were open for an equal portion of the total deployment. Upon retrieval, the sampling containers were removed from the carousel, sealed and processed within an ISO class 5, containerised clean room. The samples were filtered onto acid-washed, 2 µm polycarbonate membrane filters via a 350 µm pre-filter using a Sartorius™ PTFE filtration unit. The 350 µm
pre-filter was selected to exclude large copepods and other large plankton that would lead to unrealistic sample variability.

## 2.3 Sediment coring

An Oktopus Multicorer (www.oktopus-mari-tech.de) was used to collect 8 replicate, 610 × 95 mm sediment cores, simultaneously within a 1 m² area at each station. The uppermost 5mm of surface sediment was subsampled according to Armand et al. (2008) representing an approximate sedimentation period of < 1000 years.

## 2.4 Analysis

### 2.4.1 ISP filters for particulate metals

All digestions and evaporations were carried out within a digestion hood (SCP Science), where air was HEPA filtered during intake and subsequently extracted through a fume hood. Filter blanks and sample filters were digested in 15 mL acid cleaned, Teflon perfluoroalkoxy (PFA) screw cap vials (Savillex™) using ultra-pure nitric acid (1 mL 16 M HNO₃) (Seastar Baseline™) heated to 120 °C for 12 h on a Teflon coated hotplate (SCP Science DigiPREP™), following the method outlined in Bowie et al. (2010). Blanks containing only HNO₃ were also analysed to determine the contribution of the digestion acid without filter material.

The digest solution was diluted with 9 mL of ultra-high purity water and spiked to a final concentration of 10 ppb indium as an internal standard. Samples were analysed by Sector Field ICP-MS (Finnigan Element II, Thermo Scientific) (Cullen and Sherrell, 1999; Townsend, 2000). A full suite of trace elements was measured including Fe, Al, Mn, Ba and P. The data were quality controlled by comparison with a certified reference material with a similar composition to the material collected (BCR-414 trace metals in phytoplankton, European Commission) (Table A1).

Quartz micro-fibre (QMA) filters were chosen as they could be acid cleaned to a trace-metal-clean level and the filter material allowed high particle loading and low wash-off upon pump retrieval. Furthermore, the filters were compatible for use with both Inductively Coupled Plasma Mass Spectrometry (ICP-MS) and elemental (CHN) analysis due to their ability to be combusted. It should be noted that a compromise was made here by using QMA filters on the ISPs. The compromise is that HF acid cannot be used with QMA filters as it digests the filter material completely and leads to unacceptably high analytical blanks. Therefore, we used HNO₃ for the digestions of the QMAs and for consistency regarding the suspended particles we also digested the pre-filter with the same acid. On the other hand, we used a full HF acid digestion for the underlying sediment analysis (Sect. 2.4.2). Therefore, recoveries of lithogenic trace elements will be close to 100% for the sediment analysis, but

somewhat lower for the lithogenic suspended particles. However, a HNO₃ only digestion will recover effectively 100% of the trace elements of biogenic suspended particles (Table A1). For further information see Bowie et al. (2010).

### 2.4.2 Sediment analysis for particulate metals

Digestions and analysis were performed as per the ISP filters except that HF acid was used to digest these highly refractory samples. The HNO₃ digest used for the ISP filters is relatively weak but digests the biogenic fraction completely as evidenced by the excellent recoveries on the BCR414 certified reference material (trace metals in phytoplankton) (Table A1) but has limited recoveries of the lithogenic fraction as evidenced by the low recoveries of pAl and pTi in MESS-3 and PACS-2 sediment certified reference material (Bowie et al., 2010).

During the HF digest, a mixture of strong acids (250 µL HNO₃, 250 µL HF and 500 µL HCl) were used as per Bowie et al. (Bowie et al., 2010). After 12 h at 95 °C the digest PFA vials were uncapped and evaporated to dryness under HEPA filtered air at 60 °C for 4 h. The digest was then resuspended in 10% HNO₃ with 10 ppb indium as internal standard. A 100 × dilution factor (v : v) was considered sufficient to place the ~ 20 mg sediment samples within the calibration range of the SF-ICP-MS.

### 2.4.3 Particulate organic carbon (POC) and nitrogen (PN)

All glassware in contact with POC samples was pre-combusted prior to field work (450 °C for 12 h). Total nitrogen, carbon and hydrogen were determined at the Central Science Laboratory, University of Tasmania, using a Thermo Finnigan EA 1112 Series Flash Elemental Analyzer (estimated precision ~ 1%).

