Constraints on the Cycling of Iron Isotopes From a Global Ocean Model

Although iron (Fe) is a key regulator of primary production over much of the ocean, many components of the marine iron cycle are poorly constrained, which undermines our understanding of climate change impacts. In recent years, a growing number of studies (often part of GEOTRACES) have used Fe isotopic signatures (δ(56)Fe) to disentangle different aspects of the marine Fe cycle. Characteristic δ(56)Fe endmembers of external sources and assumed isotopic fractionation during biological Fe uptake or recycling have been used to estimate relative source contributions and investigate internal transformations, respectively. However, different external sources and fractionation processes often overlap and act simultaneously, complicating the interpretation of oceanic Fe isotope observations. Here we investigate the driving forces behind the marine dissolved Fe isotopic signature (δ(56)Fe(diss)) distribution by incorporating Fe isotopes into the global ocean biogeochemical model PISCES. We find that distinct external source endmembers acting alongside fractionation during organic complexation and phytoplankton uptake are required to reproduce δ(56)Fe(diss) observations along GEOTRACES transects. δ(56)Fe(diss) distributions through the water column result from regional imbalances of remineralization and abiotic removal processes. They modify δ(56)Fe(diss) directly and transfer surface ocean signals to the interior with opposing effects. Although attributing crustal compositions to sedimentary Fe sources in regions with low organic carbon fluxes improves our isotope model, δ(56)Fe(diss) signals from hydrothermal or sediment sources cannot be reproduced accurately by simply adjusting δ(56)Fe endmember values. This highlights that additional processes must govern the exchange and/or speciation of Fe supplied by these sources to the ocean.