Distribution and rates of nitrogen fixation in the western tropical South Pacific Ocean constrained by nitrogen isotope budgets
- 1Earth, Ocean, and Atmospheric Science Dept., Florida State University, 117 N. Woodward AVE., Tallahassee, FL 32306, USA
- 2Aix-Marseille Université, CNRS, Université de Toulon, IRD, OSU Pythéas, Mediterranean Institute of Oceanography (MIO), UM 110, 13288, Marseille, France
- 3Observatoire Océanologique de Villefranche, Laboratoire d'Océanographie de Villefranche, UMR 7093, Villefranche-sur-mer, France
- 4Aix-Marseille Université, CNRS, Université de Toulon, IRD, OSU Pythéas, Mediterranean Institute of Oceanography (MIO), UM 110, 98848 Nouméa, New Caledonia
Correspondence: Angela N. Knapp (firstname.lastname@example.org)
Constraining the rates and spatial distribution of dinitrogen (N2) fixation fluxes to the ocean informs our understanding of the environmental sensitivities of N2 fixation as well as the timescale over which the fluxes of nitrogen (N) to and from the ocean may respond to each other. Here we quantify rates of N2 fixation as well as its contribution to export production along a zonal transect in the western tropical South Pacific (WTSP) Ocean using N isotope (“δ15N”) budgets. Comparing measurements of water column nitrate + nitrite δ15N with the δ15N of sinking particulate N at a western, central, and eastern station, these δ15N budgets indicate high, modest, and low rates of N2 fixation at the respective stations. The results also imply that N2 fixation supports exceptionally high, i.e. ≥ 50 %, of export production at the western and central stations, which are also proximal to the largest iron sources. These geochemically based rates of N2 fixation are equal to or greater than those previously reported in the tropical North Atlantic, indicating that the WTSP Ocean has the capacity to support globally significant rates of N2 fixation, which may compensate for N removal in the oxygen-deficient zones of the eastern tropical Pacific.
The primary source of nitrogen (N) to the ocean is the biologically mediated reduction of dinitrogen (N2) gas to ammonia, which is then assimilated into the biomass of the organisms carrying out this process, known as diazotrophs (Gruber, 2004). While the distribution and rates of this process in the ocean play a central role in regulating the fertility and community structure of marine ecosystems, these first-order properties of marine N2 fixation remain poorly constrained. Historically, the highest rates of N2 fixation in the global ocean have been associated with the tropical North Atlantic (Mahaffey et al., 2005; Sohm et al., 2011). The high 15N2 incubation-based N2 fixation rates observed in the tropical Atlantic (Luo et al., 2012) are consistent with both the preference of diazotrophs for warm waters (Breitbarth et al., 2007; Stal, 2009) as well as the high atmospheric dust flux to the region (Mahowald et al., 2009; Prospero, 1996) that helps fulfil the high iron requirement of the enzyme, nitrogenase, carrying out N2 fixation (Berman-Frank et al., 2001; Kustka et al., 2003). Additionally, the elevated ratio of nitrate (NO to phosphate (PO concentrations (Gruber and Sarmiento, 1997) and low δ15N-NO (Knapp et al., 2008) in the upper thermocline of the North Atlantic are attributed to high regional N2 fixation rates and have supported the hypothesis that iron availability plays a key role in regulating the spatial distribution of N2 fixation in the ocean (Moore et al., 2009; Moore and Doney, 2007) (“δ15N”, where δ15N , with atmospheric N2 as the reference).