## 3 Results and discussion

### 3.1 Station types

The sampling locations of KEOPS2 (Fig. 1) were designed to capture the key regime types of the Kerguelen Archipelago including the high-nutrient, low-chlorophyll (HNLC) reference waters (station R-2), the high-trace-metal plateau waters (station A3), the northern Polar Front (station F-L) and a quasi-stationary, bathymetrically trapped recirculation structure (E-1, E-3 and E-5) to the east of Kerguelen Island (Table 1). Stations E-1, E-3 and E-5 can be thought of as a pseudo-Lagrangian time series. In addition, two stations were sampled at the eastern and western extremes of the recirculation structure (E-4W and E-4E) which proved to contrast in absolute concentrations as well as elemental ratios of particulate trace metals.
<table><caption>**Table 1.** KEOPS2 sampling locations and station types.</caption><thead><tr><th rowspan="2">Station type</th><th>A3-1</th><th>A3-2</th><th>R-2</th><th>F-L</th><th>E-1</th><th>E-3</th><th>E-5</th><th>E-4E</th><th>E-4W</th></tr><tr><th>Kerguelen Plateau 1st visit</th><th>Kerguelen Plateau 2nd visit</th><th>HNLC reference station</th><th>Northern Polar Front</th><th>Recirculation structure</th><th>Recirculation structure</th><th>Recirculation structure</th><th>Eastern recirculation structure</th><th>Western recirculation structure</th></tr></thead><tbody><tr><td>Sampling date</td><td>20/10/2011</td><td>16/11/2011</td><td>25/10/2011</td><td>6/11/2011</td><td>29/10/2011</td><td>3/11/2011</td><td>18/11/2011</td><td>13/11/2011</td><td>11/11/2011</td></tr><tr><td>Latitude (S)</td><td>50°37.7574'</td><td>50°37.4306'</td><td>50°21.52'</td><td>48°31.394'</td><td>48°29.5728'</td><td>48°42.1334'</td><td>48°24.698'</td><td>48°42.9218'</td><td>48°45.927'</td></tr><tr><td>Longitude (E)</td><td>72°4.8193'</td><td>72°3.3366'</td><td>66°43.00'</td><td>74°40.036'</td><td>72°14.1467'</td><td>71°58.0027'</td><td>71°53.7894'</td><td>72°33.7792'</td><td>71°25.51'</td></tr><tr><td>Bottom depth (m)</td><td>505</td><td>505</td><td>2528</td><td>2690</td><td>2050</td><td>1910</td><td>1920</td><td>2200</td><td>1400</td></tr><tr><td>Time series</td><td>Yes</td><td>Yes</td><td>No</td><td>No</td><td>Yes</td><td>Yes</td><td>Yes</td><td>No</td><td>No</td></tr><tr><td>Particulate trace metals</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td></tr><tr><td>POC PON</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td></tr><tr><td>Sediment samples</td><td>Yes</td><td>Yes</td><td>Yes</td><td>Yes</td><td>No</td><td>Yes</td><td>No</td><td>No</td><td>Yes</td></tr><tr><td>Sediment trap samples</td><td>No</td><td>Yes</td><td>No</td><td>No</td><td>Yes</td><td>Yes</td><td>Yes</td><td>No</td><td>No</td></tr></tbody></table>

<figure><img src="image_5.png" /><figcaption>**Figure 2.** Surface (10 m) temperature in spring–summer (a) and autumn–winter (b) as well as surface salinity in spring–summer (c) and autumn–winter (d) within the study area from 1970 until 2013. The PF is identified as a solid black line. Kerguelen and Heard Island are visible in dark grey and black respectively and the Leclaire Rise can be identified as the shallow bathymetry, north of the PF, near the western boundary of the map. Data obtained from the World Ocean Database (http://www.nodc.noaa.gov).</figcaption></figure>

## 3.2 Surface water flow around the Kerguelen Plateau

During KEOPS1, van Beek et al. (2008), Zhang et al. (2008) and Chever et al. (2010) revealed that the water column south-east of Kerguelen Island was modified by passing over the Heard Island Plateau. Park et al. (2008) demonstrated that the interaction of the water masses over the Kerguelen Plateau could be divided into the southern and northern water masses separated by the Polar Front (PF, Fig. 1). The southern water mass has source waters being derived from the Antarctic surface waters (AASW), south-west of Kerguelen which is bound to the north by the shallow bathymetry of

the Leclaire Rise. These surface waters are generally colder and saltier than to the north (Fig. 2). The AASW also flows around Heard Island and a weaker surface current flows north-west over the Kerguelen Plateau towards the north-east of Kerguelen Island where it is bound to the north by the PF. This cold surface current can be seen during winter in Fig. 2. The northern water mass has a source of easterly flowing Sub Antarctic Surface Waters (SASW). The portion of the SASW that interacts with Kerguelen Island is termed Kerguelen Island source waters and is bound to the south by the PF (Fig. 2). A broad and poorly defined mixing zone to the east of Kerguelen Island has been identified at the junction of
these southern and northern water masses. As a result of the mixing, eddies commonly form in this region. Also within this mixing zone, surface filaments, identified by elevated Chlorophyll *a*, can be seen in SeaWiFS images diverging from the PF and entering the eastern boundary of the recirculation structure (see the Supplement in Trull et al., 2014).

The Kerguelen Archipelago is isolated, being a relatively small and localised source of Fe fertilisation surrounded by the large and deep, HNLC, low Fe, Southern Ocean. Therefore, when identifying an Fe source to the region, our focus is on the plateau and the two islands, Kerguelen and Heard. Over geological timescales, all pFe distributed throughout the water column within this region must be derived from all forms of weathering of bed rock including fluvial and glacial outflow as well as dust from the islands, hydrothermal and extra-terrestrial input. Over shorter time frames, shelf sediments in the region contain recycled Fe as the vast majority of these sediments are a combination of siliceous ooze (Armand et al., 2008) and glacio-marine sediments; the exported product of the highly productive overlying waters together with some lithogenics (sourced from bed-rock) that were unutilised or non-bioavailable and fast-sinking. Therefore, understanding the pathways of supply of this new Fe is important to understanding the processes controlling the long term productivity and therefore, carbon sequestration, in the area.

