2.1 Macro-nutrient and dissolved Fe concentration analyses

Samples for the quantification of nitrate (${\mathrm{NO}}_{\mathrm{3}}^{-}$) and dissolved inorganic phosphorus (DIP) concentrations were collected at 12 depths between 0 and 200 m in acid-washed polyethylene bottles, poisoned with mercuric chloride (HgCl₂, final concentration 20 mg L⁻¹) and stored at 4 ^∘C until analysis. Concentrations were determined using standard colorimetric techniques (Aminot and Kérouel, 2007) on a Bran Luebbe AA3 autoanalyzer. Detection limits for the procedures were 0.05 µmol L⁻¹ for ${\mathrm{NO}}_{\mathrm{3}}^{-}$ and DIP.

Samples for determining dissolved Fe concentrations were collected and analyzed as described in Guieu et al. (2018). Briefly, samples were collected using a Titane rosette mounted with 24 Teflon-coated 12 L GoFlos deployed with a Kevlar cable. Dissolved Fe concentrations were measured by flow injection with online preconcentration and chemiluminescence detection according to Bonnet and Guieu (2006). The reliability of the method was monitored by analyzing the D1 SAFe seawater standard (Johnson et al., 2007), and an internal acidified seawater standard was measured daily to monitor the stability of the analysis.

The sampling and analytical methods used to analyze the other parameters reported in the correlation table (Table 2) are described in detail in the methods sections for related papers in this issue (Bock et al., 2018; Fumenia et al., 2018; Stenegren et al., 2018; Van Wambeke et al., 2018).

Table 1¹⁵N ∕ ¹⁴N ratio of suspended particulate nitrogen (PN) (average over the photic layer) across the OUTPACE transect.

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Table 2Summary of relationships between measured N₂ fixation rates and various physical and biogeochemical parameters. Also shown are correlations between measured rates and the several diazotrophic or non-diazotrophic planktonic groups enumerated at the respective stations. The corresponding unit is given for each parameter, and Spearman's rank correlation (n=102, α=0.05) is provided; significant correlations (p < 0.05) are indicated by an asterisk (^∗).

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2.2 Bulk N₂ fixation rate measurements

Whole water (bulk) N₂ fixation rates were measured in triplicate at all 17 stations using the ¹⁵N₂ isotopic tracer technique (adapted from Montoya et al., 1996). The ¹⁵N₂ bubble technique was intentionally chosen due to the time limitation on making enriched ¹⁵N₂ seawater inoculates (e.g., 6–9 depths = 6–9 inoculates) and the larger sample bottles required for making proper estimates of activity in oligotrophic environments. In addition, we aimed to avoid any potential overestimation due to trace metal and dissolved organic matter (DOM) contaminations often associated with the preparation of the ¹⁵N₂-enriched seawater (Klawonn et al., 2015; Wilson et al., 2012) in our incubation bottles as Fe and DOM have been found to control N₂ fixation or nifH gene expression in this region (Benavides et al., 2017; Moisander et al., 2011). However, the ¹⁵N ∕ ¹⁴N ratio of the N₂ pool available for N₂ fixation (the term AN₂ used in Montoya et al., 1996) was measured in all incubation bottles by membrane inlet mass spectrometry (MIMS) to ensure accurate rate calculations (see below).

Seawater samples were collected from Niskin bottles into 10 % HCl-washed, sample-rinsed (three times) light-transparent polycarbonate (2.3 L) bottles from six depths (75, 50, 20, 10, 1, and 0.1 % surface irradiance levels) at all short-duration stations SD1 to SD15 and nine depths (75, 50, 35, 20, 10, 3, 1, 0.3, and 0.1 % surface irradiance levels) at LD A, LDB and LD C, corresponding to the sub-surface (5 m) down to 80 to 180 m, depending on the station. Bottles were sealed with caps fitted with silicon septa and amended with 2 mL of 98.9 at. % ¹⁵N₂ (Cambridge isotopes). The purity of the ¹⁵N₂ Cambridge isotope stocks was previously checked by Dabundo et al. (2014) and more recently by Benavides et al. (2015) and Bonnet et al. (2016a). They were found to be lower than $\mathrm{2}\times {\mathrm{10}}^{-\mathrm{8}}$ mol : mol of ¹⁵N₂, leading to a potential N₂ fixation rate overestimation of < 1 %. Each bottle was shaken 20 times to break the ¹⁵N₂ bubble and facilitate its dissolution, and was incubated for 24 h. At SD stations, bottles were incubated in on-deck incubators connected to surface circulating seawater at the specified irradiances using blue screening as the duration of the station (8 h) was too short to deploy in situ mooring lines. At LD stations (7 days), one profile was incubated following the same methodology in on-deck incubators and another replicate profile was incubated in situ for comparison on a drifting mooring line located at the same depth from which the samples were collected. Incubations were stopped by filtering the entire incubation bottle onto pre-combusted (450 ^∘C, 4 h) 25 mm diameter glass fiber filters (GF/F, Whatman, 0.7 µm nominal pore size). Filters were subsequently dried at 60 ^∘C for 24 h before analysis of ¹⁵N ∕ ¹⁴N ratios and particulate N (PN) determinations using an elemental analyzer coupled to a mass spectrometer (EA-IRMS, Integra CN, SerCon Ltd) as described in Bonnet et al. (2011).

