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=== Classification === | === Classification === | ||
Eclogites are defined as bi-mineralic, broadly basaltic rocks which have been classified into Groups A, B and C based on the chemistry of their primary mineral phases, garnet and clinopyroxene.<ref name=":13">{{Cite journal|last=Jacob|first=D. E.|date=2004-09-01|title=Nature and origin of eclogite xenoliths from kimberlites|url=https://www.sciencedirect.com/science/article/pii/S0024493704001045|journal=Lithos|series=Selected Papers from the Eighth International Kimberlite Conference. Volume 2: The J. Barry Hawthorne Volume|language=en|volume=77|issue=1|pages=295–316|doi=10.1016/j.lithos.2004.03.038|issn=0024-4937|url-access=subscription}}</ref><ref name=":0">{{Cite journal|last1=COLEMAN|first1=R. G|last2=LEE|first2=D. E|last3=BEATTY|first3=L. B|last4=BRANNOCK|first4=W. W|date=1965-05-01|title=Eclogites and Eclogites: Their Differences and Similarities|url=https://doi.org/10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|journal=GSA Bulletin|volume=76|issue=5|pages=483–508|doi=10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|issn=0016-7606|url-access=subscription}}</ref> The classification distinguishes each group based on the jadeite content of clinopyroxene and pyrope in garnet.<ref name=":0" /> The rocks are gradationally less mafic (as defined by SiO<sub>2</sub> and MgO) from group A to C, where the least mafic Group C contains higher [[Alkaline earth metal|alkali]] contents.<ref name=":02">{{Cite journal|last1=COLEMAN|first1=R. G|last2=LEE|first2=D. E|last3=BEATTY|first3=L. B|last4=BRANNOCK|first4=W. W|date=1965-05-01|title=Eclogites and Eclogites: Their Differences and Similarities|url=https://doi.org/10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|journal=GSA Bulletin|volume=76|issue=5|pages=483–508|doi=10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|issn=0016-7606|access-date=2021-11-30|archive-date=2022-02-12|archive-url=https://web.archive.org/web/20220212025752/https://pubs.geoscienceworld.org/gsa/gsabulletin/article-abstract/76/5/483/5909/Eclogites-and-Eclogites-Their-Differences-and?redirectedFrom=fulltext|url-status=live|url-access=subscription}}</ref> | Eclogites are defined as bi-mineralic, broadly basaltic rocks which have been classified into Groups A, B and C based on the chemistry of their primary mineral phases, garnet and clinopyroxene.<ref name=":13">{{Cite journal|last=Jacob|first=D. E.|date=2004-09-01|title=Nature and origin of eclogite xenoliths from kimberlites|url=https://www.sciencedirect.com/science/article/pii/S0024493704001045|journal=Lithos|series=Selected Papers from the Eighth International Kimberlite Conference. Volume 2: The J. Barry Hawthorne Volume|language=en|volume=77|issue=1|pages=295–316|doi=10.1016/j.lithos.2004.03.038|bibcode=2004Litho..77..295J |issn=0024-4937|url-access=subscription}}</ref><ref name=":0">{{Cite journal|last1=COLEMAN|first1=R. G|last2=LEE|first2=D. E|last3=BEATTY|first3=L. B|last4=BRANNOCK|first4=W. W|date=1965-05-01|title=Eclogites and Eclogites: Their Differences and Similarities|url=https://doi.org/10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|journal=GSA Bulletin|volume=76|issue=5|pages=483–508|doi=10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|issn=0016-7606|url-access=subscription}}</ref> The classification distinguishes each group based on the jadeite content of clinopyroxene and pyrope in garnet.<ref name=":0" /> The rocks are gradationally less mafic (as defined by SiO<sub>2</sub> and MgO) from group A to C, where the least mafic Group C contains higher [[Alkaline earth metal|alkali]] contents.<ref name=":02">{{Cite journal|last1=COLEMAN|first1=R. G|last2=LEE|first2=D. E|last3=BEATTY|first3=L. B|last4=BRANNOCK|first4=W. W|date=1965-05-01|title=Eclogites and Eclogites: Their Differences and Similarities|url=https://doi.org/10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|journal=GSA Bulletin|volume=76|issue=5|pages=483–508|doi=10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|issn=0016-7606|access-date=2021-11-30|archive-date=2022-02-12|archive-url=https://web.archive.org/web/20220212025752/https://pubs.geoscienceworld.org/gsa/gsabulletin/article-abstract/76/5/483/5909/Eclogites-and-Eclogites-Their-Differences-and?redirectedFrom=fulltext|url-status=live|url-access=subscription}}</ref> | ||