### 3.3 Underlying sediment analysis

Analysis of sediments sourced from cores taken at each station revealed a distinctly different sediment signature at station R-2 compared with any other station (Table 2). The reference station signature was approximately six times enriched in Mn relative to Al (Mn:Al 0.063) in comparison to the plateau station (A3) (Mn:Al 0.011). The Mn:Al sedimentary signature at A3 was almost identical to authigenic sediments previously reported from the Amundsen Sea (Angino, 1966). We consider that the enriched Mn at R-2 could be due to either $MnO_2$ enrichment in the surface sediments during redox cycling of early diagenesis (Planquette et al., 2013), or supplied via a Mn enriched source such as hydrothermal venting near the Leclaire Rise. The extremely low carbon content of the sediment at station R-2, as evidenced by its near white colour, low diatom content (L. Armand, pers. obs., 2012) and low carbon export flux (Laurenceau et al., 2014; Planchon et al., 2014), suggests that $MnO_2$ enrichment in the surface sediments during redox cycling is more likely at R-2.

The authigenic sediment ratio of Fe:Al was also lower at station R-2 (Fe:Al = 0.73) in comparison to any other station (Fe:Al range 0.81–1.1). However, all of our observed pFe:pAl molar ratios were higher than upper crustal molar ratios (Fe:Al 0.19) (Wedepohl, 1995) or Amundsen Sea surface sediments (Fe:Al 0.26) (Angino, 1966). Interestingly, our observed pFe:pAl sedimentary ratios were sim-

ilar to the ratio found in phytoplankton such as the BCR-414 certified reference material (freshwater phytoplankton) (Fe:Al = 1.01) used in this study (Table A1). Furthermore, the pFe:pAl ratio of sinking particles captured by the free floating PPS3 sediment traps (marine snow) had similar ratios of pFe:pAl of 1.02, 1.05, 0.91 and 0.70 for stations E-1, E-3, E-5 and A3-2, respectively (Table 2). These observations highlight the major contribution of sinking biogenic material to the authigenic sediments in the area around the Kerguelen Plateau which was in contrast to the signature at station R-2 due to its low productivity. The pFe in the sediments at all stations and primarily at station R-2 (as a fraction of its total weight) were similar to Weddell Sea surface sediments (Angino and Andrews, 1968) which ranged from 0.9–3.2%. In comparison, station R-2 has a mean value of 0.1% Fe while station E-3, A3, F-L and E-4W had mean values of 0.3, 0.8, 1.5 and 2.5% respectively. The low fraction of Fe within the authigenic sediment at R-2 indicates limited pFe supply at this station in comparison to either the Weddell Sea or the Kerguelen Plateau presented here.

### 3.4 Plateau, reference and Polar Front stations

The reference station (R-2) has a bottom depth of 2528 m and is characterised by low surface $Chl \ a$ concentrations (Lasbleiz et al., 2014) and nutrient concentrations characteristic of HNLC waters (Blain et al., 2014). Station F-L is approximately 313 km northeast of Kerguelen Island with a bottom depth of 2690 m and represents the northern PF. Station F-L is downstream of Kerguelen Island, with the PF delivering waters that originated near station R-2. In this case, the waters crossing Station F-L have interacted with both the plateau and shallow coastal waters of Kerguelen Island. In contrast, station A3 is located over the Kerguelen Plateau and has a bottom depth of 527 m, making it the shallowest station sampled for trace metal analysis of suspended particles and one of the most likely to be influenced by resuspension of shelf sediments (Fig. 1). The proximity of the station to Heard and Kerguelen Island (roughly half way between the two) means that fluvial and glacial runoff may also drive fertilisation at this site. However, the hydrography of the area dictates that waters which previously interacted with upstream Heard Island are a more likely source to A3 than downstream Kerguelen Island (Park et al., 2008).

The pFe, pAl and pMn concentrations at the reference station (R-2) only increase slightly towards the sea floor; however, enrichment in pFe, pAl and primarily pMn is evident at 500 m likely due to proximity to the Leclaire Rise (Fig. 3) (discussed in detail below). The northern PF station (F-L) exhibits moderate concentrations of pFe, pAl and pMn throughout the water column, somewhat higher than the reference station, and much higher concentrations are observed in close proximity to the sea floor. It should be noted that the deepest sample at R-2 was 148 m above the seafloor, while at F-L it was only 90 m above the sea floor and this could well
<table><caption>**Table 2.** Mean elemental molar ratios of marine snow particles captured in free-floating sediment traps, particulate matter (1–53 µm) below the mixed layer and authigenic sediments at each station. Note that station TEW-1 is a near-coastal station located within Hillsborough Bay, Kerguelen Island. Station TEW-1 is not discussed in detail in the MS as no samples were collected for suspended particles; however, details are included here to show the influence of close proximity to the island and fluvial/glacial sources.</caption><thead><tr><th>Sediment trap @ 210 m</th><th>pFe : pAl</th><th>pMn : pAl</th><th>pMn : pFe</th><th>pBa : pAl</th></tr></thead><tbody><tr><td>A3-2</td><td>0.70</td><td>0.008</td><td>0.011</td><td>0.025</td></tr><tr><td>E-1</td><td>1.02</td><td>0.009</td><td>0.009</td><td>0.162</td></tr><tr><td>E-3</td><td>1.05</td><td>0.010</td><td>0.010</td><td>0.285</td></tr><tr><td>E-5</td><td>0.91</td><td>0.008</td><td>0.009</td><td>0.318</td></tr><tr><td colspan="5">Suspended particles mean (&gt; MLD)</td></tr><tr><td>A3-1</td><td>0.53</td><td>0.007</td><td>0.013</td><td>0.027</td></tr><tr><td>A3-2</td><td>0.63</td><td>0.009</td><td>0.014</td><td>0.034</td></tr><tr><td>R-2</td><td>0.65</td><td>0.036</td><td>0.059</td><td>0.322</td></tr><tr><td>F-L</td><td>0.77</td><td>0.020</td><td>0.027</td><td>0.190</td></tr><tr><td>E-4E</td><td>0.86</td><td>0.037</td><td>0.045</td><td>0.383</td></tr><tr><td>E-4W</td><td>0.63</td><td>0.014</td><td>0.021</td><td>0.078</td></tr><tr><td>E-1</td><td>0.68</td><td>0.023</td><td>0.034</td><td>0.185</td></tr><tr><td>E-3</td><td>0.71</td><td>0.024</td><td>0.033</td><td>0.258</td></tr><tr><td>E-5</td><td>0.68</td><td>0.020</td><td>0.030</td><td>0.260</td></tr><tr><td colspan="5">Sediment analysis</td></tr><tr><td>TEW-1</td><td>1.10</td><td>0.013</td><td>0.012</td><td>0.003</td></tr><tr><td>A3-1</td><td>0.87</td><td>0.011</td><td>0.013</td><td>0.026</td></tr><tr><td>R-2</td><td>0.73</td><td>0.063</td><td>0.086</td><td>0.892</td></tr><tr><td>F-L</td><td>0.82</td><td>0.016</td><td>0.019</td><td>0.040</td></tr><tr><td>E-4W</td><td>0.81</td><td>0.013</td><td>0.016</td><td>0.013</td></tr><tr><td>E-3</td><td>0.93</td><td>0.015</td><td>0.016</td><td>0.125</td></tr><tr><td>Kerguelen Archipelago</td><td>0.08–0.49</td><td>0.004–0.010</td><td>0.021–0.050</td><td>0.002–0.004</td></tr><tr><td>Basalt mean<br>(Gautier et al., 1990)</td><td></td><td></td><td></td><td></td></tr><tr><td>Upper continental crust<br>(Wedepohl, 1995)</td><td>0.19</td><td>0.003</td><td>0.017</td><td>0.002</td></tr></tbody></table>

