Tracing the effects of high-pressure metasomatic fluids and seawater alteration in blueschist-facies overprinted eclogites: Implications for subduction channel processes.

van der Straaten, François, Halama, Ralf, John, Timm, Schenk, Volker, Hauff, Folkmar and Andersen, Nils (2012) Tracing the effects of high-pressure metasomatic fluids and seawater alteration in blueschist-facies overprinted eclogites: Implications for subduction channel processes. Open Access Chemical Geology, 292/293 . pp. 69-87. DOI 10.1016/j.chemgeo.2011.11.008.

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Supplementary data:


Eclogites from the Tian Shan high-pressure/low-temperature (HP/LT) metamorphic belt show evidence for successively increasing metasomatic alteration with increasing retrograde, blueschist-facies overprint. To constrain the source(s) of the metasomatizing fluid and to evaluate elemental and isotopic changes during this overprint, two sequences of eclogite-blueschist transitions were investigated: A layered transition from eclogite to blueschist (FTS 9–1 sequence) and blueschist-facies overprinted pillow metabasalts (FTS 4 samples).

Geochemical trends based on the relationships of K, Ba, Rb and Th are consistent with HP metasomatism, but distinct from typical seafloor alteration trends. In contrast, oxygen isotope ratios in garnet (δ18OV-SMOW = 7.3–8.7‰) and omphacite (δ18OV-SMOW = 8.2–9.7‰) are similar to δ18OV-SMOW in bulk low-temperature altered oceanic crust (AOC), suggesting O isotopic preservation of a seafloor alteration signature. Carbonate crystallization related to the metasomatic overprint demonstrate CO2 mobility during subduction and potential C storage in HP metamorphic rocks. Carbon isotope ratios in the two sequences differ markedly: Disseminated calcite in the layered FTS 9–1 sequence has δ13CV-PDB = − 9.14 ± 0.19‰, whereas vein-forming ankerite in the pillow metabasalts has δ13CV-PDB = − 2.08 ± 0.12‰. The ankerite reflects an inorganic marine/hydrothermal signature, as observed in ophiolites, whereas the low δ13CV-PDB values from the calcite point to a contribution of organic carbon.

The time when the metasomatic overprint occurred is estimated to be ~ 320 ± 11 Ma based on a Rb-Sr isochron age of six blueschist samples from the pillow metabasalts, which is in agreement with active subduction in this region. Initial (T = 320 Ma) 87Sr/86Sr ratios for all HP/LT rocks range from 0.7059 – 0.7085, and εNd320Ma varies from − 0.4 to + 10.9. Both eclogite-blueschist sequences have initial Sr isotope compositions (87Sr/86Sr ~ 0.707) that are significantly higher than those of typical oceanic mantle-derived basalts. They are thought to derive from a fluid that preserved the Sr isotopic signature of seawater by fluid-rock interaction with seawater-altered oceanic lithosphere in a subduction channel. Mixing models between eclogite and various fluids suggest that the contribution of a sediment-derived fluid was likely less than 20%. A fluid predominantly derived from seawater-altered oceanic lithosphere is also supported by the calculated O isotope composition of the fluids (10.2 – 11.2‰). It is thus evident that subduction channel fluids carry complex, mixed elemental and isotopic signatures, which reflect the composition of their source rocks modified by interaction with various other lithologies.

► Eclogites from the Tian Shan show blueschist-facies metasomatic overprint ► Fluid-induced metasomatism occurred at 320 ± 11 Ma ► Fluid predominantly derived from seawater-altered oceanic lithosphere ► Carbonates reflect C sequestration of mixture of organic and inorganic components

Document Type: Article
Keywords: Geochemistry; subduction; eclogite; metasomatism; seafloor alteration; Tian Shan
Research affiliation: OceanRep > The Future Ocean - Cluster of Excellence
OceanRep > GEOMAR > FB4 Dynamics of the Ocean Floor > FB4-MUHS
OceanRep > SFB 574 > C1
OceanRep > SFB 574
Kiel University
Refereed: Yes
Open Access Journal?: No
DOI etc.: 10.1016/j.chemgeo.2011.11.008
ISSN: 0009-2541
Projects: Future Ocean, SFB574
Contribution Number:
SFB 574161
Date Deposited: 17 Sep 2010 12:01
Last Modified: 23 Sep 2019 18:13

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