High Variability of Dissolved Iron Concentrations Printer-friendly Version Interactive Discussion High Variability of Dissolved Iron Concentrations in the Vicinity of Kerguelen Island (southern Ocean) High Variability of Dissolved Iron Concentrations Printer-friendly Version Interactive Discussion H

This discussion paper is/has been under review for the journal Biogeosciences (BG). Please refer to the corresponding final paper in BG if available. Abstract Dissolved Fe (dFe) concentrations were measured in the upper 1300 m of the water column in the vicinity of Kerguelen Island as part of the second Kerguelen Ocean Plateau compared Study (KEOPS2). Concentrations ranged from 0.06 nmol L −1 in offshore , Southern Ocean waters, to 3.82 nmol L −1 within Hillsborough Bay, on the north-5 eastern coast of Kerguelen Island. Direct island runoff, glacial melting and resuspended sediments were identified as important inputs of dFe that could potentially fertilize the northern part of the plateau. A significant deep dFe enrichment was observed over the plateau with dFe concentrations increasing up to 1.30 nmol L −1 close to the seafloor, probably due to sediment resuspension and pore water release. Biological uptake was 10 identified as a likely explanation for the decrease in dFe concentrations between two visits (28 days apart) at a station above the plateau. Our results allowed studying other processes and sources, such as atmospheric inputs, lateral advection of enriched seawater , remineralization processes and the influence of the Polar Front (PF) as a vector for Fe transport. Overall, heterogeneous sources of Fe over and off the Kerguelen 15 Plateau, in addition to strong variability in Fe supply by vertical or horizontal transport, may explain the high variability in dFe concentrations observed during this study.

During the first Kerguelen Ocean Plateau compared Study (KEOPS1) held in late summer 2005, the impact of natural fertilisation on primary productivity and carbon export was demonstrated in this area (Blain et al., 2007;Savoye et al., 2008).The surface area of the observed phytoplankton bloom was about 45 000 km 2 and led to a carbon sequestration efficiency 18 times larger (Chever et al., 2010) than estimated around Crozet Islands (bloom area 90 000 km 2 ) during the CROZEX experiment in the same year (Pollard et al., 2009;Morris and Charette, 2013).It was proposed that the development of the bloom was constrained by both iron and silicate availability around Kerguelen Island (Blain et al., 2007;Mosseri et al., 2008;Park et al., 2008).A second cruise, KEOPS2 (Kerguelen Ocean and Plateau compared Study 2), which was approved as a GEOTRACES process study, was designed to study the development of the Kerguelen bloom in early spring 2011 and in the offshore fertilisation area further east (Blain et al., 2007).In this paper, we first describe the complex regional circulation, and use it to cluster the stations into 5 groups (near-coastal, plateau, recirculation, north of the polar front, HNLC area).For these groups, we present the dissolved Fe (dFe) concentrations and discuss their distributions in relation to potential new and regenerated sources.An estimate of the biological uptake of Fe is provided, where possible.The combined suite of KEOPS2 Fe results will be presented in two other papers in this special issue (van der Merwe et al., 2014;Bowie et al., 2014).Introduction

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Full 2 Materials and methods

Study area
During austral spring (7 October 2011-30 November 2011), 149 seawater samples from 15 stations were collected as part of the KEOPS2 oceanographic research cruise (Fig. 1, Table 1) in the vicinity of Kerguelen Island in the Southern Ocean ( 48• 20 -50 • 40 S and 66 • 40 -74 • 50 E).Two stations were sampled over the plateau (A3 and G-1), south of the island.A3 was visited twice, 28 days apart, first in the early stage of the bloom and secondly at the height of bloom development.An East-West (E-W) transect (from TEW-1 to F-L) was sampled from the Kerguelen coast to offshore waters, and crossed the PF twice.Finally, three additional stations were analyzed within a complex system of recirculation located in a stationary meander of the PF (E-3, E-4W-2 and E-5 ).An open ocean station (R-2), was located in the HNLC area southwest of Kerguelen Island and south of the Polar Front (PF).