While the highest inputs of N to the ocean have traditionally been associated with the North Atlantic, it has also been argued that this association results from the significant sampling bias in favour of the tropical Atlantic (Sohm et al., 2011), with large regions of the South Pacific and Indian Ocean under-sampled with respect to direct N2 fixation rate measurements (Luo et al., 2012). More recently, the eastern tropical South Pacific (ETSP) has seen increased sampling due to nutrient distribution-based modelling predictions that the highest global N2 fixation rates would be found in surface waters above and adjacent to oxygen-deficient zones (ODZs), where significant phosphorus (P) would be available to support N2 fixation (Deutsch et al., 2007). However, field campaigns have found exceedingly low rates of N2 fixation in the ETSP gyre (Knapp et al., 2016a; Raimbault and Garcia, 2008; Moutin et al., 2008), which have been attributed to limited iron availability (Dekaezemacker et al., 2013). Consequently, existing measurements indicate that the dominant sinks for N in the ocean, benthic and water column denitrification and anaerobic ammonium oxidation, focused in the ODZs of the eastern tropical Pacific and Arabian Sea (Gruber and Galloway, 2008), are spatially segregated from the dominant N2 fixation inputs in the tropical Atlantic. This spatial decoupling of N inputs and outputs necessarily corresponds to a temporal decoupling, requiring the timescale of ocean circulation for N2 fixation to respond to changes in rates of denitrification, and vice versa. In spite of the apparent spatial decoupling in the modern ocean, paleoceanographic evidence indicates that N fluxes to and from the ocean have been closely balanced over ≥ 20 kyr, requiring feedbacks in the N cycle to operate on timescales shorter than ocean circulation, and thus implying a tighter spatial coupling of N sources and sinks (Brandes and Devol, 2002; Deutsch et al., 2004). While N loss in the ocean is constrained to suboxic sediments and water column ODZs, similar constraints on the location of the largest N2 fixation fluxes to the ocean are lacking, and thus the degree to which marine N sources and sinks have been coupled through time remains uncertain.
While prior modelling analyses emphasized the importance of iron or phosphorus in supporting N2 fixation, the most recent modelling studies reflect the importance of elevated surface temperatures, adequate iron, and the potential for low surface ocean NO : PO concentration ratios to support a unique ecological niche for diazotrophs (Dutkiewicz et al., 2012; Monteiro et al., 2011; Weber and Deutsch, 2014). Attention has consequently shifted to the relatively undersampled western tropical South Pacific (WTSP) Ocean, where atmospheric dust fluxes to warm surface waters are higher than in the central and eastern tropical South Pacific (Mahowald et al., 2009), and where surface ocean NO and PO concentrations and ratios are relatively advantageous for diazotrophs (Moutin et al., 2005; Van Den Broeck et al., 2004). While seasonally some regions nearer to islands experience PO drawdown to lower levels (e.g. Van Den Broeck et al., 2004; Moutin et al., 2018), in parts of the WTSP gyre surface ocean NO concentrations are ≤ 0.1 µM and PO concentrations are ∼ 0.05 to 0.2 µM (Garcia et al., 2014), with corresponding positive P* values (where ) (Deutsch et al., 2007). Additionally, early remote sensing work detected significant and persistent blooms of Trichodesmium spp. in the WTSP (Dupouy et al., 2000), consistent with more recent direct observations of elevated Trichodesmium spp. abundance and N2 fixation rates observed near Melanesian islands (i.e. New Caledonia, Vanuatu, and Fiji) (Moisander et al., 2010; Shiozaki et al., 2014; Stenegren et al., 2018; Yoshikawa et al., 2015) and in the Solomon Sea (Bonnet et al., 2009, 2015; Berthelot et al., 2017). These high Trichodesmium spp. abundances and N2 fixation rates have been attributed to sea surface temperatures > 25 ∘C and continuous nutrient inputs of terrigenous and volcanic origin (Labatut et al., 2014; Radic et al., 2011). Prior molecular work has also shown higher rates of N2 fixation in the WTSP at locations where surface ocean dissolved iron (DFe) concentrations were higher and where Trichodesmium spp. were less stressed for iron (Chappell et al., 2012). Together, these observations and modelling-based predictions highlight the potential for significant N2 fixation rates in regions of the WTSP where diazotrophs can meet their iron and phosphorus requirements.
Here we use geochemical tools to quantify rates of N2 fixation along a zonal transect in the WTSP where surface waters are ≥ 25 ∘C and have favourable macronutrient concentrations and ratios, and where DFe concentrations are an order of magnitude higher than in the South Pacific Gyre and are mainly attributable to shallow hydrothermal input (Guieu et al., 2018). We then compare these geochemical estimates of N2 fixation rates with other metrics of N2 fixation evaluated on this cruise, as well as with the global distribution of marine N2 fixation rates.