explain the observed difference, given the strong decrease of nepheloid layers away from the seabed (Blain et al., 2007; Jouandet et al., 2014).

Profiles of pFe and pAl in the 1–53 µm size range from station R-2, A3 and F-L are shown in Fig. 3. The plateau station (A3) was sampled twice during the study (A3-1 and A3-2), separated by 20 days. Surface chlorophyll images revealed that between visits to the site, a large bloom developed in the vicinity and extended over the site, and was beginning to fade again by the time of the second sampling (Trull et al., 2014). Thus, station A3-1 can be thought of as pre-bloom and A3-2 as post-bloom conditions. Particulate Fe, Al and Mn generally increased towards the sea floor at station A3, with the exception of a slight enrichment below the mixed layer during the second visit (A3-2) to the station in the > 53 µm size fraction (Fig. 4). To investigate the progression of pFe through time, we integrated the pFe throughout the full water column, and observed a decrease in the pFe stock from 9.1 to 4.5 mmol m⁻² between the first and second visit to station A3. This translates to a 51% reduction in pFe for

all size classes combined (i.e. > 1 µm). However, if we look closer at the pFe distribution only within the surface mixed layer (165 m) between A3-1 and A3-2, we observe a loss of 70% of the integrated total pFe (> 1 µm) (Fig. 4). Concurrently, using an Underwater Vision Profiler to track particle size distribution, Jouandet et al. (2014) noted a four-fold increase in particle numerical abundance through the full water column. Their one dimensional particle dynamic model supported the hypothesis that the increase in biogenic particles, due to blooming conditions, resulted in the rapid formation of large particles due to coagulation and subsequent vertical transport to the base of the mixed layer. This result is supported in the current data set, in that we see a large decrease in small pFe particles within the mixed layer and a moderate increase in large pFe particles at the base of the mixed layer when comparing pre (A3-1) to post (A3-2) bloom conditions (Fig. 4). Furthermore, we observed an increase in biogenic pFe within the surface mixed layer between A3-1 and A3-2 (Sect. 3.7).
<figure><img src="image_6.png" /></figure>

**Figure 3.** Profiles of particulate Fe (a), Al (b) and Mn (c) (1–53 µm) at the reference HNLC station (R-2), the northern PF station (F-L) and pre- and post-bloom over the plateau station (A3-1, A3-2), highlighting the contrasting particulate trace metal supply to these locations. Biogenic Fe (d) (as a percentage of the total Fe) in surface waters shows a clear progression that can be explained by the location of each station within the study area whereby, biogenic Fe at R-2 >> F-L > A3-2 > A3-1.

<figure><img src="image_7.png" /></figure>

**Figure 4.** Particulate Fe at the plateau station (A3) by size class. The integrated full water column pFe (> 1 µm) reduced by 51 % between A3-1 and A3-2 (9.1–4.5 mMol m⁻² at A3-1 and A3-2 respectively). The integrated mixed layer pFe reduced by 70 % between A3-1 and A3-2 (1.4–0.56 mMol m⁻² at A3-1 and A3-2 respectively). The mixed layer shoaled between A3-1 and A3-2 as illustrated by the dashed horizontal line. The calculation of integrated mixed layer pFe used a constant mixed layer depth of 165 m for both A3-1 and A3-2 to allow comparison between these stations.

