Are oxygen isotope fractionation factors between calcite and water derived from speleothems systematically biased due to prior calcite precipitation (PCP)?

TL;DR

This study investigates how prior calcite precipitation (PCP) affects oxygen isotope fractionation factors between calcite and water in speleothems, revealing potential biases in temperature reconstructions from isotope data.

Contribution

The paper introduces a conceptual framework explaining how PCP causes systematic biases in isotope fractionation factors derived from speleothems.

Findings

PCP increases δ18O of dissolved bicarbonate, causing disequilibrium.

Isotope re-equilibration times vary with temperature and affect measurements.

PCP can lead to systematic biases in paleotemperature estimates.

Abstract

The equilibrium oxygen isotope fractionation factor between calcite and water (18{\alpha}calcite/H2O) is an important quantity in stable isotope geochemistry and allows in principle to infer temperature variations from carbonate {\delta}18O if carbonate formation occurred in thermodynamic equilibrium. For this reason, many studies intended to determine the value of the oxygen isotope fractionation factor between calcite and water (18{\alpha}calcite/H2O) for a wide range of temperatures using modern cave calcite and the corresponding cave drip water or ancient speleothem carbonate and fluid inclusion samples. However, the picture that emerges from all of these studies indicates that speleothem calcite is not formed in thermodynamic equilibrium but under kinetic conditions, provoking a large variability of determined 18{\alpha}calcite/H2O values. Here we present a conceptual framework that can explain the variability of 18{\alpha}calcite/H2O values obtained by cave studies. Prior calcite precipitation (PCP) is calcite precipitation before cave drip water is dripping from the cave ceiling and impinges on the surface of a stalagmite or watch glass. Prior to the karst water dripping from the cave ceiling, PCP can occur in the karst above the cave as well as on the cave ceiling, the cave walls and on the surface of stalactites. We argue that PCP leads to increasing the {\delta}18O value of the dissolved HCO3- ({\delta}18OHCO3-), resulting in an oxygen isotope disequilibrium of the {\delta}18OHCO3- values with respect to the {\delta}18O value of water ({\delta}18OH2O). The oxygen isotope disequilibrium between HCO3- and H2O is re-equilibrated by oxygen isotope exchange between H2O and HCO3. Depending on the temperature, the re-equilibration time varies from hours to days and is usually much longer than the residence time of the drip water on stalactites, but much shorter than the time ...