2.1 Sample collection
Sampling for the Oligotrophic to UlTra-oligotrophic PACific Experiment (“OUTPACE”) cruise was conducted on the R/V L'Atalante, which left Nouméa, New Caledonia, on 18 February 2015 and arrived in Papeete, Tahiti, on 2 April 2015. This cruise followed a roughly zonal transect along 18 to 19∘ S between 159∘ E and 160∘ W. Details of the cruise and experimental design are described comprehensively in Moutin et al. (2017), but briefly, sediment traps were deployed at three “long-duration” (LD) stations A, B, and C (Table 1) (Fig. 1a). Water column samples were collected from Niskin bottles deployed on a CTD rosette at both LD and “short-duration” (SD) stations (Fig. 1a), and water was stored at −20 ∘C in HDPE bottles for analysis on land.
2.2 NO NO concentration and δ15N measurements
The concentrations of NO NO in water column samples collected on the OUTPACE cruise were measured by colorimetric methods (Aminot and Kerouel, 2007). The δ15N of NO NO in samples collected on the OUTPACE cruise was measured using the denitrifier method (Casciotti et al., 2002; Sigman et al., 2001), with modifications (McIlvin and Casciotti, 2011) (Fig. 1b). Typical standard deviation of the NO NON analyses was ≤ 0.2‰, with error bars for individual analyses shown in Fig. 1c.
2.3 Sinking particulate N flux and δ15N measurements
Surface-tethered floating particle-interceptor traps (PPS5) were deployed on the OUTPACE cruise at 150, 330, and 520 m for ∼ 5 days at stations LD A and LD B, and at 150 and 330 m at LD C (Moutin et al., 2017). The mass flux (“PNsink flux”) and δ15N of the PNsink flux was determined by combustion–gas chromatography interfaced to an isotope ratio mass spectrometer at the Mediterranean Institute of Oceanography with a lower detection limit of 2.2 µg N and precision of ±0.3 ‰ for 80 µg samples, with a precision of ±1.0 ‰ for 10 to 20 µg samples typical of what was collected in the sediment traps at the LD stations.
2.4 δ15N budget calculations
Here we compare the δ15N of the two dominant sources of “new” N to surface waters, subsurface NO and N2 fixation, with the δ15N of the sinking particulate N (PNsink) flux to estimate the relative importance of both NO and N2 fixation as a source of new N to surface waters. This approach relies on subsurface NO and N2 fixation having distinct isotopic compositions. N2 fixation introduces new N to the ocean with a δ15N of ∼ −1 ‰ (Carpenter et al., 1997; Hoering and Ford, 1960; Minagawa and Wada, 1986). In contrast, in the Pacific, NO mixed up from the subsurface is impacted by water column denitrification and can have a NON > 20 ‰ (e.g. Brandes et al., 1998; Casciotti et al., 2013; Rafter and Sigman, 2016), although as upper thermocline waters move westward in the Pacific, the very high NON signal is diluted and typical values are between 5 and 10 ‰ (Lehmann et al., 2018; Rafter et al., 2013). The relative importance of each source for supporting export production can be determined using the two-endmember mixing model described in Eq. (1) (“δ15N budget”), where the fractional importance of N2 fixation for supporting export production (x) is defined as
Rearranging and solving for x yields
Multiplying the fraction of export production supported by N2 fixation (x) by the PNsink mass flux provides a time-integrated N2 fixation rate that can be compared with 15N2 incubation-based N2 fixation rate measurements (Knapp et al., 2016a). Here it is hypothesized that both rates of N2 fixation and its importance for fuelling export production will be higher at stations in the western vs. central and eastern regions of the WTSP because of their closer proximity to iron sources (Guieu et al., 2018).