Sampling and analytical methods
Cleaning, sampling, handling and processing of the samples were conducted using stringent trace metal clean protocols as recommended by the GEOTRACES program (Cutter et al., 2010;Cutter, 2013).Samples were collected using a trace metal clean rosette (TMR, model 1018, General Oceanics) equipped with twelve 10 L externally closing Teflon-lined Niskin-1010X bottles mounted on a polyurethane powder-coated aluminium frame especially designed for trace metal work (Bowie et al., 2009).Seawater was sub-sampled for dFe via a Teflon tap connected to acid cleaned 0.2 µm filter cartridges (Pall Acropak® and Sartorius Sartrobran® 300).Acid cleaned low density polyethylene bottles (60 mL) were rinsed 3 times with ∼ 20 mL of seawater before final sample collection.Dissolved Fe samples were acidified to pH ∼ 2 using concentrated ultrapure hydrochloric acid (Seastar Baseline, HCl).The sample bottles were then double bagged and stored at ambient temperature in the dark until analysis.The Introduction

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Full shallowest sample was collected at 15 m depth in order to avoid contamination from the ship.Samples were collected off plateau to a depth of 1300 m.Dissolved Fe was analysed on board at least 24 h after collection by flow injection analysis (FIA) with online solid phase extraction onto 8-hydroxyquinoline (8-HQ) resin and chemiluminescence detection, following a method adapted from Obata et al. (1993) (Sarthou et al., 2003).All analyses were conducted inside a class 100 laminar flow hood within a containerised clean laboratory, using high-efficiency particulate air (HEPA) filters.During the cruise, representative ammonium acetate buffer and HCl blanks were consistently below the detection limit (0.017±0.012 nmol L −1 , n = 22), and therefore, the system was deemed suitable for open ocean seawater analysis (Johnson et al., 2007).Each sample was analysed in triplicate with an average precision of 4.8 % (n = 149).The North Pacific SAFe Surface (SAFe S) (0.094 ± 0.003 nmol L −1 , n = 3) and SAFe Deep D2 (0.95 ± 0.05 nmol L −1 , n = 3) reference samples were measured for dFe and the results were in excellent agreement with the consensus values (S1 = 0.095 ± 0.008 nmol L −1 , n = 3 and D2 = 0.95 ± 0.24 nmol L −1 , n = 3 (Johnson et al., 2007).Temperature, salinity, oxygen and beam attenuation data were retrieved from the CTD sensors.We used the data from the CTD casts that were deployed just before or just after our TMR casts.

Clustering of stations
The presentation and discussion of results are organised by clusters, which were defined considering the hydrography and the complex regional circulation.Water masses were identified using T-S diagrams (Fig. 2).
Cluster 1 includes TEW-1 and TEW-2 stations located at the north eastern flank of Kerguelen Island and North of the Polar Front (PF), with shallow waters (∼ 85 m bot-Introduction

