50:. Arc magmas account for more than 20% of terrestrially produced magmas and are produced by the dehydration of minerals within the subducting slab as it descends into the mantle and are accreted onto the base of the overriding continental plate. Subduction zones host a unique variety of rock types formed by the high-pressure, low-temperature conditions a subducting slab encounters during its descent. The metamorphic conditions the slab passes through in this process generates and alters water bearing (hydrous) mineral phases, releasing water into the mantle. This water lowers the melting point of mantle rock, initiating melting. Understanding the timing and conditions in which these dehydration reactions occur, is key to interpreting mantle melting, volcanic arc magmatism, and the formation of continental crust.
54:
94:; however, the pelagic sediments may be accreted onto the forearc-hanging wall and not subducted. Most metamorphic phase transitions that occur within the subducting slab are prompted by the dehydration of hydrous mineral phases. The breakdown of hydrous mineral phases typically occurs at depths greater than 10 km. Each of these metamorphic facies is marked by the presence of a specific stable mineral assemblage, recording the metamorphic conditions undergone by the subducting slab. Transitions between facies cause hydrous minerals to dehydrate at certain pressure-temperature conditions and can therefore be tracked to melting events in the mantle beneath a volcanic arc.
430:
20:
358:
459:. Omphacitic pyroxene is an augite-jadeite solution. At Eclogite facies conditions, plagioclase is no longer stable. The albite component breaks down during glaucophane producing reactions and its sodium becomes incorporated into glaucophane and pyroxene. This reaction is written below. The breakdown of glaucophane is an important water producing reaction at about 600 °C, and over 1 GPa that can trigger significant mantle melting and volcanism.
372:, namely, glaucophane, for which the blueschist facies is named. Lawsonite is also diagnostic of blueschist facies and occurs in association with glaucophane. Glaucophane forming reactions are listed below. Glaucophane producing reactions are significant because they can either release water or produce the hydrous phase, lawsonite through the breakdown of hydrous phyllosilicates. At high blueschist facies pressures, albite may break down to form
438:
565:
two contrasting metamorphic facies series: one is blueschist to eclogite facies series that was produced by subducting metamorphism at low thermal gradients of <10 °C/km, and the other is amphibolite to granulite facies series that was produced by rifting metamorphism at high thermal gradients of >30 °C/km.
548:
were envisaged as a set of parallel metamorphic rock units parallel to a subduction zone displaying two contrasting metamorphic conditions and thus two distinctive mineral assemblages. Nearest to the trench is a zone of low temperature, high pressure metamorphic conditions characterized by blueschist
532:
Transition into the eclogite facies is proposed to be the source of earthquakes at depths greater than 70 km. These earthquakes are caused by the contraction of the slab as minerals transition into more compact crystal structures. The depth of these earthquakes on the subducting slab is known as
564:
However, further studies show the common occurrence of paired metamorphic belts in continental interiors, resulting in controversy on their origin. Based on inspection of extreme metamorphism and post-subduction magmatism at convergent plate margins, paired metamorphic belts are further extended to
207:
are emplaced at shallow levels. Lawsonite does not release water until approximately 300 km depth and is the last hydrous mineral to do so. Metamorphic dehydration reactions are prominent within the subducting slab during subduction, giving rise to liquid phases that contain fluid-mobile trace
253:
are microporous silicate minerals that can be produced by the reaction of pore fluids with basalt and pelagic sediments. The zeolite facies conditions typically only affect pelitic sediments undergoing burial, but is commonly displayed by the production of zeolite minerals within the vesicles of
469:
Another important water producing reaction that occurs during the eclogite facies is the dehydration of the hydrous phyllosilicate phlogopite by the reaction below. This reaction can also trigger significant mantle melting and volcanism. Aside from triggering mantle melt, this reaction may also
513:
Serpentine is another important water bearing phase that breaks down at eclogite facies conditions. Antigorite breaks down at 600–700 °C and between 2–5 GPa. Antigorite contains 13 wt.% water and therefore causes substantial mantle melting. The reaction is listed below.
