Jump to content

Dharwar Craton

From Wikipedia, the free encyclopedia

This is an old revision of this page, as edited by Skhlaw (talk | contribs) at 03:42, 13 November 2021 (→‎Archean crust accretions). The present address (URL) is a permanent link to this revision, which may differ significantly from the current revision.

The location map of the Dharwar Craton. The shaded area represents the Dharwar Craton. Generated from GeoMapApp (Ryan et al., 2009).[1]

The Dharwar Craton is an Archean continental crust craton formed between 3.6-2.5 billion years ago (Ga), which is located in southern India.

Studies in the 2010s suggest that the craton can be separated into three crustal blocks since they show different accretionary history (i.e. the history of block collisions) and thermal records. The craton includes the western, central and eastern blocks and the three blocks are divided by several shear zones.[2][3]

The lithologies of the Dharwar Craton are mainly TTG (Tonalite-trondhjemite-granodiorite) gneisses, volcanic-sedimentary greenstone sequences and calc-alkaline granitoids.[1] The western Dharwar Craton contains the oldest basement rocks, with greenstone sequences between 3.0-3.4 Ga, whereas the central block of the craton mainly contains migmatitic TTG gneisses, and the eastern block contains 2.7 Ga greenstone belts and calc-alkaline plutons.[4]

The formation of the basement rock of the Dharwar Craton was created by the intraplate hotspots (i.e. volcanic activities caused by mantle plume from core-mantle boundary) and two-stage melting of oceanic crust. The continuous melting of the oceanic arc crust and the mantle upwelling generated the TTG and sanukitoid plutons over the Dharwar Craton.[5][6]

Overview of the regional geology

Simplified geological map of the Dharwar Craton, which shows the western, central and eastern blocks. Modified from Jayananda et al., (2018).[2]

The Dharwar Craton is surrounded by the Arabian Sea in the west, the Deccan Trap in the north, the Eastern Ghats Mobile Belt in the east and the Southern Granulite Belt in the south.[7]

The Dharwar Craton is traditionally divided into two main blocks including the western Dharwar Craton and the eastern Dharwar Craton. The mylonite zone at the eastern boundary of the Chitradurga greenstone belt was considered as the boundary between the two main blocks.[8] The western Dharwar Craton is older with a cratonisation age around 3.0 Ga while the eastern Dharwar Craton is younger with the cratonisation age around 2.5 Ga.[4] The boundary between the two blocks (the eastern boundary of the Chitradurga greenstone belt) is a steep shear zone with some mylonitised granite and volcanic rocks.[7] The Chitradurga greenstone belt is an elongated linear supracrustal belt which is 400 km long from North to South.[9]

The western Dharwar Craton is dominated by 2.9 Ga to 3.35 Ga TTG gneiss. From Paleoarchean to Mesoarchean, the western Dharwar Craton are with groups of rocks including the 3.0 Ga to 3.3 Ga Sargur Group and the 2.6 to 2.9 Ga Dharwar Supergroup. Those two groups are separated by an unconformity. The Sargur Group includes quartzite, pelite, calc-silicate, basalt, komatiite, banded iron formation (BIF) and layered mafic and serpentinized or chromite-bearing ultramafics. The Dharwar Supergroup can be divided into two groups as well, including the Bababudan group with an older age (oligomitic conglomerate, quartzite, basalt and BIF) and the Chitradurga group with a younger age (polymictic conglomerate, quartzite, greywacke, pelite, basalt and BIF).[4][7]

Since the eastern Dharwar Craton cratonised later than the western Dharwar Craton, the eastern Dharwar Craton is dominated by 2.7 Ga Kolar-type greenstone belts and 2.7–2.5 Ga calc-alkaline felsic plutonic and volcanic rocks.[10] The older Kolar-type greenstone mainly contains greenschist to amphibolite facies metabasalts, as well as some subordinate felsic volcanic rocks and metasediments,[11] while the younger granitoids include TTG gneisses, high-magnesium sanukitoids and potassium-rich leucogranites.[10]