Thus, it appears that physical aggregation within the mixed layer of the particles onto biogenic phyto-aggregates during the bloom development and export to the base of the mixed layer, combined with significantly lower concentrations above the seafloor resulted in the observed 51 % reduction in pFe (> 1 µm) between A3-1 and A3-2. The significantly lower concentration at 440 m during the post-bloom

conditions of A3-2 may be due to increased small particle scavenging resulting from sinking phyto-aggregates or alternatively, small-scale variation in the thickness of the nepheloid layer.
<figure><img src="image_8.png" /></figure>

**Figure 5.** Profiles of elemental ratios at the reference station (R-2), northern PF (F-L) and pre- and post-bloom over the plateau station (A3-1, A3-2). Note the increase in pMn and pBa relative to pAl at station R-2 below 500 m.

## 3.5 Elemental ratios at stations R-2, F-L and A3

As station A3 is located over the Kerguelen Plateau and also is in close proximity to fluvial and glacial runoff from Heard Island, we would expect the trace metal source signature of suspended particles to be unique here in comparison to our reference (R-2) and PF (F-L) stations. The particles over the Kerguelen Plateau were characterised by very high pFe (0.94–30.4 nM) and pAl (1.5–58.6 nM) with concentrations an order of magnitude higher than R-2 (<DL–1.35 nM Fe and <DL–2.08 nM Al). The reference station was characterised by low surface Chl *a* concentrations characteristic of HNLC waters (Lasbleiz et al., 2014), however, it is relatively close to the Leclaire Rise; a seamount with its shallowest point 135 km west north-west of station R-2 rising up to approximately 395 m. The Leclaire Rise extends to 70km north-west of station R-2 where it reaches a depth of approximately 550 m. It is important to recall in this context that the PF divides the northeast flowing AASW from the eastward flowing SASW to the north (Park et al., 2008). Classical theory suggests that this oceanographic feature should block much of the enrichment from the Leclaire Rise to station R-2. However, enrichment was evident in the vertical profiles of pFe, pMn and pAl at station R-2 at 500 m depth (Fig. 3).

Figure 5 illustrates the full water column elemental ratios at the reference station (R-2) in comparison to the Kerguelen Plateau stations (A3-1 and A3-2) and reveals that Mn : Fe

<figure><img src="image_9.png" /></figure>

**Figure 6.** Molar ratio of pMn : pAl of suspended particles versus depth, separated by station type. Vertical lines represent the median molar ratios within Kerguelen Island basalts (Gautier et al., 1990) (black), authigenic Kerguelen Plateau sediments (red) and station R-2 authigenic sediments (green).

as well as Ba : Al are strikingly unique. At station R-2, below 500 m, we see Mn : Fe 2 × higher than A3, Mn : Al 4.5 × higher and Ba : Al ratios 10 × higher than at A3, making this source signature relatively clear (Table 2). The unique ratios below 500 m at R-2 may arise from a source of dissolved or particulate Mn (uncoupled from pFe and pAl) from the Leclaire Rise. Furthermore, the elemental ratios over station A3 are generally much lower (Fig. 5) due to high pFe and pAl supply over the Kerguelen Plateau that is relatively deficient in pMn, such as would be found in glacial runoff that has a signature which reflects fresh weathering of basaltic rocks (Doucet et al., 2005). This source theory is supported by the observation of high dissolved Mn (dMn) near the Leclaire Rise (Quéroué et al., 2015) and uniquely high pMn : pFe in sediments found below station R-2 (Table 2). Surface water particulate trace metals also reveal distinct differences. The ratios of pFe : pAl, pMn : pAl and pMn : pFe all increase from the bottom of the mixed layer to the surface at stations R-2 and F-L (Fig. 5). This profile characteristic is in contrast to stations A3-1. The observed modification of the elemental ratios in the surface mixed layer at R-2 and F-L is most likely due to biological uptake of dissolved trace elements and conversion into the biogenic particulate fraction.

Particulate Al and pFe were closely coupled across all stations (Spearman's ρ = 0.91, P < 0.01, n = 70). However, pAl and pMn, although still strongly correlated (P = 0.80
$P<0.01$ $n = 70$), appeared more variable than pFe versus pAl. Figure 6 illustrates this variability in the pMn in comparison to pAl as a function of its location within the study area. The observed variability in pMn but not pFe relative to pAl highlights the uncoupling between some of the sources of pMn and pFe. Specifically, the observed variability points to a uniquely high Mn : Fe source either in the authigenic sediments of the Leclaire Rise and/or a hydrothermal source (German et al., 1991), or a process whereby pAl is preferentially stripped out with distance from the source. A study by Shigemitsu et al. (2013) showed that the concentration of pAl in suspended particulate material in the intermediate water of the Sea of Okhotsk (western Pacific Ocean) decreased with distance from the shelf source preferentially in relation to pFe and pMn. They concluded that increasing pFe : pAl and pMn : pAl ratios occurred with distance from the source and suggested that the denser, lithogenic particles settled out preferentially, stripping out pAl. Furthermore, they found pFe became associated with organic matter more readily than pAl and therefore, remained suspended in the water column more readily than pAl. These processes could explain the observed modification of the elemental ratios between stations R-2, A3 and possibly F-L. The stations that were in close proximity to the shelf source such as A3-1 and A3-2 were indeed enriched in lithogenic pAl and as such pFe : pAl was relatively low (Fig. 5). In contrast, F-L was at the greatest distance from a sedimentary source and displayed the highest pFe : pAl ratio.