To ensure accurate rate calculations, the ¹⁵N ∕ ¹⁴N ratio of the N₂ pool in the incubation bottles was measured on each profile from triplicate surface incubation bottles from SD1 to SD14 and at all depths at SD15 and LD stations. Briefly, 12 mL was subsampled after incubation into Exetainers fixed with HgCl₂ (final concentration 20 mg L⁻¹) that were preserved upside down in the dark at 4 ^∘C until analyzed using a MIMS according to Kana et al. (1994). Lastly, we collected time zero samples at each station to determine the natural N isotopic signature of ambient particulate N (PN). The minimum quantifiable rates (quantification limit, QL) calculated using standard propagation of errors via the observed variability between replicate samples measured according to Gradoville et al. (2017) were 0.035 nmol N L⁻¹ d⁻¹.

Discrete N₂ fixation rate measurements were depth integrated over the photic layer using trapezoidal integration procedures. Briefly, the N₂ fixation at each pair of depths is averaged, and then multiplied by the difference between the two depths to get a total N₂ fixation in that depth interval. These depth interval values are then summed over the entire depth range to get the integrated N₂ fixation rate. The rate nearest the surface is assumed to be constant up to 0 m (Knap et al., 1996).

2.3 Statistical analyses

Spearman's rank correlation was used to examine the potential relationships between N₂ fixation rates and hydrological, biogeochemical, and biological parameters across the longitudinal transect (n=102, α=0.05). A non-parametric Mann–Whitney test (α=0.05) was used to compare the MIMS data obtained following on-deck versus in situ incubations, and to compare nutrient and Chl a distributions between the western part and the eastern part of the transect.

2.4 Group-specific N₂ fixation rate measurements

3.1 Environmental conditions

Seawater temperature ranged from 21.4 to 30.0 ^∘C in the sampled photic layer (0 to ∼ 80–180 m) over the cruise transect (Fig. 2a). The mixed layer depth (MLD) calculated according to the de Boyer Montégut et al. (2004) method was located around 20–40 m throughout the zonal transect: maximum temperatures were measured in the surface mixed layer (∼ 0–20∕40 m) and remained almost constant along the longitudinal transect with 29.1 ± 0.3 ^∘C in MA waters and 29.5 ± 0.4 ^∘C in GY waters.

Figure 2Horizontal and vertical distributions of (a) seawater temperature (^∘C), (b) chlorophyll fluorescence (µg L⁻¹), (c) ${\mathrm{NO}}_{\mathrm{3}}^{-}$ (µmol L⁻¹), (d) DIP (µmol L⁻¹) and (e) N₂ fixation rates (nmol N L⁻¹ d⁻¹) across the OUTPACE transect. LD stations are noted and the extent of the two defined sub-regions: MA: Melanesian archipelago waters, GY: South Pacific Gyre waters. Y axis: pressure (dbar), X axis: longitude; black dots correspond to sampling depths at the various SD and LD stations.

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Based on other hydrographic measurements (dissolved nutrients, dissolved Fe and Chl a concentrations), the longitudinal transect was divided into two sub-regions: (1) the MA region from station SD1 (160^∘ E) to LDB (165^∘ W), and (2) the GY sub-region from station LDB (165 ^∘ W) to SD15 (160^∘ W). Chl a concentration in the upper 50 m was significantly (p< 0.05) higher in MA waters (0.17 µg L⁻¹ on average) than in GY waters (0.06 µg L⁻¹ on average) (Figs. 1 and 2b). The DCM was located around 80–100 m in MA waters and deepened to ∼ 150 m in GY waters, indicating higher oligotrophy in the GY region. Surface ${\mathrm{NO}}_{\mathrm{3}}^{-}$ concentrations (Fig. 2c) were consistently close to or below the detection limit (0.05 µmol L⁻¹) in the upper water column (0–50 m) throughout the transect and the depth of the nitracline gradually deepened from ∼ 75–100 m in MA waters to ∼ 115 m in GY waters. DIP concentrations were slightly higher than or close to detection limits (0.05 µmol L⁻¹) in MA surface waters (0–50 m), and the phosphacline was shallower (20–45 m) than the nitracline and DIP concentrations increased significantly (p < 0.05) in GY waters and ranged from 0.13 to 0.17 µmol L⁻¹ (Fig. 2d).