Simplified cross-section of the Dharwar Craton from SW to NE, showing the shear zone and the granitic intrusions. Modified from Jayananda et al., (2018).[2]

Lithologies

TTG gneisses

TTG rocks are intrusive rocks with a granitic composition of quartz and feldspar but contain less potassium feldspar. In Archean craton, TTG rocks are usually present in batholiths formed by plate subduction and melting. There are two kinds of gneisses can be found on the Dharwar Craton, which includes the typical TTG-type gneisses and the dark grey TTG banded gneisses:[12]

Blocks Main TTG type Associated group Characteristics
western block typical TTG gneisses[6] Sargur Group[6]
  • some of the TTG are with minor granitic intrusions[6]
central block transitional TTG (mixture of the typical TTG and dark grey banded gneisses)[6] Kolar Group[12]
  • the TTG shows foliation
  • the abundance of the weakly foliated TTG gneisses decreases gradually from the west to the east
  • the abundance of the dark grey banded gneisses with younger age increases gradually from the west to the east [12]
eastern block banded gneisses[6] Kolar Group[2]
  • it contains less TTG than those of the western and central blocks[2]

Volcanic-sedimentary greenstone sequences

Greenstone is metamorphosed mafic to ultramafic volcanic rock that formed in volcanic eruptions in the early stage of Earth formation. The volcanic-sedimentary greenstone sequence occupies the majority of the Archean crustal record, which is about 30%. The western block comprises the greenstone sequences with adequate sediments, while the central block and the eastern block comprise the greenstone sequences with adequate volcanic rocks but minor sediments.[2]

Blocks Composition of the volcanic greenstone Associated group(s) Characteristics
western block ultramafic komatiite with interlayered sediments[13] Sargur group and Dharwar Supragroup
  • rocks were formed in calm and shallow water environments[13]
  • basaltic flows, conglomerate and some felsic volcanics can be found in the greenstone of the Dharwar Supragroup[14]
central block basalts with minor ultramafic komatiite[15] Kolar group
  • the volcanic rocks comprised with minor sediment and some felsic rocks[15]
eastern block basalts with minor ultramafic komatiite[16] Kolar group
  • basalts are with high magnesium
  • the greenstone contains interlayered sediments like carbonate[16]

Sanukitoids (Calc-alkaline granitoids)

Sanukitoids are granitoids with high-magnesium compostion that are commonly formed by plate collision events in Archean. In the Dharwar Craton, there is no sanukitoid record in the western block. However, there are a lot of granitoid intrusions in the central block, which become less in the eastern block.[2]

Blocks Main composition Rock units intruded by granitoids Characteristics
Central block monzogranite and monzodiorite[2] TTG gneisses and volcanic greenstone[17]
  • they are comprised with pink phenocrysts.[2]
  • granitoid intrusions form plutons over the block that are north-south trending
  • the largest pluton in the central block is the Closepet Batholith.[1]
Eastern block
  • The granitoids are associated with the diatexites (i.e. the granite was mixed with older rocks due to partial melting), indicating there was intense metamorphism which causes recrystallization of minerals[18]

Anatectic granites

Anatectic granite is a kind of rock formed by the partial melting of the pre-existing crustal rock, which is relatively younger than the TTG and greenstone in the Dharwar Craton. The granites usually cut across the older rocks.

Blcoks Main composition Rock units intruded by granites Characteristics
western block granite with high-potassium content[2] TTG gneisses and volcanic greenstone
  • they occupy the ductile shear zone over the TTG gneisses, forming cross-cutting dykes and veins[2]
central block
eastern block
  • they occupy a large area in the eastern block[2]
  • in the southern part of the block, many veins and dykes cut across the gneisses
  • some mafic to ultramafic xenoliths can be found[17]

