Iron limitation of kelp growth may prevent ocean afforestation

Communications Biology volume 6, Article number: 607 (2023) Cite this article

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Carbon dioxide removal (CDR) and emissions reduction are essential to alleviate climate change. Ocean macroalgal afforestation (OMA) is a CDR method already undergoing field trials where nearshore kelps, on rafts, are purposefully grown offshore at scale. Dissolved iron (dFe) supply often limits oceanic phytoplankton growth, however this potentially rate-limiting factor is being overlooked in OMA discussions. Here, we determine the limiting dFe concentrations for growth and key physiological functions of a representative kelp species, Macrocystis pyrifera, considered as a promising candidate for OMA. dFe additions to oceanic seawater ranging 0.01-20.2 nM Fe′ ‒ Fe′ being the sum of dissolved inorganic Fe(III) species ‒ result in impaired physiological functions and kelp mortality. Kelp growth cannot be sustained at oceanic dFe concentrations, which are 1000-fold lower than required by M. pyrifera. OMA may require additional perturbation of offshore waters via dFe fertilisation.

Ocean macroalgal afforestation (OMA) is one of more than 30 marine techniques proposed as suitable candidates for carbon dioxide (CO2) removal to mitigate climate change caused by increasing atmospheric CO2 levels1,2. OMA is based on the purposeful introduction of kelps (marine macroalgae or seaweed, order Laminariales) into the open ocean, where they grow on stationary seaweed farms or transit offshore attached to raft-like structures1,3. Kelps form dense underwater beds (‘forests’) in temperate, coastal marine ecosystems, providing habitat and food for higher trophic levels, and essential nitrogen and carbon cycling services. They take up CO2 from seawater and ‘fix it’ into organic matter through photosynthesis, yet whether or not this process leads to carbon sequestration (i.e., secure storage > 100 years2,4) is difficult to quantify4. Regardless, proponents of OMA consider that increasing the biomass of nearshore seaweeds by open-ocean colonisation will increase carbon sequestration1,5. Previous OMA research has determined geographical regions with sufficient macronutrient concentrations to sustain seaweed growth6. However, essential trace metals for photosynthesis, such as dFe, limit phytoplankton primary production in much of the open ocean7 and have been a major omission in the OMA debate.

Iron is the most studied trace element in the ocean with a significant influence on the functioning of the biological carbon cycle due to its crucial role in setting the rates of enzymatic activity of algal photosynthesis and nitrogen uptake8,9. Concentrations of dFe used in this study are expressed as Fe′ which is the sum of dissolved inorganic Fe(III) species, a proxy that best mimics dFe bioavailability. Concentrations of dFe vary with locale and depth, and dFe availability limits primary productivity in one-third of the global ocean10. This scarcity results in areas termed high nutrient and low chlorophyll (HNLC) where macronutrient inventories such as for nitrate (NO3−) can only be partially utilised7,11,12. In the coastal ocean, however, rivers, atmospheric inputs and sediments are significant, and often ongoing, sources of dFe, with concentrations ranging from ~0.1 to ~500 nM depending on fluvial inputs13,14. Coastal waters (defined here as waters extending from the shoreline to the outer edge of the continental margin) also have a higher concentration of bioavailable dFe compared to the open ocean due to increased concentrations of dFe binding ligands, such as humic and fulvic acids from sediment margins and riverine sources15,16. Consequently, algae which live in this coastal region are typically dFe-replete17,18.

For seaweeds, tissue iron content and its relationship to electron transport and pigment content is well documented for many species11,17,19,20,21,22,23,24; however, the role of seawater dFe concentrations for key physiological functions of seaweed—growth, dissolved organic carbon (DOC) production, photosynthesis and nitrogen metabolism—has not previously been studied and is a knowledge gap in OMA discussions8,11. However, there are likely many parallels with the multifaceted role that iron plays in other photosynthetic organisms, including oceanic phytoplankton18,25. For example, up to half of the dFe in photoautotrophs is used for photosynthesis—primarily electron transport between photosystem II (PSII) and photosystem I (PSI)9,26. dFe is essential for the synthesis of algal pigments, respiration and nitrogen assimilation with both NO3− and nitrite (NO2−) reductases containing iron-rich haem groups9,17,26,27,28. The cumulative effect of iron-mediated regulation of these physiological pathways ultimately controls phytoplankton growth. For oceanic phytoplankton, dFe concentration regulates the release of DOC, a major global carbon pool (660 Pg C per annum)29. Phytoplankton DOC production increases with dFe limitation as an energy dissipation mechanism linked to nutrient availability30. Clearly, dFe has the potential to exert major influences on multiple seaweed physiological pathways.

Here, we investigated the influence of a gradient of seven Fe′ concentrations, 0.01, 1.85, 4.67, 9.56, 20.2, 45.2 and 120 nM (equivalent to dFe additions of 0.01–40 μM), on the growth and physiology of M. pyrifera. The Fe′ gradient straddled environmentally relevant concentrations for coastal and open oceans along with higher concentrations needed to fully describe the physiological relationships between various metrics and Fe′, similar to experiments for phytoplankton31,32, in order to explore the Fe′ requirements of M. pyrifera.

Our study species was the giant kelp, Macrocystis pyrifera (phylum Ochrophyta, order Laminariales), as it has an extensive geographic range, a high growth rate (~ 2% increase per day of the foliar standing crop), a high capacity to take up nutrients from seawater and, because of these traits, is the species of choice for many planned OMA endeavours6,33. To determine the Fe′ requirements of M. pyrifera, we performed physiological assays to measure growth, DOC production, photosynthesis, respiration, chlorophyll pigment content, maximum photochemical efficiency of photosystem II (Fv/Fm), tissue carbon and nitrogen, C:N ratios and soluble tissue NO3−. Seawater for experimental treatments was collected at a site (~ 47°S, 141°E) in the Southern Ocean (Supplementary Fig. 1), where Fe′ typically ranges from 0.11 to 0.72 pM in the seasonal surface mixed layer8. All other essential macro- and micro-nutrients for M. pyrifera growth were replete using Aquil medium nutrient additions to natural ocean seawater (buffered with 100 μM ethylenediaminetetraacetic acid (EDTA)) and contained 0.01 nM background Fe′.