3.2 N isotopic signature of the N₂ pool after incubation

The ¹⁵N enrichment of the N₂ pool after 24 h of incubation with the ¹⁵N₂ tracer was on average 6.145 ± 0.798 at. % (n=54) in bottles incubated in on-deck incubators and significantly higher (p < 0.05) in bottles incubated on the mooring line (7.548 ± 0.557 at. % (n=44), Fig. 3a). However, the depth of incubation on the mooring line (between 5 and 180 m) did not have any significant effect (p > 0.05) on the isotopic signature of the N₂ pool at LDB and LDC, which remained constant over the water column (Fig. 3b).

Figure 3(a) The average measured ¹⁵N ∕ ¹⁴N ratio of the N₂ pool in the incubation bottles incubated either in on-deck incubators (n=54) or in situ (mooring line) (n=44). The dashed lines represent the theoretical value (∼ 8.2 at. %) calculated assuming complete isotopic equilibration between the gas bubble and the seawater based on gas constants. Error bars represent the standard deviation (b) depth profiles of the ¹⁵N ∕ ¹⁴N ratio of the N₂ pool in the incubation bottles incubated either in on-deck incubators (filled symbols) or on an in situ mooring line (open symbols).

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3.3 Natural isotopic signature of suspended particles and N₂ fixation rates

The natural N isotopic signature of suspended particles measured over the photic layer was on average −0.41 ‰ in MA waters and 8.06 ‰ in GY waters (Table 1). Those isotopic values were used as time zero samples to calculate N₂ fixation rates.

N₂ fixation was detected at all 17 sampled stations and the average measured N₂ fixation rates in the two previously defined sub-regions were (1) 8.9 ± 10 nmol N L⁻¹ d⁻¹ (range QL-48 nmol N L⁻¹ d⁻¹) over the photic layer in MA waters, and 2) 0.5 ± 0.6 nmol N L⁻¹ d⁻¹ (range QL-4.0 nmol N L⁻¹ d⁻¹) in GY waters (Fig. 2e). In MA waters, N₂ fixation was largely restricted to the mixed layer, where average rates were 15 nmol N L⁻¹ d⁻¹, with local maxima (> 20 nmol N L⁻¹ d⁻¹) at stations SD1, SD6 and LDB and local minima (< 5 nmol N L⁻¹ d⁻¹) at SD8 and SD10. In GY waters, maximum rates reached 1–2 nmol N L⁻¹ d⁻¹ and were located deeper in the water column (∼ 50 m). When integrated over the photic layer, N₂ fixation represented an average net N addition of 631 ± 286 $\mathrm{\mu }\mathrm{mol}\mathrm{N}{\mathrm{m}}^{-\mathrm{2}}{\mathrm{d}}^{-\mathrm{1}}$ (range 196–1153 $\mathrm{\mu }\mathrm{mol}\mathrm{N}{\mathrm{m}}^{-\mathrm{2}}{\mathrm{d}}^{-\mathrm{1}}$) in MA waters and of 85 ± 79 $\mathrm{\mu }\mathrm{mol}\mathrm{N}{\mathrm{m}}^{-\mathrm{2}}{\mathrm{d}}^{-\mathrm{1}}$ (range 18–172 $\mathrm{\mu }\mathrm{mol}\mathrm{N}{\mathrm{m}}^{-\mathrm{2}}{\mathrm{d}}^{-\mathrm{1}}$) in GY waters.