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Full tom depth), low salinity (33.6-33.8)and low density (< 27.0 kg m −3 ).Below the surface mixed layer (SML), the water masses can be defined as subsurface (shelf) waters.Cluster 2 includes stations located above the central part of the Kerguelen Plateau (A3-1, A3-2, G-1, and TEW-3, bottom depths lower than 600 m), and located south of the PF, with a minimum of temperature around 200 m.At A3-1, stratification had not yet started and surface water temperature was low (∼ 1.7 • C) and typical of winter conditions.Stations A3-2 and G-1 presented similar water masses (Fig. 2).The SMLs were observed down to 125 and 65 m, respectively.Below, Winter Water (WW) is encountered with temperatures around 1.7 • C at 225 m and 115-210 m, respectively.The inclusion of TEW-3 in cluster 2 is debatable given its location at the plateau edge.
Indeed, although TEW-3 can be considered as south of the PF, its location within the Polar Front Jet is likely more correct.However, a structure comparable to A3-1, A3-2 and G-1 was observed below the surface waters with a WW temperature just below 2 • C. East of Kerguelen plateau, the PF presents a permanent meander (Park et al., 2014).
This meander delimits a region with a complex circulation including stations TEW-4, E-2, TEW-5, E-3, E-4W-2, and E-5), and is defined as cluster 3.All these stations showed very similar T-S profiles (Fig. 2).In the upper meters, the Surface Water (SW) was sampled, but due to the decrease of the mixed layer depth (MLD) and progression into summer, warmer water was sampled during the final station (station E-5).
Below the SW, a subsurface temperature minimum (∼ 1.7-1.8 • C) was observed between 170 and 220 m, characteristic of the WW (Fig. 2).Below, the oxygen minimum around 600-800 m (175 µmol kg deeper, at 170 m (TEW-7) and 290 m (F-L) (Fig. 2).Below the AAIW, the UCDW and the LCDW were encountered.Station R-2, located in the HNLC area, stands on its own in cluster 5.A salinity minimum (33.78) and a surface temperature maximum (2.0 • C) were observed in the upper 100 m, which is characteristic of the SW (Fig. 2).At 200 m, the temperature minimum (1.6 • C) was indicative of WW.The oxygen minimum (170 µmol kg −1 ) defined the upper circumpolar deep water (UCDW).Deeper in the water column (below 1300 m), the salinity increased towards a salinity maximum (∼ 34.73) indicating the presence of the lower circumpolar deep water (LCDW).

A general overview of dFe distributions
Median dFe concentrations for the different water masses and clusters (2 to 5) are plotted on Fig. 3.
In the surface waters, near-coastal stations presented the highest concentrations (2.10 ± 0.77 nmol L −1 ).When considering the other stations, the lowest sea-surface concentrations were found at station R-2 (0.09 ± 0.01 nmol L −1 ), while the highest were observed in cluster 4 (0.26 ± 0.09 nmol L −1 ).If we compare our results in the surface waters to the dataset compiled by Tagliabue et al. (2012), R-2 had lower values than the mean value of the Indian-Antarctic zone (0.43 ± 0.51 nmol L 1 ), whereas the mean value in cluster 4 was higher than the mean value of the Indian-Subantarctic zone (0.23 ± 0.20 nmol L −1 ).Tagliabue et al. (2012) suggested that the higher mean surface value in the Antarctic than in the Subantarctic zone could be due to a lower biological activity.In our study, the biological activity was much lower at station R-2 (Antarctic zone) than in cluster 4 (Subantarctic zone).Indeed the highest integrated concentrations over 200 m for chlorophyll a (Chl a) were observed in cluster 4 (223-354 mg m −2 ) (Lasbleiz et al., 2014).So, the lower dFe value at R-2 compared to cluster 4 might not reflect differences in biological activity but, rather, in Fe inputs (see below).At intermediate depths, median dFe were not significantly different among clusters 2, 3, and 5 in the WW (ANOVA, F = 0.54, p = 0.5904), suggesting that the whole area Introduction

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Full presented similar dFe concentrations at the surface during winter time.In cluster 4, dFe in the AAIW presented relatively high values (0.46 ± 0.06 nmol L −1 ), consistent with the high dFe values in the surface waters of the Antarctic zone (Tagliabue et al., 2012).
This difference was attributed to both higher ligand concentrations at depth (Thuróczy et al., 2011) and deep Fe inputs such as hydrothermal activity, with the greatest input in the Indian Subantarctic region (Tagliabue et al., 2012).

Coastal area (cluster 1)
TEW-1 and TEW-2 stations were sampled on the same day in order to provide a nearshore data set of dFe.Stations TEW-1 and TEW-2 were in shallow waters approximately 10 and 75 km away from Hillsborough Bay coast, respectively.Median profiles of dFe, with minimum and maximum values in this cluster, are shown on Fig. 4a.At station TEW-1, dFe concentrations were high (> 1.8 nmol L −1 , Table 1), and increased steadily from 15 m depth (1.82 nmol L 1 ) to 50 m depth (2.58 nmol L −1 ).
Close to the seafloor a sharp increase at 62 m depth (3.82 nmol L 1 ) was measured.These are the highest values measured during this study.At TEW-2, dFe concentrations were lower than at TEW-1, increasing from 1.26 nmol L −1 in surface waters to 1.82 nmol L −1 at 62 m depth.

