The air-sea exchange of organic carbon (OC) remains largely unexplored, except for few organic compounds comprising a small fraction of the total aerosol and gaseous OC in the atmosphere. Observations of high atmospheric concentrations and diffusive air-sea exchanges for such individual organic compounds, suggest that air-sea exchange of total OC may contribute significantly to the oceanic carbon budget. Here we quantify the atmosphere-ocean exchanges of total OC in the NE Subtropical Atlantic. Average net gaseous diffusive air-water fluxes averaged –31 and –25 mmol C m−2 d−1 for the spring and fall, respectively, exceeding measured OC inputs by dry aerosol deposition (FDDOC, −0.98 mmol C m−2 d−1) and net CO2 exchange (FCO2, −6.3 mmol C m−2 d−1). These fluxes are important to understand the regional carbon budget of the NE Subtropical Atlantic, and depict the atmosphere as a major dynamic vector for OC exchange with the ocean.
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 Anthropogenic emissions of un- or incompletely combusted organic carbon (OC) and biogenic emissions of volatile OC constitute significant carbon inputs to the atmosphere [Schauer et al., 2002; Fuentes et al., 2000]. Once organic compounds are released to the atmosphere they undergo atmospheric transport, degradation and deposition again to the surface environments. The ocean plays a dual role as a source of some volatile compounds such as non-methane hydrocarbons [McKay et al., 1996], and as a major sink of many anthropogenic [Jurado et al., 2005] and biogenic organic compounds [Jacob et al., 2005]. There are three main mechanisms of exchange of OC between the ocean and the atmosphere; i) diffusive exchanges by volatilization (sea to air) and absorption (air to sea) of gas phase OC, ii) atmospheric aerosol OC dry deposition, and iii) by wet deposition of aerosol and gaseous OC. There are very few assessments of the magnitude and relevance of these mechanisms contributing to the atmosphere-ocean exchange of total OC. The few previous reports are limited to estimations of fluxes associated with aerosol dry and wet OC deposition [Willey et al., 2000; Durrieu de Madron et al., 2000; Kieber et al., 2002].
 The objective of this study was to estimate the magnitude and direction, and assess the relevance of atmosphere-ocean exchanges of organic carbon, especially those associated with gas-phase organic compounds, in the north east subtropical Atlantic Ocean.
2. Sampling and Methods
 Sampling: We measured the atmospheric OC concentrations (gas and aerosol phase) and simultaneously, the dissolved concentrations and exchange fluxes of OC in the NE Subtropical Atlantic, an area subject to Saharan dust influence [Eglington et al., 2002]. The dry depositional aerosol input (FDDOC), volatilization (FOC,VOL) and absorption (FOC,AB) components of the atmosphere-ocean exchange of organic carbon were quantified along with the air-sea CO2 exchange, and the enrichment of the top-cm of the ocean in organic carbon. The study was conducted during the COCA and BADE cruises along the Subtropical NE Atlantic on-board the R/V Hespérides and R/V Pelagia, respectively. The COCA cruise took place in May–June 2003 and started from the Island of Gran Canaria, sailing along 26°N to reach 26°W, following south to reach 21°N, and then heading towards the W. African Coast at Cape Blanco along this parallel. The BADE cruise took place in September–October 2004 and started south of Cape Blanco and headed along a W-NW transect to reach 25°N, 31°W (Figure 1).
 Determination of dissolved organic carbon (DOC), CO2 partial pressures, and atmospheric OC and EC aerosol concentrations were done using standard procedures as described in Table S1. In order to estimate air-water fluxes of OC, operational measurements of total volatile and semivolatile OC in the gas phase and seawater dissolved phase are needed. Therefore, we developed here a novel procedure based on the definition of two operational measures, total gas-phase organic carbon (GOC) in the atmosphere and exchangeable dissolved organic carbon (EDOC) in seawater.
