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Pseudotachylyte

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Purple and green pseudotachylyte veins in outcrop (Sierra Nevada Mountains, California)

Pseudotachylyte (sometimes written as pseudotachylite) is an extremely fine-grained to glassy, dark, cohesive rock occurring as veins[1] that form through frictional melting and subsequent quenching during earthquakes,[2] large-scale landslides, and impacts events.[3] Chemical composition of pseudotachylyte generally reflects the local bulk chemistry, though may skew to slightly more mafic compositions due to the preferential incorporation of hydrous and ferro-magnesian minerals (mica and amphibole, respectively) into the melt phase.[4]

Pseudotachylyte was first documented by Shand in the Vredefort Impact Structure and was named due to its close resemblance to tachylyte, a basaltic glass.[5] Though pseudotachylyte is reported to have a glassy appearance, they are extremely susceptible to alteration and are thus rarely found to be entirely composed of glass.[6][7] Typically, they are completely devitrified into a very fine-grained material with quench textures such as chilled margins,[8][9] radial and concentric clusters of microcrystalites (spherulites)[10][11] or as radial overgrowths of microcrystalites on clasts,[12] as well as skeletal and spinifex microcrystalites.[6][10]

Radial overgrowth of plagioclase microcrystallite laths on plagioclase survivor grain in pseudotachylyte (Asbestos Mountain Fault, California)

Formation

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Seismic faulting

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Seismic pseudotachylyte fault vein with several injection veins within mylonite (Fort Foster, Maine).

Pseudotachylytes have been referred to as "fossil earthquakes" as they represent definitive evidence of seismic slip.[2] During seismic faulting (earthquakes), pseudotachylyte forms through an extreme concentration of frictional sliding onto a thin surface of a fault. The friction creates heat, and because rocks are insulators, the temperature increases on this surface allowing the rock to melt.[13] This generates a "fault vein" which are often accompanied by "injection veins"[2] that open from the fault vein as opening mode cracks.[14] A melt origin for pseudotachylyte was controversial for some time,[15] with some researchers favouring extreme comminution for their generation (crush-origin).[16] Ample evidence of direct crystallisation from a melt[1][17] though, has more or less put this argument to rest with most researchers defining pseudotachylyte as having a melt origin.

Laboratory experiments investigating how pseudotachylytes form have shown that the initial phase of formation involves the flash melting of asperities that eventually grow and join together into larger patches of a high viscosity melt.[18] The high viscosity of these melt patches raises the fault's coefficient of friction, hindering sliding.[19] As the patches of melt continue to grow and join together, they form a continuous melt layer with a lower viscosity, which reduces the fault's coefficient of friction,[18] effectively lubricating the fault and allowing sliding to occur more easily.[19] Once the melt layer has reached some critical thickness, frictional heat can no longer be generated, and the melt begins to quench and crystallise thus again increasing the melt's viscosity and begins acting as a viscous brake to sliding.[20] Once sliding is stopped, the quenching of the melt layer welds the fault shut and restores its strength to that of the unfaulted surrounding rock.[20][21]

Abundance of seismic pseudotachylyte in nature

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There is an apparent lack of pseudotachylyte in the geologic record relative to the observed seismicity of today,[6][7] which brings into question if this is an issue of the rarity of its production, lack of recognition in the field, or its ability to be preserved.[9] It was once thought that pseudotachylyte could only be produced in dry, crystalline rock,[2] this however, has been shown to be incorrect.[8] Therefore, its production is likely not as rare as originally thought. Pseudotachylyte is often closely associated with other extremely fine grained rocks (e.g. mylonite and cataclasite),[1] and is extremely prone to alteration that often renders it unrecognisable[6][7] which supports arguments that pseudotachylyte production isn't rare, but rather is likely to go unrecognised, and thus unreported.