The transitional nature between groups A, B and C correlates with their mode of emplacement at the surface.<ref name=":0" /> Group A derive from [[craton]]ic regions of Earth's crust, brought to the surface as xenoliths from depths greater than 150 km during [[kimberlite]] eruptions.<ref name=":13"/><ref name=":0" /> Group B show strong compositional overlap with Group A, but are found as lenses or pods surrounded by [[Peridotite|peridotitic]] mantle material.<ref name=":0" /> Group C are commonly found between layers of [[mica]] or [[Glaucophane Schist Facies|glaucophane schist]], primarily exemplified by the New Caledonia tectonic block and off the coast of California.<ref name=":03">{{Cite journal|last1=COLEMAN|first1=R. G|last2=LEE|first2=D. E|last3=BEATTY|first3=L. B|last4=BRANNOCK|first4=W. W|date=1965-05-01|title=Eclogites and Eclogites: Their Differences and Similarities|url=https://doi.org/10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|journal=GSA Bulletin|volume=76|issue=5|pages=483–508|doi=10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|issn=0016-7606|access-date=2021-11-30|archive-date=2022-02-12|archive-url=https://web.archive.org/web/20220212025750/https://pubs.geoscienceworld.org/gsa/gsabulletin/article-abstract/76/5/483/5909/Eclogites-and-Eclogites-Their-Differences-and?redirectedFrom=fulltext|url-status=live|url-access=subscription}}</ref> | The transitional nature between groups A, B and C correlates with their mode of emplacement at the surface.<ref name=":0" /> Group A derive from [[craton]]ic regions of Earth's crust, brought to the surface as xenoliths from depths greater than 150 km during [[kimberlite]] eruptions.<ref name=":13"/><ref name=":0" /> Group B show strong compositional overlap with Group A, but are found as lenses or pods surrounded by [[Peridotite|peridotitic]] mantle material.<ref name=":0" /> Group C are commonly found between layers of [[mica]] or [[Glaucophane Schist Facies|glaucophane schist]], primarily exemplified by the New Caledonia tectonic block and off the coast of California.<ref name=":03">{{Cite journal|last1=COLEMAN|first1=R. G|last2=LEE|first2=D. E|last3=BEATTY|first3=L. B|last4=BRANNOCK|first4=W. W|date=1965-05-01|title=Eclogites and Eclogites: Their Differences and Similarities|url=https://doi.org/10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|journal=GSA Bulletin|volume=76|issue=5|pages=483–508|doi=10.1130/0016-7606(1965)76[483:EAETDA]2.0.CO;2|issn=0016-7606|access-date=2021-11-30|archive-date=2022-02-12|archive-url=https://web.archive.org/web/20220212025750/https://pubs.geoscienceworld.org/gsa/gsabulletin/article-abstract/76/5/483/5909/Eclogites-and-Eclogites-Their-Differences-and?redirectedFrom=fulltext|url-status=live|url-access=subscription}}</ref> | ||
=== Surface versus mantle origin === | === Surface versus mantle origin === | ||
The broad range in composition has led a longstanding debate on the origin of eclogite xenoliths as either mantle or surface derived, where the latter is associated with the [[gabbro]] to eclogite transition as a major driving force for [[subduction]].<ref name=":12">{{Cite journal|last=Jacob|first=D. E.|date=2004-09-01|title=Nature and origin of eclogite xenoliths from kimberlites|url=https://www.sciencedirect.com/science/article/pii/S0024493704001045|journal=Lithos|series=Selected Papers from the Eighth International Kimberlite Conference. Volume 2: The J. Barry Hawthorne Volume|language=en|volume=77|issue=1|pages=295–316|doi=10.1016/j.lithos.2004.03.038|issn=0024-4937|access-date=2021-11-30|archive-date=2022-02-12|archive-url=https://web.archive.org/web/20220212025749/https://www.sciencedirect.com/science/article/abs/pii/S0024493704001045|url-status=live|url-access=subscription}}</ref><ref name="O'Hara 69–133">{{Cite journal|last=O'Hara|first=M. J.