## 3.6 What are the sources of particulate trace metals over the plateau and downstream?

The high particulate trace metal concentrations found at 440 m, at A3-1 and A3-2, near the sea floor, most likely originated from resuspension of deep (~500 m) shelf sediments. The cause of the variability between A3-1 and A3-2 at this depth remains unclear, but could reflect small scale variability in the depth of the nepheloid layer or be the result of temporal variability due to the action of tides and internal waves (McCave, 1986). The pMn : pAl, pMn : pFe and pBa : pAl ratios for A3-1 and A3-2 are similar from the sea floor to the approximate base of the surface mixed layer, with values higher than the mean crustal ratios (Wedepohl, 1995), but lower than either basalt (Gautier et al., 1990) or the underlying sediment ratios (Table 2). Within the surface mixed layer, A3-1 maintains similar ratios to the deep water column, while at A3-2 the ratios diverge towards the surface. The particulate trace metal signature within the mixed layer at A3-2 increases in pMn and pBa relative to pAl, which is most likely driven by biogenic conversion of dissolved bioessential elements into biogenic particles (Sect. 3.7).

Glacial flour is the result of mechanical erosion of bed rock by glaciers. Typical particle sizes are within the silt size range but can overlap with clays (0.002–0.063 mm). Recent research suggests that Fe sourced from glacial erosion can

be a major source of bioavailable Fe to the Southern Ocean (Poulton and Raiswell, 2005; Raiswell et al., 2008a, b, 2006). Assuming no mixing and a dilute suspension, Stokes' law predicts that the small grain size of glacial flour allows it to remain suspended within a 500 m water column for between 2 and 2500 days or within a 165 m mixed layer for 1–831 days depending on particle size. Certainly, mixing within the surface mixed layer would increase this duration significantly, meaning that glacial and fluvial input from both Heard and Kerguelen Island could remain suspended in the mixed layer for long enough to travel well past any of the stations in the present study, excluding the reference station (R-2). Furthermore, it has been shown that 2–3 % of the Fe within glacial rock flour can be leached into the dissolved size fraction (<0.2 µm) with ultrapure water; a large proportion of which should be bioavailable (Schroth et al., 2009). It is thought that this dFe is leached from nanoparticulate Fe (oxyhydr)oxides in glacial rock flour over time (Raiswell, 2011; Raiswell et al., 2010) following an exponential decay, so it is possible that this source could be excluded from the <0.2 µm dissolved fraction, but included in the 1–53 µm particulate fraction presented here. This is especially true of nanoparticulate Fe that is attached to the surface of larger sediment grains as has been observed previously in glacial sediments (Shaw et al., 2011). Given that the particulate fraction is generally an order of magnitude higher in concentration than the dissolved fraction, this source may well be more significant in stimulating phytoplankton blooms than previously estimated. Overall, station A3 appeared to be directly fertilised by resuspension of shelf sediments at depth, and entrainment of this pFe-rich water occurred during events that deepen the mixed layer periodically. However, lateral supply above the mixed layer of small particles from shallow coastal sources around Heard Island, including glacial melt waters, cannot be ruled out.

## 3.7 Biogenic and sedimentary particulate trace metals

If we assume that all particulate phosphorus (pP) is of biogenic origin, we can calculate the biogenic Fe fraction of the total Fe concentration by normalising to pP and comparing with published elemental ratios of Southern Ocean diatoms (Planquette et al., 2013). For the calculations we used the upper limit of Fe : P (1.93 mmol mol⁻¹) reported by Twinning et al. (2004) for Southern Ocean diatom assemblages. Given that pP and POC are remineralised throughout the water column and are generated within the surface mixed layer, calculations of biogenic trace metals will only be valid within the surface mixed layer, as the concentration of pP and POC decreases strongly with depth. It should also be noted that Kerguelen Island basalts and upper continental crust can contribute particulate phosphorus concomitantly with pFe to the particulate pool. However the Fe : P ratio found within Kerguelen Island basalts and the continental crust is 12.8 and 25.8 (mol : mol) respectively (Gautier et al.,
1990; Wedepohl, 1995). Thus, the factor of 1000 increase in pP observed within suspended particles compared to these rock sources indicates that this pP is likely produced in situ within the mixed layer from dissolved PO₄³⁻ rather than supplied from rock weathering together with Fe. Furthermore, within the upper 200 m of the water column, biogenic Fe correlates significantly with both fluorescence (Spearman's ρ R = 0.518, P < 0.05, n = 30) and dissolved oxygen (Spearman's ρ R = 0.507, P < 0.05, n = 30) confirming the autotrophic composition of the particles identified as high in biogenic Fe. Figure 3 illustrates the contribution of biogenic Fe in surface waters at stations R-2, A3 and F-L. Station R-2 and F-L have biogenic Fe fractions that are higher near the surface than at depth (Fig. 3). In contrast, at stations A3-1 and A3-2, biogenic Fe and Mn only make up a relatively small fraction of the total pFe throughout the water column although at station A3-2 we see a slight increase in biogenic pFe towards the surface, corresponding with the development of a bloom. Biogenic Fe at stations A3-1 and A3-2 constitutes less than 1 and 5% respectively of the total Fe. The low biogenic fraction at station A3-1 most likely results from an excess of lithogenic Fe, Al and Mn to the water column from the shelf sediments as well as fluvial/glacial runoff from nearby islands of the Kerguelen Archipelago, which are excess to demand. A similar pattern was observed during a study located in the Amundsen Sea (Planquette et al., 2013) where the percentage of biogenic Fe (full water column mean) reduced with proximity to the trace metal source.