At concentrations ≤20.2 nM Fe′, M. pyrifera displayed symptoms of multifaceted physiological stress and mortality, with visible tissue degradation and fragmentation of replicates in all treatments, whereas at 45.2 and 120 nM Fe′, all replicates were highly pigmented, intact and had surface corrugations typical of healthy blades34 (Fig. 1a).

a Photographs of individual discs of M. pyrifera replicates (n = 6, labelled R1-R6) at the end of a 14-day Fe′ experiment (0.01–120 nM). Coloured panels are used to represent the disparity between healthy replicates at 45.2–120 nM Fe′ (blue panel) and those displaying symptoms of physiological stress and mortality ≤ 20.2 nM Fe′ (orange panel). Inorganic Fe (Fe′) values in the upper panel correspond to total dFe concentrations of 0, 1, 2.5, 5, 10, 20 and 40 μM for each treatment ( + 7.25 nM background dFe in nutrient-spiked seawater). b Plot of dFe concentrations (nM) against distance offshore (km). Black circles denote dFe concentrations collected on GEOTRACES-SR3 Southern Ocean voyage35 as an example of the dFe concentrations observed uniformly in the open ocean (0.1–0.6 nM)8,36 and coloured circles depict dFe concentrations collated from a comprehensive literature search on coastal sites (see Supplementary Data 1). For comparison, the dFe concentration of 1000 nM equates to 1.85 nM Fe′.

To provide a wider environmental context for the findings from Fig. 1a, we plotted observed dFe concentrations (nM) in surface waters with distance (km) offshore (Fig. 1b). dFe from between 50 and 200 km offshore (black circles) was measured along GEOTRACES-SR3 transect from Tasmania to Antarctica35. Published dFe concentrations between 0-50 km from the coast are collated in Fig. 1b. It is not possible to report Fe′ for these studies as the additional data required for such calculations is not available (see Supplementary Fig. 2). Typically, a range of dFe of 0.1–0.6 nM would equate to an Fe′ of 0.11–1.49 pM (see Supplementary Equation). In our compilation, dFe concentrations decrease sharply offshore (Fig. 1b) ranging from 573 nM (Thurso Bay, Scotland, enriched by a riverine source14) to 0–0.327 nM (Southern Ocean). For comparison, the dFe concentration of 1000 nM equates to 1.85 nM Fe′. These low dFe concentrations in oceanic surface waters are observed uniformly across the globe (< 0.2 nM and average 0.07 nM)36. When compared with the Fe′ requirements for M. pyrifera (≥ 45.2 nM, Fig. 1a), the concentrations of Fe′ available offshore (0–1.49 pM8,36) are at least 1000-fold lower than required to sustain healthy growth (Fig. 1b).

We used the findings from multiple physiological assays to understand the mechanisms that resulted in poor condition of M. pyrifera under concentrations of ≤ 20.2 nM Fe′ (Fig. 1a). Growth (cm2 d−1) of M. pyrifera increased with Fe′ concentration and although not statistically significant (P = 0.34), the relationship was best modelled using a rectangular hyperbola (Adjusted R2 = 0.122) which saturated at > 9.56 nM (Fig. 2a). At concentrations of ≤ 20.2 nM Fe′, there was a substantial increase in the amount of DOC produced (0.43–1.56 μmol C gDW−1 h−1), which was not evident ≥ 45.2 nM Fe′ (Fig. 2b). When DOC production is considered for individual kelp replicates (Fig. 1a, replicates labelled R1-R6), higher rates are observed for those with tissue disintegration, indicating that fragmentation of kelp blades enhanced DOC release (Supplementary Fig. 3)37. At ≥ 45.2 nM Fe′ any DOC released by M. pyrifera was rapidly metabolised by bacteria yielding negative DOC production rates in these incubations (Fig. 2b).

a–d Influence of Fe′ concentration on M. pyrifera showing, a growth, with a modelled rectangular hyperbola (adjusted R2 = 0.122), b DOC production was observed at ≤ 20.2 nM Fe′ but not observed for 45.2–120 nM Fe′ (one-way ANOVA, P < 0.01, F value = 8.473, df = 6). The negative DOC flux at 45.2–120 nM Fe′ likely represents consumption by the seaweed biome72. c Increased net photosynthetic rates and d respiration rates at ≥ 45.2 nM compared to ≤ 9.56 nM Fe′ (one-way ANOVAs, photosynthesis P = 0.057, F value = 2.285, df = 6 and respiration P = 0.047, F value = 2.406, df = 6). Boxes show minimum, 1st quartile, median, 3rd quartile and maximum data values (n = 6). Note no box whiskers, as the lower quartile is equal to the minimum value, and the upper quartile is equal to the maximum value. For significant results, Fe′ concentrations displaying the same letter were not significantly different in post hoc tests. The disparity between healthy replicates observed in Fig. 1a (45.2–120 nM Fe′) and those with symptoms of physiological stress (≤ 20.2 nM Fe′) is indicated by blue and orange panels, respectively. For full statistical results and post hoc tests see Supplementary Data 2 and 3.

Photosynthesis and respiration were both highly variable at concentrations ≤ 20.2 nM Fe′ yet were elevated above ≥ 45.2 nM Fe′ treatments (photosynthesis ~ 5700% greater at 45.2 than 4.67 nM Fe′ and respiration ~ 195% greater at 45.2 than 9.56 nM Fe′; Fig. 2c, d). Carbon to nitrogen ratios (C:N) of M. pyrifera were reduced at concentrations ≤ 20.2 nM Fe′, indicating carbon fixation and incorporation into kelp tissue was limited by Fe′ availability, resulting in the observed, substantial DOC release (Figs. 2b and 3a–d). Total chlorophyll pigments were higher in the 120 nM treatment compared to those at 0.01–4.67 nM Fe′ (Fig. 3a). Fv/Fm was variable (Fig. 3b), however at Fe′ concentrations ≥ 45.2 nM, the standard deviation of Fv/Fm was reduced, and the average fluorescence at 120 nM was higher than at 0.01 nM Fe′ (Fig. 3b). Soluble tissue NO3− content was greater at 120 nM compared to 1.85–9.56 nM Fe′ (Fig. 3c).

a–d Influence of Fe′ concentration on M. pyrifera showing, a increased total chlorophyll content at 120 nM Fe′ compared to 0.01–1.85 nM Fe′ (one-way ANOVAs, chlorophyll P < 0.01, F value = 7.625, df = 6), b maximum photochemical efficiency of PSII (Fv/Fm) using PAM fluorometry, c increased soluble tissue content of nitrate (NO3-) at 120 nM compared to ≤ 9.56 nM Fe′ (one-way ANOVA, P = 0.02, F value = 2.911, df = 6) and d higher tissue carbon to nitrogen ratio at ≥ 45.2 nM compared to 0.01 nM Fe′ (one-way ANOVA, P < 0.01, F value = 9.232, df = 6). Boxes show minimum, 1st quartile, median, 3rd quartile and maximum data values (n = 6). Note no box whiskers, as the lower quartile is equal to the minimum value, and the upper quartile is equal to the maximum value. For significant results, Fe′ concentrations displaying the same letter were not significantly different in post hoc tests. Coloured panels are applied to represent the disparity between healthy replicates at 45.2–120 nM Fe′ (blue panel) and those ≤ 20.2 nM Fe′ (orange panel). For statistical results and post hoc tests see Supplementary Data 2 and 3.

