Abstract
Metasomatic amphibole-eclogite sequences grew in selvages of quartz veins from the Marun-Keu complex (Polar Urals, Russia) during high-pressure metamorphism. Relicts of a pre-metasomatic eclogite-facies assemblage are present in the wallrock layers as irregular patches. Wallrock interstitial quartz trails lying at a high angle to reaction fronts provide evidence for grain-scale pore channelisation which may be produced by intergranular-fluid compositional gradients parallel to the quartz trails. Disequilibrium at vein-wallrock scale is inferred from wallrock mineral heterogeneity and from variable initial Sr isotope ratios in mineral separates. Mass-balance calculations between relicts and wallrock assemblages reveal chemical imbalances caused by open system-behaviour with two way mass-transfer. The vein-wallrock system registers a prograde history from 408–434 °C (relicts) to 526–668 °C (vein precipitates). Vein and metasomatic assemblages formed during a single fluid-rock interaction process, implying high heating rates (≥100 °C/Ma), which could result from heat advection by large-scale fluid circulation.
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Acknowledgements
We thank Muriel Erambert and Jane H. Scarrow for their constructive comments. The help of Jane H. Scarrow in improving the English is also gratefully acknowledged. We are indebted to V. Koroteev, V.I. Lennykh and V. Pease for excellent guidance and company in the field. Field work in the Polar Urals was made possible through a grant from the Nansen Foundation to H. Austrheim. We are indebted to R. Abart and S. Sorensen for constructive reviews. This work was funded by projects ERBFMRXCT96-0009 (TMR-URO Programme from the European Commission), MIUR-COFIN 2003 (Italian MURST) and BTE 2002-04618-CO2-01 (Spanish DGICYT), and by Fellowship of the University of Milan to J-F. M.
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Appendix
Appendix
The Gresens-Grant equations
According to Grant (1986), the initial and final concentrations of the i th component, respectively, \(C^{o}_{i} \) and \(C^{F}_{i} \) are related by the following expression:
where mo and mF are the equivalent masses prior to and after the transformation and ΔC i is the gain or loss of mass of the i th component, Δmi, divided by mo:
Since ΔC i is null for those components which remain immobile during the metasomatic process, from expression (A1) the following relation is derived for immobile components:
Relation (A3) implies that \(C^{F}_{i} \) and \(C^{o}_{i} \) values for immobile components must define a straight line through the origin giving by the equation:
which was named isocon by Grant (1986).
According to relation (A3), the isocon equation becomes:
for a process conserving the nth component;
for constant mass; and
for constant volume (where ρ is the rock density).
Dividing relation (A1) by \(C^{o}_{i} \) and re-arranging terms, we obtain:
which indicates that all components experiencing the same relative variation must lie on a line through the origin. It is important to note that \({\Delta C} \mathord{\left/ {\vphantom {{\Delta C} {C^{o}_{i} }}} \right. \kern-\nulldelimiterspace} {C^{o}_{i} }\) is the relative mass variation of the i th component referred to the masses of that component prior to the metasomatic transformation:
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Molina, J.F., Poli, S., Austrheim, H. et al. Eclogite-facies vein systems in the Marun-Keu complex (Polar Urals, Russia): textural, chemical and thermal constraints for patterns of fluid flow in the lower crust. Contrib Mineral Petrol 147, 484–504 (2004). https://doi.org/10.1007/s00410-004-0569-z
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DOI: https://doi.org/10.1007/s00410-004-0569-z