High precision isotopic measurements of Sn in two commercially available high purity materials and a previously analysed cassiterite from Straits Settlement, Malaysia, are presented as a basis for a new measurement procedure using the Micromass IsoProbe MC-ICP-MS. The results show that under optimised instrumental conditions two laboratory calibration standard solutions (Johnson-Matthey Puratronic Grade 1 Sn metal foil and Specpure ICP/DCP Sn solution) are isotopically identical and an external reproducibility of 0.000017 2 s.d. at 150 ppb Sn concentration ( 122 Sn/ 116 Sn 0.318597, n ~14) can be achieved. An isotopic fractionation of 10.13%/u (1.3 epsilon units) relative to these in-house standards has been verified for the cassiterite, which indicates a natural isotopic fractionation of approximately 2.8 times greater than the long-term reproducibility of the current optimised measurement procedure.

Ferrihydrite and goethite are amongst the most important substrates for the sorption of contaminants in soil and other environmental media. Isotopic studies of the transition elements, particularly those that exhibit more than one oxidation state and show pH- and/or redox-sensitive behaviour at low temperatures, have been shown to be potentially useful present-day and past proxies for redox (or palaeoredox) conditions. We have made preliminary investigations of Fe isotope fractionation that take place during the formation of FeIII (oxy)hydroxides (FeIIIox) from an aqueous FeIII(NO3)3 solution (FeIIIaq) under laboratory conditions. We have attempted to keep the chemical system simple by excluding 'vital effects' and major changes in redox through the maintenance of abiotic conditions and use of FeIIIaq. Isotopic measurements (56Fe/54Fe, 57Fe/54Fe) of the FeIII(NO3)3 stock solution, the original ferrihydrite and the mixed ferrihydrite/goethite-supernatant FeIIIaq 'pairs' were carried out using a double focusing multicollector inductively coupled plasma mass spectrometer. The results reveal an apparent systematic variation indicating larger ΔFeIIIaq—FeIIIox with decrease in the ferrihydrite:goethite ratio, which reflects the time allowed for isotopic exchange. These values range from virtually zero (0.03%) after 24 h to 0.30% after 70 h. In each FeIIIox-FeIIIaq 'pair' the lighter Fe isotope is partitioned into the FeIIIox, leaving the FeIIIaq isotopically heavier. The observed fractionation reflects isotopic exchange of Fe between the FeIIIox and FeIIIaq upon at least a two step transition of ferrihydrite to goethite.

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