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Reconstruction of the Neoproterozoic supercontinent Rodinia shows near neighbour positions of the South Indian Cratons and Western Australian Cratons. These cratonic areas are characterized by extensive Paleoproterozoic tectonism. Detailed analysis of the spatio-temporal data of the Satpura Mountains of India indicates presence of at least three ep...
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... Harris (1993) and Harris and Beeson (1993) have suggested the extension of the CITZ to the Chotanagpur Granite Gneiss Complex (CGGC) and further east up to the gneissic complex of NE India, which unconformably overlies the Shillong group from NE India to the Albany Mobile Belt (AMB). Mohanty (2010Mohanty ( , 2012 has advocated the continuation of the orogenic trend of the Satpura belt into Western Australia's Capricorn orogen at ~ 2000 Ma. The Paleo-Mesoproterozoic (2.1-1.2 ...
The Tirodi Gneissic Complex (TGC) represents the basement sequence of the Central Indian Tectonic Zone (CITZ), underlying the Proterozoic supracrustal sequences of the Sausar and Betul Groups of rocks. Lithologically, the TGC constitutes a combination of pink and grey granitic gneiss assemblages, characterised by biotite-rich, hornblende-biotite-rich, and muscovite-biotite-rich granite gneiss. Compositionally, the TGC granitoids represent tonalite-trondhjemite-granodiorite to granite, and have calc-alkaline lineage with metaluminous to peraluminous characteristics. Geochemically, they dominantly belong to A2-type granitoids. Chondrite normalised REE ratios of La/Sm, La/Yb, La/Gd, and Gd/Yb indicate diverse LREE/HREE enrichment. Multi-element patterns for the TGC granitoids are characterised by light rare earth elements (LREE) and large ion lithophile elements (LILE) enrichment and depletion of high field strength elements (HFSE: Nb, P, and Ti) and strong positive Pb and Th anomalies. The observed negative anomalies for HFSE are attributed to diverse crustal/lithospheric sources, with some influence from K-feldspar, plagioclase and Ti-oxide fractionation. Sm–Nd data presents initial ¹⁴³Nd/¹⁴⁴Nd (t = 1.7 Ga) ratios (0.509898 to 0.510508), and εNd (t = 1.7 Ga) is (+ 0.58 to -10.59), with TDM model ages ranging from 2.11 to 2.95 Ga. Such a wide range of εNd (t = 1.7 Ga), indicates heterogeneous crustal/lithosphere sources, which have probably experienced longer crustal residence times. Zircon U–Pb ages for individual TGC samples are 1506 ± 11 Ma (TG-01), 1534 ± 26 Ma (MU-5), 1675 ± 9 Ma (BT-4), 1724 ± 11 Ma (BT-3), 1730 ± 13 Ma (BT-4), and 1960 ± 2 Ga (Ms-2), respectively. These ages have probably recorded the key periods of the Columbia supercontinent's assembly, growth, and breakup. Geochemical and geochronological results suggest that the TGC granitoids have a crustal/lithospheric origin and are formed by partial melting of felsic sources in dominantly VAG (volcanic arc granite) and, to some extents, WPG (within-plate granite) settings.
... The rocks have suffered a regional low-grade metamorphism but localised domains of migmatisation and amphibolite-grade metamorphism have also been reported (Mohanty et al., 2015, and the references therein). Mohanty (2012) suggested that the first deformation event affecting the Sausar Group took place at 2.0 Ga, whereas the second event was from 1.8 to 1.5 Ga. Mohanty (2012) also considered the latter as the more ubiquitous one that affected the entire CITZ and resulted from the final amalgamation of the NIB and SIB. ...
... Mohanty (2012) suggested that the first deformation event affecting the Sausar Group took place at 2.0 Ga, whereas the second event was from 1.8 to 1.5 Ga. Mohanty (2012) also considered the latter as the more ubiquitous one that affected the entire CITZ and resulted from the final amalgamation of the NIB and SIB. However, no subsequent breakup of the Indian landmass along the CITZ during the reconfiguring of the supercontinent Columbia was considered. ...
... Orogenic evidence such as granulite metamorphism and/or granitic magmatism corresponding to 2000-2200 Ma has been widely reported from the Indian Bastar-Singhbum cratonic nuclei ( Fig. 12; Sarkar et al., 1981;Sarkar et al., 1994;Bhowmik et al., 2005). The Satpura orogenic Belt of Central Indian craton records multiple phases of granulite metamorphism and correlated episodes of granitic magmatism during the Paleoproterozoic Era (Mohanty, 2012). Signatures of ~2200 Ma Sausar orogeny I (Sarkar et al., 1981;Pandey et al., 1989;Panigrahi et al., 1993) and ~2000 Ma UHT metamorphism (Bhowmik et al., 2005) in Bastar craton are considered coeval with the Singhbum orogeny phase I and II (Sarkar and Saha, 1986), respectively in south Singhbum craton. ...