3.1 NO NO concentration and δ15N, and PNsinkδ15N
Samples collected in the upper 70 m at the LD stations had ≤ 0.1 µM NO NO (Caffin et al., 2017) and increased with depth, consistent with prior regional observations (Garcia et al., 2014) (Fig. 1c). All nutrient concentration data are available at http://www.obs-vlfr.fr/proof/php/outpace/outpace.php (last access: 10 April 2018). Water column NO NON data (Knapp et al., 2018) are available at https://www.bco-dmo.org/dataset/733237/data (last access: 11 April 2018) and show similar trends at the LD stations, with 650 m NO NO δ15N ∼ 7‰, increasing to ∼ 8.5 ‰ at 400 m (Fig. 1b, c) (Knapp et al., 2018), which fall within the range of previous regional measurements (Yoshikawa et al., 2015). The elevation of thermocline NO NON relative to the mean ocean NO NON of 5 ‰ is attributed to denitrification and/or anammox occurring in the ODZs of the ETSP, where thermocline NON can exceed 20 ‰ (e.g. Altabet et al., 2012; Casciotti et al., 2013). The average, mass-weighted δ15N of the PNsink flux collected in the 150 m trap increased from the western to eastern stations, from 0.6 ± 1.0 ‰ at LD A, to 3.1 ± 1.0 ‰ at LD B, and to 7.7 ± 1.0 ‰ at LD C (Table 1) (Fig. 1c).
3.2 Results of the δ15N budget: N2 fixation rates and their contribution to export production
Estimates of N2 fixation rates and their contribution to export production determined using δ15N budgets include the quantitatively dominant fluxes of N into and out of the surface ocean. Here, the dominant fluxes of N into the surface ocean include subsurface NO and newly fixed N introduced from diazotrophs, and the dominant loss term is represented by the PNsink flux (Eq. 1). In the event that total dissolved N (TDN) concentrations vary in space/time, they may be included as well; however, surface ocean TDN concentrations from the OUTPACE cruise show little to no zonal gradient, and were typically between 5 and 7 µM in the upper 100 m (Moutin et al., 2018), and so are not included in δ15N budget calculations. Additionally, the importance of N in atmospheric deposition has recently received significant attention, especially in the northwest Pacific (e.g. Kim et al., 2014), raising the possibility that atmospheric N deposition might also be an important source of N in the WTSP. However, the atmospheric N deposition flux measured on the OUTPACE cruise, 0.2 µmol N m−2 d−1 (Caffin et al., 2017), is several orders of magnitude lower than the mass flux captured in the 150 m sediment traps, 30–300 µmol N m−2 d−1 (Table 1), indicating that atmospheric N deposition is an insignificant source of new N to regional surface waters, and so is neglected in our δ15N budget calculations.
While gradients with depth in subsurface NO NO δ15N at the OUTPACE LD stations are modest compared to those in the ETSP, due to the relatively low sampling resolution in the upper thermocline where NO is likely sourced, we calculate δ15N budgets using a range of NO NON endmember values, which are represented by the shaded regions in Fig. 1c. At each LD station, the NO NON lower bound is represented by the 650 m sample and the upper bound is represented by the 400 m sample. Samples collected shallower than this (i.e. ≤ 200 m) either have isotopic compositions which fall within this range or show elevation in NO NON as the NO NO concentration decreases, which reflects the effect of NO assimilation. This elevation of shallow + is commonly observed below the euphotic zone in other oligotrophic regions (Knapp et al., 2016a, 2008), and is not thought to represent the δ15N of the source NO. Using the PNsinkδ15N (±1 ‰, 1 SD) and the range in subsurface NO NON endmember values in Eq. (2) corresponds to 80 to 83 ± 13 %, 50 to 56 ± 12 %, and 0 to 8 ± 11 % of export production supported by N2 fixation at stations LD A, LD B, and LD C, respectively (Table 1). Multiplying the fractional importance of N2 fixation by the PNsink mass flux yields a range of estimated N2 fixation rates of 219 to 290, 11 to 20, and 0 to 9 µmol N m−2 d−1 at stations LD A, LD B, and LD C, respectively (Table 1), where the range includes uncertainty in both the PNsinkδ15N measurement as well as the NO NON endmember.