Landslides

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Pseudotachylytes have been observed at the base of some large-scale landslide deposits.[3] The formation of pseudotachylyte along the base of a landslide occurs due to the same processes as earthquake-generated pseudotachylyte - frictional heating during gliding along the base of the detachment melts the surrounding rock.[3][22] They are similar in appearance to earthquake-generated pseudotachylyte. Some notable examples of landslide-generated pseudotachylyte in the geologic record is the Arequipa volcanic landslide deposit in Peru from approximately 2.4 million years ago,[23] and the Langtang landslide deposit in Nepal which occurred between 30,000 - 25,000 years ago.[22] Pseudotachylyte has also been found along the base of more modern landslides, such as the landslide generated by the 1999 Taiwan earthquake.[24]

Impact structures

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Pseudotachylyte breccia from Vredefort impact structure, South Africa

Pseudotachylyte has also been associated with impact structures.[25][26] Pseudotachylyte in impact craters typically occurs as abundant irregular, anastomosing, and dike-like bodies that contain several large and small rounded inclusions of the impacted, or target, rock in a dense fine-grained to glassy black to greenish matrix.[26] Individual pseudotachylyte bodies within impact craters are not uniform over long distances, and may change in size and shape drastically within meters or tens of meters.[26] The most extensive examples of impact related pseudotachylytes come from impact structures that have been deeply eroded below the floor of the crater, such as in case of the Vredefort impact structure in South Africa, and the Sudbury impact structure in Canada.[5][27][25]

Impact-generated pseudotachylytes are classified into two types depending on their method of formation.[26][25][28] S-Type pseudotachylytes, also known as "shock veins",[27][25] are found as small (<1 cm, typically <1 mm)[26][25] glassy veins that contain high-pressure mineral polymorphs like coesite and stishovite.[26][25][28] These shock veins are thought to form via frictional and shock melting due to the higher pressure compressive stages (%need to make it skip to formation section%) of the shockwave expansion.[25] E-Type (endogenic) pseudotachylytes are formed via frictional melting of the target rock due to high-speed slip caused by the collapse of the crater margin.[27][25]

Pseudotachylyte vs. impact melt in impact structures

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Though pseudotachylyte and impact melt within impact structures are visually similar, both occurring as dike-like bodies, they are chemically different.[25][26] Since pseudotachylyte is derived locally, it will reflect the composition of the wall-rock from which it formed.[25] Impact melts are generated from a much larger volume of rock by instantaneous shock melting, so their chemical compositions will be more reflective of regional-scale mixing and homogenization during melting, particularly in heterogeneous terranes.[25] In the Sudbury impact structure, researchers have been able to distinguish dikes of pseudotachylyte from dikes of impact melt based on their chemical compositions.[25][29]

See also

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  • Impactite – Rock created or modified by impact of a meteorite