... These events in Indian Bastar-Singhbum cratonic nuclei are correlated with the Opthalmian (2215-2145 Ma: Cawood and Tyler, 2004;Rasmussen et al., 2005) and Glenburgh orogenic imprints (~2000 Ma: Occhipinti et al., 2004) in Western Australian cratons, respectively. A compilation of these correlated events is given in Mohanty (2012). In the context of supercontinent-scale tectonics, the 2000-2200 Ma granulite/granite events are recorded globally in various Archean orogenic systems (e.g., global reconstructions by Grenholm, 2019). ...
... The Central Indian Tectonic Zone, or crustal domain portions thereof, is thought to be continuous with several Proterozoic orogens in neighboring continents (Fig. 4B), such as the Albany-Fraser Orogen Harris and Beeson, 1993) and the Capricorn Orogen (Mohanty, 2012) in Western Australia, and the Trans-North China Craton (Zhao et al., 2003;Santosh, 2012). In subsequent years, these trans-continental correlations were thought to be untenable GEOSPHERE | Volume 19 | Number X Compilation of non-detrital zircon data from Grenville orogen (Clay et al., 2021) Compilation of non-detrital zircon data from Sveconorwegian orogen (Bingen & Viola, 2018) (y-axis scales variable; refer to colours) (Fitzsimons, 2003;Dey, 2013;Rekha and Bhattacharya, 2014;Deshmukh et al., 2017; due to the availability of robust geochronological data (primarily U-Pb zircon dates) of geological events (reviewed by Banerjee et al., 2021), a rigorous delineation of the southern and northern margins of the Central Indian Tectonic Zone (Bhattacharya et al., 2019;Banerjee et al., 2021;, and a clearer elucidation of the structure, petrology, and geochemistry of the lithodemic units in the Central Indian Tectonic Zone (Banerjee et al., 2021(Banerjee et al., , 2022a(Banerjee et al., , 2022b(Banerjee et al., , 2022c. ...
In the paleogeographic reconstructions of the Rodinia supercontinent, the circum-global 1.1–0.9 Ga collisional belt is speculated to skirt the SE coast of India, incorporating the Rodinian-age Eastern Ghats Province. But the Eastern Ghats Province may not have welded with the Indian landmass until 550–500 Ma. Instead, the ~1500-km-long, E-striking Central Indian Tectonic Zone provides an alternate option for linking the 1.1–0.9 Ga circum-global collisional belt through India. The highly tectonized Central Indian Tectonic Zone formed due to the early Neoproterozoic collision of the North India and the South India blocks. Based on a summary of the recent findings in the different crustal domains within the Central Indian Tectonic Zone, we demonstrate that the 1.03–0.93 Ga collision involved thrusting that resulted in the emplacement of low-grade metamorphosed allochthonous units above the high-grade basement rocks; the development of crustal-scale, steeply dipping, orogen-parallel transpressional shear zones; syn-collisional felsic magmatism; and the degeneration of orogenesis by extensional exhumation. The features are analogous to those reported in the broadly coeval Grenville and Sveconorwegian orogens. We suggest that the 1.1–0.9 Ga circum-global collisional belt in Rodinia swings westward from the Australo-Antarctic landmass and passes centrally through the Greater India landmass, which for the most part welded at 1.0–0.9 Ga. It follows that the paleogeographic positions of India obtained from paleomagnetic data older than 1.1–0.9 Ga are likely to correspond to the positions of the North and South India blocks, respectively, and not to the Greater India landmass in its entirety.
... Further, Kaila et al. (1989) suggested existence of faults extending deep up to the Moho level and reactivation of faults was responsible for alkaline magmatism that occurred during 1.8 to 1.6 Ga and represented by syenites and alkali dykes ( Srivastava and Chalapathi Rao, 2007 ;Satyanarayanan et al., 2018 ). The end phase of the Mahakoshal orogeny was marked by rifting along the-southern edge of the Bundelkhand craton ( Mohanty, 2012 ;Mishra and Kumar, 2014 ). Thus, the Bari syenite intrusion in the Mahakoshal phyllite rocks along the SNNF at 1800 Ma. is portraying anorogenic tectonic settings ( Bora et al., 2015 ;Saha et al., 2016 ). ...
... The Faizabad Ridge, an extension of the Archean Bundelkhand Craton, is flanked by two deep-seated lithospheric faults: the Lucknow basement fault (Lucknow Fault) to the west, and the Pokhara basement fault (Pokhara Fault) to the east ( Fig. 1B; Godin and Harris, 2014;Godin et al., 2019;Soucy La Roche and Godin, 2019). The Mw 5.8 Jabalpur earthquake of May 21, 1997, occurred at a focal depth of approximately 35 km along Casshyap and Khan (2000), Goscombe et al. (2018), Kellett and Grujic (2012), Mohanty (2012), Soucy La Roche et al. (2018) and Yin (2006), modified from Duvall et al. (2021). Approximate traces of basement ridges after Godin and Harris (2014). ...