N₂ fixation rates were significantly positively correlated with seawater temperature and photosynthetically active radiation (PAR) (p < 0.05), significantly negatively correlated with depth and salinity (p < 0.05) and not significantly correlated with dissolved oxygen concentrations (p > 0.05) (Table 2). N₂ fixation rates were significantly positively correlated with dissolved Fe, dissolved organic N (DON), phosphorus (DOP), carbon (DOC), particulate organic N (PON), particulate organic carbon (POC), biogenic silica (BSi), Chl a concentrations, and primary and bacterial production (p < 0.05), and significantly negatively correlated with concentration of dissolved nutrients: ${\mathrm{NO}}_{\mathrm{3}}^{-}$, NH${}_{\mathrm{4}}^{+}$, DIP and silicate (p < 0.05). N₂ fixation rates were significantly positively correlated with nifH abundances for Trichodesmium spp., UCYN-B and the symbionts of DDAs (het-1, het-2) (p < 0.05) and not significantly correlated with UCYN-A1 and UCYN-A2 abundances (p > 0.05) (Table 2). Regarding non-diazotrophic plankton, N₂ fixation rates were significantly positively correlated with Prochlorococcus spp., Synechococcus spp., heterotrophic bacteria and protist abundances (p < 0.05) and significantly negatively correlated with picoeukaryotes (p < 0.05).

3.4 Contribution of Trichodesmium and UCYN-B to N₂ fixation and nitrogenase gene expression

At the three stations where cell-specific N₂ fixation rates were estimated by nanoSIMS (SD2, SD6 and LDB), the most abundant diazotroph phylotype was Trichodesmium with 1.3 × 10⁵, 3.3 × 10⁵ and 1.2 × 10⁵ cells L⁻¹, respectively, followed by UCYN-B, whose abundances were 2.0 × 10⁴, 1.5 × 10⁵ and 3.8 × 10² nifH copies L⁻¹, respectively. Het-1 and het-2 combined were 1 to 2 orders of magnitude lower, ranging from 1.0 to 9.9 × 10³ nifH copies L⁻¹, and UCYN-A1 were below detection at the three stations. In summary, Trichodesmium and UCYN-B accounted for 98.2, 99.8 and 92.1 % of the total diazotroph community (based on the phylotypes targeted here) at SD2, SD6 and LDB, respectively (Table 3).

Table 3Summary of diazotroph abundances and nanoSIMS analyses at SD2, SD6 and LDB.

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The ¹⁵N ∕ ¹⁴N ratios of individual cells/trichomes of UCYN-B and Trichodesmium were measured via nanoSIMS analyses and used to estimate single-cell N₂ fixation rates. A summary of the enrichment values and cell-specific N₂ fixation is provided in Table 3. Individual trichomes exhibited significant ¹⁵N enrichments (0.610 ±  0.269, 0.637 ± 0.355 and 0.981 ± 0.466 at. % at stations SD2, SD6 and LDB, respectively) compared with time zero samples (0.369 ± 0.002 at. %). UCYN-B were also significantly ¹⁵N-enriched, with 1.163 ± 0.531 and 0.517 ± 0.237 at. % at SD2 and SD6, respectively (note that no UCYN-B could be sorted and analyzed by nanoSIMS at LDB as they accounted for only 0.3 % of the diazotroph community). Cell-specific N₂ fixation rates of Trichodesmium were 38.9 ± 8.1, 29.3 ± 5.4 and 123.8 ± 24.8 fmol N cell⁻¹ d⁻¹ at SD2, SD6 and LDB. Cell-specific N₂ fixation of UCYN-B was 30.0 ± 6.4 and 6.1 ± 1.2 fmol N cell⁻¹ d⁻¹ at SD1 and SD6. The contribution of Trichodesmium to bulk N₂ fixation was 83.8, 47.1 and 52.9 % at stations SD2, SD6 and LDB, respectively. The contribution of UCYN-B was 10.1 and 6.1 % at SD2 and SD6, respectively (Table 3).

The in situ nifH expression for all diazotroph groups targeted by qPCR was estimated using a TaqMAN quantitative reverse transcription PCR (RT-qPCR) (Table 4). The sampling and filtering time (17:00–21:00 h) was not optimal for quantifying the nifH gene expression for all diazotrophs; however, it provides useful information about which diazotrophs were potentially active during the experiment and complements the nanoSIMS analysis which measures the in situ activity. Both Trichodesmium and UCYN-B dominated the biomass (Stenegren et al., 2018), as did their nifH gene expression at all three stations, especially SD2 and SD6. Of the two DDAs, het-1 had a higher nifH gene expression, which was consistent with its higher nifH abundance by DNA qPCR (Stenegren et al., 2018). UCYN-A1 was consistently below detection for the nifH gene expression and was also the least detected diazotroph by nifH qPCR (Stenegren et al., 2018).

Table 4Summary of nifH gene expression data determined by qRT-PCR at selected stations (SD2, SD6, LDB), where the cell-specific N₂ fixation rates were measured.