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Full were 5 to 10 fold higher (22.6 nmol L −1 ).This discrepancy was already discussed (Blain et al., 2008) and likely partly due to methodological differences (0.4 µm filtration, nitric acid acidification and 2-year storage).The elevated dFe concentrations observed at near shore sites are most certainly indicative of Fe sourced from the islands; a feature clearly evident during the present study and illustrated in Fig. 5.This source is most likely a combination of direct island runoff, glacial melt and resuspended sediments.High particle loads (as estimated by beam attenuation data) were encountered throughout the water column of TEW-1 and TEW-2, with higher concentrations at TEW-1, especially at 10 m depth and close to the seafloor (Fig. 6).Low salinities 33.63 ± 0.01, n = 61) were also measured at TEW-1, which corroborates our hypothesis of direct island runoff and/or glacial melt inputs.Moreover, the Ampère Glacier which is the largest glacier from the Cook icecap (about 500 km 2 ), thins rapidly over the last decade (Berthier et al., 2009), especially towards the east of the icecap, up to 1.5 m per year.This discharge includes small basaltderived particles (Frenot et al., 1995) (Raiswell et al., 2010;Raiswell, 2011) and LSi being weathered from silicate rich minerals (Si O 2 , Doucet et al., 2005).Sedimentary inputs (e.g.Johnson et al., 1999;Elrod et al., 2004;Chase et al., 2005;Lam et al., 2006;Planquette et al., 2011;Homoky et al., 2013;Marsay et al., 2014) could also explain the increased dFe concentrations encountered at both stations close to the seafloor (3.82 and 1.82 nmol L −1 at Stations TEW-1 and TEW-2, respectively).
Unfortunately, particulate Fe (pFe) concentrations were not measured at these nearcoastal waters, making it difficult to confirm the dissolution of pFe (oxyhydr)oxides originating from pore water reduced Fe species (Shaw et al., 2011).However, the fact that Introduction

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Full the beam attenuation increased close to the seafloor of station TEW-1 (Fig. 6) and that high dMn concentrations at TEW-1 (5.40 nmol L −1 ) and TEW-2 (1.92 nmol L −1 ) were also measured (Quéroué et al., unpublished data) strongly supports this hypothesis.Dissolved Fe concentrations in the water column may not only reflect sedimentary inputs but also inputs from remineralization processes.However, since deciphering remineralization from sedimentary inputs at shallow stations is difficult, remineralization process will only be discussed for clusters 3, 4, and 5.
Over the Kerguelen Plateau, 24 shelf stations have been investigated during several cruises (Table 2).The highest concentrations were measured during ANTARES3 (∼ 6 nmol L −1 ) in the northern part of the Kerguelen Plateau at a station located 76 km away from the shore (Station K4, 40 m).The lowest concentrations were measured during KEOPS1 (0.05 nmol L −1 ) within the top 200 m of water.Above 100 m, lower concentrations were observed during KEOPS1 compared to KEOPS2 (Table 2).This can be explained by a more advanced phytoplankton bloom during KEOPS1 (summer conditions) than KEOPS2 (spring conditions).In surface waters, dFe concentrations measured during KEOPS2 were of similar magnitude than those measured in the vicinity of the South Shetland Islands (Nielsdóttir et al., 2012;Table 2).
A deep Fe-enriched reservoir was also observed above the Kerguelen Plateau during KEOPS1 (Blain et al., 2008;Chever et al., 2010).Non reductive dissolution of resuspended sediments is a potentially important source of dFe as observed at near-coastal Introduction