Our finding that growth rates of M. pyrifera increased with Fe′ concentration is consistent with studies which found dFe fertilisation increased seaweed biomass20,23,38,39. This result supports the suggestion that low dFe concentrations (< 1 nM) associated with deforestation and urbanisation in coastal Japanese waters has caused the disappearance of many kelp species including Laminaria japonica and Undaria pinnatifida and highlights the importance of dFe for healthy kelp growth21,23,38,40. The observed increase in DOC released at concentrations ≤ 20.2 nM Fe′ is comparable to that of oceanic phytoplankton cultured under dFe-limited conditions where DOC is released as an overflow mechanism for photosynthetically fixed organic carbon which cannot be used for growth30. DOC release by M. pyrifera under limiting Fe′ concentrations (≤ 20.2 nM) may indirectly affect the microbial ecology of the open ocean through stimulating or inhibiting the microbial community with an altered bioavailability of molecules (spanning labile-refractory) compared to the naturally occurring DOC of the open ocean41,42.

Iron is essential for electron transport, and the elevated photosynthetic rates at ≥ 45.2 nM Fe′ are likely due to the synthesis of more iron-containing proteins to carry electrons between PSII and PSI, and increased ferredoxin content for NADPH reduction and subsequent oxygen production43. Respiration rates were highly correlated with net photosynthesis, indicating that differences in respiration rates were also driven by Fe′ availability (Fig. 2d)9,43. C:N ratios were higher at 20.2, 45.2 and 120 nM compared to 0.01 nM Fe′ (Fig. 3d), and this was driven by an increased percent of tissue carbon rather than tissue nitrogen at higher Fe′ concentrations (Supplementary Fig. 4a, b). These results suggest that the additional carbon fixed by M. pyrifera at ≥ 45.2 nM Fe′ (indicated by higher photosynthetic rates) could be used for growth and was not released as DOC. Low C:N can be indicative of organic carbon lability44 and correlates with the observation that M. pyrifera replicates at 0.01–20.2 nM Fe′ were quickly consumed by bacteria—as observed by cell lysis and fragmentation45 (Fig. 1a).

The increase in total chlorophyll pigment content ≥ 45.2 nM Fe′ supports other published seaweed, phytoplankton and seagrass research which found a positive correlation between chlorophyll a content and increasing dFe concentration—related to a lower content of iron-rich pigment–protein complexes20,22,26,46,47,48. Fv/Fm results were variable as damaged reaction centres can continue to fluoresce albeit less efficiently43. This is consistent with reports that dFe-limited phytoplankton have a greater decrease in PSII and PSI reaction centres compared to antenna pigments, therefore the absorbed excitation energy has a reduced potential of finding a photochemical trap and will likely be re-emitted as fluorescence18,43. In eukaryotic phytoplankton, dFe limits NO3− acquisition through its role in the photosynthetic pathway rather than through the limitation of NO3−-reducing enzymes (NO3− reductase and NO2− reductase)49; however, such mechanisms have not been studied in seaweeds. Together our results highlight the importance of Fe′ for healthy kelp growth, and provide useful physiological insights of how limiting Fe′ concentrations (≤ 20.2 nM) decrease the capacity of M. pyrifera to photosynthesise and store NO3−, resulting in an increased production of DOC.

Fe′ appears to be a primary limiting nutrient that restricts kelp from growing in the open ocean and on this basis, M. pyrifera—as well as other nearshore kelps such as Saccharina japonica38,39,50, Saccharina latissima3 and Sargassum sp1. being considered for OMA—will not subsist in the open ocean without any nutrient or trace-metal additions. We suggest that large, fleshy seaweeds are mostly confined to coastlines globally due to their high requirement for dFe, the supply of which is more abundant near coastlines. This relationship between the magnitude of dFe requirements and dFe supply has also been observed for coastal phytoplankton18. Previous estimates of suitable oceanic ‘real estate’ for kelp aquaculture considered nitrogen and phosphorus availability along with temperature6 but did not consider dFe. Our data support early studies on 'oceanic' (~ 2 km from the coastline) kelp aquaculture that ‘irrigated’ M. pyrifera using an artificial/ purposeful upwelling system but could not sustain growth with upwelled seawater (~ 300 m depth) without adding dFe51.

One departure from the geographical limits placed on seaweeds in the coastal ocean is the success of two species of brown seaweed (order Fucales) from the specious genus Sargassum (S. natans and S. fluitans) offshore in the Sargasso Sea, N. Atlantic where they naturally form ‘golden tides’52. Their ability to form a significant area of rafts in this region is probably due to a specific set of circumstances. Firstly, their distinctive clonal reproduction by fragmentation (i.e., non-reproductive vegetative growth), a mechanism of reproduction that kelps (order Laminariales) do not undergo53,54. Secondly, these Sargassum communities subsist in the Sargasso Sea under low dFe conditions (with a total dFe concentration of 0.2–0.8 nM55); however, growth is likely sustained by a combination of a high iron storage potential—a unique iron ‘plaque’ on the seaweed cell surface54—and most importantly, aeolian inputs of iron from Africa56 and the circulatory ocean current which facilitates the (recurring) transport of seaweeds past the higher dFe waters near the North American continent. The latter is evidenced by increasing productivity of both pelagic Sargassum species during their passage through North American coastal waters where dFe resupply mechanisms are prevalent and concentrations of dFe will likely be higher57.

This multi-stranded mechanism for the unique long-term success of the Sargasso sea macroalgae is supported by another example of an open-ocean seaweed population: the recent (~ 10 years) annually re-occurring trans-basin belts of floating Sargassum in the (sub)tropical North Atlantic, known as the Great Atlantic Sargassum Belt (GASB)58. The recent emergence of this Sargassum population is thought to be driven by increased anthropogenically driven nutrient runoff from the Amazon River, thus the emergence of the GASB is likely related to ocean nutrient, and in particular iron, fertilisation16,59, only reinforcing the importance of the re-circulating gyre, and nutrient resupply, in the Sargasso Sea to support offshore Sargassum populations57.

Consequently, the two case studies, one natural the other anthropogenic, support our conclusion that limiting offshore dFe concentrations will very likely prevent kelp growth in the open ocean—and may prevent OMA— unless there is additional iron fertilisation. The purposeful addition of dFe to offshore waters to stimulate phytoplankton blooms has already raised widespread concerns around multifaceted side-effects60,61,62 along with major unknowns such as its carbon sequestration potential58,63. Based on the results of this study, OMA will therefore likely require additional perturbation of offshore waters via dFe fertilisation. The need to implement OMA in conjunction with dFe supply would result in a compound perturbation of open-ocean colonisation by kelps (considered an invasion of the open ocean41) and dFe fertilisation. Together, they would increase the many uncertainties both ecological41 and biogeochemical58 associated with OMA, with implications for open-ocean ecology (competition for added dFe with resident phytoplankton) and gaining social license62.