 The total concentration of organic carbon in the gas phase (GOC) was determined indirectly by equilibrating air and water for 30 min by bubbling prefiltered air (QMA filter, Whatmann) through 50 ml of acidified (pH 1-2 with H3PO4) water (HPLC grade water, MERCK) upwind of the research vessel. After sampling, the water was immediately transferred into precombusted glass ampoules (at 450°C for 6 h) and sealed. The TOC concentration in the HPLC grade water representing the gas-phase organic carbon equilibrated in water, GOC/H′ where H′ is the dimensionless Henry's Law constant, was determined in duplicate by high temperature catalytic oxidation on a Shimadzu TOC-5000A. Standards provided by Dennis A. Hansell and Wenhao Chen (University of Miami, USA) of 44–45 μmol DOC and 2 μmol TOC were used to assess the accuracy of the estimates. Purging of samples with N2 was not performed as inorganic carbon had been evacuated during sampling. The fraction of exchangeable dissolved organic carbon (EDOC) in surface waters was determined by purging 1 L of seawater collected at 5 m depth with pure N2 (grade 5.0) for 5–8 min and equilibrating the outgassing N2 products in 40 ml of pure acidified (pH 1–2 with H3PO4) water (HPLC grade water, MERCK). Water was then transferred to precombusted ampoules and analyzed for OC content as described above. The efficiency of EDOC extraction by this procedure is 53 ± 28% and 80% ± 26% as determined using Acetone and Toluene standards. GOC and EDOC concentrations were corrected for field blanks.
 Diffusive air-water exchange was estimated using the wind speed dependence of the mass transfer velocity (k600) from instantaneous wind speeds (U10, m s−1) following the equation k600 = 0.24U102 + 0.061U10 [Nightingale et al., 2000]. OC net diffusive fluxes (FOC) were estimated as the sum of gross volatilization (FOC,VOL = k′ x EDOC) and absorption (FOC,AB = −k′ x GOC/H′), where H′ is the dimensionless Henry's law constant and k′ is the gas transfer velocity for exchangeable OC estimated from k600 values and Schmidt numbers assuming an average MW of GOC of 120 g mol−1. Further details on diffusive and dry aerosol deposition fluxes of carbon are given in Table S1. By convention, we use negative fluxes to denote inputs from the atmosphere to the ocean.
3. Results and Discussion
 The area nearest to the African coastal zone received dry deposition inputs of organic (FDDOC = −1.02 ± 4.0 mmol C m−2 d−1) and elemental carbon two-fold higher than those in the open ocean and acted as a strong sink of aerosol-phase organic carbon, but with an important variability in fluxes (Figures S1 and S2) presumably due to large proximal land aerosol sources in the upwind NE direction, especially for the coastal sites (Figures S3–S10). The dry deposition flux of aerosol organic carbon was six fold higher than that of elemental (black) carbon (Figure S1), consistent with other reports [Lim et al., 2003].
 For the spring sampling cruise, the concentration of dissolved OC exchangeable with the atmosphere (EDOC) in the coastal and open ocean surface averaged (±SE) 30 ± 6 μmol C L−1, corresponding to about 30–40% of the DOC concentration (Figure S1), while the dissolved OC concentration equilibrated with the gaseous organic carbon (GOC/H′) averaged 40 ± 5 μmol C L−1. During the fall cruise, EDOC concentrations in the open ocean were not significantly different from those obtained during the spring cruise with an average EDOC concentration of 36 μmol C L−1. However, concentrations for the coastal stations were significantly higher (91 ± 23 μmol C L−1). The atmospheric gaseous organic carbon (GOC/H′) showed the same spatial variability with concentrations in the coastal zone (106 ± 6 μmol C L−1) more than two times those of the open sea (39 ± 18 μmol C L−1). Air mass back trajectories performed for all the sampling periods (Figures S3–S10) show that coastal atmospheric OC values may have a certain anthropogenic and land influence from the NW African coast, the Canary Islands and, to a lesser extend, the Iberian Peninsula. However, potential land emissions upwind do not always result in higher GOC/H values, especially for the spring data set, which indicates a complex interplay of emissions and processes affecting the occurrence of OC during atmospheric transport such as air-sea interactions and degradation.
 This spatial covariance in exchangeable OC concentrations resulted in a significant correlation between GOC/H′ and surface concentrations of EDOC, r2 = 0.59 (P < 0.01), and r2 = 0.84 (P < 0.01) for the spring and fall cruises, respectively (Figure 2). These two measurements are completely independent, so that the tight correlation between atmospheric and seasurface exchangeable OC concentrations suggests a dynamic coupling and cycling of these compounds between the surface ocean and lower atmosphere, similar to that reported for individual semivolatile organic compounds [Jaward et al., 2004]. This air-water coupling is therefore the result of exchanges between the atmosphere and the ocean due to volatilization and atmospheric deposition.