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The variability of the deep dFe concentrations above the Plateau may be due to variability in sedimentary inputs in this highly dynamic region.All stations from this cluster except station TEW-3 had high beam attenuation values close to the seafloor, which most likely indicates the presence of resuspended particles at these depths (98 % for TEW-3 vs. 92-97 % for the other three stations, Fig. 6).Marsay et al. (2014) performed a very detailed sampling of near-bottom waters for dFe over the Ross Sea shelf and showed that dFe concentrations displayed a quasi-exponential increase with depth, with a pronounced gradient towards the seafloor.When plotting our dFe data as a function of height above the seafloor, we also observed an exponential increase with depth (Fig. 7).Clearly, TEW-3 dFe data were in the lower range of dFe vs. height above the seafloor.
Diffusion from pore waters is another important possible source of Fe for the BBL (Elrod et al., 2004).When sediment receives large amount of organic carbon, it is covered by a fluff layer composed mainly of broken cells, as observed during KEOPS1 for stations above the Plateau (Armand et al., 2008).Diagenesis then produces suboxic/anoxic conditions, which are key conditions to mobilize Fe because of the high solubility of the reduced Fe(II) form (Walsh et al., 1988).Anoxic conditions were observed 2 cm below the sediment surface at the A3 stations (P.Anschutz, personal communication, 2014) suggesting that, in pore waters above the plateau, Fe could be in the reduced form and diffuse into the bottom water column.Unfortunately, no pore water measurements were performed at G-1 and TEW-3 stations.For all the stations in cluster 2, dFe minima were observed in the SML, which could reflect biological uptake and/or particle scavenging.A significant decrease was observed in dFe concentrations in the SML between A3-1 (0.33±0.06 nmol L −1 ) and A3-2 (0.15 ± 0.02 nmol L −1 ) (t test, p < 0.05).The first visit to site A3 (A3-1, 20 October) was characteristic of early bloom conditions, while during the second visit 28 days later (A3-Introduction

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Full 2, 17 November), a large diatom bloom was observed (Lasbleiz et al., 2014).Moreover, based on the beam attenuation profiles, A3-2 seemed to have more particles (likely of biogenic origin) than A3-1 within the top 200 m.This is confirmed by the fact that at these depths, the Fe : Al ratio at A3-2 is higher than A3-1 and in all cases, well above the crustal ratios.This may indicate that more pFe of biogenic origin was present at A3-2 than at A3-1 (van der Merwe et al., 2014), and confirm an increased biological uptake at A3-2 compared to A3-1.Between the two visits, integrated dFe concentrations over 200 m decreased while the bloom was developing (62.6 vs. 28.1 µmol m −2 ), associated with an increase in concentrations of Chl a (106.2mg m −2 vs. 371.7 mg m −2 ) and particulate organic carbon (POC) (from 1259 to 2267 mmol C m −2 ) (Lasbleiz et al., 2014).
The decrease in dFe stock represents ∼ 35 % of the winter stock, defined as the dFe concentration in the WW (0.51 nmol L −1 ) multiplied by the depth of the temperature minimum (200 m) (Blain et al., 2007).Taking into account the decrease in dFe stock and the increase in POC stock, the Fe : C ratio of the biomass that developed between the two visits at A3 can be estimated to equal 34 µmol mol −1 , a ratio consistent with literature values for diatoms in Fe-replete waters of the Southern Ocean (Sunda and Huntsman, 1995;Sunda, 1997;Twining et al., 2004;Sarthou et al., 2005).Although this is a rough estimate which does not take into account any additional inputs or removal processes, this result indicates that the dFe decrease between A3-1 and A3-2 could be due, at least partly, to biological uptake.

Recirculation area (cluster 3)
Median profiles of dFe, with minimum and maximum values in this cluster, are shown on Fig. 4c.A two-way ANOVA, based on depth and location (i.e.station), showed that location had a significant effect on dFe variability (F = 24.92,df = 5, P < 0.01).