... The region occupied by the Mountain Belt and its flanking regions on both the sides have undergone tectonic activities of multiple episodes, during Paleoarchean to Recent. Preservations of rock records of the complete Earth history, barring temporal gaps of different orders, in the Satpura Mountain Belt and its bordering blocks provide impetus for researches related to geochemical evolution of Earth's crust, https Powell et al., 2001 ); (b) tectonic trends (traces of axial planes of folds) in different Precambrian provinces of the Indian Shield and distribution of Proterozoic (Purana) Basins and Phanerozoic cover rocks (modified from Saha, 1994 ); and (c) the Chhotanagpur Gneiss Complex and the surrounding blocks (modified from Mohanty, 2012 ). Nomenclatures of regional faults and additional faults in (b) are added (after Jain et al., 1995aJain et al., , 1995bBalakrishnan, 1997 ;Shanker, 1997 ). ...
... Based on an analysis of the existing paleomagnetic and geochronological data, combined with the spatio-temporal evolution of the cratonic nuclei of India, Western Australia and East Antarctica, the reconstruction was taken back to Archean Eon, indicating the existence of an Archean block comprising of South India, Western Australia and the Napier Complex and Vestfold Hills of East Antarctica; this combined block has been termed as 'SIWA', an acronym for South India and Western Australia ( Mohanty, 2010a( Mohanty, , 2010b( Mohanty, , 2011a( Mohanty, , 2011b( Mohanty, , 2011c( Mohanty, , 2011d. The breaking and dispersal of the constituent units of 'SIWA' was proposed to be an aftereffect associated with a Paleoproterozoic amalgamation on the northern and eastern margins of 'SIWA' developing the Satpura Orogenic belt and continuing towards the Ophthalmian -Glenburg -Capricorn Orogen ( Mohanty, 2010c( Mohanty, , 20122021 ). However, such attempts have slow progress for reconstructions of Indian cratons during Archean -Proterozoic Eons for debates arising out of models constructed for Rodinia and Columbia from investigations in small domains ranging from few square km to few tens of square km and raising questions regarding the time of Satpura Orogeny ( Bhowmik, 2019 , and references therein) and correlation of the Ophthalmian -Glenburg -Capricorn Orogeny and Albany -Fraser Orogeny with the counterparts in India ( Sequeira and Bhattacharya, 2021a , and references therein). ...
... Bhowmik, 2019 ). It may be noted that Mohanty (2012Mohanty ( , 2021 has proposed the amalgamation of the NIB and SIB in twophases at ∼2250 Ma and ∼1800 Ma. The age data generated by Saikia et al. (2017) and Sequeira and Bhattacharya (2021a) support the age of ∼2250-2150 Ma for the first deformation and metamorphism (D 1a ) and ∼1800 Ma for the second uplift (D 1b ) in the Satpura Mobile Belt proposed by Mohanty (2021) . ...
The Chhotanagpur Gneiss Complex, covering the eastern part of the Satpura Mountain Belt of India, has records of polyphase deformation and metamorphism of Proterozoic Eon. Analysis of structural evolution of the region, combined with the tectonothermal history, has shown that the regional ~E-W alignment was developed during the second phase of deformation, high-grade metamorphism and magmatism at ~1500 Ma. The migmatites preserve records of an early phase of deformation, metamorphism and magmatism of >1800 Ma. Relict monazite and zircon grains have two age ranges. The older age (>2531 Ma) represents the Archean cratonization event, and the younger age (~2216 Ma) corresponds to the first deformation, metamorphism and magmatism during amalgamation of the North Indian Block (Bundelkhand Craton) and the South Indian Block (Bastar and Singhbhum cratons) forming the Satpura Orogen. This Orogeny caused complete reset of the isotopic clock, and initiated it from ~2000 Ma. A phase of separation (basin opening during 2000-1750 Ma) took place on both the sides of the young orogen. The second orogenic event of ~1500 Ma has been identified to be the result of amalgamation of the Singhbhum Block and the Chhotanagpur Gneiss Complex, during the Eastern Ghats – Dalma Orogeny Phase I. The second deformation-metamorphism was followed by another phase of extension and basin opening at ~1200-1100 Ma. The third deformation and metamorphism in the Complex took place during the Eastern Ghats – Dalma Orogeny Phase II of 1100-850 Ma, having the maximum probability at ~926 Ma. This orogeny developed folds with ~NNW-SSE to N-S axial traces, nearly orthogonal to the fabric defining the Satpura trend. Records of any block amalgamation of <1800 Ma within the Chhotanagpur Gneiss Complex are not found.