 Atmospheric dry deposition (gaseous and particulate) and volatilization of organic carbon was consistently high [mean (±SE) FDDOC −0.98 ± 0.22 mmol C m−2 d−1; mean FOC,AB −104 ± 16 mmol C m−2 d−1; mean FOC,VOL 73 ± 11 mmol C m−2 d−1; Figures 1 and S1], with the average absolute magnitude of the gross volatilization and absorption fluxes exceeding the aerosol deposition by 70–100 fold. This ratio of gross diffusive to dry aerosol depositional flux of atmospheric organic carbon is comparable to that reported for hydrocarbons and other semivolatile organic compounds [Duce et al., 1991; Jurado et al., 2005] and is controlled by dynamic partitioning of organic compounds between the gas and aerosol phases [Jurado et al., 2005; Seinfeld and Pandis, 1998]. Indeed, the high ratio of dry gaseous to dry aerosol deposition fluxes suggests that atmospheric organic matter is dominated by gas-phase organic compounds.
 The gross diffusive fluxes were 2–8 times higher than the net air-sea fluxes (mean FOC −31 ± 12 mmol C m−2 d−1) for the spring sampling cruise, and 2–15 times for the fall data set (mean FOC −25 ± 23 mmol C m−2 d−1). Therefore, there are high diffusive volatilization and absorption fluxes which result in much smaller net air-water fluxes. This is consistent with the dynamic coupling of gas and dissolved organic compounds (Figure 2), especially in the open ocean. The average net air-sea exchange of total carbon, which represented a net OC input to the sea in both cruises, exceeded the magnitude of CO2 exchange by a factor of four for the spring = −6.3 mmol C m−2 d−1) sampling cruise, while OC (−8.5 ± 18.6 mmol C m−2 d−1) and CO2 (7.06 ± 2.4 mmol C m−2 d−1) net fluxes had opposite directions but were comparable in magnitude at open sea during the fall sampling cruise. CO2 exchange fluxes dominated air-sea C net fluxes only in the Mauritanian coast (Figure 1), where intense upwelling resulted in large CO2 degassing. The atmospheric deposition of organic carbon was consistent with the enrichment of the top cm of the ocean in DOC relative to subsurface waters (Figure S1) [Calleja et al., 2005].
 Our results provide compelling evidence of high exchange fluxes of volatile and semivolatile organic carbon between the ocean and the atmosphere over the NE Atlantic. The origin of the exchanged organic carbon cannot be resolved here, however, likely contains products derived from incomplete combustion of fossil fuel which constitute a significant fraction of the total combustion products [Schauer et al., 2002] and is abundant in the atmosphere [Turpin et al., 2000]. Compounds released by land vegetation [Fuentes et al., 2000] and soil organic matter are also abundant in the atmosphere even over remote oceanic regions [Eglington et al., 2002] and might contribute to the pool of exchangeable OC, as well as biogenic marine OC [McKay et al., 1996]. Even if atmospheric organic carbon has a relatively short half-life of a few days is sufficient for transoceanic transport [Seinfeld and Pandis, 1998], allowing for their interaction with the ocean. The ocean has been identified as the dominant sink for gas-phase anthropogenic semi-volatile organic contaminants [Dachs et al., 2002; Jurado et al., 2005], and biogenic organic compounds from land vegetation could also contribute to this sink as reported for specific compounds [Jacob et al., 2005].