Metamorphic record

Blocks P-T conditions Metamorphic facies Record
Western block Progressive increase from the N to the S From the greenschist facies in the N to the hornblende-granulite facies to the S[2]
  • The mineral assemblages of garnet-chloritoid, garnet-staurolite and kyanite-garnet indicate the 6–8 Kb metamorphic pressure and 500–675 °C temperature range in the Holenarsipur greenstone belt[19]
  • The mineral assemblages of garnet-hornblende-clinopyroxene in the metamorphic rocks indicate the upper amphibolite to granulite facies with a temperature range between 650 and 750 °C in the Gundlupet region[2]
Central block Progressive increase from the N to the S From the greenschist facies in the Sandur greenstone belt in the N to the granulite facies in the Kabbaldurga to the S[20]
  • The granulite facies mineral assemblages (sillimanite-spinel-quartz) in the pelite indicate the ultrahigh temperature conditions in the Pavagada region, the central part of the central block [21]
  • The mineral assemblages in the metamorphic rocks indicate the amphibolite to granulite facies with the P-T conditions from 600–775 °C and 5–9 Kb in the B.R Hills region[2]
Eastern block Poorly understood Poorly understood
  • The dykes indicate the amphibolite facies in the northernmost part of the eastern block, around the Hutti greenstone belt[22]
  • The amphibolite-granulite facies transition indicates a progressive increase in temperature condition from 650 to 800 °C in the Krishnagiri-Dharmapuri region, the southern part of the eastern block[23]

Archean crust accretions

For finding when the Archean crust accretions happened, the parent-daughter isotopes dating, like uranium-lead (U-Pb) decay could be used to find out the ages of the events.

According to the zircon U-Pb ages of the TTG gneisses from the Dharwar Craton, there were five major accretion events leading to the formation of the Archean felsic continental crust. The events occurred with the ranges of age 3450–3300, 3230–3200, 3150–3000, 2700–2600 and 2560–2520 million years ago (Ma).[2]

The western block records the two earliest crust accretion events, that happened in 3450 Ma and 3230 Ma. The rates of the continental growth of the two events are fast since the events led to the widespread of greenstone volcanism.[4]

The central block records four major accretion events, that occurred in 3375 Ma, 3150 Ma, 2700 Ma and 2560 Ma. The isotopic data suggests that the scale of the continental growth due to felsic crust accretion was large during 2700–2600 Ma and 2560–2520 Ma, leading to the large scale bimodal greenstone volcanism at that time. [15]

The eastern block records the two latest major accretion events occurring in 2700 Ma and 2560 Ma with massive continental growth.[24]

Crustal reworking events

The crustal reworking events happened in the time range of 3100–3000 Ma.[6] All three crustal blocks record the crustal reworking events in 2520 Ma due to the final assembly of the Superia supercontinent. [3]

For the western block, there are two reworking events. The first event happened in 3100–3000 Ma accounting to the high-grade metamorphism and emplacement of high potassium granite.[6] The second reworking event led to the intrusions of 2640–2600 Ma high-K plutons of Arsikere-Banavara and Chitradurga granites.[25]

For the central block, the earliest reworking event occurred in 3140 Ma due to the TTG accretion event between 3230–3140 Ma. The second high-temperature reworking event in the central of the eastern block happening in 2640–2620 Ma is related to the greenstone volcanism of the TTG accretion event in 2700 Ma.[21]

Formation and evolution

Intraplate hotspot model

The annotated diagram of the intraplate hotspot model before 3400 Ma, forming the oceanic plateaus. Modified from Jayananda et al, (2018).[2]

Before 3400 Ma, the magma upwelling from the mantle led to the intraplate hotspot setting. the upwelling magma formed the oceanic plateaus with komatiites and komatiitic basalts in the oceanic crust.[5][26]

Two-stage melting of oceanic crust

The evolutionary diagram of the two-stage melting of the oceanic crust during 3350-3100 Ma, forming the TTG plutons. Modified from Jayananda et al, (2018) and Tushipokla et al, (2013).[2][5]

After the mantle plume hotspots were formed, the tectonic setting was followed by the two-stage melting, which include the melting of the subducted oceanic crust and the melting of the thickened oceanic arc crust.[27]

