GEOPHYSICAL RESEARCH LETTERS, VOL. 30, NO. 6, 1300, doi:10.1029/2002GL016542, 2003
Biogeochemical signatures of nitrogen fixation in the eastern North Atlantic Claire Mahaffey,1 Richard G. Williams,1 George A. Wolff,1 Natalie Mahowald,2 William Anderson,3 and Malcolm Woodward4 Received 30 October 2002; accepted 5 February 2003; published 22 March 2003.
[1] Stable nitrogen isotopic determination of particulate organic matter over the eastern North Atlantic in spring 2000 reveal a region of low natural abundance of 15N relative to 14 N between 26N and 32N along 20W. This light isotopic signal, together with phytopigment data and persistently elevated nitrate to phosphate ratios in the upper thermocline, suggest that nitrogen fixation provides a local dominant supply of nitrogen to phytoplankton over part of the eastern North Atlantic. These independent biogeochemical proxies are coincident with a region of enhanced atmospheric dust deposition, as suggested by an atmospheric transport model. Hence, the atmospheric dust events may spatially and temporally constrain the distribution of N2 fixers. INDEX TERMS: 4805 Oceanography: Biological and Chemical: Biogeochemical cycles (1615); 4845 Oceanography: Biological and Chemical: Nutrients and nutrient cycling; 4870 Oceanography: Biological and Chemical: Stable isotopes; 0315 Atmospheric Composition and Structure: Biosphere/atmosphere interactions. Citation: Mahaffey, C., R. G. Williams, G. A. Wolff, N. Mahowald, W. Anderson, and M. Woodward, Biogeochemical signatures of nitrogen fixation in the eastern North Atlantic, Geophys. Res. Lett., 30(6), 1300, doi:10.1029/2002GL016542, 2003.
[3] The eastern North Atlantic is potentially an important region of N2 fixation given the enhanced inputs of atmospheric dust from the Sahara. In this study, we examine independent biogeochemical proxies and chemotaxonomic biomarkers for N2 fixation along a meridional transect passing through the eastern North Atlantic. In addition, we compare our ocean observations with independent predictions of dust transport from an atmospheric model. [4] The stable nitrogen isotopic composition (ratio of 15N to 14N, expressed as d15N) [Mariotti et al., 1981] of phytoplankton reflects the isotopic composition of the nitrogen (N) source and biological isotopic fractionation during the uptake and assimilation of the N source. The ratio of d15N of atmospheric N2 (0 %) is lower than nitrate from the deep ocean (5 %) [Liu and Kaplan, 1989]. Thus, primary production fuelled by N derived from N2 fixation will be depleted in 15 N relative to 14N. Inputs of N to the surface ocean through N2 fixation are unaccompanied by inputs of phosphorus (P). Elevated N to P, both in the dissolved inorganic and organic pools, may therefore be indicative of N2 fixation [Gruber and Sarmiento, 1997].
2. Methodology 1. Introduction [2] Biological fixation of nitrogen (N2) in oligotrophic subtropical gyres is important in supplying nitrogen to surface phytoplankton communities in an otherwise nitrogen-starved environment. The global distribution and significance of N2 fixation have been inferred from direct observations of N2 fixing cyanobacteria (the most well studied being Trichodesmium spp.) [Capone et al., 1998; Orcutt et al., 2001], and indirectly, from nutrient inventories [Gruber and Sarmiento, 1997] and SeaWiFS remote sensing observations [Subramaniam et al., 2002]. In addition, the distribution and fluxes of iron [Berman-Frank et al., 2001] and phosphorus [Wu et al., 2000] have been used as a proxy to predict the potential and geographic differences of N2 fixation in the Atlantic and Pacific. 1 Oceanography Laboratories, Department of Earth Sciences, University of Liverpool, Liverpool, UK. 2 Bren School of Environmental Science and Management, University of California, Santa Barbara, California, USA, and National Center for Atmospheric Research, Boulder, Colorado, USA. 3 Earth Science Department and the Southeast Environmental Research Center, Florida International University, Miami, Florida, USA. 4 Plymouth Marine Laboratories, West Hoe, Plymouth, UK.
