399: have long been noted by researchers. Adakites are one type of modern arc lavas, which differ from common arc lavas (mostly granitoids) in their felsic and sodic nature with high LREE but low HREE content. Their production is interpreted to be the partial melting of young and hot subducting oceanic slabs with minor interaction with surrounding mantle wedges, rather than mantle wedge melts like other arc-granitoids. Based on geochemical features (e.g.
314:. To produce the very low HREE pattern, the melting should be conducted under a garnet-stable pressure-temperature field. Given that garnet stability rises dramatically with increasing pressure, strongly HREE-depleted TTG melts are expected to form under relatively high pressure. Besides the source composition and the pressure, the degree of melting and temperature also influence the melt composition.
387:
31:
457:
235:
485:
of plateau bases. Mantle upwellings add mafic basement to the crust and the pressure due to the cumulation thickness may reach the requirement of low pressure TTG production. The partial melting of the plateau base (which can be induced by further mantle upwelling) would then lead to low pressure TTG
469:
Various evidence has shown that
Archean TTG rocks were directly derived from preexisting mafic materials. The melting temperature of meta-mafic rocks (generally between 700 °C and 1000 °C) depends primarily on their water content but only a little on pressure. Different groups of TTG should
464:
into the lighter mantle. The pressure and temperature increases induce the partial melting of the delaminated mafic block to generate TTG magma, which rises and intrudes to the crust. In the lower figure, mantle plume rises to the base of the mafic crust and thicken the crust. The partial melting of
390:
Hypothesized
Archean hot subduction induced Archean TTG generation model. The heavier oceanic crust sinks into the lighter mantle. The subducting slab is young and hot, thus when it is heated, it partially melts to generate TTG magmas, which rise and intrude into the continental crust. Light green:
365:
but no amphibole or plagioclase. The medium pressure group has transitional features between the other two groups, corresponding to melting under a pressure around 15 kbar with the source rock containing amphibole, much garnet, but little rutile and no plagioclase. Medium pressure TTGs are the
489:
The high pressure TTGs have experienced geotherms lower than 10 °C/km, which are close to modern hot subduction geotherms experienced by young slabs (but around 3 °C/km hotter than other modern subduction zones), whilst the geotherms for the most abundant TTG subseries, medium pressure
431:
in the
Philippines), they argue that due to a higher mantle potential temperature of the Earth, a hotter and softer crust may have enabled intense adakite-type subduction during Archean time. TTGs packages were then generated in such settings, with large scale proto-continents formed by
422:
This geochemical similarity let some researchers infer that the geodynamic setting of
Archean TTGs was analogous to that of modern adakites. They think that Archean TTGs were generated by hot subduction as well. Although modern adakites are rare and only found in a few localities (e.g.
1283:
Kemp, A.I.S.; Wilde, S.A.; Hawkesworth, C.J.; Coath, C.D.; Nemchin, A.; Pidgeon, R.T.; Vervoort, J.D.; DuFrane, S.A. (July 2010). "Hadean crustal evolution revisited: New constraints from Pb–Hf isotope systematics of the Jack Hills zircons".
584:
at the base of the continental crust. Tonalitic composition rock crystallised first before the magma differentiated to granodioritic and later granitic composition at a shallow depth. Some island arc plutonic roots also have TTG rocks, e.g.
1070:
Martin, H.; Smithies, R.H.; Rapp, R.; Moyen, J.-F.; Champion, D. (January 2005). "An overview of adakite, tonalite–trondhjemite–granodiorite (TTG), and sanukitoid: relationships and some implications for crustal evolution".
238:
TTG rock sample (Tsawela gneiss) with foliation from the
Kaapvaal Craton, South Africa. The white minerals are plagioclase; the light grey ones are quartz; the dark, greenish ones are biotite and hornblende, which developed
317:
Archean TTGs are classified into three groups based on geochemical features, that are low, medium, and high pressure TTGs, although the three groups form a continuous series. The low pressure group shows relatively low
502:
extraction. Those delaminated meta-mafic bodies then sink down, melt, and interact with surrounding mantle to generate TTGs. Such delamination induced TTG generation process is petrogenetically similar to that of
34:
Archean TTG rock outcrop in
Kongling Complex, South China Craton. The white TTG rock body is intruded by dark mafic dikes, as well as light color felsic dikes. The mafic minerals in the TTG rock body, possibly
1051:
Drummond, M. S. and Defant, M. J., 1990, A model for tronhjemite-tonalite-dacite genesis and crustal growth via slab melting: Archean to modern comparisons: J. Geophysical Res., v. 95, p. 21,503 - 21,521.
