Dharwar Craton: Difference between revisions
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Anatectic granite is a kind of rock formed by the partial melting of the pre-existing crustal rock, which is relatively |
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. |
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Revision as of 07:05, 31 October 2021
![](http://upload.wikimedia.org/wikipedia/commons/thumb/5/5e/Dharwar_Craton.jpg/451px-Dharwar_Craton.jpg)
The Dharwar Craton is an Archean continental crust formed between 3.6-2.5 billion years ago (Ga), which is located in the Southern India.
Recent studies 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 serveral 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. [4] 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.[5]
The formation of the basement rock of the Dharwar Craton was proposed by the plume-arc model, including intraplate hotspot model 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.[6] [7]
Overview of the regional geology
![](http://upload.wikimedia.org/wikipedia/commons/thumb/8/8f/Simplified_Geological_map_of_Dharwar_Craton.png/453px-Simplified_Geological_map_of_Dharwar_Craton.png)
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.[8]
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.[9] 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.[5] 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.[8] The Chitradurga greenstone belt is an elongated linear supracrustal belt which is 400 km long from North to South.[10]
The WDC 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).[5][8]
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.[11] The older Kolar-type greenstone mainly contains greenschist to amphibolite facies metabasalts, as well as some subordinate felsic volcanic rocks and metasediments,[12] while the younger granitoids include TTG gneisses, high-magnesium sanukitoids and potassium-rich leucogranites.[11]
![](http://upload.wikimedia.org/wikipedia/commons/thumb/b/b0/Xscn_of_dharwar_craton.png/456px-Xscn_of_dharwar_craton.png)
Lithlogies
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:[13]
Blocks | Main TTG type | Associated group | Characteristics |
---|---|---|---|
western block | typical TTG gneisses[7] | Sargur Group[7] |
|
central block | transitional TTG (mixture of the typical TTG and dark grey banded gneisses)[7] | Kolar Group[13] |
|
eastern block | banded gneisses[7] | Kolar Group[2] |
|
Volcanic-sedimentary greenstone sequences
Greenstone is 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[14] | Sargur group and Dharwar Supragroup | |
central block | basalts with minor ultramafic komatiite[16] | Kolar group |
|
eastern block | basalts with minor ultramafic komatiite[17] | Kolar group |
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[18] |
|
Eastern block |
|
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 granite | Characteristics |
---|---|---|---|
western block | Granite with high-potassium content[2] | TTG gneisses and volcanic greenstone |
|
central block | |||
eastern block |
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] |
|
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[22] |
|
Eastern block | Poorly understood | Poorly understood |
|
Archean crust accretions
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 Ma, 3230–3200 Ma, 3150–3000 Ma, 2700–2600 Ma and 2560–2520 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 leading to the widespread of greenstone volcanism.[5]
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. [16]
The eastern block records the two latest major accretion events occurring in 2700 Ma and 2560 Ma with massive continental growth.[26]
Crustal reworking events
The crustal reworking events happened in the time range of 3100–3000 Ma.[7] 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.[7] The second reworking event led to the intrusions of 2640–2600 Ma high-K plutons of Arsikere-Banavara and Chitradurga granites.[27]
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.[23]
Formation and evolution
Intraplate hotspot model
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.[6][28]
![](http://upload.wikimedia.org/wikipedia/commons/thumb/3/34/%E8%9E%A2%E5%B9%95%E6%88%AA%E5%9C%96_2021-10-26_%E4%B8%8B%E5%8D%886.31.16.png/457px-%E8%9E%A2%E5%B9%95%E6%88%AA%E5%9C%96_2021-10-26_%E4%B8%8B%E5%8D%886.31.16.png)
![](http://upload.wikimedia.org/wikipedia/commons/thumb/c/cd/Model_noah.png/456px-Model_noah.png)
Two-stage melting of oceanic crust
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.[29]
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][6]
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.[30]
![](http://upload.wikimedia.org/wikipedia/commons/thumb/4/4c/Model_for_DC21.png/457px-Model_for_DC21.png)
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.[31]
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.[32]
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.[33]
Sanukitoid magmatism
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.[11] 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.[34] This can be explained by the mixing of the previous TTG melts.[35] 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.[36]
Implication for global crust history
Possible relationships with the Dharwar Craton | |
---|---|
Bundelkhand Craton |
|
North China Craton |
|
Kaapvaal Craton |
|
Pilbara Craton |
|
Yilgarn Craton |
|
Tanzania Craton |
|
Antongil Craton |
See also
References
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- ^ a b c d e f g h i j k l m n o p q r s t M, J., M, S., & K.R, A. (2018). Formation of Archean (3600–2500 Ma) continental crust in the Dharwar Craton, southern India. Earth-science Reviews, 181, 12-42.
- ^ a b c Peucat, J., Jayananda, M., Chardon, D., Capdevila, R., Fanning, C., & Paquette, J. (2013). The lower crust of the Dharwar Craton, Southern India: Patchwork of Archean granulitic domains. Precambrian Research, 227, 4-28.
- ^ a b c Jayananda, M., Peucat, J., Chardon, D., Rao, B., Fanning, C., & Corfu, F. (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.
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