Iron (Fe) is an essential trace element that shapes ocean biogeochemical cycles. Photosynthetic primary productivity and nitrogen fixation in the surface ocean depend on the supply of Fe from lithogenic sources. Predicting the extent to which primary productivity is limited by Fe supply is dependent on our understanding of Fe sources and sinks in the open ocean Published by Copernicus Publications on behalf of the European Geosciences Union. (Tagliabue et al., 2017). This is particularly important in Felimited regions such as the Southern Ocean, where changes in the supply of Fe to the surface ocean may dramatically shift the Earth's atmospheric CO2 content (Gottschalk et al., 2019) and where hydrothermal vents may play an important role as a source of Fe (Tagliabue et al., 2010;Tagliabue and Resing, 2016;Ardyna et al., 2019;Weber, 2020;Schine et al., 2021).
The magnitude and importance of Fe supplied from different sources (i.e. glaciers, rivers, aerosols, sediments and hydrothermal vents) is an ongoing subject of debate. In the last 15 years, the role of hydrothermal vents in supplying Fe to the deep ocean, that may subsequently upwell in the Southern Ocean, has received significant attention, with questions surrounding the biogeochemical processes that could facilitate long-range transport of Fe from the seafloor (Toner et al., 2009;Tagliabue et al., 2010;Yucel et al., 2011;Saito et al., 2013;Resing et al., 2015;Fitzsimmons et al., 2017). In order to examine the hydrothermal flux of Fe to the deep ocean, changes in Fe concentration are frequently compared to excess helium (xs 3 He), derived from 3 He, which is an inert tracer of hydrothermal activity (Lupton and Craig, 1981;Wu et al., 2011;Saito et al., 2013;Resing et al., 2015;Fitzsimmons et al., 2017). Primordial helium (He) degasses from the Earth's mantle and as a result hydrothermal fluids are enriched in 3 He relative to background seawater (Lupton et al., 1977). As He is an unreactive dissolved gas, it is an ideal source tracer for hydrothermal plumes. The ratio of Fe to xs 3 He has been used as a basis for modelling the impact of hydrothermal Fe on surface ocean primary productivity and the associated carbon export (Tagliabue et al., 2010).
Recent field studies have found a linear relationship between dissolved Fe (dFe) and xs 3 He, interpreted as conservative behaviour of Fe. In some cases, Fe appears to behave conservatively over thousands of kilometres, while in others the conservative relationship of dFe=xs 3 He is only apparent over the ridge (Saito et al., 2013;Resing et al., 2015). The observation of conservative behaviour was unexpected for a reactive metal such as Fe, as previous studies working at the < 1 km scale had estimated that up to 90 % of Fe released from seafloor vents precipitates as Fe-sulfide and Feoxyhydroxide mineral particles, as the Fe and hydrogen sulfide (H2S) rich vent fluids are released into cold, welloxygenated, deep ocean waters (German et al., 1991;Field and Sherrell, 2000;Severmann et al., 2004). It is the remaining hydrothermal Fe that does not form fast settling mineral particles that is ultimately exported, as an effective flux to the deep ocean of fine colloidal particles and/or organic Fe complexes (Bennett et al., 2008;Hawkes et al., 2013;Kleint et al., 2016). It is thought that the off-axis linear relationship of dFe with xs 3 He arises because dFe species formed in the plume exhibit relatively unreactive behaviour (Bennett et al., 2008;Yucel et al., 2011). An alternative hypothesis is that Fe is added to the dissolved fraction continuously by the dissolution/disaggregation of larger particulate phases as the plume Biogeosciences, 20, 405-420, 2023 disperses (Fitzsimmons et al., 2017), at a rate that maintains the dFe=xs 3 He ratio, giving the appearance of conservative behaviour.
Studies that have used xs 3 He as a tool for understanding hydrothermal Fe have typically sampled at the basin scale whereas studies focusing on the < 1 km scale tend to use other shorter lived tracers such as dissolved manganese (dMn) (James and Elderfield, 1996;Field and Sherrell, 2000;Lough et al., 2017Lough et al., , 2019b, a), a), magnesium (Findlay et al., 2015) or rare earth element anomalies (Severmann et al., 2004). Furthermore, the Fe and He sampled at the basin scale may represent an amalgamation of several vent sources from a ridge or several ridge crests whereas the studies at < 1 km scale focus on Fe released from individual or at least fewer vent sites. Different vent sites are known to display substantial variations in dFe=xs 3 He ratios (Table 1) (Tagliabue et al., 2010) but the extent to which sampling scale, strategy and use of different tracers affects the interpretation of the effective hydrothermal iron flux is a barrier to further refining the conceptual and numerical models we rely on for larger scale integration.
To address this knowledge gap, this study sampled hydrothermal plumes along the same ridge from multiple vent sources at a scale of 10's of km's, using both short-lived (dMn, weeks; Cowen et al., 1990;Trocine and Trefry, 1988;Field and Sherrell, 2000;Massoth et al., 1994;Lavelle et al., 1992) and long-lived (xs 3 He) as conservative tracers. We examined the variability in dFe=xs 3 He produced from different methods of estimation (Saito et al., 2013;Resing et al., 2015;Fitzsimmons et al., 2017) in plumes originating from four vent sites along the northern part of the Mid-Atlantic Ridge (MAR) (GEOTRACES GA13 section). These vents cover a range of geological settings, plume dFe concentrations and importantly Fe=H2S ratios, which have been shown to correlate with colloid concentration in nascent plumes (i.e. 1-2 m above the vents) (Gartman et al., 2014). Calculated Fe=xs 3 He values are used to compare the separation of Fe between particulate-dissolved fractions for the TAG and Rainbow plumes as they disperse within the ridge valley.