Alternatively, the relative importance of sedimentary input at each of the stations can be gauged by observing the pMn : pAl molar ratio within suspended particles and comparing these to known molar ratios of pMn : pAl within Kerguelen Island basalts, A3 authigenic sediments and R-2 authigenic sediments (Fig. 6). At station A3 we see that almost all the suspended particles lie within the ratio of plateau sediments and Kerguelen Island basalts with the remaining suspended particles associated with the development of a bloom in surface waters at A3-2, which is also where we see an increase in biogenic Fe. Mid-depth suspended particles at E4-W (red dots) also lie between Kerguelen Island basalts and plateau sediments, indicating a similar source to station A3. The reference station exhibits highly modified pMn : pAl molar ratios within the suspended particles and its underlying sediment. This modification is most likely due to biogenic incorporation of bioessential elements such as Mn into particles. The remaining stations are intermediate between A-3 and R-2.

## 3.8 Pseudo-Lagrangian, recirculation structure

Station E-4W has trace metal concentrations, elemental ratios and community size structure (Trull et al., 2014) similar to A3 and as such, will be excluded from the discussion in this section. The remaining recirculation structure stations exhibit profiles of pFe and pMn which show a minimum at

approximately 150–175 m (Fig. 7). Our detailed depth profile indicates that the pFe and pMn minima coincide with the remnant winter water temperature minimum (Fig. 8). Interestingly, Blain et al. (2014) also estimated a winter water depth of approximately 150 m. They observed, at 150 m, that nitrate and phosphate profiles within the recirculation feature, from multiple years and seasons, converged with striking consistency. Particulate Fe and pMn, concentrations increase above and below the temperature minimum, however, pAl only increases below 175 m. Particulate Al is stripped out preferentially with settling lithogenics while pFe and pMn are retained either through conversion to the biogenic particulate fraction (uptake) or adsorbed onto organic particles. It should be noted here that the work of Raiswell (2011) indicates that iceberg and glacially derived Fe nanoparticulate material is typically high in Fe and low in Al. Thus, supply of glacially derived nanoparticulate Fe from Kerguelen Island, via the north-east of the recirculation structure could also cause the observed high Fe, low Al surface enrichment within the recirculation structure.

Given that the pFe and pMn minima coincide with the remnant-winter-water temperature minimum, the total amount of particulate trace metals distributed throughout the winter mixed layer must be lower than during summer. This is counterintuitive if sediment resuspension is the primary source of particulate trace metals into the recirculation feature. During winter we would expect increased wind mixing, leading to more entrainment of pFe over the plateau and more supply into the recirculation feature leading to a maximum at the temperature minimum. Given that we observe the inverse situation, supply into the recirculation structure must be low during winter. Thus, we suggest that the lateral supply of fluvial and glacial derived particulate trace metals must be an important source. This source would be expected to reduce in winter when precipitation as snow and glacial freezing is at a maximum and conversely, during spring, snow and ice melt and rainfall increases runoff into the coastal areas and induces a fertilisation event downstream of Heard and Kerguelen Islands. Kerguelen Island is a subantarctic island, and its climatology is cold and wet, with the Port-aux-Français weather station recording mean daily temperatures of 2.1 °C in winter and 8.2 °C in summer and year round consistent precipitation (730 mm annually) (Meteo France). It should be noted that due to its sheltered location and sea-level altitude, the Port-aux-Français location is relatively mild compared to the west coast and interior of the island which is estimated to receive three times the rainfall of the east coast, or 2124 mm annually. Therefore, having a climate of high precipitation and seasonal thawing, increased seasonal runoff can be expected in spring and summer from Kerguelen Island.

The importance of glacial/fluvial sources in supplying dissolved Fe and Mn into coastal waters to the north-east of Kerguelen, north of the PF, has been shown previously by Buciarelli et al. (2001). The authors found a linear relationship between dissolved Fe and lithogenic silica and suggested
<figure><img src="image_10.png" /></figure>

**Figure 7.** Profiles of particulate trace metals during the pseudo-Lagrangian recirculation-structure study. Station E-4W (gray triangle) exhibits unique trace metal profiles in comparison to the remaining stations (see text for details). Note the distinct pFe and pMn minima at 150–175 m. Particulate Al exhibits a similar profile albeit without surface enrichment.

<figure><img src="image_11.png" /></figure>

**Figure 8.** Temperature profiles within the upper 500 m within the recirculation structure are shown alongside particulate Fe (1–53 µm) within the upper 500 m within the recirculation structure. Correspondence between the temperature minimum depth of winter water and pFe minimum is illustrated.

that this was indicative of weathering of silicate rich minerals that characterise the Kerguelen Islands with a concomitant release of dissolved Fe and Mn. Indeed, in the present study, using the lithogenic and biogenic silica data presented in Closset et al. (2014), total particulate Fe correlated significantly with total lithogenic silica (R = 0.76, P < 0.01) but not with biogenic silica. However, this significant correlation was not limited to the coastal regions in the present study and instead was observed for all stations and depths combined. Bucciarelli et al. (2001) found an exponential decrease in dissolved Fe with distance from the coast, further supporting their theory of a dominant coastal source in this region.

This exponential decrease would be expected to apply to the particulate fraction also; however, it appears that even with an exponential decrease in pFe with distance from the coast, particulate Fe enrichment, sourced from fluvial runoff, is evident on the southern side of the PF within the recirculation feature.

The hypothesis of pFe supply from north of the PF into the eastern side of the recirculation feature via the mixing zone is supported by radium isotope data (Sanial et al., 2014) collected during the KEOPS2 mission. Apparent radium ages derived from the ratio of $^{224}$Ra/$^{223}$Ra (and using the ratio observed within the Baie des Baleiniers as the starting time) suggest that the age of water since fertilisation within the recirculation feature was only 5–8 days. This indicates that there is likely rapid transfer across the PF of fertilised waters which were sourced from nearby shallow coastal areas such as the Baie des Baleiniers, Kerguelen Island. The authors go on to highlight that the heterogeneous distribution of $^{224}$Ra and $^{223}$Ra indicates that transfer across the Polar Front is sporadic in nature.