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consists of 7–16% gabbro and diorite, 48–60% tonalite (including trondhjemite), and 20–30% granodiorite, with 1–4% granite. These TTG rocks in continental arc batholiths may partially originate from the
361:
and possibly amphibole or garnet. The high pressure group shows the opposite geochemical features, corresponding to melting at a pressure over 20 kbar, with the source rock containing garnet and
378:
of the
Archean TTG rock generation is currently not well understood. Competing hypotheses include subduction related generation involving plate tectonics and other non-plate tectonic models.
1000:
Moyen, Jean-François (April 2011). "The composite
Archaean grey gneisses: Petrological significance, and evidence for a non-unique tectonic setting for Archaean crustal growth".
419:
adakites (LSA). It was then noted that the
Archean TTGs were geochemically almost identical to high silica adakites (HSA), but slightly different from low silica adakites (LSA).
1224:
Johnson, Tim E.; Brown, Michael; Gardiner, Nicholas J.; Kirkland, Christopher L.; Smithies, R. Hugh (2017-02-27). "Earth's first stable continents did not form by subduction".
864:
Johnson, Tim E.; Brown, Michael; Kaus, Boris J. P.; VanTongeren, Jill A. (2013-12-01). "Delamination and recycling of
Archaean crust caused by gravitational instabilities".
1369:
Smithies, R.H.; Champion, D.C.; Van Kranendonk, M.J. (2009-05-15). "Formation of Paleoarchean continental crust through infracrustal melting of enriched basalt".
920:
Foley, Stephen; Tiepolo, Massimo; Vannucci, Riccardo (June 2002). "Growth of early continental crust controlled by melting of amphibolite in subduction zones".
1471:
Bédard, Jean H. (March 2006). "A catalytic delamination-driven model for coupled genesis of Archaean crust and sub-continental lithospheric mantle".
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299:
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melt at depth. However, the large volume of such TTG rocks infer their major generation mechanism is by the crustal thickening induced
440:
by pointing out the absence of major plate tectonic indicators during most of the Archean Eon. It is also noted that Archean TTGs were
1042:
Martin, H., 1986, Effect of steeper Archean geothermal gradient on geochemistry of subduction zone-magmas: Geology, v. 14, p. 753-756.
1117:
Defant, Marc J.; Drummond, Mark S. (October 1990). "Derivation of some modern arc magmas by melting of young subducted lithosphere".
744:
122:
minerals in TTG rocks is usually larger than 20% but less than 60%. In tonalite and trondhjemite, more than 90% of the
1181:
Clemens, J.D; Droop, G.T.R (October 1998). "Fluids, P–T paths and the fates of anatectic melts in the Earth's crust".
391:
continental crust; dark green: oceanic crust; red: TTG melts; orange: mantle. Modified from Moyen & Martin, 2012.
821:
Martin, H. (1986-09-01). "Effect of steeper Archean geothermal gradient on geochemistry of subduction-zone magmas".
490:
group, are between 12 and 20 °C/km. Other than hot subduction, such geotherms may also be possible during the
460:
The delamination and underplating induced Archean TTG generation models. In the upper figure, heavier mafic crust
560:
674:
Hernández-Montenegro, Juan David; Palin, Richard M.; Zuluaga, Carlos A.; Hernández-Uribe, David (4 March 2021).
465:
the mafic crust due to the plume heating generates TTG magma intrusions. Modified from Moyen & Martin, 2012.
1167:
Condie, K. C., & Kröner, A. (2008). When did plate tectonics begin? Evidence from the geologic record. In
842:
310:
Confirmed by geochemical modelling, TTG type magma can be generated through partial melting of hydrated meta-
602:
565:
1330:
Moyen, Jean-François; Laurent, Oscar (March 2018). "Archaean tectonic systems: A view from igneous rocks".