The UK GEOTRACES GA13 voyage sailed along the northern Mid-Atlantic Ridge (MAR) during its passage from Southampton, UK, to Guadeloupe, France (22 December 2017-27 January 2018). The fieldwork campaign sampled the rising buoyant and neutrally-buoyant hydrothermal plumes of a set of known hydrothermal vent sites along the northern MAR (Fig. 1). At each site, hydrothermal plumes were detected using a combination of sensors. A traditional CTD (conductivity-temperature-depth) package (Seabird 911) was used to identify anomalous changes in https://doi.org/10.5194/bg-20-405-2023 MORB is mid-ocean ridge basalt; E-MORB is enriched mid-ocean ridge basalt. Endmember vent fluid data from published studies are calculated by extrapolating to 0 Mg concentration (Douville et al., 2002). salinity and temperature relative to background N. Atlantic waters. Bespoke light scattering (LSS) and oxidation reduction potential (ORP) sensors were used to identify particle dense plumes and young plume waters containing reducing chemical species (i.e. Fe 2C , HS and H2). Sampling casts were repeated over the TAG and Rainbow sites to examine the reproducibility of plume sampling relative to tidal forces and bottom currents that shift the plumes position in the water column.
As part of the GEOTRACES programme, Fe and Mn were sampled according to the detailed procedures described previously (Cutter et al., 2010) that we briefly outline below. However, He and additional Mn samples were collected from a standard (stainless steel) rosette, and we show that Mn can be sampled cleanly without a clean lab or a titanium rosette frame (Fig. S1 in the Supplement). https://doi.org/10.5194/bg-20-405-2023 Helium sampling methods followed those described in Jenkins et al. (2015b). Briefly, 30 in: of copper pipe was rinsed several times through with seawater collected from Niskin bottles (Ocean Test Equipment) on the standard rosette, using plastic tubing (TYGON). Once all air bubbles had been removed, the copper tubing was crimped at both ends to seal the pipe and sent for analysis at Woods Hole Oceanographic Institution (USA). The 3 He isotope anomaly is defined relative to an atmospheric standard in Eq. (1) with 3 He expressed in percent. The xs 3 He represents the mantle derived 3 He that is approxi-mate to the non-atmospheric 3 He over saturation. The He isotope ratio anomaly 1.384 10 6 is the atmospheric 3 He= 4 He ratio, THeU is the molar concentration of He and 1.7 is the solubility equilibrium constant (Jenkins et al., 2015a).
Seawater samples for trace metal analysis were collected using a titanium-frame CTD with 24 trace metal clean, 10 L, Teflon-coated Niskin bottles (Ocean Test Equipment) deployed on a plasma rope. A Sartobran 300 (Sartorius) filter capsule (0.2 μm) was used to filter seawater into clean lowdensity polyethylene (LDPE) bottles for dissolved trace metals. A separate aliquot of 0.2 μm filtered seawater was further filtered through 0.02 μm syringe filters (Anotop, Whatman) into LDPE bottles for soluble Fe (sFe) (Ussher et al., 2010). Unfiltered seawater samples were collected for total dissolvable (TD) metals. All samples were acidified onboard to 0.024 M (UpA HCl, ROMIL).
Dissolved and total dissolvable samples were analysed onshore for Fe and Mn by ICP-MS (Thermo Scientific, Element X R ) using a standard addition method (Lough et al., 2017). Certified values for GEOTRACES reference material D2 (0.96 nM Fe and 0.36 nM Mn) compared well with our measured values of 0.95 0.06 nM Fe and 0.34 0.03 nM Mn (n D 6). ICP-MS analysis of 2009 GEOTRACES coastal surface seawater (GSC) reference material (measured GSC: 2.04 0.03 nM Mn and 1.48 0.13 nM Fe n D 3) also com-pared well with the preliminary consensus values (GSC 2.18 0.08 nM Mn, 1.54 0.12 nM Fe). In-house standards with higher concentrations of Fe and Mn in the concentra-tion range of hydrothermal samples were measured repeat-edly with relative standard deviations of 6 % for Mn and 7 % for Fe. Soluble Fe was measured by flow injection analy-sis with chemiluminescence detection (Obata et al., 1993;Kunde et al., 2019a) with measured values of 0.94 0.04 (n D 6) for D2 reference material. Measurements of 2009 GEOTRACES Pacific surface seawater (GSP) and GSC reference materials using flow injection also agree with the preliminary consensus values (consensus: GSP 0.16 0.05, GSC 1.54 0.12 nM, measured GSP 0.15 0.01 nM n D 7, GSC 1.52 0.06, n D 10). Colloidal Fe (cFe) is opera-tionally defined as the difference between dFe (< 0.2 μm) and sFe (< 0.02 μm). Apparent particulate Fe (appPFe) is fur-ther operationally defined as the difference between TDFe (unfiltered) and dFe (< 0.2 μm).
Dissolved Mn samples from the standard rosette were analysed at sea by flow injection analysis with in-line pre-concentration on resin-immobilised 8-hydroxyquinoline and colorimetric detection (Resing and Mottl, 1992). The SAFe reference samples were analysed to determine the accuracy and precision of the method giving results for SAFe S, 0. The grey shaded area indicates where there are samples taken at the same depth for xs 3 He and dFe. Notice that at the same depth for different casts dFe is increasing with depth whilst xs 3 He is decreasing with depth due to the offset in the plume anomaly.