In 3350 Ma, due to the ridge push from the oceanic spreading centres (mid-oceanic ridges), some oceanic crust subducted under the mantle. The low angle subduction of the crust at shallow levels (40–60 km) led to the melting of the subducted crust and formed magma that rose to the oceanic crust and formed oceanic island arc crust.[2]

During 3350–3270 Ma, the mafic to ultramafic hydrous melt formed by the slab melting melted the base of the thickened oceanic arc crust, which formed the TTG melt, as well as magmatic protoliths of TTGs in the oceanic arc crust.[2][5]

During 3230–3100 Ma, the continuous collision of the oceanic island arc crust, newly formed TTG and the oceanic plateaus caused the melting of the juvenile crust in the oceanic island arc, which generated trondhjemite plutons in 3200 Ma. The trondhjemite emplacement generated heat and fluid that led to the low degree melting that made the low-density TTG crust rose while the high-density greenstone volcanics sank, which developed the dome-keel structures between the TTG and greenstone.[28]

Transitional TTGs in the central and eastern blocks

The transitional TTGs in the central and eastern blocks during 2700–2600 Ma are relatively enriched in incompatible elements like LREE, K, Ba, Sr etc., compared to the TTGs with older age. The enrichment of the incompatible elements could be account for the high-angle subduction and the chemical interaction between the mantle wedge and the melt from the subducted crust.[29]

During the 2700 Ma, the central and eastern block of the Dharwar Craton had developed into microcontinents. The weathering and erosion of the microcontinents led to a large amount of detrital input to the ocean floor and subduction zone. Therefore, the subducted slab with a large amount of sediment brought incompatible elements into the mantle due to a high-angle subduction. The mantle wedge interacted with the slab, leading to the partial enrichment of the incompatible elements in the wedge and generated mafic to intermediate magma. The mafic magma rose and accumulated under the oceanic arc crust, leading to the partial melting of the thickened, incompatible element enriched arc crust and their magma mixed to form the transitional TTGs during 2700–2600 Ma.[30]

Shifting from oceanic crust melting to mantle melting

After the transitional TTG accretion, the inflexible subducted oceanic crust broke and fell into the asthenosphere, leading to the mantle upwelling under the pre-existing crust. The upwelling mantle rock rose to the shallow depth and melted the upper mantle to generate intermediate to mafic magma. Then, the magma intruded into the middle part of the crust. It underwent differentiation in magma chambers. The heat from the magma transferred into the surrounding rock leading to the partial melting of gneisses and the formation of calc-alkaline granitoids.[31]

Sanukitoid magmatism

The model showing the transitional TTG accretion, shifting from the melting of oceanic crust to the melting of the mantle, as well as the sanukitoid magmatism during 2740-2500 Ma. Modified from Jayananda et al, (2013, 2018).[2][1]

Sanukitoids were formed during the Neoarchean magmatic accretion events, that are originated from the mantle with low silicon dioxide and high magnesium, but some of them are with incompatible elements like LREE, K and Ba and lower magnesium.[10] The sanukitoid magma could be generated by either plate subduction or plume setting.

The sanukitoids created by subduction might lead to the metasomatism of the mantle wedge and the melting of the metasomatized mantle wedge. The peridotitic mantle wedge was mixed with intermediate to felsic melts.[32] This can be explained by the mixing of the previous TTG melts.[33] The sanukitoids created by plume setting would lead to the sanukitoid intrusions with high magnesium content and low silicon dioxide.