|date=1968-01-01|title=The bearing of phase equilibria studies in synthetic and natural systems on the origin and evolution of basic and ultrabasic rocks|url=https://dx.doi.org/10.1016/0012-8252%2868%2990147-5|journal=Earth-Science Reviews|language=en|volume=4|pages=69–133|doi=10.1016/0012-8252(68)90147-5|issn=0012-8252|url-access=subscription}}</ref><ref>{{Cite journal|last1=Ringwood|first1=A. E.|last2=Green|first2=D. H.|date=1966-10-01|title=An experimental investigation of the Gabbro-Eclogite transformation and some geophysical implications|url=https://dx.doi.org/10.1016/0040-1951%2866%2990009-6|journal=Tectonophysics|language=en|volume=3|issue=5|pages=383–427|doi=10.1016/0040-1951(66)90009-6|issn=0040-1951|url-access=subscription}}</ref> | The broad range in composition has led a longstanding debate on the origin of eclogite xenoliths as either mantle or surface derived, where the latter is associated with the [[gabbro]] to eclogite transition as a major driving force for [[subduction]].<ref name=":12">{{Cite journal|last=Jacob|first=D. E.|date=2004-09-01|title=Nature and origin of eclogite xenoliths from kimberlites|url=https://www.sciencedirect.com/science/article/pii/S0024493704001045|journal=Lithos|series=Selected Papers from the Eighth International Kimberlite Conference. Volume 2: The J. Barry Hawthorne Volume|language=en|volume=77|issue=1|pages=295–316|doi=10.1016/j.lithos.2004.03.038|bibcode=2004Litho..77..295J |issn=0024-4937|access-date=2021-11-30|archive-date=2022-02-12|archive-url=https://web.archive.org/web/20220212025749/https://www.sciencedirect.com/science/article/abs/pii/S0024493704001045|url-status=live|url-access=subscription}}</ref><ref name="O'Hara 69–133">{{Cite journal|last=O'Hara|first=M. J.|date=1968-01-01|title=The bearing of phase equilibria studies in synthetic and natural systems on the origin and evolution of basic and ultrabasic rocks|url=https://dx.doi.org/10.1016/0012-8252%2868%2990147-5|journal=Earth-Science Reviews|language=en|volume=4|pages=69–133|doi=10.1016/0012-8252(68)90147-5|bibcode=1968ESRv....4...69O |issn=0012-8252|url-access=subscription}}</ref><ref>{{Cite journal|last1=Ringwood|first1=A. E.|last2=Green|first2=D. H.|date=1966-10-01|title=An experimental investigation of the Gabbro-Eclogite transformation and some geophysical implications|url=https://dx.doi.org/10.1016/0040-1951%2866%2990009-6|journal=Tectonophysics|language=en|volume=3|issue=5|pages=383–427|doi=10.1016/0040-1951(66)90009-6|bibcode=1966Tectp...3..383R |issn=0040-1951|url-access=subscription}}</ref> | ||
Group A eclogite xenoliths remain the most enigmatic in terms of their origin due to [[Metasomatism|metasomatic]] overprinting of their original composition.<ref>{{Cite journal|date=1980-07-24|title=Chemical variations in upper mantle nodules from southern African kimberlites|url=https://royalsocietypublishing.org/doi/10.1098/rsta.1980.0215|journal=Philosophical Transactions of the Royal Society of London. Series A, Mathematical and Physical Sciences|language=en|volume=297|issue=1431|pages=273–293|doi=10.1098/rsta.1980.0215|s2cid=123640184 |issn=0080-4614|access-date=2021-11-30|archive-date=2021-11-04|archive-url=https://web.archive.org/web/20211104080455/https://royalsocietypublishing.org/doi/10.1098/rsta.1980.0215|url-status=live|url-access=subscription}}</ref><ref name=":13"/> Models proposing a primary surface origin as seafloor [[protolith]]s strongly rely on the wide range in [[Isotopes of oxygen|oxygen isotope]] composition, which overlaps with obducted oceanic crust, such as the Ibra section of the [[Semail Ophiolite|Samail ophiolite]].