549:
to eclogite facies assemblages. This assemblage is associated with subduction along the trench and low heat flow. Nearest the arc is a zone of high temperature-low pressure metamorphic conditions characterized by amphibolite to granulite facies mineral assemblages such as
338:, which is associated with blueschist facies. The onset of a low-pressure phase of lawsonite is the most significant marker of prehnite-pumpellyite facies metamorphism. The occurrence of lawsonite is significant because lawsonite contains 11 wt.% H
106:
formed at mid-ocean ridges. The subducting oceanic crust consists of four major units. The topmost unit is a thin cap of pelagic sediments up to 0.3 km thick composed of siliceous and calcareous shells, meteoric dusts, and variable amounts of
208:
elements due to the breakdown of hydrous minerals such as phengite, lawsonite and zoisite. This forms a unique type of trace element distribution pattern for arc magma. Arc magmas and the continental crust formed from arc magmas are enriched in
89:
and prehnite-pumpellyite facies assemblages may or may not be present, thus the onset of metamorphism may only be marked by blueschist facies conditions. Subducting slabs are composed of basaltic crust topped with
199:
O). Phlogopite does not release water until approximately 200 km depth whereas amphibole releases water at approximately 75 km depth. Serpentine is also an important hydrous phase (13 wt% H
102:
Arc magmas are produced by partial melting of metasomatic domains in the mantle wedge, which have reacted with liquid phases derived from dehydration melting of minerals contained in the subducting
334:
may occur at higher grade. Aside from albite, these characteristic minerals are water bearing, and may contribute to mantle melting. These minerals are also vital in the formation of
1045:
Noll, P.D.; et al. (1995). "The role of hydrothermal fluids in the production of subduction zone magmas: Evidence from siderophile and chalcophile trace elements and boron".
798:
Zheng, Y.-F., Chen, R.-X., 2017. Regional metamorphism at extreme conditions: Implications for orogeny at convergent plate margins. Journal of Asian Earth
Sciences 145, 46-73.
228:
fluids released from the slab mobilize these elements and allow them to be incorporated into arc magmas, distinguishing arc magmas from those produced at mid-ocean ridges and
155:
Every year, 1–2 x 10 trillion kilograms of water descends into subduction zones. Approximately 90–95% of that water is contained in hydrous minerals, including
663:"Redistribution of trace elements during prograde metamorphism from lawsonite blueschist to eclogite facies; implications for deep subduction-zone processes"
290:
of the subducting slab, such as gabbro and basaltic sheeted dikes, remain stable until greater depth, when the sodium endmember of plagioclase feldspar,
254:
vesicular basalt. The glassy rinds on pillow basalts are also susceptible to metamorphism under zeolite facies conditions, which produces the zeolites
717:
488:
into the mantle that can trigger partial melting of the slab and of the overlying mantle. The breakdown reaction of lawsonite is listed below.
1341:
Brown, M., 2006. A duality of thermal regimes is the distinctive characteristic of plate tectonics since the
Neoarchean. Geology 34, 961–964.
65:
is characterized by a stable mineral assemblage specific to a pressure-temperature range and specific starting material. Subduction zone
1307:
Oxburgh, E.R.; et al. (February 10, 1971). "Origin of Paired
Metamorphic Belts and Crustal Dilation in Island Arc Regions".
1247:
1179:
986:
913:
Peacock, Simon M. (1 January 2004). "Thermal
Structure and Metamorphic Evolution of Subducting Slabs". In Eiler, John (ed.).
828:
596:
53:
1002:
Zheng, YongFei; Chen, RenXu; Xu, Zheng; Zhang, ShaoBing (20 January 2016). "The transport of water in subduction zones".
853:
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70:
707:
Zheng, Y.-F., Chen, Y.-X., 2016. Continental versus oceanic subduction zones. National
Science Review 3, 495-519.
480:
Lawsonite remains stable up to 1080 °C and 9.4 GPa. The breakdown of lawsonite releases massive amounts of
1357:
123:, that represent cooled magma conduits. The bottom units represent the crystallized magma chamber, feeding the
448:
is typically encountered around 80–100 km depth and is characterized by the presence of green omphacitic
636:
616:
1123:
Pawley, A. R. (May 3, 1994). "The pressure and temperature stability limits of lawsonite: Implications for H
433:
Transition from blueschist to eclogite facies rock, containing glaucophane, omphacitic pyroxene, and garnet
311:
721:
1072:
Liou, Juhn (1979). "Zeolite facies metamorphism of basaltic rocks from the East Taiwan
Ophiolite".
561:. This assemblage is associated with high heat flow generated by melting beneath the volcanic arc.
545:
534:
963:
1195:
Maekawa, Hliokazu (August 5, 1993). "Blueschist metamorphism in an active subduction zone".
882:
115:, formed by the quenching of basaltic magma as it erupts into ocean water. Under the pillow
1316:
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917:. Geophysical Monograph Series. Vol. 138. American Geophysical Union. pp. 12–15.
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under blueschist conditions. Other common minerals of blueschist facies metabasites are
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At paths up to 220–320 °C and below 4.5 kbars, subducting slabs may encounter the
62:
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Miyashiro, A., 1961. Evolution of metamorphic belts. Journal of
Petrology 2, 277–311.
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Bebout, Grey E. (May 31, 2007). "Metamorphic
Chemical Geodynamics of Subduction".