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4.1 Methodological considerations: the importance of measuring the ¹⁵N ∕ ¹⁴N ratio of the N₂ pool

Our understanding of the marine N cycle relies on accurate estimates of N fluxes to and from the ocean. Here we decided to use the “bubble addition method” to minimize potential trace metal and organic matter contaminations, which may have resulted in overestimating rates (Klawonn et al., 2015). Moreover, a recent extensive meta-analysis (13 studies, 368 observations) between bubble and enriched amendment experiments to measure ¹⁵N₂ rates reported that underestimation of N₂ fixation is negligible in experiments that last 12–24 h (e.g., error is −0.2 %); hence our 24 h based experiments should be within a small amount of error (Wannicke et al., 2018). However, we paid careful attention to accurately measure the term AN₂ to avoid any potential underestimation and reveal that the way bottles are incubated (on-deck versus in situ) has a great influence on the AN₂ value, and thus on N₂ fixation rates.

Our MIMS results measured a significantly (p < 0.05) lower ¹⁵N enrichment of the N₂ pool (6.145 ± 0.798 at. %) when bottles were incubated in on-deck incubators compared to when bottles were incubated on the mooring line (7.548 ± 0.557 at. %). This suggests that the ¹⁵N₂ dissolution is much more efficient when bottles are incubated in situ, probably due to the higher pressure in seawater at the depth of incubation (1.5 to 19 bars between 5 and 180 m) compared to the pressure in the on-deck incubators (1 bar). The seawater temperature checked regularly in the on-deck incubators was equivalent to ambient surface temperature and likely did not explain the differences observed. This result highlights the need to perform routine MIMS measurements to use the most accurate AN₂ value for rate calculations, independently of the ¹⁵N₂ approach used (gas or dissolved). In our study, the theoretical AN₂ value based on gas constant calculations (Weiss, 1970) was ∼ 8.2 at. %, so the deviation from this value is more important when bottles are incubated in on-deck incubators as compared to when they are incubated in situ. This suggests that the use of the bubble addition method without MIMS measurement potentially leads to higher underestimations when bottles are incubated in on-deck incubators, which is the case in the great majority of marine N₂ fixation studies published so far (Luo et al., 2012). We are aware that the dissolution kinetics of ¹⁵N₂ in the incubation bottles may have been progressive along the 24 h of incubation (Mohr et al., 2010); therefore, the N₂ fixation rates provided here represent conservative values.

Despite the AN₂ value being different according to the incubation mode, it did not change with the depth of incubation on the mooring line, indicating that a slightly higher pressure than atmospheric pressure (1.5 bar at 5 m depth) is enough to promote the ¹⁵N₂ dissolution. It also indicates that the slightly lower seawater temperature (22–24 ^∘C) recorded at ∼ 100–180 m where the deepest samples were incubated likely did not affect the solubilization of the ¹⁵N₂ gas. In our study, the vertical profiles performed at LD stations and incubated either on-deck in triplicate or in situ in triplicate reveal identical (p > 0.05) N₂ fixation rates regardless of the incubation method used (Caffin et al., 2018b). This indicates that in situ incubations and on-deck incubations that simulate appropriate light levels are a valid methodology for ¹⁵N₂ fixation rate measurements on cruises during which mooring lines cannot be deployed, as long as routine measurements of the isotopic ratio of the N₂ pool are performed in incubation bottles.

