Iron transport by subglacial meltwater indicated by stable iron isotopes in fjord sediments of King George Island, Antarctica


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Susann.Henkel [ at ] awi.de

Abstract

Polar regions are critical for future climate evolution, and they experience major environmental changes. A particular focus of biogeochemical investigations in these regions lies on iron (Fe). This element drives primary productivity and, thus, the uptake of atmospheric CO2 in vast areas of the ocean. Due to the Fe-limitation of phytoplankton growth in the Southern Ocean, Antarctica is a key region for studying the change of iron fluxes as glaciers progressively melt away. The respective climate feedbacks can currently hardly be quantified because data availability is low, and iron transport and reaction pathways in Polar coastal and shelf areas are insufficiently understood. We show how novel stable Fe isotope techniques, in combination with other geochemical analyses, can be used to identify iron discharges from subglacial environments and how this will help us assessing short and long term impacts of glacier retreat on coastal ecosystems. Stable Fe isotopes (δ56Fe) may be used to trace Fe sources and reactions, but respective data availability is low. In addition, there is a need to constrain δ56Fe endmembers for different types of sediments, environments, and biogeochemical processes. δ56Fe data from pore waters and sequentially extracted solid Fe phases at two sites in Potter Cove (King George Island, Antarctica), a bay affected by fast glacier retreat, are presented. Close to the glacier front, sediments contain high amounts of easily reducible Fe oxides and show a dominance of ferruginous conditions compared to sediments close to the ice-free coast, where surficial oxic meltwater discharges and sulfate reduction dominates. We suggest that high amounts of reducible Fe oxides close to the glacier mainly derive from subglacial sources, where Fe liberation from comminuted material beneath the glacier is coupled to biogeochemical weathering. A strong argument for a subglacial source is the predominantly negative δ56Fe signature of reducible Fe oxides that remains constant throughout the ferruginous zone. In situ dissimilatory iron reduction (DIR) does not significantly alter the isotopic composition of the oxides. The composition of the easily reducible Fe fraction therefore suggests pre-depositional microbial cycling as it occurs in subglacial environments. Sediments influenced by oxic meltwater discharge show downcore trends towards positive δ56Fe signals in pore water and reactive Fe oxides, typical for in situ DIR as 54Fe becomes less available with increasing depth. We found that a quantification of benthic Fe fluxes and subglacial Fe discharges based on stable Fe isotope geochemistry will be complicated because (1) diagenetic processes vary strongly at short lateral distances and (2) the variability of δ56Fe in subglacial meltwater has not been sufficiently well investigated yet. However, isotope mass balance models that consider the current uncertainties could, in combination with an application of ancillary proxies, lead to a much better quantification of Fe inputs into polar marine waters than currently available. This would consequently allow a better assessment of the flux and fate of Fe originating from the Antarctic Ice Sheet. Henkel et al. (2018) Diagenetic iron cycling and stable Fe isotope fractionation in Antarctic shelf sediments, King George Island. GCA 237, 320-338.



Item Type
Conference (Poster)
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Primary Division
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Not peer-reviewed
Publication Status
Published
Event Details
EGU General Assembly 2020, 04 May 2020 - 08 May 2020, Sharing Geoscience Online.
Eprint ID
51902
DOI 10.5194/egusphere-egu2020-8940

Cite as
Hartmann, J. F. , Henkel, S. , Kasten, S. , Busso, A. S. and Staubwasser, M. (2020): Iron transport by subglacial meltwater indicated by stable iron isotopes in fjord sediments of King George Island, Antarctica , EGU General Assembly 2020, Sharing Geoscience Online, 4 May 2020 - 8 May 2020 . doi: 10.5194/egusphere-egu2020-8940


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