Copyright 2003 by the American Geophysical Union. 0094-8276/03/2002GL016542$05.00
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[5] Suspended particulate matter (SPM) and filtered seawater samples were collected along an Atlantic Meridional Transect (AMT10) between 35S, 49W and 48N, 20W (Figure 1) in April and May 2000. [6] SPM was filtered (200– 1000 L) from the underway seawater supply (7 m) onto pre-combusted (450C for over 4 hours) 150 mm Whatman GF/F filters using a Sartorius GmBH large volume filtration unit. Filtered (250 mL) seawater and SPM ( pre-combusted 47 mm GF/F filters) were collected from 7 to 10 depths using Niskin bottles (10 L). All samples were stored at 20C prior to analysis. [7] Underway chlorophyll a (mg m 3) [Welschmyer, 1994] and phytoplankton pigment distributions (expressed as percentage of total pigments) [Barlow et al., 1997] were determined, and chemotaxonomic marker pigments were grouped to assess the relative contribution of three functional classes of phytoplankton [Gibb et al., 2000]. [8] Particulate organic nitrogen (PON) concentrations were determined using a Carlo Elba elemental analyser (CE-EA) ( precision 22 %; Figure 2b, solid line). [11] Along the northern flanks of the subtropical gyre (north of 40N), elevated nitrate concentrations (> 5mM; Figure 2a, black circle) and phytoplankton biomass (chlorophyll a < 0.4 to 0.9 mg m 3, PON 0.9 to 1.6 mM; Figures 1 and 2a), was probably due to convection and lateral winddriven transfer of nutrients [Williams and Follows, 1998]. Chemotaxonomic data revealed a dominance of eukaryotic nanoflagellates ( prymnesiophytes, chrysophytes and chlorophytes) (> 21 %; Figure 2b, dashed line), with a contribution from large eukaryotes (diatoms and dinoflagellates; 10%; Figure 2b, dotted line). 3.2. Stable Nitrogen Isotopes [12] Isotopically light phytoplankton were observed at 26– 32N, (1.23 to 2.58 %, n = 9), and at 40– 48N, (1.3 to 3.0 %, n = 13) (Figure 2c). The lightest isotopic signal at 40– 48N (mean ± standard deviation, 0.72 ± 0.52 %) coincided with the spring bloom and reflected net isotopic fractionation by phytoplankton during uptake and assimila-
Figure 2. Latitudinal variation in (a) chlorophyll a (mg m 3) (black line) and particulate organic nitrogen (PON, mM) (white circle) and nitrate (black circle) concentrations in the mixed layer, (b) percentage (%) contribution to total pigments of three chemotaxonomic groups indicating the presence of cyanobacteria and prochlorophytes (zeaxanthin + divinyl chlorophyll a; solid line), diatoms and dinoflagellates (fucoxanthin + peridinin; dotted line) and prymnesiophytes, chrysophytes and chlorophytes (19’butanoyloxyfucoxanthin, 19’hexanoyloxyfucoxanthin + chlorophyll b; dashed line) after Gibb et al. [2000], (c) stable nitrogen isotopic composition (d15N) of PON collected from the underway supply at 7m (black circle) and CTD casts at 7m (white circle), with dashed lines representing a light and heavy source of N of 0% and 5%, (d) ratio of nitrate to phosphate observed during AMT 2 (22 April to 28 May, 1996; white circle), AMT 4 (21 April to 27 May, 1997; white square), AMT 6 (5 April to 4 May, 1998, white triangle) and AMT 10 (12 April to 7 May, 2000; black circles), with a dashed line representing a Redfield ratio of 16.
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tion of nitrate at high ambient concentrations (Figure 2a, 2c) [Mariotti et al., 1981]. However, isotopically light phytoplankton were also observed in the eastern flank of the subtropical gyre at 26– 32N (2.25 ± 0.36%) where net isotopic fractionation is not expected [Altabet and McCarthy, 1985] (Figure 2a, 2c). Hence, these light signals suggest that the phytoplankton were utilising a light isotopic source of N, possibly provided by N2 fixation (0%) from regenerated N ( 1.5 to 2.1%) [Altabet, 1988] or DON (1 to 2 %) [Liu et al., 1996; Abell et al., 1999]. Although it is not possible to directly identify which light isotopic N source is responsible for the observed isotopically light PON, we speculate that the N was supplied by N2 fixation due to the dominance of phytopigments indicative of cyanobacteria in this region. [13] Here, we assume negligible isotopic fractionation and that there is a light (0%) and a heavy (5%) source of N, possibly representing N2 fixation and a supply of deep nitrate, respectively [Liu and Kaplan, 1989]. Using this simple two-member mixing model, we estimate that the light isotopic source provides between 48% to 75% of the N demand of phytoplankton (63%) over this region. 3.3. Excess N Versus P [14] Over the transect in the eastern North Atlantic, elevated nitrate to phosphate ratios (greater than 16: 1) in the thermocline (> 100m black circles; Figure 2d) were observed during AMT 10. This ‘‘excess’’ nitrate signal appears to be a persistent feature over the North Atlantic subtropical region during spring, occurring for three previous AMT’s (Figure 2d). In agreement, Gruber and Sarmiento [1997] diagnose elevated nitrate to phosphate ratios in the thermocline (as measured by N*) between 16N and 44N along a 20 to 30W transect from GEOSECS. This appears to be a persistent feature in the eastern North Atlantic subtropical gyre. In the same region, there is also an increase in the DON to DOP ratio from the gyre flanks [Mahaffey et al., manuscript in preparation, 2003]. Consequently, the elevated nitrate to phosphate ratios in the thermocline are probably a result of additional nitrogen supply from N2 fixation, although other processes, such as differential recycling, may also modify the N to P ratio [Karl et al., 2002]. 