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 (delta Fe-56) to disentangle different aspects of the marine Fe cycle. Characteristic delta Fe-56 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 (delta Fe-56(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 delta Fe-56(diss) observations along GEOTRACES transects. delta Fe-56(diss) distributions through the water column result from regional imbalances of remineralization and abiotic removal processes. They modify delta Fe-56(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, delta Fe-56(diss) signals from hydrothermal or sediment sources cannot be reproduced accurately by simply adjusting delta Fe-56 endmember values. This highlights that additional processes must govern the exchange and/or speciation of Fe supplied by these sources to the ocean.