Trace-metal-clean seawater was obtained from near the Southern Ocean Time Series (SOTS) site located at 47°S and 141°E southwest of Tasmania, Australia on RV Investigator voyage IN2019_V02. Seawater was collected from a depth of 12 m using acid-cleaned, Teflon-coated, externally-sprung, 12-litre Niskin bottles attached to an autonomous rosette (SeaBird) equipped with an SBE 911plus CTD unit (SeaBird). Upon retrieval, the Niskin bottles were transferred into a clean container laboratory. Carboys were filled with filtered seawater (0.2 μm, Supor AcroPak 200, Pall), sealed, and covered in plastic to avoid potential trace-metal contamination.

Experiment containers (n = 48) were constructed using high-density polyethylene (HDPE) bottles (250 mL, Nalgene®) with holes drilled in the lids for silicon tubing to pass through for aeration and sampling of seawater. HDPE bottles, LDPE bottles, all-plastic syringes (Thermo Scientific™ Titan3™), silicon tubing, Teflon forceps and PPE clamps used during the dFe experiment were trace metal cleaned following procedures outlined in the ‘Sampling and Sample-handling Protocols for GEOTRACES Cruises’64. HDPE sample bottles, low-density polyethylene (LDPE, Nalgene®) and silicon tubing were soaked in 2% v/v Decon-90 for one week, rinsed with ultra-high purity water (Milli-Q) four times and submerged in 10% hydrochloric acid (HCl) at 80 °C for one week and finally rinsed with Milli-Q water four times prior to drying inside a laminar flow hood. A trace-metal free, positive pressurised HEPA-filtered air ‘bubble’ was constructed from plastic sheeting and erected in a temperature-controlled room. All sample handling was undertaken within the bubble using trace-metal-clean protocols. The temperature inside the trace-metal free bubble was 13 °C, and water motion in each flask was provided by bubbling filtered air (0.22 μm). Overhead irradiance was provided by cool white fluorescent lights (Thorn Lighting Cadet Batten, HPF) set to 150 μmol photons m−2 s−1 on a 14:10 light:dark cycle (measured using a LI-COR LI-250 light metre).

Dissolved organic carbon (DOC) vials (Shimadzu TOC) were soaked overnight in 2% v/v Decon-90, rinsed twice in distilled water, washed another night in HCl (ACS reagent, 37%) 10% v/v, rinsed three times in distilled water and—in addition to glass filter paper (Whatman GF/F)—combusted in a furnace overnight to remove any residual carbon. Nutrient tubes were soaked overnight in 2% v/v Decon-90, rinsed twice in distilled water, soaked another night in HCl 10% v/v and finally rinsed three times in distilled water.

Open-ocean seawater (pH 8.05) was spiked with Aquil medium ethylenediaminetetraacetic acid (EDTA) and nutrient additions using trace-metal-clean techniques so that the final concentrations in flasks were as follows: 100 µM EDTA, 200 μM nitrogen as sodium nitrate (NaNO3), 10 μM phosphorus as dibasic sodium phosphate (NaH2PO4), 0.1 μM Molybdenum (Na2MoO4•2H2O), 0.05 μM Cobalt (CoCl2•6H2O), 0.0781 μM Zinc (ZnSO4•7H2O), 0.0198 μM Copper (CuSO4•5H2O) and 0.456 μM Manganese (MnCl2•4H2O).

To determine the effect of dFe limitation on M. pyrifera physiology, seven treatments with dFe concentrations (added from acidified FeCl3 solutions) of 0, 1, 2.5, 5, 10, 20 and 40 μM were set up. Using these dFe concentrations, Fe′ concentrations were calculated for the FeEDTA media following Sunda and Huntsman65 at the mean incubation temperature (13 °C), irradiance (150 μmol photons m−2 s−1, adjusted for the 14:10 h light:dark cycle – Ihv = 0.163), and pH 8.05—the mean of the initial ocean seawater. An overall conditional steady-state dissociation constant for FeEDTA chelates of 1.807 × 10−7 was used to calculate a Fe′:Fe(tot) ratio of between 1.18 × 10−3 at 0.01 nM Fe′ and 2.99 × 10−3 at 120 nM Fe′. The overall conditional steady-state dissociation constant (K′(light)) was calculated as the sum of the conditional stability constant in the dark (Kd′ (dark); 4.98 × 10−8) and the conditional photo-dissociation constant (Khv; 8.01 × 10−7; adjusted for irradiance (Ihv)) of EDTA at 13 °C. Here we define the Fe′ as the sum of dissolved inorganic Fe(III) species. Defining Fe′ for culture work is important as most incubation experiments involve adding the synthetic chelator EDTA to buffer metal ion concentrations in the culture medium (see Supplementary Fig. 2a–c). The addition of EDTA strongly influences dFe bioavailability. Final Fe′ concentrations were set to simulate the concentration range for biologically available dFe from the open ocean through to the coastal environment. In all except our lowest Fe′ treatments, Fe(oxy)hydroxides formed due to the solubility limit of Fe′ at > 700 pM32 and may have been utilised by M. pyrifera. Note it was not possible to report Fe′ for the published dFe concentrations in Fig. 1b, as the additional data required for such calculations is not available (see Supplementary Fig. 2). However, a typical range of dFe of 0.1–0.6 nM would equate to an Fe′ of 0.11–1.49 pM (see Supplementary Equation).

Six replicate flasks were enriched to each concentration of Fe′, and four flasks (two with 0.01 nM and two with 120 nM) were used as controls with no added seaweed to ensure results were driven by seaweed not Fe′ addition. The trace-metal ion buffered synthetic seawater medium was sampled for analysis of trace-metal concentrations to determine background concentrations of Fe′ in the seawater prior to enrichment with Fe′. The synthetic seawater samples were acidified for preservation with distilled HCl (Savillex PFA distillation system, DST-1000), triple bagged and stored at 4 °C, until analysis.

M. pyrifera apical blades (i.e., first blade divided from the apical meristem, n = 42) were collected using snorkel from ~ 1 m depth at Fortescue Bay, Tasmania, Australia (43.13°S, 147.96°E) on October 12, 2021. Seaweeds were placed in an insulated container with seawater for transport to the laboratory 2 h away.