References

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  1. ^ a b c Trouw, R.A.J., C.W. Passchier, and D.J. Wiersma (2010) Atlas of Mylonites- and related microstructures. Springer-Verlag, Berlin, Germany. 322 pp. ISBN 978-3-642-03607-1
  2. ^ a b c d Sibson, R.H. (1975). "Generation of pseudotachylyte by ancient seismic faulting". Geophysical Journal International. 43 (3): 775–794. Bibcode:1975GeoJ...43..775S. doi:10.1111/j.1365-246x.1975.tb06195.x.
  3. ^ a b c Lin, A. (2007). Fossil earthquakes: the formation and preservation of Pseudotachylytes. Lecture Notes in Earth Sciences. Vol. 111. Springer. p. 348. ISBN 978-3-540-74235-7. Retrieved 2009-11-02.
  4. ^ Magloughlin, J.F.; Spray, J.G. (1992). "Frictional melting processes and products in geological materials: introduction and discussion". Tectonophysics. 204 (3–4): 197–206. Bibcode:1992Tectp.204..197M. doi:10.1016/0040-1951(92)90307-R – via Elsevier Science Direct.
  5. ^ a b Shand, S. James (1916-02-01). "The Pseudotachylyte of Parijs (Orange Free State), and its Relation to 'Trap-Shotten Gneiss' and 'Flinty Crush-Rock'". Quarterly Journal of the Geological Society. 72 (1–4): 198–221. doi:10.1144/GSL.JGS.1916.072.01-04.12. ISSN 0370-291X. S2CID 129174160.
  6. ^ a b c d Kirkpatrick, James D.; Rowe, Christen D. (2013). "Disappearing ink: How pseudotahcylytes are lost from the rock record". Journal of Structural Geology. 52: 183–198. Bibcode:2013JSG....52..183K. doi:10.1016/j.jsg.2013.03.003.
  7. ^ a b c Fondriest, Michele; Mecklenburgh, Julian; Francois Xavier, Passelegue; Gilberto, Artioli; Nestola, Fabrizio; Spagnuolo, Elena; Rempe, Marieke; Di Toro, Guilio (2020). "Pseudotachylyte alteration and the rapid fade of earthquake scars from the geological record". Geophysical Research Letters. 47 (22). Bibcode:2020GeoRL..4790020F. doi:10.1029/2020GL090020. hdl:11577/3377649. S2CID 228918611.
  8. ^ a b Bjornerud, Marcia (2010). "Rethinking conditions necessary for pseudotachylyte formation: Observations from the Otago schists, South Island, New Zealand". Tectonophysics. 490 (1–2): 68–80. Bibcode:2010Tectp.490...69B. doi:10.1016/j.tecto.2010.04.028.
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  11. ^ Dunkel, K.G.; Morales, L.F.G.; Jamveit, B. (2021). "Pristine microstructures in pseudotachylytes formed in dry lower crust, Lofoten, Norway". Philosophical Transactions A. 379 (2193). Bibcode:2021RSPTA.37990423D. doi:10.1098/rsta.2019.0423. PMC 7898121. PMID 33517873.
  12. ^ Prante, Mitchell R.; Evans, James P. (2015). "Pseudotachylyte and fluid alteration at seismogenic depths (Glacier Lakes and Granite Pass Faults), Central Sierra Nevada, USA". Pure and Applied Geophysics. 172 (5): 1203–1227. Bibcode:2015PApGe.172.1203P. doi:10.1007/s00024-014-0989-2. S2CID 129906270 – via Springer.
  13. ^ Sibson, R.H. (1986). "Earthquakes and rock deformation in crustal fault zones". Annual Review of Earth and Planetary Sciences. 14: 149–175. Bibcode:1986AREPS..14..149S. doi:10.1146/annurev.ea.14.050186.001053.
  14. ^ Rowe, Christen D.; Kirkpatrick, James D.; Brodsky, Emily E. (2012). "Fault rock injections record paleo-earthquakes". Earth and Planetary Science Letters. 335: 154–166. Bibcode:2012E&PSL.335..154R. doi:10.1016/j.epsl.2012.04.015.
  15. ^ Spray, John G. (1995). "Pseudotachylyte controversy: Fact or friction?". Geology. 23 (12): 1119–1122. Bibcode:1995Geo....23.1119S. doi:10.1130/0091-7613(1995)023<1119:PCFOF>2.3.CO;2 – via GeoScience World.
  16. ^ Wenk, H.-R. (1978). "Are pseudotachylites products of fracture or fusion?". Geology. 6 (8): 507–511. Bibcode:1978Geo.....6..507W. doi:10.1130/0091-7613(1978)6<507:APPOFO>2.0.CO;2.
  17. ^ Maddock, R.H. (1983). "Melt origin of fault-generated pseudotachylytes demonstrated by textures". Geology. 11 (2): 105–108. Bibcode:1983Geo....11..105M. doi:10.1130/0091-7613(1983)11<105:MOOFPD>2.0.CO;2.