The observation of pFe enrichment in surface waters of the recirculation structure without proportional concentrations of pAl may be due to biological uptake and conversion from a bioavailable pool into the biogenic particulate pool. Settling of refractory lithogenics that are high in Al may also partially explain the observation. Alternatively or in combination, a high pFe, low pAl source such as nanoparticulate Fe characteristic of glacial/fluvial runoff (Hawkings et al., 2014; Raiswell et al., 2008b, 2006) on Kerguelen Island could explain this observation. Indeed, temperature and salinity profiles within the recirculation structure reveal
fresher and warmer water within the upper 110 m than either the R-2 or A3 stations, suggesting that glacial/fluvial runoff from Kerguelen Island may well be delivering this high pFe, low pAl surface enrichment.

## 4 Conclusions

This study has identified two distinct areas of Fe fertilisation in the vicinity of Kerguelen Island. Firstly, the plateau itself is a major source of resuspended shelf sediments to station A3 especially below the mixed layer. Secondly, fluvial and glacial runoff into coastal waters in combination with resuspension of shallow coastal sediments fertilises areas to the north of the PF, east of Kerguelen Island, but also across the PF and into the recirculation feature from the north-east. Indications of particle transport across the PF were observed at station R-2 sourced from the Leclaire Rise to the north of the PF. Satellite imagery also revealed filaments clearly diverging from the main jet of the PF and into the north east of the recirculation structure. Within the recirculation structure, the correspondence of the winter water temperature minimum with the particulate trace metal minimum implies that a seasonal cycle is involved in the supply of trace elements. This is most likely driven by increased fluvial and glacial runoff in summer, associated with rainfall and basal melt and reduced supply in winter when snowfall and freezing conditions pre dominate. In this complex region, it appears that weathering of the islands themselves are direct sources of new Fe and help stimulate the seasonal bloom that is significant in terms of the regional carbon cycle.

Over the mesoscale, it appears that physical processes associated with settling of refractory lithogenic particles was an important process in modifying the particulate elemental ratios. However, on the individual profile scale, biological processes seem important in modifying the elemental ratios in surface waters through preferential uptake of bio-essential elements, even from the particulate fraction.

Repeat sampling over the plateau provided a perspective on the persistence of the particulate Fe availability. Small particles containing pFe were efficiently transported out of the mixed layer during a bloom event over stations A3. This resulted in a 70% reduction in the integrated pFe stock within the mixed layer as a result of physical aggregation of small particles onto phyto-aggregates, presumably decreasing particle buoyancy and increasing export out of the mixed layer. This is likely to be an important aspect of the complex interaction between iron supply and biological availability, capable of mediating bloom duration and thus the efficiency of carbon sequestration.
## Appendix A: Certified reference material analysis

<table><caption>**Table A1.** Percentage recoveries of BCR-414 certified reference material. Certified and single lab values taken from the final report of the Commission of the European Communities, Community Bureau of Reference for BCR-414, EUR14558.</caption><thead><tr><th>mg kg<sup>-1</sup></th><th>Rep 1</th><th>Rep 2</th><th>Rep 3</th><th>Mean</th><th>SD</th><th>RSD (%)</th><th>Certified</th><th>% recovery</th><th>Single lab analysis</th><th>% recovery</th></tr></thead><tbody><tr><td>Ba</td><td>34</td><td>26</td><td>32</td><td>31</td><td>4.0</td><td>13.1</td><td></td><td></td><td>31</td><td>99</td></tr><tr><td>Al</td><td>2243</td><td>1349</td><td>1943</td><td>1845</td><td>454.6</td><td>24.6</td><td></td><td></td><td>1800</td><td>102</td></tr><tr><td>Mn</td><td>278</td><td>284</td><td>283</td><td>282</td><td>3.4</td><td>1.2</td><td>299</td><td>94</td><td></td><td></td></tr><tr><td>Fe</td><td>1874</td><td>1850</td><td>1878</td><td>1867</td><td>15.0</td><td>0.8</td><td>1850</td><td>101</td><td></td><td></td></tr></tbody></table>
*Acknowledgements.* This work was supported by the Antarctic Climate and Ecosystems Cooperative Research Centre, University of Tasmania, Australia. This work was also supported by the French research program of INSU-CNRS LEFE-CYBER (Les enveloppes fluides et l'environnement – Cycles biogéochimiques, environnement et ressources), the French ANR (Agence Nationale de la Recherche, SIMI-6 program, ANR-10-BLAN-0614), the French CNES (Centre National d'Etudes Spatiales) and the French Polar Institute IPEV (Institut Polaire Paul-Emile Victor). We would like to thank the captain and the crew of the R/V *Marion Dufresne*, Stephane Blain and Bernard Quéguiner as chief scientist and project coordinator of the KEOPS2 cruises, respectively. L. Armand was supported by grant Australian Antarctic Division, AAS grant #3214. Access to Sector Field ICP-MS instrumentation was supported through ARC LIEF funding (LE0989539). F. Dehairs was supported by Belgian Science Policy grant SD/CA/05A; Flinders Research Foundation grant G071512N and Vrije Universiteit Brussel, Strategic Research Plan.

Edited by: I. Obernosterer

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