Each seaweed blade (n = 42) was cut into a 5-cm round disk using a plastic cutter and wiped with Kimtech™ wipes to ensure seaweed surface was visibly epiphyte free. Each seaweed disc was an independent replicate. Seaweeds were photographed and weighed for growth measurements (see below), then introduced to experimental flasks in a laminar flow hood. The experiment was run for 14 days, with seawater refreshed and enriched with nutrients every three days to ensure seaweeds were not limited. On day 12, seawater samples were taken from each flask for initial NO3− and DOC analysis. Samples were periodically collected using all-plastic syringes (Thermo Scientific™) through silicon tubing. Seawater was sampled at 4 and 8 h after initial sample collection for NO3− uptake (depletion from the media) and 24 h after initial sample collection for DOC production. Seawater samples for NO3− and DOC production were filtered using pre-combusted Whatman GF/F (0.7 μM) filter paper. NO3− seawater samples were stored in 12-mL polyethylene tubes (kept at −20 °C until analysis) and DOC samples were stored in 40-mL glass vials (Shimadzu TOC, preserved with 0.05% Orthophosphoric acid and kept at 4 °C until analysis). On day 13, initial and final photosynthetic measurements were taken as well as initial respiration measurements (see below). On day 14, final respiration measurements were taken, and seaweeds were removed from flasks for final weight, Fv/Fm, ETR and surface area measurements then preserved for the following biological assays.

Images were taken of each replicate before (day 0) and after the experiment (day 14) using a light board (A3 LED light pad) for analysis of surface area using the image processing programme, ImageJ. Growth rates were calculated using the following equation:

where SAF is the surface area (cm2) of the seaweed at the end of the 2-week experiment, SAI is the surface area (cm2) of the seaweed at the start of the 2-week experiment, and d is number of experiment days (14).

Pulse amplitude modulated (PAM) fluorometry was used to determine the maximum photochemical efficiency of PSII (Fv/Fm, where Fv = Fm – Fo and Fo and Fm, are the minimum and maximum fluorescence in the dark-acclimated state, respectively). Fv/Fm of all replicates was measured prior to (day 0) and at the conclusion of the experiment (day 14) using a JUNIOR-PAMTM chlorophyll fluorometer (Heinz Walz GmbH, Germany), and individuals were dark-acclimated for 15 min prior to Fv/Fm measurement.

DOC samples were analysed using an automated total organic carbon analyser (Analytica Jena Multi N/C 3100) via combustion at 720 °C over a platinum catalyst in accordance with method 5310 D66. Net DOC release rates were based on the rate of change in concentration between initial and final samples and were normalised to flask volume, incubation period, and seaweed biomass (gDW−1). Positive rates of net DOC production indicate DOC release, while negative values indicate net DOC uptake in the system.

Background dFe concentrations in the oceanic seawater, and media-spiked seawater, were determined using the isotope dilution (ID) technique using enriched isotopes (57Fe, 67Zn, 65Cu, 61Ni, 110Cd and 206Pb), or by the method of standard additions (Mn and Co). The trace metals in the seawater media were preconcentrated on the Nobias Chelate PA1 resin using a home-built preconcentration system. Prior to preconcentration, spiked samples were left for 24 h and then buffered to a pH of around 5.2. Metals were eluted from the Nobias resin with 1 mol L−1 nitric acid and then determined by ICPMS (iCap, Thermo Scientific) in helium Kinetic Energy Discrimination (He KED) mode to remove argon oxide inferences on iron. The background Fe′ concentrations in nutrient-spiked seawater were 0.01 nM.

Soluble tissue NO3− content was analysed following the boiling extraction method Hurd et al.67 using fresh seaweed tissue after the completion of the incubation experiment. Boiling tubes were filled with 20 mL of distilled water and 0.2 ± 0.05 g pieces of alga tissue were added. Tubes were removed after overnight refrigeration, capped in aluminium foil and placed in a boiling water bath (~ 100 °C) for 40 min. The solution was left to cool before filtration (Whatman, GF/F) and stored at –20 °C. Boiling extraction was repeated twice to ensure all soluble nitrogen was removed from the alga tissue. The subsequent extract was analysed for concentrations of N(NO3− + nitrite (NO2−)) using a QuickChem® 8000 automated Ion Analyser (LaChat Instruments). Results were standardised to wet weight using the following formula:

where N1, N2 are the N(NO3− + NO2−) concentrations (µM) in the supernatant after the first and second extractions, 0.02 is the volume of liquid in each boiling tube (L), and WW is the wet weight (g) of the seaweed.

On day 13, net photosynthesis was measured (i.e., oxygen (O2) evolution, μmol O2 produced gWW−1 h−1) within each culture flask over 3 h under the experimental irradiance (150 μmol photons m−2 s−1). Respiration (i.e., μmol O2 consumed gWW−1 h−1) was measured for 12 h overnight in the dark. Water motion was provided by an orbital shaker (100 rpm, RATEK). Net photosynthetic measurements were made between 8:00 and 13:00, and respiration measurements between 18:00 and 09:00 + 1 day. Dissolved O2 measurements were made with a portable oxygen metre and optical probe (PreSens Fibox 4 trace with OXYPro® Series probe).

Pigment content (Chlorophyll a + Chlorophyll c) was determined following methods outlined in refs. 68,69,70 using 0.1 g frozen tissue, preserved at −80 °C after the completion of the incubation experiment. Seaweed pieces (0.1 gWW ± 0.05) were placed in individual centrifuge tubes (15 mL) with 4 ml of dimethyl sulfoxide (DMSO) and left to extract for 15 min. Seaweed pieces were then removed from the DMSO solution and placed in separate tubes with 90% acetone (v/v) and left to extract until algae pieces were colourless (~ 30 min). The absorbance of extracts were measured with a S-22 UV/Vis Spectrophotometer (Halo RB-10, Dynamica Scientific Ltd.), DMSO extract at wavelengths 665, 631, 582, and 480 nm and acetone at 664, 631, 581 and 470 nm. Pigment content was subsequently determined using the equations given by Seely et al.68,69,70.

The percent tissue content of carbon (C) and nitrogen (N), and the C:N ratio were determined using a NA1500 elemental analyser coupled to a Thermo Scientific Delta V Plus via a Conflo IV using 0.05 g of oven-dried (60 °C, three nights) seaweed tissue. Combustion and oxidation were achieved at 1020 °C and reduction at 650 °C, respectively, in a column packed with chromium oxide (Cr2O3), copper oxide (CuO) and silvered cobaltous oxide71. Organic carbon and nitrogen contents were determined by comparison of instrument response (area) calibrated using standards with known carbon and nitrogen content. Tissue C and N content were expressed as a percentage of the alga's dry weight and C:N ratios were based on their atomic weights.

Statistical analysis was conducted using R version 2.2 (R Development Core Team, 2012), and graphs were created using SigmaPlot (Systat Software Inc). Results are shown as boxplots indicating minimum, 1st quartile, median, 3rd quartile and maximum data values (n = 6). ANOVA test assumptions were assessed using diagnostic plots of model residuals and data were transformed where necessary using the package, bestNormalize. To compare the parameters for growth, DOC production, photosynthesis, respiration, pigments, Fv/Fm and soluble tissue NO3− with Fe′ concentration, one-way ANOVAs were run. Where statistical significance was observed (P < 0.05), a Tukey's HSD multiple comparison test was run to distinguish which means were statistically significant from others and significance was marked on our plots using letters assigned by a multiple comparison boxplot. A Michaelis–Menten rectangular hyperbola best fit the growth results using the equation:

where V is the increase in growth, Vmax is the maximum growth, S is the concentration of the dFe, and Km is the half-saturation constant. The rectangular hyperbola was fitted to growth data using SigmaPlot.