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437:
275:
67:
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Kröner, A.; Layer, P. W. (1992-06-05). "Crust Formation and Plate Motion in the Early Archean".
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279:
223:
577:
520:
499:
295:
278:(LREE) content yet low heavy rare earth element (HREE) content. However, they do not show
215:
106:(although of a small proportion), while Archean TTG rocks are major components of Archean
83:
1619:
1549:
1484:
1425:
1339:
1237:
1194:
1130:
1084:
1013:
933:
877:
834:
791:
676:"Archean continental crust formed by magma hybridization and voluminous partial melting"
736:
704:
675:
448:
in nature, thus their magma should differ in composition, especially in water content.
445:
441:
256:
51:
1202:
1643:
1573:
778:
Moyen, Jean-François; Martin, Hervé (September 2012). "Forty years of TTG research".
727:
Barker, F. (1979), "Trondhjemite: Definition, Environment and Hypotheses of Origin",
614:
597:
Tonalites (including trondhjemites) can be found above the layered gabbro section in
203:
171:
1457:
1154:
965:
601:, below or within sheeted dykes. They are often irregular in shape and produced by
581:
573:
516:
482:
187:
135:
131:
95:
87:
79:
75:
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127:
1390:
1305:
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556:
504:
211:
159:
143:
39:, were weathered, which introduced a brownish coating on the TTG rock surface.
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291:
252:
155:
103:
99:
55:
1449:
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957:
713:
498:
or an increase in density of the mafic crustal base due to metamorphism or
411:
contents), adakites can be further divided into two groups, namely high SiO
386:
274:
In terms of trace element characteristics, Archean TTGs exhibit high light
428:
408:
358:
346:
139:
123:
71:
63:
1628:
1603:
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540:
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91:
36:
1171:(Vol. 440, pp. 281-294). Geological Society of America Special Papers.
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885:
586:
552:
536:
507:, both of which involves deep burial of mafic rocks into the mantle.
404:
362:
287:
263:
244:
175:
167:
119:
107:
59:
731:, Developments in Petrology, vol. 6, Elsevier, pp. 1–12,
30:
481:
around 20–30 °C/km, which are comparable to those during the
311:
207:
456:
436:
at a later stage. However, other authors doubt the existence of
354:
234:
494:
of mafic crustal base. The delamination may be attributed to
1536:
Pitcher, W. S. (March 1978). "The anatomy of a batholith".
843:
10.1130/0091-7613(1986)14<753:eosagg>2.0.co;2
474:, which corresponding to different geodynamic settings.
357:
with the source rock mineral assembly of plagioclase,
243:
Archean TTG rocks appear to be strongly deformed grey
535:
Continental arc TTG rocks are often associated with
353:
content, corresponding to melting under 10–12
294:, but no plagioclase in the residual phase during
1604:"Essentials of igneous and metamorphic petrology"
142:, with most of the plagioclase in the rock being
27:Intrusive rocks with typical granitic composition
661:Principles of igneous and metamorphic petrology
395:Geochemical similarity shared between TTGs and
1169:When did plate tectonics begin on planet Earth
1112:
1110:
1065:
1063:
1061:
1059:
1057:
1325:
1323:
995:
515:Post Archean TTG rocks are commonly found in
259:. TTG rock is one of the major rock types in
94:(after 2.5 Ga) TTG rocks are present in
8:
1516:
1514:
1512:
1510:
993:
991:
989:
987:
985:
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981:
979:
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527:also contains a small amount of TTG rocks.
286:. These features indicate the presence of
226:added together commonly smaller than 5%).
210:element content (the weight percentage of
1627:
893:
729:Trondhjemites, Dacites, and Related Rocks
703:
693:
66:) but containing only a small portion of
477:The low pressure group has formed along
455:
385:
247:, showing banding, lineation, and other
233:
29:
636:
182:) content (commonly over 70 percent SiO
366:most abundant among the three groups.
134:, this number is between 65% and 90%.