<ref name="onlinelibrary.wiley.com">{{Cite journal|last1=MacGregor|first1=Ian D.|last2=Manton|first2=William I.|date=1986|title=Roberts victor eclogites: Ancient oceanic crust|url=https://onlinelibrary.wiley.com/doi/abs/10.1029/JB091iB14p14063|journal=Journal of Geophysical Research: Solid Earth|language=en|volume=91|issue=B14|pages=14063–14079|doi=10.1029/JB091iB14p14063|issn=2156-2202|url-access=subscription}}</ref><ref>{{Cite journal|last1=Gregory|first1=Robert T.|last2=Taylor|first2=Hugh P.|date=1981|title=An oxygen isotope profile in a section of Cretaceous oceanic crust, Samail Ophiolite, Oman: Evidence for δ18O buffering of the oceans by deep (>5 km) seawater-hydrothermal circulation at mid-ocean ridges|url=https://onlinelibrary.wiley.com/doi/abs/10.1029/JB086iB04p02737|journal=Journal of Geophysical Research: Solid Earth|language=en|volume=86|issue=B4|pages=2737–2755|doi=10.1029/JB086iB04p02737|s2cid=46321182 |issn=2156-2202}}</ref> The variation found in some eclogite xenoliths at the Roberts Victor kimberlite pipe are a result of [[hydrothermal alteration]] of basalt on the seafloor.<ref name="onlinelibrary.wiley.com"/> This process is attributed to both low- and high-temperature seawater exchange, resulting in large fractionations in oxygen isotope space relative to the upper mantle value typical of mid ocean ridge basalt glasses.<ref>{{Cite journal|last=Muehlenbachs|first=Karlis|date=1998-04-15|title=The oxygen isotopic composition of the oceans, sediments and the seafloor|url=https://www.sciencedirect.com/science/article/pii/S0009254197001472|journal=Chemical Geology|language=en|volume=145|issue=3|pages=263–273|doi=10.1016/S0009-2541(97)00147-2|issn=0009-2541|url-access=subscription}}</ref><ref>{{Cite journal|last1=Mattey|first1=David|last2=Lowry|first2=David|last3=Macpherson|first3=Colin|date=1994-12-01|title=Oxygen isotope composition of mantle peridotite|url=https://dx.doi.org/10.1016/0012-821X%2894%2990147-3|journal=Earth and Planetary Science Letters|language=en|volume=128|issue=3|pages=231–241|doi=10.1016/0012-821X(94)90147-3|issn=0012-821X|url-access=subscription}}</ref> Other mechanisms proposed for the origin of Group A eclogite xenoliths rely on a [[cumulate]] model, where garnet and clinopyroxene bulk compositions derive from residues of [[partial melting]] within the mantle.<ref name="O'Hara 69–133"/> Support of this process is result of metasomatic overprinting of the original oxygen isotope composition, driving them back towards the mantle range.<ref>{{Cite journal|last1=Huang|first1=Jin-Xiang|last2=Gréau|first2=Yoann|last3=Griffin|first3=William L.|last4=O'Reilly|first4=Suzanne Y.|last5=Pearson|first5=Norman J.|date=2012-06-01|title=Multi-stage origin of Roberts Victor eclogites: Progressive metasomatism and its isotopic effects|url=https://www.sciencedirect.com/science/article/pii/S002449371200093X|journal=Lithos|language=en|volume=142-143|pages=161–181|doi=10.1016/j.lithos.2012.03.002|issn=0024-4937|url-access=subscription}}</ref> | Group A eclogite xenoliths remain the most enigmatic in terms of their origin due to [[Metasomatism|metasomatic]] overprinting of their original composition.<ref>{{Cite journal|date=1980-07-24|title=Chemical variations in upper mantle nodules from southern African kimberlites|url=https://royalsocietypublishing.org/doi/10.1098/rsta.1980.0215|journal=Philosophical Transactions of the Royal Society of London. Series A, Mathematical and Physical Sciences|language=en|volume=297|issue=1431|pages=273–293|doi=10.1098/rsta.1980.0215|bibcode=1980RSPTA.297..273G |s2cid=123640184 |issn=0080-4614|access-date=2021-11-30|archive-date=2021-11-04|archive-url=https://web.archive.org/web/20211104080455/https://royalsocietypublishing.org/doi/10.1098/rsta.1980.0215|url-status=live|url-access=subscription |last1=Gurney |first1=J. J. |last2=Harte |first2=B. }}</ref><ref name=":13"/> Models proposing a primary surface origin as seafloor [[protolith]]s strongly rely on the wide range in [[Isotopes of oxygen|oxygen isotope]] composition, which overlaps with obducted oceanic crust, such as the Ibra section of the [[Semail Ophiolite|Samail ophiolite]].