The sanukitoid magmatism is not related to the TTG accretion events during 3450–3000 Ma. The magmatism was followed by the transitional TTG accretion event in 2600 Ma (50–100 Ma after the transitional TTG accretion) and only occurred in the central and eastern blocks. Since the sanukitoids are enriched in both incompatible and compatible elements, while the TTGs are not, it indicates the appearance of the sanukitoid magmatism shows the tectonic change from oceanic crust melting to mantle melting during 2600–2500 Ma.[2]

Closure of subduction zones

During 2560–2500 Ma, the three blocks joined together to form the Dharwar Craton and all the subduction zones closed, followed by the regional metamorphism due to heat release from the mantle during 2535–2500 Ma. The final cratonisation finished in 2400 Ma through slow cooling.[34]

Implication for global crust history

Possible relationships with the Dharwar Craton
Bundelkhand Craton
  • They have similar lithologies with the typical units like TTG gneisses, volcanic-sedimentary greenstone sequences and calc-alkaline granitoids.
  • There were 3 major crust creating events during 3327–3270 Ma, 2700 Ma and 2578–2544 Ma in the Bundelkhand Craton, which occurred at the same time as the TTG accretion event and the sanukitoid intrusions of the Dharwar Craton.[35]
North China Craton
  • The accretion events with the continental growth and assembly of micro-blocks were recorded during 2720–2600 Ma, 2550–2500 Ma from the North China Craton.[36] The North China Craton shows a similar late Neoarchean crustal history of magmatism, crustal reworking and high rates of continental growth with that of the central and eastern blocks of the Dharwar Craton.[36]
  • The magmatic, sedimentological and metamorphic history of the North China Craton is similar to those of the peninsular India so they may be the same continent from the Mesoarchaean to the Palaeoproterozoic.[37]
Kaapvaal Craton
  • The zircon ages of the TTG gneisses and granitoids from the Kaapvaal Craton are the same as the 3400–3200 Ma TTG gneisses and 2650–2620 Ma potassic granites from the western Dharwar Craton.[12]
  • The sanukitoids from the central part of the Limpopo belt in the Kaapvaal Craton showed the ages of 2617–2590 Ma. Those sanukitoids share the same ages as the 2600 Ma transitional TTGs, as well as the early formation of the sanukitoids in the central and eastern block of the Dharwar craton.[38]
Pilbara Craton
  • The Pilbara Craton recorded the accretion event with a large number of gneisses and granitoids in 3500–3220 Ma, which occurred at a similar time to the 3450–3200 Ma TTG accretion event in the western Dharwar Craton.[3]
  • The detrital zircons in the TTG gneisses of the western Dharwar Craton showed the ages of 3700–3800 Ma. The zircons might come from the old crust of the Pilbara Craton.[4]
Yilgarn Craton
  • The 2700–2630 Ma gneisses and granitoids are abundant in the Yilgarn Craton. The ages corresponded with the transitional TTGs accretion event in the central and eastern blocks of the Dharwar craton.[39]
Tanzania Craton
  • The basement gneisses in the Tanzania Craton indicated the U-Pb ages of 3234-3140 Ma, which corresponded to the ages TTG gneisses and detrital zircons in the western Dharwar Craton.[6]
  • The granitoids and greenstone sequences are with the ages of 2720-2640 Ma and 2815 Ma respectively. They share the same ages with the transitional TTGs and the greenstone sequences in the central and the eastern blocks of the Dharwar Craton.[40]
Antongil Craton
  • The TTG gneisses in the Antongil Craton formed during 3320-3231 Ma, and 3187-3154 Ma.[41] The zircon ages indicate the crust forming events in the Antongil Craton occurred at the same time with the crust building and reworking events in the western Dharwar Craton.[6]