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Full depth (∼ 0.37-0.39nmol L −1 , at 1300 m) (Table 1).A dFe maximum was observed at intermediate depths (500-600 m, 0.34-0.43nmol L −1 ).The dFe profile at station TEW-4 is homogeneous below 150 m.The dFe maximum at 600 m is 0.39 nmol L −1 and, at 1300 m, dFe reaches 0.42 nmol L −1 .Concentrations at stations TEW-5 and E-4W-2 were close to those at stations TEW-4 in the upper 150 m (0.11-0.22 nmol L −1 ), but these stations showed higher concen- ).This sampling depth was located less than 200 m away from the seafloor and was associated with an increase in beam attenuation (see Fig. 6), which indicated a high number of particles and potential sedimentary inputs.
In this cluster, dFe concentrations were comparable to concentrations measured at stations off Crozet plateau that were not under HNLC conditions (Planquette et al., 2007).However during KEOPS2, water column dFe concentrations were lower than those observed during ANTARES 3 and in the South Shetland Islands sites, most likely due to the greater distance of the KEOPS2 stations from the shore (Table 2).
The maximum sea-surface dFe concentrations at stations TEW-4, E-4W-2, and E-3, may be indicative of atmospheric inputs.In the Southern Ocean, atmospheric inputs are considered to be small compared to the Northern Hemisphere because of its remoteness from land masses (Jickells et al., 2005;Mahowald et al., 2005;Wagener et al., 2008).However, a recent study performed in the Kerguelen region showed that atmospheric deposition fluxes have historically been underestimated (Heimburger et al., 2013).The NOAA HYSPLIT 1-day backward trajectory atmospheric model supports the hypothesis of an atmospheric input from the Kerguelen Island for stations Introduction

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Full E-4W-2 and E-3, as it shows that air masses flowed over the Island the day before we sampled these stations (Fig. 8).However no particulate aluminium (pAl, a proxy for atmospheric inputs) surface enrichment in the recirculation area was observed during the study (van der Merwe et al., 2014), suggesting that air-masses were not carrying enough aerosols to enhance pAl surface concentrations.For stations TEW-4, the 1-day and 5-day backward trajectories did not show any evidence of air masses flowing over potentially dry dust emission areas, suggesting other sources of Fe at seasurface (Fig. 8).Significant 224 Ra and 223 Ra activities were detected in offshore waters south of the Polar Front (Sanial et al., 2014).These observations clearly indicated that dissolved sediment-derived inputs of Ra can be rapidly transferred towards offshore waters.These Ra-enriched waters could also be enriched with dissolved sedimentderived Fe.Within the waters characterised by an oxygen minimum, remineralization of sinking organic matter may exert a primary control on dFe distribution.To assess this hypothesis, we looked at the relationship between dFe and the apparent oxygen utilisation (AOU), from the start of the oxycline (∼ 150-200 m) to the bottom of the UCDW (700-1100 m).In these waters, the AOU indicates the amount of oxygen that has been consumed during remineralization since the waters left the surface, whereas dFe concentration equals the preformed dFe plus any dFe released from remineralization, minus any dFe scavenged by particles (Hatta et al., 2014).Dissolved Fe concentrations showed a significant positive correlation with the AOU for all the stations in the recirculation area (ANOVA, p < 0.01), meaning that remineralization was likely a significant source of dFe at these depths.Station E-3 clearly presented a different behaviour compared to the other stations of cluster 3 (Fig. 9).Indeed, although the slopes were not significantly different (0.0016 ± 0.0003 mmol mol −1 for E-3 and 0.0018±0.0002mmol mol −1 for all stations except E-3, ANOVA, p > 0.1), the intercepts were different (0.26±0.05 nmol L −1 for E-3 and 0.08±0.03nmol L −1 for all the other stations, ANOVA, p < 0.01).This suggests that a pre-formed dFe signal was present at E-3, which could explain the highest dFe values observed at this station.Using this Introduction

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Full slope of the dFe : AOU relationship and a modified oxygen consumption ratio of 1.6 moles O 2 per mole of carbon remineralized (Martin et al., 1987), a net Fe : C ratio for the remineralization process equal to 2.6-2.9 µmol mol −1 was estimated.This ratio is very similar to Fe : C ratios of Fe-limited diatoms from culture studies and in-situ Southern Ocean data (Martin et al., 1987;Sunda, 1997;Sarthou et al., 2005).