... In addition to the Mahakoshal, Betul, and Sausar supracrustal belts, the CITZ also hosts major granulite terranes such as the Balaghat-Bhandara belt in the south, the Ramakona-Katangi belt in the central region, and Makrohar belt in the northern part). The tectonic evolution of the CITZ has been a topic of discussion and debate for the last three decades Roy and Prasad, 2003;Acharyya, 2003;Naganjaneyulu and Santosh, 2010;Mohanty, 2010Mohanty, , 2012Chattopadhyay and Khasdeo,2011;Bhowmik and Chakraborty, 2017;Deshmukh and Prabhakar, 2019;Bhowmik, 2019;Chattopadhyay et al.,2020;Giri et al.,2021;Sharma et al.,2022;Phukon,2022). Several tectonic models of its crustal evolution have been published, briefly summarized below. ...
... Malanjkhand Granite and Dongargarh Granite have been studied extensively by different workers (Ramachandra and Roy, 1998;Narayana et al., 2000;Ramachandra et al., 2001;Panigrahi et al., 2004;Kumar et al., 2004;Kumar and Rino, 2006;Ahmad et al., 2008, Srivastava and Gautam, 2009, 2015Pandit and Panigrahi, 2012;Mohanty, 2012Mohanty, , 2015Pandit et al., 2014;Bickford et al., 2014;Hazarika et al., 2019); limited work has been carried out on the Kanker Granites (Ramachandra and Roy, 1998;Ramachandra et al., 2001;Elangovan et al., 2017;Asokan et al., 2020;Martha et al., 2021). ...
Heterogeneous nature, textural variation, and compositional diversity are reported from the north-western part of the Kanker Granites, exposed in parts of Kanker District, Chhattisgarh, India, where the possible petrogenesis and tectonic history of the same, with special emphasis on its REE mineralogy and genesis. The granites are ferroan, alkalic to sub-alkalic, per-aluminous and oxidized A-type in nature. An integrated field-petrography-whole rock analysis-mineral chemistry approach indicates injection of mafic magma into crystallizing felsic host with different stages of interaction through mixing, mingling and hybridization. Major oxides, trace elements and REE geochemistry suggest derivation from a predominant crustal source involving a variable degree of mantle input, with a key role of fractional crystallization from mafic magma and partial melting of quartzo-feldspathic igneous sources during petrogenesis. The evolution of the granites can be best explained in an accretionary post-orogenic (collision) phase in subduction setting (A2-type granites) during the Archean-Proterozoic transition. The granites are enriched in LREE, the REE bearing phases being monazite, xenotime, allanite, parisite, and zircon. Occurrence of the REEs in granites probably have occurred through magmatic processes, hydrothermal fluid mobilization and precipitation. The REE contents in granites can be a potential resource in terms of economic geology.
... Sarkar [9][10][11] suggested a tentative temporal relationship between the three phases of structural deformation, metamorphism and granite emplacement. Based on reviews of petrological, geochemical, metamorphic, deformational, and geochronological data on the CGGC given as summarised as [12][13][14][15] : M 1 metamorphic stage (around 1870 Ma and followed by the D 1 deformation, > 900 °C at ~5-8 kbar pressure). M 2 metamorphic phase between 1660 Ma and 1270 Ma, the D 2 deformation, 700-800 °C at 5-7 kbar pressure). ...
The Rb-Sr whole-rock isochron, age 1636 ± 66 Ma of Mirgarani granite, is the one of the oldest granite dated in the northwestern part of the Chhotanagpur Granite Gneiss Complex (CGGC). The initial Sr ratio is 0.715 ± 0.012 (MSWD = 0.11), showing an S-type affinity. The Mirgarani granite has intruded the migmatite complex of the Dudhi Group and forms the Mirgarani formation comparable to the granites of the Bihar Mica Belt around Hazaribagh (1590 ± 30 Ma). The present studies have established the chronostratigraphy of the Dudhi Group and adjoining areas in CGGC. Petro-graphic and geochemical studies revealed that the granite is enriched in Rb (271 ppm), Pb (77 ppm), Th (25 ppm), and U (33 ppm) and depleted in Sr (95 ppm), Nb (16 ppm), Ba (399 ppm) and Zr (143 ppm) contents as compared to the normal granite. The Mirgarani granite is a peraluminous (A/CNK = 1.23), high potassic (K 2 O 6.42%), Calc-Alkalic to Alkali-Calcic {(Na 2 O+K 2 O)-CaO = 6.29} S-Type granite, a feature supported by the presence of modal garnet and normative corundum (2.68%). The Mirgarani granite is considered to have been formed by the anatexis of a crustal sedimentary protolith at a depth of approximately 30 km with temperatures ranging from 685-700 °C during the Co-lumbian-Nuna Supercontinent.