See also

References

  1. ^ a b c d Jayananda, M.; Peucat, J.-J.; Chardon, D.; Rao, B. Krishna; Fanning, C.M.; Corfu, F. (April 2013). "Neoarchean greenstone volcanism and continental growth, Dharwar craton, southern India: Constraints from SIMS U–Pb zircon geochronology and Nd isotopes". Precambrian Research. 227: 55–76. doi:10.1016/j.precamres.2012.05.002.
  2. ^ a b c d e f g h i j k l m n o p q r s t u v M., Jayananda; M., Santosh; K.R., Aadhiseshan (June 2018). "Formation of Archean (3600–2500 Ma) continental crust in the Dharwar Craton, southern India". Earth-Science Reviews. 181: 12–42. doi:10.1016/j.earscirev.2018.03.013.
  3. ^ a b c Peucat, Jean-Jacques; Jayananda, Mudlappa; Chardon, Dominique; Capdevila, Ramon; Fanning, C. Mark; Paquette, Jean-Louis (April 2013). "The lower crust of the Dharwar Craton, Southern India: Patchwork of Archean granulitic domains". Precambrian Research. 227: 4–28. doi:10.1016/j.precamres.2012.06.009.
  4. ^ a b c d e Lancaster, Penelope J.; Dey, Sukanta; Storey, Craig D.; Mitra, Anirban; Bhunia, Rakesh K. (December 2015). "Contrasting crustal evolution processes in the Dharwar craton: Insights from detrital zircon U–Pb and Hf isotopes". Gondwana Research. 28 (4): 1361–1372. doi:10.1016/j.gr.2014.10.010.
  5. ^ a b c d Tushipokla, M. Jayananda. “Geochemical Constraints on Komatiite Volcanism from Sargur Group Nagamangala Greenstone Belt, Western Dharwar Craton, Southern India： Implications for Mesoarchean Mantle Evolution and Continental Growth.” Di Xue Qian Yuan., vol. 4, no. 3, 2013, pp. 321–340.
  6. ^ a b c d e f g h i j Jayananda, M.; Chardon, D.; Peucat, J.-J.; Fanning, C.M. (October 2015). "Paleo- to Mesoarchean TTG accretion and continental growth in the western Dharwar craton, Southern India: Constraints from SHRIMP U–Pb zircon geochronology, whole-rock geochemistry and Nd–Sr isotopes". Precambrian Research. 268: 295–322. doi:10.1016/j.precamres.2015.07.015.
  7. ^ a b c Gao, Pin; Santosh, M. (September 2020). "Mesoarchean accretionary mélange and tectonic erosion in the Archean Dharwar Craton, southern India: Plate tectonics in the early Earth". Gondwana Research. 85: 291–305. doi:10.1016/j.gr.2020.05.004.
  8. ^ Ramakrishnan, M.; Nath, J. Swami (1981). Early Precambrian Supracrustals of Southern Karnataka. Geological Survey of India. p. 350.
  9. ^ Hokada, T., Horie, K., Satish-Kumar, M., Ueno, Y., Nasheeth, A., Mishima, K., & Shiraishi, K. (2013). An appraisal of Archaean supracrustal sequences in Chitradurga Schist Belt, Western Dharwar Craton, Southern India. Precambrian Research, 227, 99-119.
  10. ^ a b c Jayananda, M., Moyen, J.-F., Martin, H., Peucat, J.-J., Auvray, B., Mahabaleswar, B., 2000. Late Archaean (2550–2520 Ma) juvenile magmatism in the Eastern Dharwar craton, southern India: constraints from geochronology, Nd-Sr isotopes and whole rock geochemistry. Precambrian Research 99, 225–254. http://dx.doi.org/10.1016/S0301-9268(99)00063-7.
  11. ^ Balakrishnan, S., Hanson, G.N., Rajamani, V., 1991. Pb and Nd isotope constraints on the origin of high Mg and tholeiitic amphibolites, Kolar Schist Belt, South India. Contributions to Mineralogy and Petrology 107, 279–292. http://dx.doi.org/10.1007/BF00325099.