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Melt production and accretion of melt onto continental crust in a subduction zone
429:
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O) that is only present in oceanic crust formed at a slow spreading ridge where
890:
246:
172:
1023:
686:
1351:
1091:
Frey, M.; et al. (1991). "A new petrogenetic grid for low-metabasites".
720:. San Diego State University Department of Geological Science. Archived from
558:
393:
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103:
36:
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replaces the zeolite heulandite and the phyllosilicate chlorite is common.
225:
127:
at which the crust was formed. It is composed of 1–5 km thick layered
108:
66:
44:
1263:
Green, Harry (September 1994). "Solving the
Paradox of Deep Earthquakes".
357:
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O which is released at higher grade and can initiate significant melting.
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conditions (50–150 °C and 1–5 km depth) during subduction.
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Facies transitions and dehydration reactions of a subducting slab
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662:
617:"The subduction factory: How it operates in the evolving Earth"
456:
453:
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Eclogite facies rock, containing omphacitic pyroxene and garnet
291:
283:
187:. The most significant hydrous minerals are lawsonite (11 wt% H
140:
128:
16:
Changes of rock due to pressure and heat near a subduction zone
496:
209:
47:
111:. The next unit is composed of 0.3–0.7 km thick pillow
417:
Pumpellyite + Chlorite + Albite = Glaucophane + Epidote + H
361:
Blueschist containing the sodic blue amphibole, glaucophane
298:. Also at greater depth in the zeolite facies, the zeolite
213:
176:
156:
747:"Slab melting versus slab dehydration in subduction zones"
131:
atop <7 km thick layer of ultramafic rocks (e.g.
314:, characterized by the presence of the hydrous chlorite,
224:
derived from the dehydration within the subducting slab.
637:
10.1130/1052-5173(2005)015[4:TSFHIO]2.0.CO;2
462:
Glaucophane + Paragonite = Pyrope + Jadeite + Quartz + H
330:
and the loss of the zeolites heulandite and laumontite.
150:
470:
trigger partial melting of the subducting slab itself.
413:
Tremolite + Chlorite + Albite = Glaucophane + Lawsonite
368:is characterized by the formation of a sodic, blue
85:facies stability zones of subducted oceanic crust.
147:). Oceanic crust is referred to as a metabasite.
1349:
1001:
908:
906:
904:
902:
900:
718:"How Volcanoes work – Subduction Zone Volcanism"
582:
580:
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57:Pressure-temperature pathway for subducted crust
1240:Principles of Igneous and Metamorphic Petrology
1172:Principles of Igneous and Metamorphic Petrology
979:Principles of Igneous and Metamorphic Petrology
821:Principles of Igneous and Metamorphic Petrology
794:
792:
751:Proceedings of the National Academy of Sciences
589:Principles of Igneous and Metamorphic Petrology
406:+ Chlorite + Albite = Glaucophane + Epidote + H
305:
897:
575:
1118:
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812:
810:
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806:
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31:is a region of the Earth's crust where one
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1129:Contributions to Mineralogy and Petrology
1111:
801:
772:
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667:Contributions to Mineralogy and Petrology
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608:
473:Phlogopite + Diopside + Orthopyroxene = H
843:
660:
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428:
356:
52:
18:
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69:is characterized by a low temperature,
39:gets recycled back into the mantle and
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245:Basalts may first metamorphose under
151:Hydrous minerals of a subducting slab
1090:
1084:
1071:
1044:
1038:
931:
744:
661:Spandler, Carl; et al. (2003).
352:
35:moves under another tectonic plate;
871:Earth and Planetary Science Letters
823:. Prentice Hall. pp. 541–548.
735:
710:
591:. Prentice Hall. pp. 344–345.
345:Laumontite = Lawsonite + Quartz + H
71:high-ultrahigh pressure metamorphic
13:
1127:O recycling in subduction zones".
1105:10.1111/j.1525-1314.1991.tb00542.x
424:
380:will commonly pseudomorphose into
43:gets produced by the formation of
14:
1374:
1285:10.1038/scientificamerican0994-64
745:Mibe, Kenji; et al. (2011).
240:
937:
844:Reynolds, Stephen (2012-01-09).
97:
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1309:Journal of Geophysical Research
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1047:Geochimica et Cosmochimica Acta
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1242:. Prentice Hall. p. 648.
1174:. Prentice Hall. p. 575.
1093:Journal of Metamorphic Geology
981:. Prentice Hall. p. 249.
837:
701:
1:
915:Inside the subduction factory
568:
1059:10.1016/0016-7037(95)00405-x
1004:Science China Earth Sciences
848:. McGraw-Hill. p. 124.
294:, replaces detrital igneous
7:
941:; et al. "Ophiolite".
615:Tatsumi, Yoshiyuki (2005).