<ref name="onlinelibrary.wiley.com">{{Cite journal|last1=MacGregor|first1=Ian D.|last2=Manton|first2=William I.|date=1986|title=Roberts victor eclogites: Ancient oceanic crust|url=https://onlinelibrary.wiley.com/doi/abs/10.1029/JB091iB14p14063|journal=Journal of Geophysical Research: Solid Earth|language=en|volume=91|issue=B14|pages=14063–14079|doi=10.1029/JB091iB14p14063|bibcode=1986JGR....9114063M |issn=2156-2202|url-access=subscription}}</ref><ref>{{Cite journal|last1=Gregory|first1=Robert T.|last2=Taylor|first2=Hugh P.|date=1981|title=An oxygen isotope profile in a section of Cretaceous oceanic crust, Samail Ophiolite, Oman: Evidence for δ18O buffering of the oceans by deep (>5 km) seawater-hydrothermal circulation at mid-ocean ridges|url=https://onlinelibrary.wiley.com/doi/abs/10.1029/JB086iB04p02737|journal=Journal of Geophysical Research: Solid Earth|language=en|volume=86|issue=B4|pages=2737–2755|doi=10.1029/JB086iB04p02737|s2cid=46321182 |issn=2156-2202}}</ref> The variation found in some eclogite xenoliths at the Roberts Victor kimberlite pipe are a result of [[hydrothermal alteration]] of basalt on the seafloor.<ref name="onlinelibrary.wiley.com"/> This process is attributed to both low- and high-temperature seawater exchange, resulting in large fractionations in oxygen isotope space relative to the upper mantle value typical of mid ocean ridge basalt glasses.<ref>{{Cite journal|last=Muehlenbachs|first=Karlis|date=1998-04-15|title=The oxygen isotopic composition of the oceans, sediments and the seafloor|url=https://www.sciencedirect.com/science/article/pii/S0009254197001472|journal=Chemical Geology|language=en|volume=145|issue=3|pages=263–273|doi=10.1016/S0009-2541(97)00147-2|bibcode=1998ChGeo.145..263M |issn=0009-2541|url-access=subscription}}</ref><ref>{{Cite journal|last1=Mattey|first1=David|last2=Lowry|first2=David|last3=Macpherson|first3=Colin|date=1994-12-01|title=Oxygen isotope composition of mantle peridotite|url=https://dx.doi.org/10.1016/0012-821X%2894%2990147-3|journal=Earth and Planetary Science Letters|language=en|volume=128|issue=3|pages=231–241|doi=10.1016/0012-821X(94)90147-3|bibcode=1994E&PSL.128..231M |issn=0012-821X|url-access=subscription}}</ref> Other mechanisms proposed for the origin of Group A eclogite xenoliths rely on a [[cumulate]] model, where garnet and clinopyroxene bulk compositions derive from residues of [[partial melting]] within the mantle.<ref name="O'Hara 69–133"/> Support of this process is result of metasomatic overprinting of the original oxygen isotope composition, driving them back towards the mantle range.<ref>{{Cite journal|last1=Huang|first1=Jin-Xiang|last2=Gréau|first2=Yoann|last3=Griffin|first3=William L.|last4=O'Reilly|first4=Suzanne Y.|last5=Pearson|first5=Norman J.|date=2012-06-01|title=Multi-stage origin of Roberts Victor eclogites: Progressive metasomatism and its isotopic effects|url=https://www.sciencedirect.com/science/article/pii/S002449371200093X|journal=Lithos|language=en|volume=142-143|pages=161–181|doi=10.1016/j.lithos.2012.03.002|bibcode=2012Litho.142..161H |issn=0024-4937|url-access=subscription}}</ref> | ||
==Eclogite facies== | ==Eclogite facies== | ||
Latest revision as of 05:49, 4 June 2025
Eclogite (Template:IPAc-en) is a metamorphic rock containing garnet (almandine-pyrope) hosted in a matrix of sodium-rich pyroxene (omphacite). Accessory minerals include kyanite, rutile, quartz, lawsonite, coesite, amphibole, phengite, paragonite, zoisite, dolomite, corundum and, rarely, diamond. The chemistry of primary and accessory minerals is used to classify three types of eclogite (A, B, and C). The broad range of eclogitic compositions has led to a longstanding debate on the origin of eclogite xenoliths as subducted, altered oceanic crust.