  12. ^ a b c d Chardon, D., Jayananda, M., Peucat, J.-J., 2011. Lateral contrictional flow of hot orogenic crust: insights from the Neoarchean of South India, geological and geophysical implications for orogenic plateaux. Geochem. Geophys. Geosyst. 12 http://dx.doi.org/10.1029/2010GC003398.(Q02005).
  13. ^ a b Maya, J.M., Bhutani, R., Balakrishnan, S., Rajee Sandhya, S., 2017. Petrogenesis of 3.15 Ga old banasandra komatiites from the Dharwar craton, India: implications for early mantle heterogeneity. Geosci. Front. 8, 467–481.
  14. ^ Kumar, A., Bhaskar Rao, Y.J., Sivaraman, T.V., Gopalan, K., 1996. Sm-Nd ages of Archaean metavolcanic of the Dharwar craton, South India. Precambrian Res. 80, 206–215.
  15. ^ a b c Balakrishnan, S., Rajamani, V., Hanson, G.N., 1999. U–Pb ages for zircon and titanite from the Ramagiri area, southern India: evidence for accretionary origin of the eastern Dharwar craton during the late Archaean. J. Geol. 107, 69–86. http://dx.doi.org/10.1086/314331.
  16. ^ a b Manikyamba, C., Kerrich, R., 2012. Eastern Dharwar craton, India: continental lithosphere growth by accretion of diverse plume and arc terranes. Geosci. Front. 3, 225–240.
  17. ^ a b Jayananda, M., Gireesh, R.V., Sekhamo, Kowete-u, Miyazaki, T., 2014. Coeval Felsic and Mafic Magmas in Neoarchean Calc-alkaline Magmatic Arcs, Dharwar Craton, Southern India: Field and Petrographic Evidence from Mafic to Hybrid Magmatic Enclaves and Synplutonic Mafic Dykes. J. Geol. Soc. India 84, 5–28.
  18. ^ Harish Kumar, S.B., Jayananda, M., Kano, T., Shadakshara Swamy, N., Mahabaleshwar, B., 2003. Late Archean juvenile accretion process in the Eastern Dharwar Craton; Kuppam–Karimangala area. Mem. Geol. Soc. India 50, 375–408.
  19. ^ Bouhallier, H., 1995. Evolution structurale et métamorphique de la croûte continentale archéenne (craton de Dharwar, Inde du sud). Mém. Doc.. 60 Géosciences-Rennes (277p).
  20. ^ Pichamuthu, C.S., 1965. Regional metamorphism and charnockitisation in Mysore state, India. Indian Mineralogist 6, 116–126.
  21. ^ a b Jayananda, M., Banerjee, M., Pant, N.C., Dasgupta, S., Kano, T., Mahesha, N., Mahableswar, B., 2011. 2.62Ga high-temperature metamorphism in the central part of the Eastern Dharwar Craton: implications for late Achaean tectonothermal history. Geol. J. 46. http://dx.doi.org/10.1002/gj.1308.
  22. ^ Prabhakar, B.C., Jayananda, M., Shareef, M., Kano, T., 2009. Synplutonic mafic injections into crystallizing granite pluton in the northern part of the eastern Dharwar craton: implications for the magma chamber processes. J. Geol. Soc. India 74, 171–188.
  23. ^ Hansen, E.C., Newton, R.C., Janardhan, A.S., Lindenberg, S., 1995. Differentiation of late Archean crust in the eastern Dharwar craton, Krishnagiri–Salem area, South India. J. Geol. 103, 629–651.
  24. ^ Balakrishnan, S., Hanson, G.N., Rajamani, V., 1990. Pb and Nd isotope constraints on the origin of high Mg and tholeiitic amphibolites, Kolar Schist belt South India. Contrib. Mineral. Petrol. 107, 272–292.
  25. ^ Jayananda, M., Chardon, D., Peucat, J.-J., Capdevila, R., 2006. 2.61 Ga potassic granites and crustal reworking in the western Dharwar craton, southern India: tectonic, geochronologic and geochemical constraints. Precambrian Res. 150, 1–26.
  26. ^ Jayananda, M., Kano, T., Peucat, J.-J., Channabasappa, S., 2008. 3.35 Ga komatiite volcanism in the western Dharwar craton: constraints from Nd isotopes and whole rock geochemistry. Precambrian Res. 162, 160–179. http://dx.doi.org/10.1016/j.precamres.2007.07.010 Elsevier.