North Polar Front stations (cluster 4)
Stations TEW-7 and F-L were located northeast of the Polar Front, approximately 270 and 313 km northeast of Kerguelen Island with bottom depths of 2500 and 2700 m, respectively.These stations presented comparable vertical profiles (Fig. 4d).In the upper 50 m, dFe concentrations were depleted at 0.22 and 0.17 nmol L −1 (at 40 m at station TEW-7, and 35 m at station F-L, respectively) and then gradually increased within the mesopelagic zone to finally reach 0.59 nmol L −1 at 1300 m depth (Station TEW-7) and 0.67 nmol L −1 at 1000 m depth (Station F-L).
During ANTARES 3, station K14, which was also sampled northeast of the Polar Front, exhibited higher values than those measured during KEOPS2, especially at the surface (4.11 nmol L −1 at 40 m depth).This was interpreted as the result of a mixing between SASW and water masses coming from the West and enriched by sweeping the plateau (Bucciarelli et al., 2001), at a time when no significant sink occurred (beginning of spring, ∼ 0.4 µg L −1 of Chl a).
During KEOPS2, however, the decrease in dFe concentration within the SASW, This biological uptake is also reflected in the composition of suspended particles (van der Merwe et al., 2014).In surface waters, higher pFe:pAl elemental ratios were observed compared to those from the base of the SML, which is indicative of a conversion Introduction

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Full of dFe into biogenic pFe.However, compared to the less productive recirculation area (see Sect. 3.5), the surface dFe concentrations are higher by 0.1 nmol L −1 .This could be explained by the fact that, like during ANTARES 3, a portion of the water masses found at TEW-7 and F-L likely interacted more with both the plateau and shallow coastal waters of Kerguelen Island than the water masses from the recirculation area.This hypothesis is supported by the general circulation in this region (Park et al., 2014) that shows that water masses are carried northwards between the island and the recirculation area and finally looped back east of the recirculation area.A Lagrangian model of Fe transport based on altimetry (d 'Ovidio et al., 2014) also confirms that the water at F-L and TEW-7 are mainly coming from the northern part of plateau.
As for the recirculation area, dFe concentrations in the mesopelagic zone may also reflect remineralization processes.Dissolved Fe concentrations present a significant positive relationship with AOU for both stations (dFe = 0.0014 ± 0.0003 × AOU + 0.32 ± 0.03, n = 5, r 2 = 90 %, p < 0.05, and dFe = 0.0020±0.0005×AOU+0.24±0.07,n = 7, r 2 = 74 %, p < 0.05 for stations TEW-7 and F-L, respectively).The two slopes are not significantly different (ANOVA, p > 0.1).When combining the two data sets (Fig. 9), the slope is also not significantly different from the slope in the recirculation area (ANOVA, p > 0.1), suggesting that Fe and C are remineralized at the same rates in both regions (Fe : C ∼ 2 µmol mol −1 ).However, the intercept is significantly different from the intercept of the recirculation area (without the station E-3, see above) and from zero (ANOVA, p < 0.01), suggesting the presence of preformed Fe in these waters.
The KEOPS, CROZEX and South Shetland Islands studies (Planquette et al., 2007;Blain et al., 2008;Nielsdóttir et al., 2012) presented comparable ranges of dFe at open ocean stations (Table 2).Dissolved Fe concentrations at R-2 were similar to those Introduction