4.1 Comparison of δ15N budget results with other N2 fixation metrics from the OUTPACE cruise
The N2 fixation rates derived from the δ15N budgets described above are lower than those measured by in situ 15N2 incubations at the same OUTPACE stations, with depth-integrated average N2 fixation rates of 593 ± 51, 706 ± 302, and 59 ± 16 µmol N m−2 d−1 at LD A, LD B, and LD C, respectively (Caffin et al., 2017). Previous work has also found lower δ15N budget-derived N2 fixation rates relative to 15N2 incubation-based N2 fixation rates (Knapp et al., 2016a). To the extent that sediment traps under collect the export flux, the two different metrics of N2 fixation may be reconciled by multiplying x from Eq. (2), the fractional importance of N2 fixation for export production, by other metrics of new or export production such as O2 ∕ Ar ratios, 234Th deficits, or 14C uptake rates (Knapp et al., 2016a). This explanation may reconcile the δ15N budget and 15N2 incubation-based N2 fixation rate estimates at LD A, which differ by a factor of ∼ 2.5, and potentially the rates at LD C as well, which, while they differ by a factor ≥ 6, both correspond to relatively low N2 fixation rates. However, the δ15N budget and 15N2 incubation-based N2 fixation rates observed at LD B, 11 to 20 and 706 µmol N m−2 d−1, respectively, are more difficult to reconcile based on sediment trap under-collection alone, and may be partially attributable to variability encountered while sampling at the end of a phytoplankton bloom as well as the fate of newly fixed N at that station (Caffin et al., 2018; de Verneil et al., 2017). We note that the zonal trend in increasing PNsinkδ15N to the east is similar to a zonal gradient in suspended particulate N (PNsusp)δ15N (Bonnet et al., 2018), suggesting that the δ15N of the PNsink observed at LD B is consistent with other regional geochemical data. Additionally, the 15N2 incubation-based N2 fixation rate at LD B has relatively large error bars, resulting from observations of decreasing in situ N2 fixation rates over the course of several daily observations at LD B (Caffin et al., 2017), which may also contribute to the offset between the 15N2 incubation and δ15N budget-based N2 fixation rate estimates. Further, the PNsink flux collected in the 150 m trap at LD B, 0.030 mmol N m−2 d−1, was somewhat lower than the PNsink flux collected in the 330 and 520 m traps at the same station, 0.034 and 0.036 mmol N m−2 d−1, respectively, which is unexpected given the more typical mass flux attenuation with depth observed at LD A and LD C, as well as elsewhere in the ocean (Martin et al., 1987). This unusual trend in mass flux with depth suggests either non-steady-state sinking flux conditions (Caffin et al., 2018) or a problem with the sediment trap sample collection at LD B. Regardless, using the 14C-uptake-based estimate of net N community production at LD B, 1.91 mmol N m−2 d−1, instead of the PNsink mass flux to multiply x from Eq. (2) by yields an N2 fixation rate of 2300 µmol N m−2 d−1. These significant disparities in productivity metrics and resulting N2 fixation rates at LD B suggests the potential for temporal decoupling of production and export and/or the underestimation of the export flux by the sediment trap, and indicate that N2 fixation rates are probably higher than those resulting from δ15N budget calculations based on the mass flux to the 150 m trap at LD B. Regardless, we take the zonal trend in PNsinkδ15N to indicate a decreasing contribution from N2 fixation to export from the west to the east to be robust as it is consistent with both the PNsuspδ15N measurements and the broad trends in 15N2 incubation-based N2 fixation rate estimates that decrease from the west to east.