Samples collected for helium analysis were quantitatively gas-extracted from Cu sampling pipes into 30 mL glass vials and analysed for helium isotope ratios. Analysis was conducted using a triple quadrupole mass filter mass spectrometer (HIDEN P/N PCI 1000 1.2HAL/3F 1301-9 PIC type 570,309). Measurements have a precision of 0.1 % as determined by repeat measurements of gas standards, all measurements of gas abundances are references to a marine atmospheric standard. Full details of helium gas analysis are described in (Jenkins et al., 2019).
3.1 Quantifying Fe=xs 3 He ratios A drawback to using xs 3 He as a tracer of hydrothermal Fe is that Fe, under GEOTRACES protocols, is sampled using trace metal clean bottles mounted on a trace metal clean rosette, while He is sampled separately from a standard rosette to avoid metal contamination from Cu tubes used to collect 3 He. At the Fe concentrations observed close to the vent sites, such caution is likely unwarranted; however, to trace the full reach of a hydrothermal plume, trace concentrations 0.1 nM above background concentrations need to be detected. The best way to guarantee this resolution is to follow GEOTRACES trace metal clean sampling protocols; as a result, Fe and 3 He are never sampled from the same sampling bottle, same cast or at the same time (Fig. 2). Furthermore, sampling 3 He requires the Cu pipes to be flushed with co- https://doi.org/10.5194/bg-20-405-2023 pious amounts of sample water, which would leave limited water available from the trace metal clean rosette to sample for trace metal concentrations, their isotopes and chemical speciation (samples collected during GA13 that will be discussed in future publications). Given the complex physical dynamics of a dispersing plume within a ridge valley (Vic et al., 2018;Lahaye et al., 2019), sampling the same point in the plume twice is nearly impossible. Here we apply the following three different ways of calculating dFe=xs 3 He to assess which best represent the plume: https://doi.org/10.5194/bg-20-405-2023 1. Plume integration method. Integrate dFe and xs 3 He data across the plume depth for samples taken from each cast (e.g. trace metal clean and standard rosette) (Resing et al., 2015;Fitzsimmons et al., 2017). This approach assumes that multiple depths through the plume have been sampled on both casts and are representative of a vertical cross-section of the plume. In a sampling scenario such as that shown in Fig. 2 the plume integration approach is likely to lead to unrealistic dFe=xs 3 He ratios and is more suited to an off-axis setting where the plume position is less variable.
ND denotes no data, either no dMn data available from the trace metal rosette or no 3 He data available from the standard rosette at the equivalent depth. The concentration depth profiles used for the integration at each station are shown in the supplementary figures.
Note that the number of samples captured within the plume differs between the S R and TMR casts because a different number of samples were taken at different depths. b The young rising plume was identified over Rainbow close to the seafloor with density lower than that of other stations at the same depth (supplementary information, Figs. S8 and S10 in the Supplement). This signal is separated as these samples will be from a cross-section of the young rising plume as the CTD rosette passed through it. An extended version of this table with data from all stations is presented in the supplementary information (Table S1).
2. Dual-Mn method. Constrain the xs 3 He corresponding to the dFe data using measurements of dMn on both rosette systems. This approach relies on the conservative behaviour of dMn over timescales of weeks (Cowen et al., 1986;Lough et al., 2017Lough et al., , 2019a) (Fig. S2 in the Supplement) and uses the linear relationship between dMn=xs 3 He measured from the standard rosette (Fig. 4a) to extrapolate the expected xs 3 He for samples taken with the trace metal clean rosette. The dMn derived xs 3 He values can then be integrated across the same sample depths as for dFe, which would account for between cast variability in the plume dynamics in a consistent manner. Furthermore, using a site-specific approach helps us to account for any variability in background xs 3 He present in North Atlantic water masses, where decay of tritium from historic nuclear bomb tests has added 3 He (Jenkins et al., 2015b).
3. xs 3 He interpolation method. A third method of estimation was explored using the depth profile of xs 3 He on the standard rosette and interpolating between depths, to calculate xs 3 He at the depths sampled by the trace metal clean rosette. This is similar to the approach used by Saito et al. (2013), however the xs 3 He interpolation method gave significantly different results from the other two methods, generating negative numbers in some instances (Table S1 in the Supplement). The xs 3 He interpolation method relies on the assumption that the xs 3 He depth profile is the same on both sampling casts. While the assumption that the shape of the depth concentration profiles is unchanging between casts is likely safe in an off-axis setting, Figs. 3 and S4 Biogeosciences, 20, 405-420, 2023 in the Supplement show that this assumption cannot be applied within the ridge valley. We therefore focus on the integration methods explained above.
Any samples with xs 3 He < 0.1 fM, dFe < 0.5 nM, dMn < 0.15 nM and neutral density 27 kg m 3 were excluded from analysis as these waters are deemed to have not been influenced by hydrothermal activity. These background values were selected based on the N. Atlantic values of waters at the same depth range to that of the plume anomalies in this study but from the GEOTRACES Equatorial Atlantic (GA03) and western Atlantic (GA02) at open ocean stations away from any margin sources. Profiles shown in Fig. 3 and the Supplement only show samples characterised as plume samples, i.e. having concentrations greater than that of typical N. Atlantic seawater at the same depth which are included in this analysis. The full data set can be viewed or downloaded through the GEOTRACES international data product (Schlitzer et al., 2018).
