Ultra-high-temperature metamorphism

Metamorphism of crustal rocks in which peak temperature exceeds 900 °C, recognized either by robust thermobarometry or by the presence of a diagnostic mineral assemblage in an appropriate bulk composition and oxidation state, such as assemblages with orthopyroxene + sillimanite + quartz, sapphirine + quartz or spinel + quartz, generally at pressure conditions of sillimanite stability in metapelites [after Brown (2007)[2] following proposal by Harley (1998)[1]].

Petrological indicators of UHT metamorphism are usually preserved in extremely Mg-Al-rich rocks which are usually dry and restitic in nature. Mineral assemblages such as sapphirine + quartz, orthopyroxene + sillimanite ± quartz, osumilite and spinel + quartz provide straight away evidence for such extreme conditions. Occasionally widespread assemblages like garnet + orthopyroxene, ternary feldspars, (F-Ti) pargasite or metamorphic inverted pigeonite are taken as typical indicators of UHT metamorphism.

UHT rocks are now identified in all major continents and span different geological ages ranging from c. 3178 to 35 million years associated with major geological events. More than 46 localities/terranes with diagnostic UHT indicators have been reported over the globe, related to both extensional and collisional tectonic environments; the two fundamental types of Earth orogenic systems.[3][5] The major Archean UHT rocks are distributed in East-Antarctica, South Africa, Russia and Canada.[6][7][8][9][10] Paleoproterozoic UHT granulites were reported from the North China Craton (during the accretion of the supercontinent Columbia),[11][12][13] Taltson magmatic zone, northwestern Canada[14] and South Harris, Lewisian complex, Scotland.[15][16][17][18] UHT rocks from the Neoproterozoic Grenville orogeny are distributed in the Eastern Ghats Province, India.[19] Neoproterozoic-Cambrian (Pan-African) UHT occurrences are mainly distributed in Lutzow-Holm Bay, East Antarctica,[20] southern Madagascar,[21] Sri Lanka[22][23][24] and southern India.[11][25][26][27][28][29][30][31][32][33] UHT rocks are also reported from younger terranes like the Triassic Kontum Massif, Vietnam,[34] Cretaceous Higo belt, Japan[35][36] and Paleogene Gruf Complex, central Alps.[37] Three-million-year-old xenoliths erupted in Qiangtang imply that UHT metamorphism is ongoing beneath central Tibet.[38]

A correlation was proposed between the episodic formation of UHT metamorphic rocks and the episodic assembly of supercontinents in the Precambrian.[39] However, inspection of extreme metamorphism at convergent plate margins indicates that supercontinental assembly is associated with regional HP to UHP eclogite-facies metamorphism at low thermal gradients of less than 10 °C/km, whereas continental rifting plays a crucial role in causing regional HT to UHT granulite-facies metamorphism at high thermal gradients of greater than 30 °C/km.[40] In this regard, the episodic formation of HT to UHT granulite-facies metamorphic rocks is temporally and spatially coupled with the breakup or attempting rupture of supercontinents in the plate tectonics context.

Because UHT rocks are generally characterized by low water contents, this led to an illusion for the involvement of CO₂-rich fluids in generating diagnostic UHT assemblages according to the finding of abundant pure CO₂ fluid inclusions in these rocks.[13] However, the extraction of liquid phases such as aqueous solutions and hydrous melts from anatectic systems during UHT metamorphism is so efficient that the common occurrence of pure CO₂ fluid inclusions looks as if the incoming CO₂ could have buffered the water activity and stabilized the anhydrous mineralogy of UHT rocks. Anatectic melts were variably extracted from anatectic systems, leading to granulite-migmatite-granite associations in accretionary and collisional orogens.[41] Metamorphic core complexes were emplaced due to the buoyant entrainment of granitic melts. The abundant water was liberated by heating dehydration of the lowest orogenic crust, contributing aqueous solutions to amphibolite-facies retrogression of the overlying crust.

• Clark, C., I.C.W. Fitzsimons, D. Healy, and S.L. Harley, 2011, How does the continental crust get really hot?, Elements, 7 (4), 235-240.
• Brown, M. and White, R.W. 2008, Processes in granulite metamorphism Journal of Metamorphic Geology, v. 26, p. 125-299.
• Sajeev, K. and Santosh, M. 2006, Extreme crustal metamorphism and related crust-mantle processes. Lithos v. 92 n. 3-4, p. 321-624.
• Santosh, M., Osanai, Y. and Tsunogae, T. 2004, Ultrahigh temperature metamorphism and deep crustal processes Journal of Mineralogical and Petrological Sciences v. 99 (part 1 & 2), n. 4-5, 137-365.
• Harley, S.L., 2008, Refining the P–T records of UHT crustal metamorphism. Geological Society, London, Special Publications, v. 138, p. 81-107.
• Zheng, Y.-F., Chen, R.-X., 2017. Regional metamorphism at extreme conditions: Implications for orogeny at convergent plate margins. Journal of Asian Earth Sciences, v. 145, p. 46-73.