Further information on research design is available in the Nature Portfolio Reporting Summary linked to this article.

The datasets generated during the current study are available from the corresponding author on reasonable request. Numerical sources for Figs. 2 and 3 are available in Supplementary Data 1.

N’Yeurt, A. D. R., Chynoweth, D. P., Capron, M. E., Stewart, J. R. & Hasan, M. A. Negative carbon via ocean afforestation. Process. Saf. Environ. Prot. 90, 467–474 (2012).

Article Google Scholar

GESAMP. High level review of a wide range of proposed marine geoengineering techniques. 144 (IMO/FAO/UNESCO-IOC/UNIDO/WMO/IAEA/UN/UN Environment/UNDP/ISA Joint Group of Experts on the Scientific Aspects of Marine Environmental Protection, London, 2019).

Stripe. General application. https://github.com/stripe/carbon-removalsource-materials/blob/master/Project%20Applications/Spring2021/Running%20Tide%20-%20Stripe%20Spring21%20CDR%20Purchase%20Application.pdf (2021).

Hurd, C. L. et al. Forensic carbon accounting: assessing the role of seaweeds for carbon sequestration. J. Phycol. 58, 347–363 (2022).

Article CAS PubMed Google Scholar

Duarte, C. M., Wu, J., Xiao, X., Bruhn, A. & Krause-Jensen, D. Can seaweed farming play a role in climate change mitigation and adaptation? Front. Mar. Sci. 4, https://doi.org/10.3389/fmars.2017.00100 (2017).

Froehlich, H. E., Afflerbach, J. C., Frazier, M. & Halpern, B. S. Blue growth potential to mitigate climate change through seaweed offsetting. Curr. Biol. 29, 3087–3093.e3083 (2019).

Article CAS PubMed Google Scholar

Moore, C. M. et al. Processes and patterns of oceanic nutrient limitation. Nat. Geosci. 6, 701–710 (2013).

Article CAS Google Scholar

Boyd, P. W. & Ellwood, M. J. The biogeochemical cycle of iron in the ocean. Nat. Geosci. 3, 675 (2010).

Article CAS Google Scholar

Raven, J. A. The iron and molybdenum use efficiencies of plant growth with different energy, carbon and nitrogen sources. N. Phytol. 109, 279–287 (1988).

Article CAS Google Scholar

Boyd, P. W. et al. Mesoscale iron enrichment experiments 1993-2005: Synthesis and future directions. Science 315, 612–617 (2007).

Article CAS PubMed Google Scholar

Anton, A. et al. Iron deficiency in seagrasses and macroalgae in the Red Sea is unrelated to latitude and physiological performance. Front. Mar. Sci. 5, https://doi.org/10.3389/fmars.2018.00074 (2018).

Boyd, P. Ironing out algal issues in the Southern Ocean. Science 304, 396–397 (2004).

Article CAS PubMed Google Scholar

de Baar, H. J. W. & de Jong, J. T. M. in Biogeochemistry of Iron in Seawater, Vol. 7 (eds Turner, D. & Hunter, K. A.) 123–253 (Wiley 2001).

Batchelli, S., Muller, F. L. L., Chang, K. C. & Lee, C. L. Evidence for strong but dynamic iron-humic colloidal associations in humic-rich coastal waters. Environ. Sci. Technol. 44, 8485–8490 (2010).

Article CAS PubMed Google Scholar

Natsuike, M. et al. Iron uptake kinetics by coastal micro- and macro-algae in relation to riverine and coastal organic matter. Estuar. Coast. Shelf Sci. 235, https://doi.org/10.1016/j.ecss.2019.106580 (2020).

Vieira, L. H. et al. Unprecedented Fe delivery from the Congo River margin to the South Atlantic Gyre. Nat. Commun. 11, 556 (2020).

Article CAS PubMed PubMed Central Google Scholar

Cooke, R. R. M. et al. Iron and zinc content of Hormosira banksii in New Zealand. N. Z. J. Mar. Freshw. Res. 38, 73–85 (2004).

Article CAS Google Scholar

Strzepek, R. F. & Harrison, P. J. Photosynthetic architecture differs in coastal and oceanic diatoms. Nature 431, 689–692 (2004).

Article CAS PubMed Google Scholar

North, W. J. Trace metals in Giant Kelp, Macrocystis. Am. J. Bot. 67, 1097–1101 (1980).

Article CAS Google Scholar

Liu, J., Dong, S., Liu, X. & Ma, S. Responses of the macroalga Gracilaria tenuistipitata var. liui (Rhodophyta) to iron stress. J. Appl. Phycol. 12, 605–612 (2000).

Article CAS Google Scholar

Suzuki, Y., Kuma, K. & Matsunaga, K. Bioavailable iron species in seawater measured by macroalga (Laminaria japonica) uptake. Mar. Biol. 123, 173–178 (1995).

Article CAS Google Scholar

Matsunaga, K., Suzuki, Y., Kuma, K. & Kudo, I. Diffusion of Fe(II) from an iron propagation cage and its effect on tissue iron and pigments of macroalgae on the cage. J. Appl. Phycol. 6, 397–403 (1994).

Article CAS Google Scholar

Suzuki, Y., Kuma, K., Kudo, I. & Matsunaga, K. Iron requirement of the brown macroalgae Laminaria japonica, Undaria pinnatifida (Phaeophyta) and the crustose coralline alga Lithophyllum yessoense (Rhodophyta), and their competition in the northern Japan Sea. Phycologia 34, 201–205 (1995).

Article Google Scholar

Manley, S. L. Iron uptake and translocation by Macrocystis pyrifera. Plant Physiol. 68, 914 (1981).

Article CAS PubMed PubMed Central Google Scholar

Boyd, P. W. et al. A mesoscale phytoplankton bloom in the polar Southern Ocean stimulated by iron fertilization. Nature 407, 695–702 (2000).

Article CAS PubMed Google Scholar

Raven, J. A., Evans, M. C. W. & Korb, R. E. The role of trace metals in photosynthetic electron transport in O2-evolving organisms. Photosynth. Res. 60, 111–149 (1999).

Article CAS Google Scholar

Timmermans, K. R., Stolte, W. & de Baar, H. J. W. Iron-mediated effects on nitrate reductase in marine phytoplankton. Mar. Biol. 121, 389–396 (1994).