Comparing the absolute magnitude of the δ15N-budget-based N2 fixation rates with previous measurements, we find that the 219 to 290 µmol N m−2 d−1 rate estimated for LD A represents a significant N2 fixation rate relative to prior global measurements (Luo et al., 2012), in particular if it should be revised upwards to account for the under-collection of the export flux by the sediment trap. In contrast, the estimated rate range at LD B, 11 to 21 µmol N m−2 d−1, is quite low, as is the range of 0 to 9 µmol N m−2 d−1 at LD C, and both of these rates are broadly similar to the rates previously measured in the ETSP (Knapp et al., 2016a; Moutin et al., 2008; Raimbault and Garcia, 2008). Similarly, the δ15N-budget-based estimate of the contribution of N2 fixation to export production at LD C is low and similar to previous δ15N-budget measurements in the North Pacific (Casciotti et al., 2008) and North Atlantic (Altabet, 1988; Knapp et al., 2005). However, the fractional contribution of N2 fixation to export production at LD A, 80 to 83 %, is higher than all previous δ15N budget results. The contribution of N2 fixation to export production at LD B, 50 to 57 %, is also notably high. While the previous δ15N budgets of Karl et al. (1997) and Dore et al. (2002) found evidence for ∼ 50 % of export production being supported by N2 fixation near Hawaii, newer methods capable of measuring the NO NON at the lower NO NO concentrations found in the upper thermocline that represent a more realistic estimate of the endmember NO source suggest that N2 fixation may support closer to 25 % of export during the summer in the North Pacific Gyre (Bottjer et al., 2017; Casciotti et al., 2008). Consequently, the findings of 50 to 57 % and 80 to 83 % of export production being supported by N2 fixation at stations LD B and LD A, respectively, indicate that N2 fixation plays a significant role in supporting carbon fixation and export production in this region of the WTSP, consistent with the high e ratios (up to 9.7) reported by Caffin et al. (2017). Direct export of diazotrophs has been reported by Caffin et al. (2017), but most export is likely indirect, i.e. after the transfer of diazotroph-derived N to non-diazotrophic plankton, which is subsequently exported (Caffin et al., 2018), as has been observed elsewhere in the WTSP (Bonnet et al., 2016; Knapp et al., 2016b).
4.2 Environmental sensitivities of N2 fixation and the basin-scale coupling of N sources and sinks
The zonal gradient in both N2 fixation rates as well as their contribution to export production in the OUTPACE study supports emerging hypotheses regarding the controls on the distribution of marine N2 fixation fluxes in the global ocean. Specifically, the low rates of N2 fixation documented in this study at LD C and in the ETSP (Knapp et al., 2016a) indicate that low NO : PO concentration ratios in the absence of adequate iron (Blain et al., 2008; Fitzsimmons et al., 2014) are insufficient to support significant fluxes of new N to the ocean. Instead, the results presented here are consistent with recent modelling work that has included both the high iron requirements of diazotrophs and the potential for low NO : PO concentration ratios to support elevated diazotroph abundance and N2 fixation inputs to the ocean (Dutkiewicz et al., 2012; Monteiro et al., 2011; Weber and Deutsch, 2014). Indeed, these new modelling efforts have identified the WTSP as a unique region where PO concentrations are relatively high, NO concentrations are low, and atmospheric dust fluxes provide a moderate source of iron to warm surface waters, conditions seemingly favourable for significant N2 fixation fluxes. While regions within the WTSP nearer to islands experience significant PO drawdown, with seasonal PO turnover times comparable to those observed in the Sargasso Sea (Van Den Broeck et al., 2004; Van Mooy et al., 2009), these modelling predictions are supported by recent reports of high regional 15N2 incubation-based N2 fixation rates (Bonnet et al., 2017).
However, prior to the OUTPACE cruise, our knowledge of DFe concentrations and their sources in the WTSP was limited, especially in the western and central sectors. During OUTPACE, Guieu et al. (2018) reported high DFe concentrations in the western sector of the WTSP (from 160∘ E to 165∘ W, average 1.7 nM within the photic layer), i.e. significantly (p<0.05) higher than those reported in the eastern sector (165–160∘ W, average 0.3 nM within the photic layer). The high DFe concentrations measured in the west were previously undocumented and reveal several maxima (> 50 nM), suggesting significant iron inputs to this region. Guieu et al. (2018) found that atmospheric deposition in this region was too low to explain the observed DFe concentrations in the water column, and that the iron in the euphotic layer may instead derive from shallow (∼ 500 m) hydrothermal sources associated with the Tonga–Kermadec subduction zone.