547:, which forms a plutonic sequence in
7:
470:therefore have experienced distinct
1602:Frost, B. R.; Frost, C. D. (2013).
1371:Earth and Planetary Science Letters
1286:Earth and Planetary Science Letters
737:10.1016/b978-0-444-41765-7.50006-x
44:Tonalite–trondhjemite–granodiorite
25:
18:Tonalite-Trondhjemite-Granodiorite
1589:Igneous and metamorphic petrology
1538:Journal of the Geological Society
1523:Igneous and metamorphic petrology
551:. They are formed by hundred of
1473:Geochimica et Cosmochimica Acta
589:, but they are rarely exposed.
298:or precipitation phase during
174:, TTG rocks often have a high
1:
1434:10.1126/science.256.5062.1405
1203:10.1016/s0024-4937(98)00020-6
1348:10.1016/j.lithos.2017.11.038
1093:10.1016/j.lithos.2004.04.048
1022:10.1016/j.lithos.2010.09.015
800:10.1016/j.lithos.2012.06.010
572:) of the subduction induced
444:while the modern adakite is
337:content and relatively high
306:Formation and classification
118:The quartz percentage among
452:Non-plate tectonic settings
202:O ratio) compared to other
1666:
1391:10.1016/j.epsl.2009.03.003
1306:10.1016/j.epsl.2010.04.043
695:10.1038/s41598-021-84300-y
570:fractional crystallisation
415:adakites (HSA) and low SiO
300:fractional crystallization
1493:10.1016/j.gca.2005.11.008
561:Coastal Batholith of Peru
555:that directly related to
531:Continental arc TTG rocks
1591:. John Wiley & Sons.
1558:10.1144/gsjgs.135.2.0157
82:often occur together in
1587:Best, Myron G. (2013).
1525:. Blackwell Publishers.
1383:2009E&PSL.281..298S
1298:2010E&PSL.296...45K
580:of the former gabbroic
659:J. D., Winter (2013).
593:TTG rocks in ophiolite
511:Post Archean TTG rocks
466:
392:
382:Plate tectonic setting
249:metamorphic structures
240:
194:O) content (with low K
40:
1608:American Mineralogist
603:magma differentiation
566:magma differentiation
459:
389:
237:
150:of TTG rocks include
138:is a special kind of
86:, indicating similar
33:
1521:M. G., Best (2003).
663:. Pearson Education.
472:geothermal gradients
270:Geochemical features
1629:10.2138/am-2015-657
1620:2015AmMin.100.1655K
1550:1978JGSoc.135..157P
1485:2006GeCoA..70.1188B
1426:1992Sci...256.1405K
1420:(5062): 1405–1411.
1340:2018Litho.302...99M
1334:. 302–303: 99–125.
1246:10.1038/nature21383
1238:2017Natur.543..239J
1195:1998Litho..44...21C
1131:1990Natur.347..662D
1085:2005Litho..79....1M
1014:2011Litho.123...21M
942:10.1038/nature00799
934:2002Natur.417..837F
878:2014NatGe...7...47J
835:1986Geo....14..753M
792:2012Litho.148..312M
370:Geodynamic settings
895:20.500.11937/31170
681:Scientific Reports
620:Archean subduction
496:mantle downwelling
467:
438:Archean subduction
393:
376:geodynamic setting
276:rare earth element
241:
148:accessory minerals
84:geological records
68:potassium feldspar
41:
1232:(7644): 239–242.
1125:(6294): 662–665.
928:(6891): 837–840.
866:Nature Geoscience
625:Eoarchean geology
230:Archean TTG rocks
220:manganese dioxide
16:(Redirected from
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1292:(1–2): 45–56.
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1008:(1–4): 21–36.
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1079:(1–2): 1–24.
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615:Acasta Gneiss
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172:Geochemically
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146:. The major
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57:
54:with typical
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1611:
1607:
1597:
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1541:
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1476:
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1417:
1413:
1407:
1374:
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1364:
1331:
1289:
1285:
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1229:
1225:
1219:
1186:
1182:
1176:
1168:
1163:
1122:
1118:
1076:
1072:
1047:
1038:
1005:
1001:
925:
921:
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869:
865:
859:
826:
822:
816:
783:
779:
728:
722:
685:
679:
669:
660:
596:
574:mantle wedge
534:
517:arc settings
514:
500:partial melt
492:delamination
488:
486:generation.
