Fig. 5: Representation of Fe isotope composition of marine sedimentary sulfides through time (modified from refs. 53,72).
From: Expansion of the aerobic iron biogeochemical cycle during the Paleoproterozoic Lomagundi event
The data show that large Fe isotope fractionation in pyrite is mainly driven by diagenetic processes involving both equilibrium and kinetic effects, and that the previously defined late Proterozoic to modern stage III (53; now stage III-2) was already reached at least for the duration of the ca. 2.22-2.06 Ga LE (stage III-1). The previously described stage II (53) remains restricted during the early part of the GOE when Mn and Fe were still co-precipitating significantly in shelf environments. The shaded gray band represents the boundary of the near-to-zero δ56Fe values of 0 ± 0.5‰. (The plotted literature data are presented in the Supplementary Data 1).
