|Title:||Experimental calibration of oxygen isotope fractionation between quartz and zircon|
|Authors:||D. Trail, I.N. Bindeman, E.B. Watson, and A.K. Schmitt|
|Publication:||Geochim. Cosmochim. Acta., v. 73, p. 7110‐7126.|
We report the results of an experimental calibration of oxygen isotope fractionation between quartz and zircon. Data were collected from 700 to 1000 °C, 10‐20 kbar, and in some experiments the oxygen fugacity was buffered at the fayalite‐magnetite‐quartz equilibrium. Oxygen isotope fractionation shows no clear dependence on oxygen fugacity or pressure. Unexpectedly, some high‐temperature data (900‐1000 °C) show evidence for disequilibrium oxygen isotope partitioning. This is based in part on ion microprobe data from these samples that indicate some high‐temperature quartz grains may be isotopically zoned. Excluding data that probably represent non‐equilibrium conditions, our preferred calibration for oxygen isotope fractionation between quartz and zircon can be described by: 1000ln(alpha)qtz−zrc = (2.33 ± 0.24) × 106/T2(in K). This relationship can be used to calculate fractionation factors between zircon and other minerals. In addition, results have been used to calculate WR/melt−zircon fractionations during magma differentiation. Modeling demonstrates that silicic magmas show relatively small changes in δ18O values during differentiation, though late−stage mafic residuals capable of zircon saturation contain elevated δ18O values. However, residuals also have larger predicted melt−zircon fractionations meaning zircons will not record enriched δ18O values generally attributed to a granitic protolith. These results agree with data from natural samples if the zircon fractionation factor presented here or from natural studies is applied.