The name eclogite is derived from the Ancient Greek word for 'choice' (Template:Wikt-lang, Template:Grc-transl), meaning 'chosen rock' on account of its perceived beauty. It was first named by René Just Haüy in 1822 in the second edition of his work Traité de minéralogie.[1]
Origins
Eclogites typically result from high to ultrahigh pressure metamorphism of mafic rock at low thermal gradients of <Template:Cvt as it is subducted to the lower crust to upper mantle depths in a subduction zone.[2]
Classification
Eclogites are defined as bi-mineralic, broadly basaltic rocks which have been classified into Groups A, B and C based on the chemistry of their primary mineral phases, garnet and clinopyroxene.[3][4] The classification distinguishes each group based on the jadeite content of clinopyroxene and pyrope in garnet.[4] The rocks are gradationally less mafic (as defined by SiO2 and MgO) from group A to C, where the least mafic Group C contains higher alkali contents.[5]
The transitional nature between groups A, B and C correlates with their mode of emplacement at the surface.[4] Group A derive from cratonic regions of Earth's crust, brought to the surface as xenoliths from depths greater than 150 km during kimberlite eruptions.[3][4] Group B show strong compositional overlap with Group A, but are found as lenses or pods surrounded by peridotitic mantle material.[4] Group C are commonly found between layers of mica or glaucophane schist, primarily exemplified by the New Caledonia tectonic block and off the coast of California.[6]
Surface versus mantle origin
The broad range in composition has led a longstanding debate on the origin of eclogite xenoliths as either mantle or surface derived, where the latter is associated with the gabbro to eclogite transition as a major driving force for subduction.[7][8][9]
Group A eclogite xenoliths remain the most enigmatic in terms of their origin due to metasomatic overprinting of their original composition.[10][3] Models proposing a primary surface origin as seafloor protoliths strongly rely on the wide range in oxygen isotope composition, which overlaps with obducted oceanic crust, such as the Ibra section of the Samail ophiolite.[11][12] The variation found in some eclogite xenoliths at the Roberts Victor kimberlite pipe are a result of hydrothermal alteration of basalt on the seafloor.[11] This process is attributed to both low- and high-temperature seawater exchange, resulting in large fractionations in oxygen isotope space relative to the upper mantle value typical of mid ocean ridge basalt glasses.[13][14] Other mechanisms proposed for the origin of Group A eclogite xenoliths rely on a cumulate model, where garnet and clinopyroxene bulk compositions derive from residues of partial melting within the mantle.[8] Support of this process is result of metasomatic overprinting of the original oxygen isotope composition, driving them back towards the mantle range.[15]
Eclogite facies
This facies reflects metamorphism at high pressure (at or over 12kbar) and moderately high to very high temperatures. The pressures exceed those of greenschist, blueschist, amphibolite or granulite facies.
Eclogites containing lawsonite (a hydrous calcium-aluminium silicate) are rarely exposed at Earth's surface, although they are predicted from experiments and thermal models to form during normal subduction of oceanic crust at depths between about Template:Cvt.[16]
Importance
Formation of igneous rocks from eclogite
Partial melting of eclogite has been modeled to produce tonalite-trondhjemite-granodiorite melts.[17] Eclogite-derived melts may be common in the mantle, and contribute to volcanic regions where unusually large volumes of magma are erupted.[18] The eclogite melt may then react with enclosing peridotite to produce pyroxenite, which in turn melts to produce basalt.[19]
Distribution
Occurrences exist in western North America, including the southwest[20] and the Franciscan Formation of the California Coast Ranges.[21] Transitional granulite-eclogite facies granitoid, felsic volcanics, mafic rocks and granulites occur in the Musgrave Block of the Petermann Orogeny, central Australia. Coesite- and glaucophane-bearing eclogites have been found in the northwestern Himalaya.[22] The oldest coesite-bearing eclogites are about 650 and 620 million years old and they are located in Brazil and Mali, respectively.[23][24]
References
External links
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- ↑ Script error: No such module "Citation/CS1".
- ↑ Script error: No such module "Citation/CS1".
- ↑ Script error: No such module "Citation/CS1".
- ↑ Script error: No such module "Citation/CS1".
- ↑ Script error: No such module "citation/CS1".
- ↑ Script error: No such module "Citation/CS1".
- ↑ William Alexander Deer, R. A. Howie and J. Zussman (1997) Rock-forming Minerals, Geological Society, 668 pages Template:ISBN
- ↑ Script error: No such module "citation/CS1".
- ↑ Script error: No such module "Citation/CS1".
- ↑ Script error: No such module "Citation/CS1".
- ↑ Script error: No such module "Citation/CS1".