4.2 Drivers of high N₂ fixation rates in the WTSP?

N₂ fixation rates measured in MA waters (average 631 ± 286 $\mathrm{\mu }\mathrm{mol}\mathrm{N}{\mathrm{m}}^{-\mathrm{2}}{\mathrm{d}}^{-\mathrm{1}}$) are 3 to 4 times higher than model predictions for this area (150–200 $\mathrm{\mu }\mathrm{mol}\mathrm{N}{\mathrm{m}}^{-\mathrm{2}}{\mathrm{d}}^{-\mathrm{1}}$, Gruber, 2016). They are in the upper range of the higher category (100–1000 $\mathrm{\mu }\mathrm{mol}\mathrm{N}{\mathrm{m}}^{-\mathrm{2}}{\mathrm{d}}^{-\mathrm{1}}$) of rates defined by Luo et al. (2012) in the N₂ fixation MAREDAT database for the global ocean and thus identify the WTSP as an area for high N₂ fixation in the global ocean. Recent studies performed in the western part of the WTSP, i.e., in the Solomon, Bismarck (Berthelot et al., 2017; Bonnet et al., 2009, 2015) and Arafura (Messer et al., 2015; Montoya et al., 2004) seas, also reveal extremely high rates (> 600 $\mathrm{\mu }\mathrm{mol}\mathrm{N}{\mathrm{m}}^{-\mathrm{2}}{\mathrm{d}}^{-\mathrm{1}}$), indicating that this high N₂ fixation activity area extends geographically west–east from Australia to Tonga and north–south from the Equator to 25–30^∘ S, covering a vast ocean area of ∼ 13×106 km² (i.e., ∼ 20 % of the South Pacific Ocean area). However, the driver(s) for diazotrophy in this region is(are) still poorly resolved and raise(s) the question of which factors influence the distribution and activity of N₂ fixation in the ocean. In a global-scale study conducted by Luo et al. (2014), which investigated the correlations between N₂ fixation and a variety of environmental parameters commonly accepted to control this process, they concluded that SST (or surface solar radiation) was the best predictor to explain the spatial distribution of N₂ fixation in the surface ocean. Below we highlight the most plausible factors explaining such high N₂ fixation rates in our study area.

Seawater temperature. Seawater temperature was unlikely to be the factor explaining the differences in N₂ fixation rates observed between MA and GY waters, as it was consistently high (> 28 ^∘C in the surface mixed layer) and optimal for the growth and nitrogenase activity of most diazotrophs (Breitbarth et al., 2007; Nübel et al., 1997) all along the cruise transect. This indicates that other factors such as nutrient availability may explain the distribution of N₂ fixation.

DIP availability. The ∼ 4000 km transect was divided into two main sub-regions: (1) the MA waters, harboring typical oligotrophic conditions with surface ${\mathrm{NO}}_{\mathrm{3}}^{-}$ and DIP concentrations close to detection limits (0.05 µmol L⁻¹), a nitracline located at 75–100 m, moderate surface Chl a concentrations (∼ 0.17 µg L⁻¹), a DCM located at ∼ 80–100 m and very high N₂ fixation rates (631 ± 286 $\mathrm{\mu }\mathrm{mol}\mathrm{N}{\mathrm{m}}^{-\mathrm{2}}{\mathrm{d}}^{-\mathrm{1}}$ on average), and (2) the GY waters harboring ultra-oligotrophic conditions with undetectable ${\mathrm{NO}}_{\mathrm{3}}^{-}$, a deeper nitracline (115 m), and comparatively high DIP concentrations (0.15 µmol L⁻¹), very low Chl a concentrations (0.06 µg L⁻¹, DCM ∼ 150 m) and low N₂ fixation rates (85 ± 79 $\mathrm{\mu }\mathrm{mol}\mathrm{N}{\mathrm{m}}^{-\mathrm{2}}{\mathrm{d}}^{-\mathrm{1}}$).

In the ${\mathrm{NO}}_{\mathrm{3}}^{-}$-depleted MA waters, low DIP concentrations are indicative of the consumption of DIP by the planktonic community, including diazotrophs. This is consistent with the negative correlation found between N₂ fixation and DIP turnover time (the ratio between DIP concentrations and DIP uptake rates) (Table 2) and suggests a higher DIP limitation when N₂ fixation is high and consumes DIP. The high DIP concentrations (> 0.1 µmol L⁻¹) in GY surface waters compared to MA waters are consistent with former studies that consider the South Pacific Gyre as a high phosphate, low chlorophyll ecosystem (Moutin et al., 2008), in which DIP accumulates in the absence of ${\mathrm{NO}}_{\mathrm{3}}^{-}$ and low N₂ fixation activity. In the high phosphate, low chlorophyll scenario, the community is limited by temperature and/or Fe availability (Moutin et al., 2008; Bonnet et al., 2008). During the OUTPACE cruise, the DIP turnover time was variable but close to or below 2 days in MA waters (Moutin et al., 2018), indicating a potential limitation by DIP at some stations. Trichodesmium, the most abundant and major contributor to N₂ fixation during the cruise, is known to synthesize hydrolytic enzymes in order to acquire P from the dissolved organic phosphorus pool (DOP) (Sohm and Capone, 2006). Moreover, Trichodesmium spp. differs from the other major diazotroph UCYN-B enumerated on the cruise in the forms of organic P it can synthesize. It is thus likely that DOP species that favored Trichodesmium over UCYN-B played a role in maintaining high Trichodesmium biomass in MA waters. It has to be noted that average DIP turnover times in MA waters were always much higher than those typically measured in severely DIP-limited environments such as the Mediterranean and Sargasso seas (e.g., Moutin et al., 2008), suggesting that DIP concentrations are generally favorable for the development of certain diazotrophs in the WTSP, and do not alone explain why N₂ fixation is high in MA waters and low in GY waters. However, it is likely that the depletion of DIP stocks at the end of the austral summer season forces the decline of diazotrophic blooms in the WTSP (Moutin et al., 2005), concomitantly with the decline of SST.