  18. ^ a b Hirose, T; Shimamoto, T (2005). "Growth of molten zone as a mechanism of slip weakening of simulated faults in gabbro during frictional melting". Journal of Geophysical Research: Solid Earth. 110 (B5). Bibcode:2005JGRB..110.5202H. doi:10.1029/2004JB003207.
  19. ^ a b Di Toro, Giulio; Hirose, Takehiro; Nielsen, Stefan; Pennacchioni, Giorgio; Shimamoto, Toshihiko (2006-02-03). "Natural and Experimental Evidence of Melt Lubrication of Faults During Earthquakes". Science. 311 (5761): 647–649. Bibcode:2006Sci...311..647D. doi:10.1126/science.1121012. ISSN 0036-8075. PMID 16456076. S2CID 43080301.
  20. ^ a b Mitchell, Thomas M.; Toy, Virginia; Di Toro, Giulio; Renner, Jörg; Sibson, Richard H. (2016-10-20). "Fault welding by pseudotachylyte formation". Geology. 44 (12): 1059–1062. Bibcode:2016Geo....44.1059M. doi:10.1130/g38373.1. ISSN 0091-7613.
  21. ^ Proctor, B; Lockner, D.A. (2016). "Pseudotachylyte increases the post-slip strength of faults". Geology. 44 (12): 1003–1006. Bibcode:2016Geo....44.1003P. doi:10.1130/g38349.1. Retrieved 2022-11-03.
  22. ^ a b Masch, L.; Wenk, H.R.; Preuss, E. (1985). "Electron Microscopy Study of Hyalomylonites - Evidence for Frictional Melting in Landslides". Tectonophysics. 115 (1–2): 131–160. Bibcode:1985Tectp.115..131M. doi:10.1016/0040-1951(85)90103-9.
  23. ^ Legros, F.; Cantagrel, J.-M.; Devouard, B. (2000). "Pseudotachylyte (Frictionite) at the Base of the Arequipa Volcanic Landslide Deposit (Peru): Implications for Emplacement Mechanisms". The Journal of Geology. 108 (5): 601–611. Bibcode:2000JG....108..601L. doi:10.1086/314421. S2CID 128761395.
  24. ^ Lin, Aiming; Chen, Allen; Liau, Ching-Fei; Lin, Chyi-Chia; Lin, Po-Shen; Wen, Shu-Ching; Ouchi, Toru (2001). "Frictional fusion due to coseismic landsliding during the 1999 Chi Chi (Taiwan) ML 7.3 earthquake". Geophysical Research Letters. 28 (20): 4011–4014. doi:10.1029/2001GL013253. S2CID 140161341.
  25. ^ a b c d e f g h i j k l Spray, John G. (2010). "Frictional Melting Processes in Planetary Materials: from Hypervelocity Impact to Earthquakes". Annual Review of Earth and Planetary Sciences. 38: 359–374. Bibcode:2010AREPS..38..221S. doi:10.1146/annurev.earth.031208.100045.
  26. ^ a b c d e f g Chapter 5 of the online book, French, B.M. 1998. Traces of Catastrophe, A handbook of shock-metamorphic effects in terrestrial meteorite impact structures, Lunar and Planetary Institute 120pp.
  27. ^ a b c Spray, J.G. (1998). "Localized shock- and friction-induced melting in response to hypervelocity impact". In Grady, M.M.; Hutchinson, R.; Rothery, D.A.; McCall, G.J.H. (eds.). Meteorites: Flux with Time and Impact Effects. Special Publications, Geological Society, London. Vol. 140. pp. 195–204. doi:10.1144/GSL.SP.1998.140.01.14. ISBN 9781862390171. S2CID 128704900.
  28. ^ a b Martini, J.E.J. (1991). "The nature, distribution and genesis of the coesite and stishovite associated with the pseudotachylite of the Vredefort Done, South Africa". Earth and Planetary Science Letters. 103 (1–4): 285–300. Bibcode:1991E&PSL.103..285M. doi:10.1016/0012-821X(91)90167-G.
  29. ^ Thompson, Lucy M.; Spray, John G. (1996). "Pseudotachylyte petrogenesis: constraints from the Sudbury impact structure". Contributions to Mineralogy and Petrology. 125 (4): 359–374. Bibcode:1996CoMP..125..359T. doi:10.1007/S004100050228. S2CID 128762378.


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Wieland, F. (2006) Chapter 4: Pseudotachylitic breccias, other breccias and veins. Structural analysis of impact-related deformation in the collar rocks of the Vredefort Dome, South Africa. unpublished PhD. dissertation. School of Geosciences, University of the Witwatersrand, Johannesburg, South Africa.

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