  27. ^ Adams, J., Rushmer, T., O'Neil, J., Francis, D., 2012. Hadean greenstones from Nuvvuagittuq fold belt and origin of the early continental crust. Geology 40, 363–366.
  28. ^ Bouhallier, H., Choukroune, P., Ballèvre, M., 1993. Diapirism, bulk homogeneous shortening and transcurrent shearing in the Archaean Dharwar craton: the Holenarsipur area, southern India. Precambrian Res. 63, 43–58.
  29. ^ Martin, H., Moyen, J.-F., 2002. Secular changes in TTG composition as markers of the progressive cooling of the Earth. Geology 30, 319–322.
  30. ^ Foley, S., Tiepolo, M., Vannucci, R., 2002. Growth of early continental crust controlled by melting of amphibolite in subduction zones. Nature 417, 837–840.
  31. ^ Friend, C.R.L., 1984. The origins of the closepet granites and implications of crustal evolution in southern Karnataka. J. Geol. Soc. India 25, 73–84.
  32. ^ Kelemen, P.B., 1995. Genesis of high Mg andesites and the continental crust. Contrib. Mineral. Petrol. 120, 1–19.
  33. ^ Smithies, R.H., Champion, D.C., 2000. The Archaean high-Mg diorite suite: links to tonalite–trondhjemite–granodiorite magmatism and implications for early Archaean crustal growth. J. Petrol. 41, 1653–1671.
  34. ^ Peucat, J.-J., Jayananda, M., Chardon, D., Capdevila, R., Fanning Marc, C., Paquette, Jean-Louis, 2013. The lower crust of Dharwar craton, south India: patchwork of Archean granulitic domains. Precambrian Res. 227, 4–29. http://dx.doi.org/10.1016/j.precamres.2012.06.009.
  35. ^ Kaur, P., Zeh, A., Chaudhri, N., 2014. Characterization and U–Pb–Hf isotope record of the 3.55 Ga felsic crust from the Bundelkhand Craton, northern India. Precambrian Res. 255, 236–244.
  36. ^ a b Zhai, M.G., Santosh, M., 2011. The early Precambrian odyssey of the North China Craton: a synoptic overview. Gondwana Res. 20, 6–25.
  37. ^ Zhao, G., Sun, M., Wilde, S.A., 2003. Correlations between the Eastern Block of the North China Craton and the South Indian Block of the Indian Shield: an Archaean to Palaeoproterozoic link. Precambrian Research 122, 201–233. http://dx.doi.org/10.1016/S0301-9268(02)00212-7.
  38. ^ Laurent, O., Martin, H., Doucelance, R., Moyen, J.-F., Paquatte, J.-E., 2011. Geochemistry and petrogenesis of high-K ‘sanukitoids’ from Bulai pluton, Central Limpopo belt, south Africa: implications for geodynamic changes at the Archean –Proterozoic boundary. Lithos 123, 73–91.
  39. ^ Cassidy, K.F., Champion, D.C., Krapez, B., Barley, M.E., Brown, S.J.A., Blewett, R.S., Groenewald, P.B., Tyler, I.M., 2006. A Revised Geological Framework for the Yilgarn Craton: Geological Survey of Western Australia. (Record 2006/8, 8p).
  40. ^ Kabete, J.M., McNaughton, N.J., Groves, D.I., Mruma, A.H., 2012. Reconnaissance SHRIMP 851 U-Pb zircon geochronology of the Tanzania Craton: evidence for Neoarchean granitoid-greenstone belts in the Central Tanzania Region and the Southern East Africa Orogen. Precambrian Res. 216−219, 232–266.
  41. ^ Scholfield, D.I., Thomas, R.J., Good enough, K.M., De Waele, B., Pitfield, P.E.J., Key, R.M., Baur, W., Walsh, G.J., Lidke, D.J., Ralison, A.V., Rabarimanana, M., 2010. Geological evolution of the Antongil craton, NE Madagascar. Precambrian Res. 182, 187–203.
Retrieved from "https://en.wikipedia.org/w/index.php?title=Dharwar_Craton&oldid=1054981718"