312:prehnite-pumpellyite facies
306:Prehnite-pumpellyite facies
10:
1379:
891:10.1016/j.epsl.2007.05.050
1024:10.1007/s11430-015-5258-4
687:10.1007/s00410-003-0495-5
195:O) and amphibole (2 wt% H
1238:Winter, John D. (2010).
1170:Winter, John D. (2010).
977:Winter, John D. (2010).
945:. McGraw-Hill Education.
819:Winter, John D. (2010).
587:Winter, John D. (2010).
546:Paired metamorphic belts
541:Paired metamorphic belts
77:, prehnite-pumpellyite,
1329:10.1029/jb076i005p01315
883:2007E&PSL.260..373B
764:10.1073/pnas.1010968108
191:O), phlogopite (2 wt% H
442:
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1358:Metamorphic petrology
1074:American Mineralogist
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296:plagioclase feldspar
121:sheeted dike complex
1321:1971JGR....76.1315O
1277:1994SciAm.271c..64G
1265:Scientific American
1209:1993Natur.364..520M
1141:1994CoMP..118...99P
1016:2016ScChD..59..651Z
679:2003CoMP..146..205S
535:Wadati–Benioff zone
400:, and pumpellyite.
1149:10.1007/BF00310614
443:
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396:, quartz, albite,
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63:metamorphic facies
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25:
1249:978-0-321-59257-6
1203:(6437): 520–523.
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958:Missing or empty
846:Exploring Geology
830:978-0-321-59257-6
757:(20): 8177–8182.
598:978-0-321-59257-6
366:Blueschist facies
353:Blueschist facies
92:pelagic sediments
73:path through the
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55:
51:
49:
46:
42:
38:
37:oceanic crust
34:
30:
21:
1337:
1312:
1308:
1302:
1293:
1271:(3): 64–71.
1268:
1264:
1258:
1239:
1233:
1200:
1196:
1190:
1171:
1165:
1132:
1128:
1096:
1092:
1086:
1077:
1073:
1067:
1050:
1046:
1040:
1007:
1003:
997:
978:
972:
942:
933:
914:
877:(3–4): 375.
874:
870:
864:
845:
839:
820:
754:
750:
726:. Retrieved
722:the original
712:
703:
670:
666:
641:. Retrieved
627:
623:
588:
563:
544:
531:
516:
509:
491:Lawsonite =
490:
479:
472:
468:
461:
444:
416:
412:
402:
388:, chlorite,
376:and quartz.
364:
344:
309:
262:and hydrous
244:
226:Hydrothermal
154:
109:volcanic ash
101:
67:metamorphism
60:
26:
1099:: 497–509.
643:December 3,
336:glaucophane
320:pumpellyite
137:harzburgite
1363:Subduction
1352:Categories
960:|url=
939:Liou, Juhn
728:2015-01-11
569:References
555:cordierite
519:Forsterite
511:Antigorite
501:Stishovite
386:paragonite
332:Actinolite
318:, albite,
300:laumontite
268:celadonite
256:heulandite
185:serpentine
79:blueschist
1157:128408585
1032:130912355
695:140693326
624:GSA Today
523:Enstatite
493:Grossular
477:O + Melt
404:Tremolite
382:aragonite
370:amphibole
324:tremolite
276:kaolinite
169:lawsonite
165:amphibole
951:cite web
783:21536910
630:(7): 4.
452:and red
450:pyroxene
398:sericite
390:titanite
316:prehnite
272:smectite
266:such as
260:stilbite
251:Zeolites
230:hotspots
222:antimony
173:chlorite
161:phengite
145:chromite
133:wehrlite
83:eclogite
1317:Bibcode
1273:Bibcode
1225:4315927
1205:Bibcode
1137:Bibcode
1012:Bibcode
879:Bibcode
774:3100975
675:Bibcode
378:Calcite
374:jadeite
328:epidote
218:arsenic
181:zoisite
117:basalts
113:basalts
87:Zeolite
75:zeolite
1246:
1223:
1197:Nature
1178:
1155:
1030:
985:
921:
852:
827:
781:
771:
693:
595:
557:, and
457:garnet
454:pyrope
326:, and
292:albite
284:quartz
220:, and
183:, and
143:, and
141:dunite
129:gabbro
81:, and
48:magmas
1221:S2CID
1153:S2CID
1028:S2CID
691:S2CID
620:(PDF)
497:Topaz
278:, or
210:boron
1244:ISBN
1176:ISBN
983:ISBN
964:help
919:ISBN
850:ISBN
825:ISBN
779:PMID
645:2014
593:ISBN
533:the
214:lead
177:talc
157:mica
1325:doi
1281:doi
1269:271
1213:doi
1201:364
1145:doi
1133:118
1101:doi
1055:doi
1020:doi
887:doi
875:260
769:PMC
759:doi
755:108
683:doi
671:146
632:doi
525:+ H
503:+ H
258:or
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