Article CAS Google Scholar

Viaroli, P. et al. Nutrient and iron limitation to Ulva blooms in a eutrophic coastal lagoon (Sacca di Goro, Italy). Hydrobiologia 550, 57–71 (2005).

Article CAS Google Scholar

Shen, Y. & Benner, R. Mixing it up in the ocean carbon cycle and the removal of refractory dissolved organic carbon. Sci. Rep. 8, 2542 (2018).

Article PubMed PubMed Central Google Scholar

Wood, A. M. & Van Valen, L. M. Paradox lost on the release of energy rich compounds by phytoplankton. Mar. Microb. Food Webs 4, 103–116 (1990).

Google Scholar

Strzepek, R. F., Maldonado, M. T., Hunter, K. A., Frew, R. D. & Boyd, P. W. Adaptive strategies by Southern Ocean phytoplankton to lessen iron limitation: uptake of organically complexed iron and reduced cellular iron requirements. Limnol. Oceanogr. 56, 1983–2002 (2011).

Article CAS Google Scholar

Sunda, W. G. & Huntsman, S. A. Iron uptake and growth limitation in oceanic and coastal phytoplankton. Mar. Chem. 50, 189–206 (1995).

Article CAS Google Scholar

Schiel, D. R. & Foster, M. S. The Biology and Ecology of Giant Kelp Forests (University of California Press, 2015).

Leal, P. P., Roleda, M. Y., Fernández, P. A., Nitschke, U. & Hurd, C. L. Reproductive phenology and morphology of Macrocystis pyrifera (Laminariales, Ochrophyta) from southern New Zealand in relation to wave exposure. J. Phycol. 57, 1619–1635 (2021).

Article PubMed Google Scholar

GEOTRACES Intermediate Data Product Group. The GEOTRACES Intermediate Data Product 2021 (IDP2021). (NERC EDS British Oceanographic Data Centre NOC, 2021). https://doi.org/10.5285/cf2d9ba9-d51d-3b7c-e053-8486abc0f5fd.

Johnson, K. S., Gordon, R. M. & Coale, K. H. What controls dissolved iron concentrations in the world ocean? Mar. Chem. 57, 137–161 (1997).

Article CAS Google Scholar

Weigel, B. L. & Pfister, C. A. The dynamics and stoichiometry of dissolved organic carbon release by kelp. Ecology 102, e03221 (2021).

Article PubMed Google Scholar

Yamamoto, M., Kato, T., Kanayama, S., Nakase, K. & Tsutsumi, N. Effectiveness of iron fertilization for seaweed bed restoration in coastal areas. J. Water Environ. Technol. 15, 186–197 (2017).

Article Google Scholar

Yamamoto, M. & Liu, D. Effectiveness of iron supply in the coastal areas of Tsushima for restoring seaweed beds. 2012 Oceans - Yeosu, Yeosu, Korea (South), 1–5, (2012), https://doi.org/10.1109/OCEANS-Yeosu.2012.6263440.

Matsunaga, K., Kawaguchi, T., Suzuki, Y. & Nigi, G. The role of terrestrial humic substances on the shift of kelp community to crustose coralline algae community of the southern Hokkaido Island in the Japan Sea. J. Exp. Mar. Biol. Ecol. 241, 193–205 (1999).

Article Google Scholar

Boyd, P. W. et al. Potential negative effects of ocean afforestation on offshore ecosystems. Nat. Ecol. Evol. 6, 675–683 (2022).

Article PubMed Google Scholar

Paine, E. R., Schmid, M., Boyd, P. W., Diaz-Pulido, G. & Hurd, C. L. Rate and fate of dissolved organic carbon release by seaweeds: a missing link in the coastal ocean carbon cycle. J. Phycol. 57, 1375–1391 (2021).

Article CAS PubMed Google Scholar

Falkowski, P. G. & Raven, J. A. Aquatic Photosynthesis. 2nd edn, 375 (Princeton University Press, 2007).

Zakem, E. J. & Levine, N. M. Systematic variation in marine dissolved organic matter stoichiometry and remineralization ratios as a function of lability. Glob. Biogeochem. Cycles 33, 1389–1407 (2019).

Article CAS Google Scholar

Egan, S. et al. The seaweed holobiont: understanding seaweed–bacteria interactions. FEMS Microbiol. Rev. 37, 462–476 (2013).

Article CAS PubMed Google Scholar

Rueter, J. G. & Ades, D. R. The role of iron nutrition in photosynthesis and nitrogen assimilation in Scenedesmus quadricauda (Chlorophyceae). J. Phycol. 23, 452–457 (1987).

Article CAS Google Scholar

Miki, O. et al. Effects of Fe fertilizer eluate on the growth of Sargassum horneri at the germling and immature stages. J. Appl. Phycol. 28, 1775–1782 (2016).

Article CAS Google Scholar

Duarte, C. M., Martín, M. & Margarita, G. Evidence of iron deficiency in seagrasses growing above carbonate sediments. Limnol. Oceanogr. 40, 1153–1158 (1995).

Article CAS Google Scholar

Milligan, A. J. & Harrison, P. J. Effects of non-steady-state iron limitation on nitrogen assimilatory enzymes in the marine diatom Thalassiosira weissflogii (Bacillariophyceae). J. Phycol. 36, 78–86 (2000).

Article CAS Google Scholar

Yamamoto, M. et al. Application of iron humates to barren ground in a coastal area for restoring seaweed beds. J. Chem. Eng. Jpn. 43, 627–634 (2010).

Article CAS Google Scholar

North, W. J. Experimental cultivation of giant kelp in oceanic environments. Proceedings of the ASME ASME 1979 International Gas Turbine Conference and Exhibit and Solar Energy Conference. Vol. 2. Solar Energy. March 12–15, (San Diego, California, USA, 1979). V002T03A030. ASME. https://doi.org/10.1115/79-SOL-30.

Smetacek, V. & Zingone, A. Green and golden seaweed tides on the rise. Nature 504, 84–88 (2013).

Article CAS PubMed Google Scholar

Godínez-Ortega, J. L., Cuatlán-Cortés, J. V., López-Bautista, J. M. & van Tussenbroek, B. I. A natural history of floating sargassum Species (Sargasso) from Mexico. (ed. Hufnagel, L.) Natural History and Ecology of Mexico and Central America. 59–94 (IntechOpen, London, 2021).

Devault, D. et al. The silent spring of Sargassum. Environ. Sci. Pollut. Res. 28, https://doi.org/10.1007/s11356-020-12216-7 (2021).

Wu, J. & Boyle, E. Iron in the Sargasso Sea: Implications for the processes controlling dissolved Fe distribution in the ocean. Glob. Biogeochem. Cycles 16, 33–38 (2002).