Directly over the TAG and Rainbow sites, where the plume was sampled repeatedly, the range of dFe=xs 3 He across the integration methods was extensive, ranging from 4 to 87 at TAG and 4 to 63 nmol fmol 1 at Rainbow (Table 2). Integrated values were different even when the two methods are applied to data from the same casts. The differences in integrated values between casts at the same site is likely to be due to the casts intersecting different areas of the plume (i.e. margins or core) during sampling and/or changes in plume depth over time (time between standard and trace metal clean casts was 2-9 h) (Figs. 2 and3). The degree of dFe=xs 3 He variability between integration methods was also observed in the single station estimates from the Menez Gwen and https://doi.org/10.5194/bg-20-405-2023 Lucky Strike locations, where ratios were 5 to 12 and 4 to 26 nmol fmol 1 , respectively (Table 2), highlighting the different values that can be produced just by using a different method of calculating dFe=xs 3 He. The difference in calculated dFe=xs 3 He ratios was consistently lower (maximum difference of 7 nmol fmol 1 ) at stations away from the main vent sites (Table S1). Hence, the variability in calculated dFe=xs 3 He directly over the vent sites is largely down to the changing position of the plume over the vent site relative to the sampling rosette between casts, despite the ship maintaining the same position (Fig. 2).
We focus on the dual-Mn method as the most robust means to estimate the dFe=xs 3 He ratio. As it can account for differences in position of the plume between sampling devices (Figs. 2 and3) and background xs 3 He. Applying site-specific dMn=xs 3 He relationships from the standard rosette system to the dMn of the TMR rosette, the dual-Mn method finds dFe=xs 3 He ratios of 12, 4-8, 4-44 and 4-86 nmol fmol 1 at Menez Gwen, Lucky Strike, Rainbow and TAG, respectively, for the hydrothermal plumes' directly over these vent https://doi.org/10.5194/bg-20-405-2023 sites (Table 2, Fig. 4c). Although the dual-Mn method is less sensitive to differences between casts at the same site, large differences in dFe=xs 3 He remain over each vent site, with dFe=xs 3 He still differing by a factor of 2-21 when comparing different casts. The results shown in Table 2. highlight the practical challenges of determining site-specific Fe=xs 3 He ratios, even in a focused study effort, as a result of complex bottom currents frequently shifting plume waters (Lahaye et al., 2019).
The extent to which sample depths over the vent sites are representative of the core of the hydrothermal plume can be appraised by (1) assessing L S S and ORP sensor profiles, (2) comparing plume dMn and xs 3 He from the standard rosette (Fig. 3) and (3) comparing TDFe to xs 3 He from the trace metal clean rosette (estimated from the dual-Mn method) with the respective vent fluid endmember ratios (Fig. 4). The vent fluid endmember dFe represents the majority of Fe released from the vent source because vent fluids have a low pH < 2 and significant quantities of particulates are yet to form. In the neutrally buoyant plume emplaced directly over each vent site, Fe removal by particle settling should be in the range of 0 %-30 % Fe endmember vent fluid values and 0 % of the Mn (Mottl and McConachy, 1990;Severmann et al., 2004;Findlay et al., 2015;Lough et al., 2019a).
The majority of Fe bearing particles in the unfiltered TDFe samples will be Fe-oxyhydroxides that will dissolve at pH 1.8 after > 1 year storage. A possible exception being that a fraction of the particulates will be FeS2 which may not dissolve with the addition of HCl (German et al., 1991;Gartman et al., 2014). Extrapolation of experimental data of FeS2 oxidation rates in seawater and acidic solution (Gartman and Luther, 2014;Constantin and Chiriţa, 2013) indicate that 80 %-100 % of any FeS 2 present in our samples should have oxidised during the 1 year between sampling and analysis. We anticipate that any FeS2 present in our sam-ples dissolved during sample storage and is included in our measured dFe concentrations and we do not need to be concerned about sample artefacts as a result of FeS2 nanoparticles.
The plume TDFe=xs 3 He and dMn=xs 3 He ratios can be compared to vent dFe=xs 3 He and dMn=xs 3 He ratios, to examine whether the samples from a given cast capture the full extent of the plume rather than just the margins. TDFe=xs 3 HeMn and dMn=xs 3 He values less than vent fluid values would indicate rapid particle formation and settling has removed Fe and/or Mn from the early plume. The similarity between vent dFe=xs 3 He and plume TDFe=xs 3 HeMn at 0 km indicates minimal Fe has been lost from parti-cle settling in the immediate plume over each vent site and that the plume cores were indeed sampled from the trace metal rosette (Fig. 4d). Similar results are apparent when comparing vent dMn=xs 3 He and plume dMn=xs 3 He from the standard rosette (Fig. 4b). One station at Rainbow shows TDFe=xs 3 HeMn higher than the 1 V 1 vent plume ratio (Fig. 4d); however, this plume signal was located within 50 m of vents on the seafloor (2300 m) and therefore likely represents the narrow (usually < 1 to several metres wide) buoyant rising plume (see Table 1 caption and Fig. S8). The TDFe=xs 3 HeMn value higher than the 1 V 1 line is likely the result of resuspended benthic Fe entrained in the rising plume near the seafloor elevating the TDFe=xs 3 HeMn to values higher than the vent dFe=xs He. Alternatively, the range of TDFe=xs 3 He at the different sites may represent the combined uncertainty from the dual-Mn integration method.
Values of plume dMn=xs 3 He fall marginally below the 1 V 1 ratio line for Lucky Strike and Rainbow (Fig. 4b) and could be a result of lower sampling resolution on the standard rosette (Figs. S3 and S4 in the Supplement), uncertainties associated with the plume integration, uncertainties associated with vent fluid endmembers or enhanced removal of Biogeosciences, 20, 405-420, 2023 dMn by particulates at Lucky Strike and Rainbow. In the case of Rainbow, dMn=xs 3 He lower than 1 V 1 could be the result of a higher particulate Fe-oxyhydroxide concentrations in the plume due to the significantly higher Fe=H2S ratio of the vent fluids (Fe=H2S D 26); however, for Lucky Strike particle removal is less likely to explain dMn=xs He lower than 1 V 1 as Lucky Strike vent Fe=H2S is lower (Fe=H2S D 0.18) and sulfide concentrations are enough to potentially consume all the Fe.