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Full observed during KEOPS1 at C11 and the Kerfix station within the upper 170 m of the water column, but also between 700 and 1300 m (Blain et al., 2008).However, dFe concentrations were up to 6.5 fold higher between 200 and 500 m at R-2 compared to C-11 and Kerfix, despite the close proximity of Kerfix and R-2.While sea-surface lithogenic silica (LSi) concentrations (Lasbleiz et al., 2014) were low at station R-2 (< 0.042 µmol L −1 ), they were maximum at 500 m depth (0.12 µmol L −1 ).Particulate Fe, manganese and aluminium (fraction between 1 and 55 µm) enrichments were also observed at 500 m (van der Merwe et al., 2014).These authors also observed a unique particulate trace metal composition signature at this station, which could originate from the Leclaire rise, contrasting with the basaltic signature observed above the Kerguelen Plateau (Doucet et al., 2005).The Leclaire Rise is a remarkable oceanic feature that consists of a submerged volcano with an area of 6500 km 2 , with the shallowest depth up to 100 m.It is located 75 km north west of R-2 and could release dissolved and particulate material.Similarly to clusters 3 and 4, remineralization may also partly explain dFe concentrations in the mesopelagic zone (dFe = 0.0012 ± 0.0002 × AOU + 0.22 ± 0.02, n = 6, r 2 = 91.8%,p < 0.01).Fe and C are also remineralized at the same rates as in clusters 3 and 4 (ANOVA, p > 0.1) and the intercept, significantly different from zero (ANOVA, p < 0.01), confirms the hypothesis of dFe sedimentary inputs at this station.tilised surface waters of the eastern part of the studied area.Furthermore, filaments crossing the PF allowed a more direct natural Fe fertilisation of surface water in the recirculation area.Due to variable water mass origin and variable horizontal advection mechanism (along or across the PF), the recirculation area evidenced strong dFe concentration variability.The PF is an important Southern Ocean feature that should not be neglected with regards to Southern Ocean fertilisation offshore from the Kerguelen Plateau through fast lateral Fe transport from the north of the Kerguelen Plateau.

BGD Introduction
Full  Full  Full ) over the East-West transect.The PF position is indicated with black dashed lines.Stations TEW-1, TEW-2, TEW-3, TEW-4, E-2, TEW-5, TEW-7 and F-L were included in this section as they were sampled consecutively in a short time period (7 days) (Table 1).
Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | −1 ) can be attributed to the Upper Circumpolar Deep Water (UCDW).Deeper in the water column (below 1300 m), the salinity increased towards a salinity maximum (∼ 34.75) indicating the presence of the Lower Circumpolar Deep Water (LCDW).Stations TEW-7 and F-L (cluster 4), located north of the PF and east of the Plateau presented the warmest surface waters of the study (4.2 • C) characteristic of the Sub-Antarctic Surface Water (SASW).The Antarctic Intermediate Water (AAIW) occurred Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | trations at intermediate depths (150-200 m, 0.21-0.30nmol L −1 ).Below 150-200 m, concentrations reached values of ∼ 0.4 nmol L −1 , except for the deepest value at station E-4W-2 (0.61 ± 0.02 nmol L −1 , 1100 m Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | around 35-40 m depth, can result from biological uptake.This is suggested by the high biomass reported at stations TEW-7 and F-L(Lasbleiz et al., 2014), with the highest integrated concentrations over 200 m for Chl a (> 220 mg m −2 ), biogenic silica (> 300 mmol Si m −2 ), particulate organic carbon (> 1200 mmol C m −2 ), particulate organic nitrogen (> 200 mmol N m −2 ), and particulate organic phosphorus (> 30 mmol P m −2 ).
Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | over the Kerguelen Plateau allowed new insight into dFe sources and internal cycling.Atmospheric inputs were negligible during the KEOPS2 cruise while direct runoff, glacial and sedimentary inputs can be considered as important sources of dFe in the vicinity of Kerguelen Island.Remineralization of sinking particles can explain the high concentrations of dFe in intermediate waters offshore.The strong jet of the PF was enriched with dFe from the north of the plateau as it flowed northward close to Kerguelen Island and later eastward to loop back into the recirculation area.This fer-Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper |