This article appeared in a journal published by Elsevier. The attached copy is furnished to the author for internal non-commercial research and education use, including for instruction at the authors institution and sharing with colleagues. Other uses, including reproduction and distribution, or selling or licensing copies, or posting to personal, institutional or third party websites are prohibited. In most cases authors are permitted to post their version of the article (e.g. in Word or Tex form) to their personal website or institutional repository. Authors requiring further information regarding Elsevier’s archiving and manuscript policies are encouraged to visit: http://www.elsevier.com/copyright Author's personal copy Available online at www.sciencedirect.com Geochimica et Cosmochimica Acta 74 (2010) 6669–6689 www.elsevier.com/locate/gca Effects of changing solution chemistry on Fe3+/Fe2+ isotope fractionation in aqueous Fe–Cl solutions Pamela S. Hill a,⇑, Edwin A. Schauble a, Edward D. Young a,b a Department of Earth and Space Sciences, University of California, Los Angeles, CA 90095, USA b Institute of Geophysics and Planetary Physics, University of California, Los Angeles, CA 90095, USA Received 3 September 2009; accepted in revised form 12 August 2010; available online 15 October 2010 Abstract The range in 56Fe/54Fe isotopic compositions measured in naturally occurring iron-bearing species is greater than 5&. Both theoretical modeling and experimental studies of equilibrium isotopic fractionation among iron-bearing species have shown that significant fractionations can be caused by differences in oxidation state (i.e., redox effects in the environment) as well as by bond partner and coordination number (i.e., nonredox effects due to speciation). To test the relative effects of redox vs. nonredox attributes on total Fe equilibrium isotopic fractionation, we measured 2+ 3+ changes, both experimentally and theoretically, in the isotopic composition of an Fe –Fe –Cl–H2O solution as the chlorin- À ity was varied. We made use of the unique solubility of FeCl4 in immiscible diethyl ether to create a separate spectator phase against which changes in the aqueous phase could be quantified. Our experiments showed a reduction in the redox isotopic fractionation between Fe2+- and Fe3+-bearing species from 3.4& at [ClÀ] = 1.5 M to 2.4& at [ClÀ] = 5.0 M, due to changes in speciation in the Fe–Cl solution. This experimental design was also used to demonstrate the attainment of isotopic equilib- rium between the two phases, using a 54Fe spike. To better understand speciation effects on redox fractionation, we created four new sets of ab initio models of the ferrous chloride complexes used in the experiments. These were combined with corresponding ab initio models for the ferric chloride complexes from previous work. At 20 °C, 1000 ln b (b = 56Fe/54Fe reduced partition function ratio relative to a dissociated 2+ + Fe atom) values range from 6.39& to 5.42& for Fe(H2O)6 , 5.98& to 5.34& for FeCl(H2O)5 , and 5.91& to 4.86& for FeCl2(H2O)4, depending on the model. The theoretical models predict ferric–ferrous fractionation about half as large (depending on model) as the experimental results. Our results show (1) oxidation state is likely to be the dominant factor controlling equilibrium Fe isotope fractionation in solution and (2) nonredox attributes (such as ligands present in the aqueous solution, speciation and relative abundances, and ionic strength of the solution) can also have significant effects. Changes in the isotopic composition of an Fe-bearing solution will influence the resultant Fe isotopic signature of any precipitates. Ó 2010 Elsevier Ltd. All rights reserved. 1. INTRODUCTION mation)) have been found in natural samples (e.g., Beard and Johnson, 2004, and references therein; Rouxel et al., Large variations in isotopic composition (56Fe/54Fe) 2005; Hofmann et al., 2009), laboratory experiments (e.g., among iron-bearing species in geological and biological sys- Anbar et al., 2000; Johnson et al., 2002; Welch et al., tems at Earth-surface temperatures (from d56Fe = À3.6& 2003), and in theoretical models (e.g., Polyakov and (sedimentary pyrite) to 1.6& (Fe-oxide in banded-iron for- Mineev, 2000; Schauble et al., 2001; Anbar et al., 2005; Hill and Schauble, 2008). Such variations have primarily been attributed to redox effects in the environment upon fractio- ⇑ Corresponding author. nations among iron-bearing species, suggesting that E-mail address: [email protected] (P.S. Hill). 56Fe/54Fe may be an indicator of past oxygen fugacity levels 0016-7037/$ - see front matter Ó 2010 Elsevier Ltd. All rights reserved. doi:10.1016/j.gca.2010.08.038 Author's personal copy 6670 P.S. Hill et al. / Geochimica et Cosmochimica Acta 74 (2010) 6669–6689 in the sedimentary record (e.g., Rouxel et al., 2005; Table 1 Yamaguchi and Ohmoto, 2006; Yamaguchi et al., 2007) Ferric and ferrous chloride complexes, abbreviations, and and/or of bacterial processes (e.g., Johnson et al., 2008, geometries. and references therein). Complex Abbreviation # Fe–Cl Charge Structure However, theoretical studies (Polyakov and Mineev, (# Cl atoms) bonds 2000; Schauble et al., 2001; Liu and Tang, 2006; Tang Ferric 3+ and Liu, 2007; Domagal-Goldman and Kubicki, 2008; Hill Fe(H2O)6 C0 0 +3 Octahedral 2+ and Schauble, 2008) and experimental studies (Fujii et al., FeCl(H2O)5 C1 1 +2 Octahedral + 2006; Hill et al., 2009) indicate that changes in the nonredox FeCl2(H2O)4 C2 2 +1 Octahedral bond environment (i.e., different ligands or coordination (trans) numbers) should also result in significant equilibrium isoto- FeCl3(H2O)3 C3 3 0 Octahedral (fac) pic fractionation among iron-bearing species. In earlier À studies we demonstrated the effects of both coordination FeCl4 C4 4 À1 Tetrahedral number and bond partner on fractionation among ferric Ferrous 2+ chloride complexes in aqueous solutions by developing Fe(H2O)6 D0 0 +2 Octahedral + and comparing ab initio models for ferric chloride species FeCl(H2O)5 D1 1 +1 Octahedral (Hill and Schauble, 2008) and by conducting experiments FeCl2(H2O)4 D2 2 0 Octahedral on fractionation among aqueous Fe3+–Cl complexes as (trans) the solution chemistry was varied (Hill et al., 2009). In the experiments, changes in the isotopic fractionation be- tween an aqueous solution of ferric chloride complexes quantitatively separated from that solution without dis- 3+ À À (Fe(H2O)6 to FeCl4 ) and a spectator phase (FeCl4 turbing the equilibrium. The two-phase design is also used dissolved in ether) were measured as the chlorinity of the in a reversal experiment to show that the experiments reach solution was increased. As would be expected, speciation isotopic equilibrium within a reasonable time (60 min). models showed that the relative abundances of the ferric The geochemical importance of these experiments lies chloride complexes change as the chlorinity of the solution mainly in their potential generalization to other iron-ligand changes; this, in turn, was observed to alter the isotopic systems in which changing speciation under different aque- fractionation between the aqueous and ether phases. Our ous conditions might bring about changes in the overall iso- experimental data showed an average decrease in iron iso- tope signature. The results of our studies of the Fe–Cl tope fractionation of 0.18&/M ClÀ (from 0.5 to 5.0 M system should be expandable to other Fe systems found ClÀ at a constant ionic strength of 5) between the aqueous in nature, such as sulfides, small organic ligands, and sid- and ether phases. Our theoretical models predicted a similar erophores, but which are more difficult to study at equilib- decrease in iron fractionation between the aqueous and rium in the lab. By necessity in the experimental design, the ether phases of 0.16–0.22&/M ClÀ (depending on the mod- chlorinity of our experiments is higher and the pH lower el method and basis set—see Section 2.4). than that found in most natural systems. However, it is In this work we investigate the relative effects of redox worth pointing out that Fe–Cl complexes do occur natu- vs. nonredox attributes on 56Fe/54Fe fractionation via: (1) rally in some oxidized, low-pH or highly saline fluids, such new experiments that combine aqueous ferric and ferrous as sulfate-chloride lakes near volcanoes, evaporative basins, chloride complexes under varying solution chemistries and and mine runoff, and that they can coexist with Fe–S spe- (2) new ab initio models of the ferrous chloride complexes, cies. Though uncommon on Earth today, these environ- which we combine with ab initio models of the ferric chlo- ments are of intrinsic interest as potential habitats for ride complexes (developed in Hill and Schauble, 2008). The extremophiles, and as terrestrial analogs for Mars (e.g., Fe–Cl complexes of interest are detailed in Table 1, includ- Delmelle and Bernard, 1994; Jamieson et al., 2005; Tosca ing the species abbreviations used hereafter. et al., 2005; Amils et al., 2007; Bowen et al., 2007). We adapted the same two-phase experimental design Further, the experimental techniques developed in these used in our ferric chloride experiments (detailed in Hill studies can be potentially expanded to measure fractiona- et al., 2009), this time employing an aqueous phase contain- tions associated with small, labile organic ligands analogous ing both ferric chloride and ferrous chloride complexes and to biological molecules and more broadly to measurements À an ether phase containing FeCl4 (the only Fe–Cl complex of species-dependent isotopic fractionations of other ele- dissolvable in ether (Nachtrieb and Conway, 1948)). Key to ments in solution. the experimental design is the change in the relative abun- dances of the Fe–Cl complexes as the chlorinity of the aque- 2.