All vents on the North Mid-Atlantic Ridge have similar endmember xs 3 He concentrations (18 6 pmol kg 1 , n D 4 vents (Jean-Baptiste et al., 2004), Table 1). Therefore, differences in vent dFe=xs 3 He are solely driven by differences in Fe concentration, which range from 16 to 24 100 μmol kg 1 across the four vent sites (Beaulieu et al., 2013;Chavagnac et al., 2018;Koschinsky et al., 2020) determined by the geochemistry of each vent site (Table 1). The endmember vent fluids at Rainbow have the highest dFe=xs 3 He (964 nmol fmol 1 at Rainbow in contrast to 278 nmol fmol 1 at TAG) as the higher temperature, higher Cl and low pH of fluids leach more Fe (along with other metals and rare earth elements) from the host rock in comparison to flu-ids circulating through the sites with basaltic rocks (Dou-ville et al., 2002). Therefore, between-site differences in the plume dFe=xs 3 HeMn are not simply related to the vent fluid endmember dFe=xs He ratio of each vent. For instance, the highest dFe=xs 3 HeMn plume ratio was observed over TAG (86 nmol fmol ), which was double that of the highest dFe=xs 3 HeMn ratio over Rainbow (44 nmol fmol 1 ) (Table 1, Fig. 4c), despite the five-fold greater Fe content of Rainbow fluids. In contrast, the TDFe=xs 3 HeMn values were correlated with the vent fluid endmembers across our sites (Fig. 4d).
At the 10-40 km sampling distance, a decrease in the Fe=xs 3 HeMn ratio was seen across both the total and dissolved Fe size fractions, relative to the maximum ratios sampled over the vent sites (Fig. 5). We interpret this as a difference in plume age between samples taken over the vent site and samples taken in the 10-40 km range, where plume waters are older in the 10-40 km range (therefore more dilution of the vent fluid by seawater) and there has been more time for Fe to precipitate and be removed from the water column. Within 40 km of both the Rainbow and TAG sites, tween 4 and 15 nmol fmol 1 (except for one station 30 km west of TAG which had a ratio of 38 nmol fmol 1 , Fig. 5d) in comparison to maximum values over the vent sites at 0 km. The difference between vent fluid dFe=xs 3 He and plume dFe=xs 3 HeMn at the 10-40 km range indicates the importance of Fe removal by precipitation of particulates and the subsequent settling of large and/or heavy particulates within 0-10 km of the vent source at both sites, on timescales of days to weeks, leading to a smaller range of dFe=xs 3 HeMn that may represent broader transport to the ocean interior.
It is particularly notable that despite the TDFe concentrations at Rainbow being an order of magnitude greater than those at TAG (Figs. 5 and4d), the dFe=xs 3 HeMn and sFe=xs HeMn values within 40 km are very similar. One exception is station 30, located 30 km west of TAG, where a dFe=xs 3 HeMn of 38 nmol fmol 1 is consistent with a younger plume signal with less time for particle formation and settling (Table S1). It is unlikely that there is a new hydrothermal source adding additional Fe to this region west of TAG, given how extensively the area around TAG has been surveyed (Kinoshita et al., 1998). Experimental data examining the oxidation kinetics of Fe at station 30 west of TAG found anomalous rate constants for Fe 2C oxidation (logK values), possibly as a result of interactions with organic matter (González-Santana et al., 2021). Anomalous Fe 2C oxidation rate constants likely relate to the anomalously high dFe=xs 3 HeMn at station 30, however we are unable to explain why this site would have higher concentrations of organic matter or why dFe would interact differently with organic matter at this station compared to the other sites. https://doi.org/10.5194/bg-20-405-2023
The average cFe=dFe ratio of the TAG plume (0.82 0.12, n D 6) is similar to the Rainbow plume (0.84 0.10, n D 7), indicating that dFe is predominantly colloidal within 40 km of the vent source at both sites, with little change over these distances (Fig. 6a). In contrast, there is a clear difference in the appPFe=dFe ratio (Fig. 6b), which is elevated in the Rainbow plume and consistent with the higher concentration Fe source at Rainbow. The difference in the appPFe=dFe ratio between Rainbow and TAG highlights a substantially larger role for dissolved-particulate interactions at the Rainbow site, relative to TAG. It is due to these strong particulatedissolved exchanges that the dFe=xs 3 HeMn ratios 40 km from source are largely similar for both TAG and Rainbow, despite the Rainbow neutrally buoyant plume having initially half the dFe=xs 3 He over the vent site (44 nmol fmol 1 ) relative to TAG (86 nmol fmol 1 ) (Fig. 5c andd). If dFe was behaving entirely conservatively, we would anticipate the range of dFe=xs 3 He at the 10-40 km stations around Rainbow (4-15 nmol fmol 1 ) to be lower than that of the equivalent sites around TAG (4-9 fmol nmol 1 , excluding the anomalous western station). The similarity in dFe=xs 3 He at 10-40 km suggests the dFe=xs 3 He ratio in the Rainbow plume was buffered by disaggregating or dissolving particles. Specifically, particles which were too large to initially be part of the dissolved phase (> 0.2 μm) but not large or dense enough to form particles that rapidly settle out of the plume within the 40 km sampling area.