483:underplating
476:
468:
421:
394:
373:
316:
309:
284:Sr anomalies
273:
242:
188:sodium oxide
136:Trondhjemite
132:granodiorite
117:
88:petrogenetic
80:granodiorite
76:trondhjemite
50:) rocks are
47:
43:
42:
1614:(7): 1655.
786:: 312–336.
688:(1): 5263.
462:delaminates
425:Adak Island
312:mafic rocks
130:, while in
128:plagioclase
114:Composition
829:(9): 753.
631:References
599:ophiolites
582:underplate
557:subduction
549:batholiths
505:subduction
434:collisions
253:protoliths
239:foliation.
212:iron oxide
206:, and low
160:hornblende
156:amphiboles
144:oligoclase
104:ophiolites
100:batholiths
1574:130036558
1566:0016-7649
1501:0016-7037
1442:0036-8075
1399:0012-821X
1356:0024-4937
1314:0012-821X
1254:0028-0836
1211:0024-4937
1147:0028-0836
1101:0024-4937
1030:0024-4937
950:0028-0836
904:1752-0894
851:0091-7613
808:0024-4937
525:Ophiolite
479:geotherms
446:extrusive
292:amphibole
124:feldspars
98:-related
1644:Category
1458:35201760
1450:17791608
1262:28241147
958:12075348
714:33664326
609:See also
429:Mindanao
397:adakites
359:pyroxene
251:, whose
186:), high
140:tonalite
72:Tonalite
64:feldspar
56:granitic
1616:Bibcode
1546:Bibcode
1481:Bibcode
1422:Bibcode
1414:Science
1379:Bibcode
1336:Bibcode
1294:Bibcode
1234:Bibcode
1191:Bibcode
1155:4267494
1127:Bibcode
1081:Bibcode
1010:Bibcode
966:4394308
930:Bibcode
874:Bibcode
831:Bibcode
823:Geology
788:Bibcode
705:7933273
553:plutons
545:granite
541:diorite
264:cratons
261:Archean
164:epidote
152:biotite
108:cratons
92:Archean
37:biotite
1572:
1564:
1499:
1456:
1448:
1440:
1397:
1354:
1332:Lithos
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1270:281446
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1252:
1226:Nature
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1099:
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1002:Lithos
964:
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902:
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780:Lithos
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587:Tobago
568:(i.e.
543:, and
537:gabbro
407:, and
363:rutile
349:, and
288:garnet
245:gneiss
222:, and
176:silica
168:zircon
166:, and
158:(e.g.
120:felsic
78:, and
60:quartz
1570:S2CID
1454:S2CID
1266:S2CID
1151:S2CID
962:S2CID
255:were
1562:ISSN
1497:ISSN
1446:PMID
1438:ISSN
1395:ISSN
1352:ISSN
1310:ISSN
1258:PMID
1250:ISSN
1207:ISSN
1143:ISSN
1097:ISSN
1026:ISSN
954:PMID
946:ISSN
900:ISSN
847:ISSN
804:ISSN
741:ISBN
710:PMID
374:The
355:kbar
329:, Na
290:and
282:and
198:O/Na
178:(SiO
126:are
62:and
1624:doi
1612:100
1554:doi
1542:135
1489:doi
1430:doi
1418:256
1387:doi
1375:281
1344:doi
1302:doi
1290:296
1242:doi
1230:543
1199:doi
1135:doi
1123:347
1089:doi
1018:doi
1006:123
938:doi
926:417
890:hdl
882:doi
839:doi
796:doi
784:148
733:doi
700:PMC
690:doi
333:O,
190:(Na
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96:arc
48:TTG
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409:Cr
405:Ni
403:,
401:Mg
351:Nb
347:Ta
345:,
343:Yb
341:,
335:Sr
320:Al
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280:Eu
266:.
218:,
214:,
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