Article Google Scholar

Carder, K. L., Steward, R. G., Betzer, P. R., Johnson, D. L. & Prospero, J. M. Dynamics and composition of particles from an aeolian input event to the Sargasso Sea. J. Geophys. Res. Atmos. 91, 1055–1066 (1986).

Article Google Scholar

Lapointe, B. E. A comparison of nutrient-limited productivity in Sargassum natans from neritic vs. oceanic waters of the western North Atlantic Ocean. Limnol. Oceanogr. 40, 625–633 (1995).

Article CAS Google Scholar

Bach, L. T. et al. Testing the climate intervention potential of ocean afforestation using the Great Atlantic Sargassum Belt. Nat. Comm. 12, 2556 (2021).

Article CAS Google Scholar

Subramaniam, A. et al. Amazon River enhances diazotrophy and carbon sequestration in the tropical North Atlantic Ocean. Proc. Natl Acad. Sci. USA 105, 10460–10465 (2008).

Article CAS PubMed PubMed Central Google Scholar

Tollefson, J. Iron-dumping ocean experiment sparks controversy. Nature 545, 393–394 (2017).

Service, R. F. Legal? Perhaps. But Controversial Fertilization Experiment May Produce Little Science. Science Insider. Science, Portland, Oregon. Science Insider (Science, 2012).

Strong, A. L., Cullen, J. J. & Chisholm, S. W. Ocean fertilization science, policy, and commerce. Oceanography 22, 236–261 (2009).

Article Google Scholar

Temple, J. Running Tide is facing scientist departures and growing concerns over seaweed sinking for carbon removal. MIT Technol. Rev. (2022). https://www.technologyreview.com/2022/06/16/1053758/running-tide-seaweed-kelp-scientist-departures-ecological-concerns-climate-carbon-removal/.

Cutter, G. et al. Sampling and Sample-handling Protocols for GEOTRACES Cruises. In: (ed. Committee, G. S. a. I.). 3.0 ed., 125 (2017).

Sunda, W. & Huntsman, S. Effect of pH, light, and temperature on Fe–EDTA chelation and Fe hydrolysis in seawater. Mar. Chem. 84, 35–47 (2003).

Article CAS Google Scholar

Standard Methods Committee of the American Public Health Association, American Water Works Association and Water Environment Federation. In Standard Methods For the Examination of Water and Wastewater (eds Lipps, W. C. et al.) (APHA Press, 2017).

Hurd, C. L., Berges, J. A., Osborne, J. & Harrison, P. J. Erratum: an in vitro reductase assay for marine microalgae: optimization and characterization of the enzyme for Fucus gardneri (Phaeophyta) (Journal of Phycology 31 (835-431)). J. Phycol. 32, 1094 (1996).

Google Scholar

Seely, G. R., Duncan, M. J. & Vidaver, W. E. Preparative and analytical extraction of pigments from brown algae with dimethyl sulfoxide. Mar. Biol. 12, 184–188 (1972).

Article CAS Google Scholar

Wheeler, W. N. Pigment content and photosynthetic rate of the fronds of Macrocystis pyrifera. Mar. Biol. 56, 97–102 (1980).

Article CAS Google Scholar

Stephens, T. A. & Hepburn, C. D. Mass-transfer gradients across kelp beds influence Macrocystis pyrifera growth over small spatial scales. Mar. Ecol. Prog. Ser. 515, 97–109 (2014).

Article Google Scholar

Pella, E. & Colombo, B. Study of carbon, hydrogen and nitrogen determination by combustion-gas chromatography. Mikrochimica Acta 61, 697–719 (1973).

Article Google Scholar

Nelson, C. E. et al. Coral and macroalgal exudates vary in neutral sugar composition and differentially enrich reef bacterioplankton lineages. ISME J. 7, 962–979 (2013).

Article CAS PubMed PubMed Central Google Scholar

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The authors thank to Dr. Abigail Smith, Dr. Pauline Latour and Olivia Wynn for their laboratory assistance and the reviewers for providing useful feedback on the manuscript. The GEOTRACES 2021 Intermediate Data Product (IDP2021) represents an international collaboration and is endorsed by the Scientific Committee on Oceanic Research (SCOR). The many researchers and funding agencies responsible for the collection of data and quality control are thanked for their contributions to the IDP2021, as are the researchers and staff aboard the RV Investigator voyage IN2019_V02 who collected the base seawater for the experiment. We acknowledge and pay our respects to the Palawa people of Lunawanna-Allonah and Nipaluna, whose water and land upon which we work. Laureate Fellowship FL160100131 to P.W.B., ARC DP160103071 funding to GD-P and C.L.H., AAPP ASCI000002 funding to R.F.S., and ARC DP200101467 to C.L.H. MS was funded consecutively through a Science Foundation Ireland grant (18/FR/6198) and a European Commission Marie Skłodowska-Curie Actions Postdoctoral Fellowship (Project 101066815 —ASPIRE).

Institute for Marine and Antarctic Studies, University of Tasmania, Hobart, TAS, 7001, Australia

Ellie R. Paine, Philip W. Boyd, Matthias Schmid & Catriona L. Hurd

Australian Antarctic Program Partnership (AAPP), Institute for Marine and Antarctic Studies, University of Tasmania, Hobart, TAS, Australia

Robert F. Strzepek

Research School of Earth Sciences, The Australian National University, Canberra, ACT, 0200, Australia

Michael Ellwood

CSIRO Oceans and Atmosphere, Castray Esplanade, Hobart, TAS, 7001, Australia

Elizabeth A. Brewer

School of Environment and Science, Coastal and Marine Research Centre, and Australian Rivers Institute—Coast and Estuaries, Nathan Campus, Griffith University, Brisbane, QLD, 4111, Australia

Guillermo Diaz-Pulido

Trinity College Dublin, University of Dublin, Dublin, Ireland

Matthias Schmid

School of Biological and Chemical Sciences, University of Galway, Galway, Ireland

Matthias Schmid

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E.R.P., P.W.B. and C.L.H. conceived and designed the study. E.R.P. performed the experiment, analysed the results and wrote the manuscript. R.F.S. provided trace-metal expertise for the duration of the study and contributed to writing the manuscript. E.A.B. analysed seaweed dry tissue carbon and nitrogen samples. M.E. analysed the trace-metal concentrations of seawater samples and provided trace-metal expertise. G.D.-P. and M.S. contributed to writing the manuscript. All co-authors equally contributed to editing the manuscript.

Correspondence to Ellie R. Paine.

The authors declare no competing interests.

Communications Biology thanks Professor Michael Stekoll and the other, anonymous, reviewer(s) for their contribution to the peer review of this work. Primary Handling Editor: David Favero.

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Paine, E.R., Boyd, P.W., Strzepek, R.F. et al. Iron limitation of kelp growth may prevent ocean afforestation. Commun Biol 6, 607 (2023). https://doi.org/10.1038/s42003-023-04962-4

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