Separating whether particle disaggregation or dissolution is the driving mechanism behind the buffering of dFe concentrations between the 0 and 40 km stations at Rainbow is difficult from these results. We would anticipate particle dis- solution would transfer appPFe to the sFe fraction as aqueous ions, causing a shift in the cFe=dFe ratio (Fig. 6) and we did not observe this. Therefore, we deem it more likely that dFe=xs 3 He at 10-40 km range is buffered by disaggregation of appPFe particles rather than dissolution, or there is dissolution followed by rapid re-precipitation as inorganic colloidal Fe or immediate binding to colloidal sized Fe ligands.
Our results do not show constant linear trends between dFe and xs 3 He (Fig. 5) that have been observed over larger distances in basin-scale sampling efforts in the Pacific (Resing et al., 2015). As well as looking at integrated values, we examined the correlation between xs 3 HeMn and dFe across individual samples and found r values of 0.956 to 0.811 for Lucky Strike and Menez Gwen, and 0.442 and 0.587 for Rainbow and TAG, respectively (Fig. S11 in the Supplement). Interestingly, sites like TAG and Rainbow with higher particle concentrations had lower r 2 values. These deviations from linear relationships likely indicate ongoing particulatedissolved Fe exchange at the 0-10 km scale, which has been observed previously at smaller scale sampling resolution (Lough et al., 2019a).
The large differences in appPFe-dFe dynamics over 10's of km between the TAG and Rainbow plumes highlight the potential importance of particulate-dissolved Fe exchange in governing hydrothermal Fe transport from distinct vent sources. If particulate Fe concentrations extend the longevity of hydrothermal Fe in the deep ocean as hypothesised (Fitzsimmons et al., 2017), then it is likely that the residence time of hydrothermal Fe will depend on the amount of Fe released from vents on the seafloor and the presence of ligands to facilitate particulate-dissolved Fe exchange. In the particle exchange conceptual model, we would anticipate the residence time of dFe in the Rainbow plume to be longer Biogeosciences, 20, 405-420, 2023 than the TAG plume, due to higher particulate Fe concentrations facilitating transport over longer distances. Alternatively, if hydrothermal dFe behaves conservatively (Resing et al., 2015) (and dissolved-particulate Fe exchange is negligible), then the longevity of hydrothermal Fe will depend on how much Fe forms colloidal and soluble phases in the early stages of the plume. In the conservative colloids framework, we would anticipate dFe in the TAG plume to have a longer residence time in the water column due to initially higher dFe=xs 3 He (Fig. 4c and Table 1). In both conceptual models, Fe-binding ligands are likely to play a key role by either facilitating particulate-dissolved Fe exchange or by stabilising dFe species. However, if the formation of colloids in the first several metres of plume rise is largely a result of inorganic precipitation of dFe, then the role of ligands will be less important in the conservative colloids model. The "conservative Fe colloids" model has been tested in global biogeochemical models (Resing et al., 2015) and estimates a global hydrothermal Fe flux of 4 1 Gmol yr 1 . A version of the "particulate-dissolved Fe exchange" model has also been tested and this produces a much lower flux estimate of 0.12 0.07 Gmol yr 1 (Roshan et al., 2020). Refining these models and deciding which is closer to the truth requires experimental data on the rate of particulate-dissolved Fe exchange and stability of colloidal phases in both hydrothermal plumes and the deep ocean.
4.1 What controls ridge axis dissolved Fe to helium ratios?
Given the significantly higher vent fluid dFe=xs 3 He at Rainbow compared with TAG (Table 1), the dFe=xs 3 He at distances 10 to 40 km from the vent sites is remarkably similar (8 4 versus 12 14 nmol fmol 1 , respectively, n D 5). The similarity in dFe=xs 3 He at the 10-40 km range between Rainbow and TAG would suggest there is a cap on the amount of vent fluid dFe that can be converted into dFe in the plume, which is possibly the result of similar Fe-binding https://doi.org/10.5194/bg-20-405-2023 ligand concentrations and/or strength at both sites. Ligands could be sourced from weakly binding pervasive background Fe-binding ligands present in deep ocean waters or Febinding ligands sourced locally from the ecosystems of both vents present at similar concentrations and binding strengths (Kleint et al., 2016). Alternatively, Fe 2C oxidation rates may determine the extent to which Fe is separated between dissolved and particulate phases and hence the dFe=xs 3 He ratio.
Rates of Fe 2C oxidation measured at both these sites show a similar range of Fe 2C half-lives in the plumes (TAG D 1-130 min, Rainbow D 20-160 min; González-Santana et al., 2021). The initial concentration of Fe released from Rainbow vents is 5 times higher than at TAG, despite a similar He concentration, and if Fe 2C oxidation rates were the main driver of dFe concentrations, the Rainbow plume should have higher ratios of dFe=xs 3 He. This contrasts with our observations, suggesting that Fe 2C oxidation rates are less important in establishing plume dFe=xs 3 He at scales of 10's of km than ligand strength, concentration or inorganic colloid formation.
Vent fluids with molar Fe=H2S < 1 are likely to precipitate higher concentrations of FeS2 nanoparticles in plumes (Gartman et al., 2014). Given that TAG has a lower Fe=H S ratio than Rainbow (Fe/H S is 1 mmol mmol 1 for TAG vents and 26 mmol mmol 1 for Rainbow; Table 1), we should anticipate a higher concentration of FeS2 nanoparticles in the TAG plume. Higher concentrations of FeS2 nanoparticles may offer an explanation as to why the maximum dFe=xs He of the TAG plume (86 fmol nmol 1 ) was high in comparison to Rainbow (44 fmol nmol 1 ). The twofold difference in maximum plume dFe=xs 3 He between TAG and Rainbow is small compared to the 18-fold difference in vent fluid Fe=H2S (Table 1), and based on the observed trend between FeS2 nanoparticle concentration and Fe=H2S shown in Gartman et al. (2014), we would only anticipate an additional 4 % FeS2 concentration in the dissolved phase at TAG. This suggests that the formation of FeS2 nanoparticles in the nascent plume cannot fully explain differences in plume dFe=xs 3 He between sites. From our comparison, it would seem that for vent sites located along the same ridge, ligand concentration and strength are likely to be a more important control on dFe=xs 3 He over the ridge axis than vent fluid chemistry and Fe 2C oxidation rate (set by water column O2 and pH; Santana-Casiano et al., 2000;Millero et al., 1987).
