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      Surfactant control of gas transfer velocity along an offshore coastal transect: results from a laboratory gas exchange tank

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      Biogeosciences

      Copernicus GmbH

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          Abstract

          Understanding the physical and biogeochemical controls of air–sea gas exchange is necessary for establishing biogeochemical models for predicting regional- and global-scale trace gas fluxes and feedbacks. To this end we report the results of experiments designed to constrain the effect of surfactants in the sea surface microlayer (SML) on the gas transfer velocity (<i>k</i><sub>w</sub>; cm h<sup>−1</sup>), seasonally (2012–2013) along a 20 km coastal transect (North East UK). We measured total surfactant activity (SA), chromophoric dissolved organic matter (CDOM) and chlorophyll <i>a</i> (Chl <i>a</i>) in the SML and in sub-surface water (SSW) and we evaluated corresponding <i>k</i><sub>w</sub> values using a custom-designed air–sea gas exchange tank. Temporal SA variability exceeded its spatial variability. Overall, SA varied 5-fold between all samples (0.08 to 0.38 mg L<sup>−1</sup> T-X-100), being highest in the SML during summer. SML SA enrichment factors (EFs) relative to SSW were ∼  1.0 to 1.9, except for two values (0.75; 0.89: February 2013). The range in corresponding <i>k</i><sub>660</sub> (<i>k</i><sub>w</sub> for CO<sub>2</sub> in seawater at 20 °C) was 6.8 to 22.0 cm h<sup>−1</sup>. The film factor <i>R</i><sub>660</sub> (the ratio of <i>k</i><sub>660</sub> for seawater to <i>k</i><sub>660</sub> for “clean”, i.e. surfactant-free, laboratory water) was strongly correlated with SML SA (<i>r</i> ≥ 0.70, <i>p</i> ≤ 0.002, each <i>n</i> = 16). High SML SA typically corresponded to <i>k</i><sub>660</sub> suppressions ∼  14 to 51 % relative to clean laboratory water, highlighting strong spatiotemporal gradients in gas exchange due to varying surfactant in these coastal waters. Such variability should be taken account of when evaluating marine trace gas sources and sinks. Total CDOM absorbance (250 to 450 nm), the CDOM spectral slope ratio (<i>S</i><sub>R</sub> = <i>S</i><sub>275 − 295</sub>∕<i>S</i><sub>350 − 400</sub>), the 250 : 365 nm CDOM absorption ratio (<i>E</i><sub>2</sub> : <i>E</i><sub>3</sub>), and Chl <i>a</i> all indicated spatial and temporal signals in the quantity and composition of organic matter in the SML and SSW. This prompts us to hypothesise that spatiotemporal variation in <i>R</i><sub>660</sub> and its relationship with SA is a consequence of compositional differences in the surfactant fraction of the SML DOM pool that warrants further investigation.

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          Author and article information

          Journal
          Biogeosciences
          Biogeosciences
          Copernicus GmbH
          1726-4189
          2016
          July 11 2016
          : 13
          : 13
          : 3981-3989
          Article
          10.5194/bg-13-3981-2016
          © 2016
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