Fe availability. Before OUTPACE, our knowledge on Fe sources and concentrations in the WTSP was limited, especially in MA waters. During OUTPACE, Guieu et al. (2018) reported high dissolved Fe concentrations in MA waters (range 0.2–66.2 nmol L⁻¹, 1.7 nmol L⁻¹ on average over the photic layer), i.e., significantly (p < 0.05) higher than those reported in GY waters (range 0.2–0.6 nmol L⁻¹, 0.3 nM on average over the photic layer). The low dissolved Fe concentrations measured in the GY waters agree well with previous reports for the same region (Blain et al., 2008; Fitzsimmons et al., 2014). However, the high dissolved Fe concentrations measured in MA waters were previously undocumented and reveal several maxima (> 50 nmol L⁻¹) between stations SD7 and SD11, indicative of intense fertilization processes taking place in this region. Guieu et al. (2018) found that atmospheric deposition measured during the cruise in this region was too low to explain the observed dissolved Fe concentrations in the surface water column. The seafloor of the WTSP hosts the Tonga–Kermadec subduction zone which stretches 2500 km from New Zealand to the Tonga archipelago (Fig. 1). It has among the highest densities of submarine volcanoes associated with hydrothermal vents recorded in the ocean (2.6 vents / 100 km, Massoth et al., 2007), which discharge large quantities of material into the water column, including biogeochemically relevant elements such as Fe and Mn. Guieu et al. (2018) used hydrological data recorded by Argo float in situ measurements, atlas data and simulations from a general ocean circulation model to argue that the high dissolved Fe concentrations may be sustained by a submarine source. They show that such Fe inputs could spread throughout the WTSP through mesoscale activity mainly westward through the South Equatorial Current, SEC (Fig. 1). Guieu et al. (2018) hypothesize that the high dissolved Fe concentrations in MA waters compared to the GY ones is due to shallow inputs of hydrothermal origin together with potential Fe input from islands themselves (Shiozaki et al., 2014). In our study, dissolved Fe concentrations were significantly positively correlated with N₂ fixation and help to explain the distribution of N₂ fixation rates measured across the OUTPACE transect.

In summary, our hypothesis to explain the spatial distribution of N₂ fixation in MA waters is the following: when high DIP waters flow westward from the ETSP through the SEC and cross the South Pacific Gyre, N₂-fixing organisms do not develop despite optimal SST (> 25 ^∘C), likely because GY waters are Fe-depleted (Moutin et al., 2008; Bonnet et al., 2008). When the high DIP, low DIN (dissolved inorganic N) waters from the gyre are advected west of the Tonga trench in Fe-rich and warm (> 25 ^∘C) waters, all environmental conditions are fulfilled for diazotrophs to bloom extensively. According to Moutin et al. (2018), the strong depth difference between the nitracline and the phosphacline in MA waters associated with winter mixing allows a seasonal replenishment of DIP, which creates an excess of P relative to N and thus also favors N₂ fixation in this region. Further investigations are required to better quantify Fe input from both islands and shallow volcanoes and associated hydrothermal activity along the Tonga volcanic arc for the upper mixed layer, study the fate of hydrothermal plumes in the water column at the local and regional scales, and investigate the potential impact of such hydrothermal inputs on diazotrophic communities at the scale of the whole WTSP.

