High field strength element/rare earth element fractionation during partial melting in the presence of garnet: Implications for identification of mantle heterogeneities

TLDR

Garnet‑melt partition coefficients are highly sensitive to changes in garnet major element composition. The study synthesizes recent garnet‑melt partitioning data to compare trace element signatures imparted on mantle melts by peridotitic versus eclogitic garnets. A crystal‑lattice strain model and simple batch‑melting calculations explain how Ca‑rich garnet alters HFSE partitioning and how melt fraction affects trace element ratios. High‑pressure experiments and calculations show that Ca‑rich garnet transforms HFSE from incompatible to compatible, raises U and Th partitioning, leaves HREE largely unchanged, and that ratios such as Zr/HREE, Hf/HREE, Hf/Sm, and Zr/Sm can fingerprint Ca‑rich garnet, though no single universal garnet signature exists.

Abstract

A synthesis of recent garnet‐melt trace element partitioning data for key trace elements (Ti, Hf, Zr, U, Th, Sm, and Yb) is used to compare and contrast the trace element signatures imparted on mantle melts by garnets from peridotitic and eclogitic source rocks. Garnet‐melt partition coefficients D Grt/Melt are very sensitive to changes in garnet major element composition. Specifically, high‐pressure, high‐temperature experimental studies show that high field strength elements (HFSE) Zr, Hf, and Ti are incompatible in garnets with <19 ± 1 mol% Ca on their X site, with D Ti < D Zr ≤ D Hf < 1, while at higher Ca levels, all three become compatible with D Zr > D Hf > D Ti > 1. U and Th also have higher partition coefficients at higher garnet Ca contents, while the amount of fractionation between the two decreases. In contrast, the heavy rare earth element partition coefficients D HREE are hardly affected by a change in garnet Ca content. We provide a semiquantitative explanation for the behavior of the high field strength elements based on a crystal lattice strain model in which Zr and Hf are split between the X and Y sites in Ca‐rich garnet and in which significant changes in garnet elasticity occur as a function of garnet composition. The large variations in both absolute D Grt/Melt values and D Grt/Melt ratios (e.g., D Zr / D Yb ), in conjunction with compositional differences between natural peridotitic (Ca poor) and eclogitic (Ca richer) garnets, allow identification of trace element ratios that may best serve as a fingerprint for the presence of eclogitic garnet. We present simple batch melting calculations for two end‐member melting scenarios (anhydrous garnet peridotite melting and anhydrous bimineralic eclogite melting). Our calculations show that near‐uniform Zr/HREE and Hf/HREE as a function of melt fraction, in combination with Hf/Sm and Zr/Sm ratios that are smaller than the source ratio, could serve as fingerprints for the presence of Ca‐rich garnet in the source of mantle melts. Our calculations show that it is impossible to define one unique “garnet signature” to determine the presence or absence of garnet in basalt sources but rather that different garnet‐bearing sources are likely to produce distinctly different “garnet signatures.”