If we only consider the dFe flux from plumes, excluding any contribution from particulates, site-to-site differences in the chemistry of hydrothermal systems give a range of 8-12 nmol fmol 1 (averages from Rainbow and TAG at 10-40 km) for dFe=xs 3 He within the ridge valley (Fig. 5). Therefore, any subsequent dFe flux calculated based on dFe=xs 3 He will only vary by a similar magnitude. This would mean that current biogeochemical models using a global dFe=xs 3 He ra- https://doi.org/10.5194/bg-20-405-2023 tio of 10 nmol fmol 1 (within the 8-12 nmol fmol 1 range observed at 10-50 km) are using a reasonably well-defined input flux of "dissolved" hydrothermal Fe into the deep ocean. However, given the differences between sites in appFe=dFe (Fig. 6), we need to consider the impact of particulate Fe on the hydrothermal Fe flux and how this may vary across the global ocean ridge crest. Models of hydrothermal Fe fluxes are calculated based on a fixed dFe=xs 3 He value, estimating dFe flux based on xs 3 He fluxes which vary with ridge spreading rate. We found no indication of a relationship between vent endmember and plume dFe=xs 3 He over each vent site, however we did find a relationship between TDFe=xs 3 He and the vent endmember (Fig. 4), suggesting this parameter may be more relevant for linking the Fe flux from vents with xs 3 He fluxes from ridges. Fine-grained suspended particulates maintain TDFe=xsHe above dFe=xs 3 He and clearly persist at the 10-40 km range and are likely to be transported beyond the ridge. There is an argument to be made that these fine-grained suspended particles should be represented in the values used to estimate hydrothermal Fe fluxes in global biogeochemical models.
All stations maintain a cFe=dFe ratio greater than open ocean N. Atlantic cFe=dFe values of 0.5 (Fig. 6a). Clearly within the ridge valley, plume waters maintain a higher colloidal Fe load than open ocean N. Atlantic waters. If the residence time of Fe-rich plumes trapped within the Mid-Atlantic Ridge valley are similar to the time it takes Lagrangian particles to exit the ridge valley in dispersion models (Vic et al., 2018), then wherever deep waters escape the ridge valley they may also carry elevated concentrations of particulate and dissolved Fe to the deep Atlantic ocean.
Using Stokes' law, we can calculate if it is reasonable to expect plume waters exiting the ridge valley to carry sufficient colloidal and particulate Fe or whether it will have settled out of the water column to the sediment. Plume waters from Lucky Strike take 30 d to exit the ridge valley based on Lagrangian particle dispersion experiments (Vic et al., 2018). As there are no other comparative dispersion experiments for other sites on the MAR, we can assume that the dispersion time for plume waters to exit the ridge valley is the same for other vents on the MAR as it is at Lucky Strike. The approximate distance from sources of venting at the centre of the valley to the outer ridge flank is 100 km. We can then calculate that an average particle of ferrihydrite 6 μm in size (average of 6 6 μm, n D 28, based on pub-lished microscopy images, Table S2 in the Supplement; Feely et al., 1994;Breier et al., 2014;Lough et al., 2019bLough et al., , a, 2017;;Toner et al., 2009Toner et al., , 2016;;Von Der Heyden et al., 2012) would have settled 87 m through the water column as plume waters travel from the vent source out of the ridge valley. Given the abyssal seafloor depths outside the ridge are 4000 m and neutrally buoyant plume heights along the ridge are in the range of 800-3200 m (Fig. S7 in the Supplement), we can conclude that there is not enough time for the average sized Fe oxyhydroxide particle to reach the seafloor. Settling of 87 m during transport out of the ridge valley is likely still a conservative estimate of settling when we consider that (1) microscopy techniques used to estimate particle diame-ter will be biased towards observing larger particles that are easier to detect and image, (2) particles are often a mix of Fe oxyhydroxide minerals and organic carbon making them less dense than pure ferrihydrite (Toner et al., 2009;Yucel et al., 2011;Gartman et al., 2014;Lough et al., 2017;Hoffman et al., 2018;Lough et al., 2019b;Lough et al., 2019a), and (3) Lagrangian particles in dispersion models are carried 100 m vertically beyond the neutrally buoyant plume depth by turbulent mixing across the ridge (Vic et al., 2018) and tidal forces can shift neutrally buoyant plume depths by 100 m within the ridge valley (Jean-Baptiste et al., 2004). Therefore, physical mixing processes should counteract the effects of particle settling and we see some evidence of this in Fig. 3 where the maximum concentration of elements is at a shallower depth (1900 m) at stations away from the vent source (Fig. 3d ande) in comparison to stations over the vents (2000-2300 m, Fig. 3a andb). It is therefore likely that the TDFe concentrations we observe within 10-40 km of the vents will be similar to those of waters exiting the ridge valley and entering the deep ocean with the majority of fast particulate Fe removal to sediments happening within 10 km of the vent site (i.e. timescale of days, particles > 30 μm in diameter that are exclusively Fe oxyhydroxide or Fe sulfide minerals).
