Generally speaking, ligands act to buffer the dissolved Fe concentration by restricting its loss via scavenging and precipitation. Due to their role in governing the residence time of Fe in the ocean, varying the assumptions regarding the concentrations of ligands has significant impacts on atmospheric CO2 (Tagliabue et al., 2014). The electrochemical methods used to determine oceanic ligand concentrations

often discriminate between two ligand classes, a strong and weak ligand pool (Rue and Bruland, 1995). Surface water ligand concentrations are variable (from 0.2 to > 10 nmol L− 1) and their sources reflect the combination of a number of different production pathways (see: Gledhill and Buck (2012) and references therein). For example, the Fe stressed biota Selleck Pifithrin �� can ‘actively’ produce strong binding ligands (so-called L1 ligands with a conditional stability constant similar to known bacterial siderophores) to complex Fe (Wilhelm and Trick, 1994 and Gledhill et al., 2004). However, while recent work has identified siderophore-like groups in seawater (Macrellis et al., 2001 and Mawji et al., 2008), their concentrations are very low relative to the total ligand concentration. But there are also other pathways that may explain the observed covariance of ligands 17-AAG nmr with

phytoplankton (Gerringa et al., 2006): Weaker binding ligands can be produced by ‘passive’ processes linked to exudates

(such as exopolysaccharides, Hassler et al., 2011) or the cellular debris arising from mortality and heterotrophic activity (e.g., the chlorophyll breakdown product phaeophytin or hemes and other porphyrins, Hutchins et al. (1999)), similar to dissolved organic carbon (DOC) L-NAME HCl cycling. Indeed, ligand concentrations have increased following enhanced biological activity in Fe addition experiments (e.g., Boye et al., 2005) and in response to increased grazing rates in shipboard experiments (Sato et al., 2007). Further support for ‘passive’ production similar to DOC comes from Mediterranean mesocosm observations of a strong covariance between ligands and DOC (Wagener et al., 2008). Away from the surface, vertical profiles of ligands from the Southern (e.g., Ibisanmi et al., 2011) and Atlantic Oceans (e.g. Mohamed et al., 2011) show elevated concentrations of ligands at mid water depth coincident with macronutrient maxima, implying a remineralisation source (Wu et al., 2001). This is supported by the first measurements of ligand production rates from particle degradation during incubation experiments (Boyd et al., 2010) and in situ correlations between nitrate (NO3−) or phosphate (PO43−) and Fe solubility (indicative of ligand concentrations, e.g. Schlosser and Croot (2009)).