3.4. Why is Nitrogen Fixation Locally Enhanced? [15] The distribution and rate of N2 fixation is limited by iron [Berman-Frank et al., 2001] and phosphorus [SanudoWilhelmy et al., 2001]. Atmospheric dust inputs from the Sahara can provide a source of iron [Berman-Frank et al., 2001] and possibly phosphate [Ridame and Guieu, 2002] to the surface ocean. Our depleted isotopic values observed between 24 – 32N were coincident with a region of anomalously strong injection of Saharan dust observed for a series of atmospheric events from February to mid-April 2000, as independently suggested by an atmospheric transport model (Figure 3a) (N. Mahowald et al., Interannual variability in atmospheric mineral aerosols from a 22-year mineral aerosol simulation and observational data, submitted to Journal of Geophysical Research, 2002) and TOMS images (Figure 3b, 3c). The atmospheric transport model predicts the source, transport and wet and dry deposition of dust using NCEP/NCAR meteorological reanalysis from
Figure 3. Dust deposition along the cruise transect: (a) time-series of atmospheric model predictions of anomalous deposition of dust ((monthly deposition-monthly mean)/ monthly mean) along 20W, where the monthly mean at each point is separately evaluated from 1979 to 2000. The predicted dust deposition is twice the climatological monthly mean between 22 to 35N during the spring of 2000. Total Ozone Mapping Spectrometer (TOMS) aerosol index image of a Saharan dust outbreak for (b) March 2000 and (c) April 2000. Note the enhanced dust deposition during March 2000 in both (a) and (b). 1979 to 2000. The model predictions of dust deposition are significantly correlated with the observed aerosol index from TOMS over the AMT 20W transect, (correlation coefficient 0.6 at a 95% confidence level), as well as with in situ surface observations. The model predicts that the dust deposition from February to mid-April of 2000, was twice the climatological monthly mean between 22N and 35N. In view of the residence time of dissolved and total iron in the surface ocean (200 and 18 days, respectively) [Jickells, 1999], turnover time of phosphorus (weeks to months) [Benitez-Nelson and Karl, 2002] and the response time of Trichodesmium (days to weeks) [Lenes et al., 2001], it is plausible that the atmospheric dust injection in March 2000 (Figure 3a, b) led to natural iron and phosphorus
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MAHAFFEY ET AL.: BIOGEOCHEMICAL SIGNATURES OF NITROGEN FIXATION
fertilisation, and thus may be responsible for the biogeochemical signals observed between 27 April and 1 May during AMT 10. [16] However, Trichodesmium spp., a dominant cyanobacterial N2 fixer, usually shows enhanced abundance in the tropics [Tyrrell et al., 2003], rather than in the subtropical gyre as implied in this study. This apparent inconsistency might be due to utilisation of inorganic nutrients by Trichodesmium spp. [Mulholland et al., 2001], the presence of N2 fixing cyanobacteria other than Trichodesmium spp. [Zehr et al., 2000] and the temporal variability in N2 fixation [Orcutt et al., 2001; Dore et al., 2002].
4. Conclusions [17] A range of independent biogeochemical proxies when viewed together suggest that N2 fixation provides a dominant supply (63%) of N over part of the oligotrophic eastern North Atlantic: (i) 15N depleted phytoplankton between 24N and 32N along 20W; (ii) phytopigments indicative of cyanobacteria and prochlorophytes at 26N and 30N, and (iii) persistently elevated nitrate to phosphate ratios in the thermocline between 20N and 45N revealed in a series of spring Atlantic Meridional Transects. [18] These biogeochemical proxies are coincident with independent atmospheric transport model predictions of enhanced atmospheric dust deposition in spring 2000 around 24N and 28N. Hence, the atmospheric dust inputs probably created an ecological niche for N2 fixers in the eastern Atlantic. The atmospheric dust inputs vary episodically with atmospheric synoptic-scale events, as revealed in sequences of satellite images and model predictions, and thus might drive temporal variability in N2 fixation. [19] Acknowledgments. We would like to acknowledge the officers and crew of RRS James Clark Ross, and support from the UK NERC, AMT Programme NER/O/S/2001 and NERC studentship GT04/99/MS/134 (CM). We are grateful for assistance from V. Roussenov, M. Follows, T. O’Higgins, A. Poulton, V. Hill and S. Groom and NASA/GSFC TOMS Ozone Processing Team (OPT). N.M gratefully acknowledges assistance from C. Luo, C. Zender, J. del Corral and support from NCAR, NSF and NASA. This is AMT contribution number 73.
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W. Anderson, Earth Science Department, Florida International University, Miami, FL 33199, USA. C. Mahaffey, R. G. Williams, and G. A. Wolff, Oceanography Laboratories, Department of Earth Sciences, University of Liverpool, Liverpool, L69 7ZL, UK. (
[email protected]) N. Mahowald, Bren School of Environmental Science and Management, University of California, Santa Barbara, CA, USA. M. Woodward, Plymouth Marine Laboratories, West Hoe, Plymouth, PL1 3DH, UK.