For slow spreading mid-ocean ridges (i.e. ridges with a substantially deep ridge valley), we should conceptualise them as "leaky ridges" rather than individual "leaky vents" in order to fully understand their impact of the deep ocean Fe budget. As it is the point at which plume waters exit the ridge valley, the Fe carrying capacity of these waters (particulates and dissolved phase) and the rate at which Fe is removed from the plume as settling particles are key to determining the impact of hydrothermal vents on deep ocean Fe concentrations. The extent to which Fe is removed from the plume before exiting the ridge valley is dependent on the time it takes from plume waters to be transported and diluted, making particle collisions and therefore aggregation less likely. Hence understanding the physical mixing regimes of waters moving through ridge valleys is of key importance to further constraining hydrothermal Fe fluxes, especially for slow spreading ridges where plumes will initially be topographically constrained. Focusing research efforts on understanding changes in Fe concentrations within physical mixing regimes will provide an improved ability to understand Fe removal from hydrothermal plumes with transport away from vent sources, in comparison to assessing Fe removal within the context of the path of a ship across the ocean (Nishioka et al., 2013;Saito et al., 2013;Resing et al., 2015;Fitzsimmons et al., 2017).
It is possible for global biogeochemical models to overestimate Fe fluxes from some mid-ocean ridges, as the complex mesoscale mixing regimes through ridge valleys are not pa-Biogeosciences, 20, 405-420, 2023 rameterised at the global scale. In order for this to be the case, the pathways that ridge valley waters travel from the vent source to exiting the ridge valley would have to be significantly longer than those modelled for Lucky Strike (Vic et al., 2018), allowing for an extended period of time for scavenging and precipitation of Fe (resulting in lower dFe=xs 3 He values than those used in models and observed in this study) leading to lower Fe fluxes. If we lead with our assumption that plume dispersion time at Lucky Strike (Vic et al., 2018) is representative of most plumes emanating from mid-ocean ridges (given that the physical mixing regimes acting on the plume and topographic controls will be similar along the ridge), and that particulates at the 10-40 km distance are likely to remain suspended in the wa-ter column or re-dissolve, then using TDFe=xs 3 He ratios of 55 24 n D 7 (average all TAG and Rainbow stations at 10-40 km distance) in biogeochemical models may be more representative of the hydrothermal Fe flux which is 5 greater than the ratio of 10 used currently (Tagliabue et al., 2010;Resing et al., 2015).
Similar process studies that sample plumes from vents with different geochemistry along a ridge will be needed to test the ideas discussed here further. Specifically focusing on the dispersion of plumes through the ridge valley walls and whether there is any difference in Fe-binding ligand strength or concentration between vent sites with different amounts of diffuse flow that likely act as a source of ligands. Our findings from the comparison of TAG and Rainbow show that the inorganic geochemistry of individual vents sites plays a minor role in dictating the near-field plume dFe concentration; however, an excess of plume pFe resulting from higher vent fluid Fe concentrations may support dFe longevity via dFe-pFe exchange, provided the particulates remain suspended, disaggregate or re-dissolve in the water column. It is therefore possible that vents situated in an ultramafic setting (i.e. low pH and high Cl content due to interaction with ultramafic rocks during hydrothermal circulation) may provide more Fe to the deep ocean in comparison to basalt hosted systems. However, constraining the full impact of ultramafic vent sites on the net global hydrothermal Fe flux requires more knowledge about the frequency of their occurrence along the global ridge crest (Baker et al., 2016).
To improve our estimates of how much hydrothermal Fe fertilises surface ocean productivity, we need further information on the location and frequency of vent systems along the global ridge crest, how much variability there is in the hydrothermal ligand source between vent sites, what controls the rate of particulate dissolved exchange in the plume and how rapidly hydrothermal Fe is scavenged from the deep ocean.
https://doi.org/10.5194/bg-20-405-2023 5 Conclusions Our results show that care must be taken when extrapolating Fe=xs 3 He results from ocean survey sampling, e.g. as part of GEOTRACES. This is due to uncertainties associated with the at-sea sampling strategy and the temporal nature of plume dynamics that can yield significant variability in Fe=xs 3 He ratios. We recommend that measurements of dMn across different casts at the same site are a useful means by which to minimise sampling uncertainties, especially when combined with ORP and L S S sensors to target plume sampling across different deployments. We show that when dMn and xs 3 He measurements are used alongside both dFe and TDFe observations, it is possible to link the observed plume dynamics to vent fluid endmembers and determine the important dissolved-particulate dynamics that shape the Fe=xs 3 He signals that integrate at broader spatial scales.
Despite 5 higher concentrations of Fe (but similar xs 3 He) venting from Rainbow relative to TAG, we observed lower dFe=xs 3 He in the Rainbow plume over the vent site (Fig. 4c). The additional Fe venting at Rainbow was converted into particulates and this was reflected in the ratio of appPFe=dFe at Rainbow which is higher than TAG (Fig. 6b). These results suggest that there is a threshold placed on the amount of venting dFe that can be converted to plume dFe; we hypothesise that this threshold is set by the concentration of Fe-binding ligands. Greater than 80 % of vent fluid Fe formed large dense particulates that settled rapidly within 10 km's and a smaller but significant fraction remained suspended in the water column. The particulate Fe persisting beyond the 10 km distance may enhance the longevity of plume dFe through particulate-dissolved exchange. The extent of ongoing particulate-dissolved Fe exchange with further plume dispersion will depend on the speciation and size distribution of particulates as well as ligand strength, concentration and longevity which may differ between these two sites. Future work examining any differences in particle speciation and size between these two sites will be better placed to determine whether the higher concentration of suspended particulates at Rainbow will enhance the longevity of the hydrothermal plume relative to the TAG plume.
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https://doi.org/10.5194/bg-20-405-2023