N₂ fixation rates were significantly negatively correlated with ${\mathrm{NO}}_{\mathrm{3}}^{-}$ concentrations, consistent with the high energetic cost of N₂ fixation compared to ${\mathrm{NO}}_{\mathrm{3}}^{-}$ assimilation (Falkowski, 1983). They were also negatively correlated with depth and logically positively correlated with PAR and seawater temperature, two parameters which are depth dependent. Most N₂ fixation took place in the surface mixed layer and rates were ∼ 15 nmol N L⁻¹ d⁻¹ in MA waters with local maxima at stations SD1, SD6 and LDB and local minima at SD8 and SD10. Trichodesmium, the most abundant diazotroph enumerated at those stations (Stenegren et al., 2018), is buoyant, and horizontal advection is well known to result in patchy distributions of Trichodesmium in the surface ocean (Dandonneau et al., 2003), with huge surface accumulations named slicks, as observed during OUTPACE (Stenegren et al., 2018), surrounded by areas with lower accumulations. These physical processes may explain the differences between stations rather than local enrichments of nutrients due to islands as those three stations where the highest rates were measured are not located close to islands. However, the huge surface bloom observed at LDB (Fig. 1) and extensively studied by de Verneil et al. (2017) was mainly sustained by N₂ fixation (secondary fueling picoplankton and diatoms, Caffin et al., 2018a), rather than deep nutrient inputs (de Verneil et al., 2017). This bloom had been drifting eastwards for several months and initially originated from Fiji and Tonga archipelagoes (https://outpace.mio.univ-amu.fr/spip.php?article160, last access: February 2016), which may have provided sufficient Fe to alleviate limitation and trigger this exceptional diazotroph bloom.

4.3 Trichodesmium: the major contributor to N₂ fixation in the WTSP

In MA waters, the dominant diazotroph phylotypes quantified using nifH quantitative PCR assays were Trichodesmium spp. and UCYN-B (Stenegren et al., 2018), which commonly peaked at > 10⁶ nifH copies L⁻¹ in surface (0–50 m) waters. DDAs (mainly het-1, but het-2 and het-3 were also detected) were the next most abundant diazotrophs (Stenegren et al., 2018). This result is consistent with the fact that abundances of those phylotypes co-varied and were significantly positively correlated with N₂ fixation rates (Table 2). The two UCYN-A lineages (UCYN-A1 and UCYN-A2) were less abundant (< 1.0–1.5 % of total nifH copies, Stenegren et al., 2018) and not significantly correlated with N₂ fixation rates (Table 2).

The relative contribution of different diazotroph phylotypes to bulk N₂ fixation has been largely investigated through bulk and size fractionation measurements (usually comparing > and < 10 µm size fraction N₂ fixation rates), which may be misleading since some small-size diazotrophs are attached to large-size particles (Benavides et al., 2016; Bonnet et al., 2009) or form colonies or symbioses with diatoms (e.g., UCYN-B, Foster et al., 2011, 2013) and some diazotrophic-derived N released by diazotrophs is assimilated by small and large non-diazotrophic plankton (e.g., Bonnet et al., 2016a). Here we directly measured the in situ cell-specific N₂ fixation activity of the two dominating diazotroph groups in MA waters: Trichodesmium and UCYN-B.

At all three studied stations, Trichodesmium dominated, accounting for 68.0–91.8 % of the diazotroph community, followed by UCYN-B, accounting for 0.3–31.7 %. In addition, Trichodesmium and UCYN-B had the highest measured gene expression (10²–10⁵ cDNA nifH copies L⁻¹). It was not surprising that UCYN-B had a high gene expression given that the sampling time occurred later in the day (17:00–21:00); however, both Trichodesmium and het-1 (which typically reduce N₂ and express nifH highest during the day, Church et al., 2005) had a detectable and often equally as high expression as UCYN-B. Cell-specific N₂ fixation rates reported here are on the same order of magnitude as those reported for field populations of Trichodesmium (Berthelot et al., 2016; Stenegren et al., 2018) and UCYN-B (Foster et al., 2013). Trichodesmium was always the major contributor to N₂ fixation, accounting for 47.1–83.8 % of bulk N₂ fixation, while UCYN-B never exceeded 6.1–10.1 %, despite accounting for > 30 % of the diazotroph community at SD6. This may be linked with the lower ¹⁵N enrichment at SD6 (0.517 ± 0.237 at. %), which is due to a high proportion of inactive cells (at. % close to natural abundance) compared to SD2, where the majority of cells were active and highly ¹⁵N-enriched (1.163 ± 0.531 at. %). Such heterogeneity in N₂ fixation rates among UCYN-B-like cells has already been reported by Foster et al. (2013). Overall, these results show that the most abundant phylotype (Trichodesmium) accounts for the majority of N₂ fixation, but not in the same proportion, further indicating that the abundance of micro-organisms in seawater cannot be equated to activity, which has already been reported for other functional groups such as bacteria (Boutrif et al., 2011). In the North Pacific Gyre (station ALOHA), Foster et al. (2013) report a higher contribution of UCYN-B to daily bulk N₂ fixation (24–63 %) during the summer season, indicating that this group likely contributes more to the N budget at station ALOHA than in the WTSP, where Trichodesmium seems to be the major player.