 Since gross fluxes are significantly higher than net fluxes, relatively small changes in the former may trigger a change in the direction of the net air-sea fluxes and thus, some regions of the ocean may act as source and others as sink of organic C to the atmosphere. Such a dual sink-source role would support an internal redistribution of organic carbon within the ocean supplementing that mediated by water mass transport. Even for the NE Atlantic, our results show an important regional variability in net fluxes ranging from a net absorption flux of −140 mmol m−2 d−1 to a net volatilization flux of 40 mmol m−2 d−1 across the region, considering the spring data set as an example. Extrapolating the average diffusive net organic carbon exchange (mean net FOC −28 mmol C m−2 d−1) measured here during the two sampling cruises to the entire subtropical NE Atlantic with an aereal extent of 5.26 106 km2 yields an estimated input of 0.64 ± 0.3 Gt C yr−1. This estimated diffusive net organic carbon exchange is similar to the estimated organic carbon deficit for this region of 0.5 Gt C yr−1derived from the metabolic imbalance of the planktonic community [Duarte et al., 2001]. This imbalance cannot be accounted for by internal transport via oceanic circulation or wet deposition alone [Hansen et al., 2004]. This finding is consistent with previous suggestions that atmospheric input of OC may help explain net heterotrophy (i.e., excess organic carbon respiration over authochtonous production) in the NE Atlantic [del Giorgio and Duarte, 2002; Duarte et al., 1999]. The specific role of atmospheric OC inputs on regional carbon budgets depends, however, on the fraction of labile and refractory exchangeable organic carbon, which remains untested. Labile components would fuel heterotrophic processes, thereby yielding CO2, whereas refractory and hydrophobic compounds would eventually add to the downward OC flux at the ultimate sink areas.
 The exchange fluxes of volatile and semivolatile organic carbon between the atmosphere and the ocean reported here cannot be extrapolated to the global ocean, as these are likely to be particularly high for the subtropical NE Atlantic, due to proximate upwind anthropogenic and continental sources, marine regions with high primary productivity, and under strong and persistent wind speeds (about 10 m s−1). A global estimate of OC air-sea exchanges can only be attempted once a cross-regional survey of fluxes, comparable to that available for CO2 fluxes [Takahashi et al., 2002], becomes available. However, exchange fluxes of total OC between the ocean and the atmosphere would remain of global significance even if the global-average flux would be an order of magnitude lower than that reported here for the NE Atlantic. Previous assessments of atmospheric deposition of organic C to the global oceans, considering wet deposition alone, arrived at an estimate of 0.1 Gt C yr−1 [Willey et al., 2000]. Yet, it is well known that diffusive volatilization and absorption fluxes for most organic compounds are up to 20 times higher than wet and dry aerosol deposition fluxes [Duce et al., 1991; Jurado et al., 2005]. Therefore, the global air-sea exchange flux of total organic carbon can be significantly higher than the modest flux reported due to wet deposition, which is already sizeable to the estimated oceanic CO2 uptake of about 2 Gt C yr−1.[IPCC, 2001; Takahashi et al., 2002].
 Whereas these comparisons highlight the air-sea organic carbon exchange as major component of the global carbon cycle, the global direction of this flux, rendering the ocean a net source or sink of OC to the atmosphere, cannot be ascertained yet. The few previous attempts to estimate fluxes of total OC between the atmosphere and the ocean have been limited to assessments of wet and/or dry aerosol deposition [Willey et al., 2000; Durrieu de Madron et al., 2000; del Giorgio and Duarte, 2002], but neglected diffusive fluxes, which dominate the atmosphere-ocean exchange of individual organic compounds [Duce et al., 1991; Dachs et al., 2002; Jurado et al., 2005]. Here, we demonstrated an approach to estimate air-sea OC fluxes, and the significant of these in the Subtropical NE Atlantic. The evaluation of regional and global rates of air-sea organic carbon fluxes and elucidating the origin and fate of these materials must, therefore, receive urgent attention as an essential step to better understand the carbon budgets of the ocean and the atmosphere and test the suggested role of the atmosphere as a major vector for OC fluxes in the biosphere.
 This research is part of the COCA, DEPOCEC, and BADE-Spain projects, which were funded by the Spanish “Plan Nacional de I+D.” The BADE project is funded by the Dutch Science Foundation (NWO-ALW). S.d.V. and M.Ll.C. acknowledge PhD fellowships from “Generalitat de Catalunya” and Spanish Research Council (CSIC), respectively. We thank the crews of the R/V Hespérides and R/V Pelagia, the technical UTM personnel involved for professional assistance, J.C. Alonso, N. Cantero and R. Santiago for assistance in the laboratory. L. Méjanelle and R. Simó are acknowledged for helpful and insightful discussions.