Recent studies performed in the western end of the WTSP 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 N2 fixation rates (> 600 µmol N m−2 d−1), indicating that high N2 fixation rates have been found over a significant region of the WTSP, extending west to east from Australia to Tonga and north to south from the Equator to 25 to 30∘ S, or ∼ 13×106 km2 (i.e. ∼ 20 % of the South Pacific Ocean area). These significant N inputs may offset the N loss occurring in the ODZs of the eastern tropical Pacific. The ability for marine N inputs and outputs to compensate for each other within the same ocean basin corresponds to a spatial and thus temporal coupling on the scale of years to decades, consistent with the paleoceanographic record (Brandes and Devol, 2002; Deutsch et al., 2004; Weber and Deutsch, 2014), and represents an intermediate view of the distribution of global marine N2 fixation fluxes consistent with that proposed by Weber and Deutsch (2014), where iron availability controls local N2 fixation rates but phosphorus availability regulates basin-scale N2 fixation rates (Moutin et al., 2008, 2018).
The goal of this study was to address the question: do regions other than the tropical Atlantic contribute significantly to global N2 fixation fluxes? While our results should be taken as a “snapshot” view that cannot necessarily be scaled up to annual fluxes, at stations proximal to iron sources, geochemically derived N2 fixation rates of 219 to 290 µmol N m−2 d−1 were observed, and could potentially represent a lower bound of N2 fixation rates due to the potential under-collection of the PNsink flux by sediment traps. Moreover, at stations LD A and LD B, separated by ∼ 27∘ longitude, N2 fixation was found to support > 50 % of export production, a finding that has not been replicated elsewhere with sensitive NO NON methods to our knowledge. Together with similar findings from 15N2 uptake experiments, these results suggests that N2 fixation can support a significant fraction of export production over a large region of the WTSP. At the eastern station most distant from iron sources, both rates and the contribution of N2 fixation to export production were low, ∼ 0 to 9 µmol N m−2 d−1 and 0 to 8 %, respectively, similar to previous measurements in the ETSP where diazotrophs may also be challenged by iron availability (Dekaezemacker et al., 2013; Knapp et al., 2016a; Moutin et al., 2008). Significant N2 fixation fluxes in the WTSP may provide a means of balancing N loss occurring in the ODZs of the eastern tropical Pacific, and thus may help reconcile the paleoceanographic record requiring N inputs and losses to balance each other on timescales shorter than ocean circulation (Dutkiewicz et al., 2012; Monteiro et al., 2011; Weber and Deutsch, 2014).
All data and metadata are available at the French INSU/CNRS LEFE CYBER database (scientific coordinator: Hervé Claustre; data manager and webmaster: Catherine Schmechtig) at the following web address: http://www.obs-vlfr.fr/proof/php/outpace/outpace.php. The data supporting the conclusions of this paper may be obtained at the BCO-DMO database https://www.bco-dmo.org/dataset/733237 (Knapp et al., 2018).
The authors declare that they have no conflict of interest.
This article is part of the special issue “Interactions between planktonic organisms and biogeochemical cycles across trophic and N2 fixation gradients in the western tropical South Pacific Ocean: a multidisciplinary approach (OUTPACE experiment)”. It is not associated with a conference.
This is a contribution of the OUTPACE (Oligotrophy to Ultra-oligoTrophy
PACific Experiment) project (https://outpace.mio.univ-amu.fr/) funded
by the French national research agency (ANR-14-CE01-0007-01), the LEFE-CyBER
programme (CNRS-INSU), the GOPS programme (IRD) and the CNES. Funding for the
contribution of Angela N. Knapp and Kelly M. McCabe was provided by the U.S.
National Science Foundation OCE #1537314. The OUTPACE cruise
(https://doi.org/10.17600/15000900) was managed by the MIO (OSU Institut Pytheas, AMU)
from Marseilles (France). The authors thank the crew of the R/V
L'Atalante for outstanding shipboard operation. Gilles Rougier and
Marc Picheral are warmly thanked for their efficient help in CTD rosette
management and data processing, as is Catherine Schmechtig for the LEFE CYBER
database management and Carlos Miranda for analytical
Edited by: Emilio Marañón
Reviewed by: two anonymous referees
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