Proterozoic Orogenesis and Crustal Evolution in the Central Indian
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Proc Indian Natn Sci Acad 86 No. 1 March 2020 pp. 99-106 Printed in India. DOI: 10.16943/ptinsa/2020/49780 Status Report 2016-2019 Proterozoic Orogenesis and Crustal Evolution in The Central Indian Tectonic Zone: Current Understanding from Recent Works ANUPAM CHATTOPADHYAY* Department of Geology, University of Delhi, Delhi 110 007, India (Received on 09 August 2019; Accepted on 29 September 2019) In the past few years, a huge amount of geological, geochemical and geochronological data have been generated from the southern margin of the Central Indian Tectonic Zone (CITZ) which gives enough clues for understanding the tectonothermal history and Proterozoic orogenesis of the central Indian craton and its implication for the Proterozoic supercontinent assembly. Relevant works published in last four years (2015-2019), with the background geological and tectonic context, are briefly reviewed here. The outstanding geological controversies are also outlined. Keywords: Central Indian Tectonic Zone; Sausar Group; Granulites; Tectonothermal History; Proterozoic Orogeny Introduction (Acharyya and Roy, 2000; Roy and Prasad, 2003). Thus, the evolution of CITZ overlapped with the The Peninsular Indian landmass is a mosaic of several assembly and dismemberment of two major cratonic nuclei, viz., Bundelkhand craton, Bastar supercontinents, viz., Columbia (ca. 2.1-1.8 Ga) craton, Dharwar craton, Singhbhum craton etc., skirted (Rogers and Santosh, 2003) and Rodinia (ca. 1.2-0.9 by a number of prominent mobile belts. It is now Ga) (Pisarevsky et al., 2003). The tectonothermal generally accepted that the North Indian Block (NIB) history of CITZ and its correlation with other major comprising the Bundelkhand and Marwar cratons transcontinental mobile belts therefore provides us (BKC) and the South Indian Block (SIB), comprising clues for understanding the Proterozoic supercontinent the combined Bastar-Dharwar-Singhbhum cratons cycle. A huge amount of work has been carried out (BC) were stitched together in the Proterozoic along on the CITZ (in central India) in the last two decades a prominent E-W trending crustal scale mobile belt and a variety of tectonic models have been proposed called the Central Indian Tectonic Zone (CITZ) (e.g. at different points of time (e.g. Acharyya and Roy, Radhakrishna and Naqvi, 1986; Roy and Prasad, 2003; 2000;Roy and Prasad, 2003; Naganjaneyulu and Bhowmik et al., 2012 and references therein). CITZ Santosh, 2010; Bhowmik et al., 2012; Chattopadhyay (or its equivalents) has been traced upto Madagascar et al., 2017; Bhowmik, 2019 - to name a few). In this in the west (Katz and Premoli, 1979) and to the east short communication, I shall attempt to review and through Chhotanagpur Gneissic Complex (CGGC) synthesize the major research works published within and Shillong Plateau (Acharyya, 2001) upto Western the last four years (2015 onward), with necessary Australia (i.e. Albani-Fraser Orogen) (Harris, 1993). references to some of the earlier works for maintaining This proposed trans-continental nature of CITZ makes the geological context. A more detailed, comprehensive it a potential study area for understanding the crustal review of the geology, geochronology, and tectonics evolutionary history in the Proterozoic. In its type area, of CITZ is available in a separate publication (to be i.e. in the central Indian craton, the CITZ records a published in Episodes: IGC 2020 legacy volume). tectonothermal evolutionary history spanning nearly 1000 Myrs from Paleoproterozoic to Neoproterozoic The Central Indian Tectonic Zone (CITZ) *Author for Correspondence: E-mail: [email protected] 100 Anupam Chattopadhyay dissects the Indian landmass in an E-W to ENE-WSW 2015), whereas some workers (e.g. Mohanty, 2010, direction, and has a maximum width of about 200 km and references therein) have argued that migmatization in central India. Three major supracrustal belts, viz., of Sausar sediments has generated TBG. Four phases Mahakoshal, Betul and Sausar belts occur within the of deformation – an early phase of southward thrusting CITZ from north to south. These belts are set in a and associated recumbent/reclined folding (D1/F1), vast country of unclassified gneiss-migmatite-granitic followed by E-W trending upright/steeply inclined rocks, locally named as Tirodi Biotite Gneiss, Amgaon folding (F2) of the thrust allochthon (‘Deolapar Gneiss, Betul Gneissic Complex etc. The CITZ is Nappe’) characterize the deformation of the Sausar traversed by a few major tectonic lineaments parallel Group. Minor F3 folds, locally distorting the F2 hinges, to its length, viz. Son-Narmada North Fault (SNNF), and late F4 cross-folds are also observed Son-Narmada South Fault (SNSF), Gavilgarh-Tan (Chattopadhyay et al., 2003a,b). The Sausar Group Shear Zone (GTSZ) and Central Indian Suture/Shear rocks have undergone Barrovian-type regional (CIS) from north to south (Fig. 1). While the metamorphism, varying in grade from low greenschist Mahakoshal supracrustal belt is confined between facies in the south and southeast to upper amphibolite SNNF and SNSF, GTSZ separates the Betul belt from facies (TMax~675°C at P~7 kbar) in the northwest the Sausar Belt and CIS is considered as the southern (near the contact with RKG domain) (Bhowmik et limit of the CITZ, south of which N-S structural grain al., 1999). Sausar Group metasediments show a of the Bastar craton is observed. Three granulite belts clockwise metamorphic P-T path of evolution are identified within CITZ, viz., Makrohar granulite indicating a continental collisional set-up during (MG) in the south of the Mahakoshal belt, Ramakona- orogenesis (Bhowmik et al., 2012). Similarly, four Katangi granulite (RKG) along the northern margin phases of deformation and three phases of of the Sausar belt, and Balaghat-Bhandara granulite metamorphism have been established from metabasic (BBG) along the CIS (Fig. 1). Geological information granulites of the RKG domain (Bhowmik and Roy, from the Makrohar granulite is limited, but a lot of 2003). The peak metamorphic condition reached P~9- information is now available on the tectonothermal 10kbar, T~750°-800°C, followed by isothermal evolution of the RKG and BBG belts (Bhowmik 2019 decompression at about 7 kbar/775°C and a later near- and references therein). In the last four years (2015- isobaric cooling at 6 kbar/650°C, recording a clockwise 2019), maximum work has been carried out in the P-T path. A similar P-T path was established from southern part of CITZ i.e. on the Sausar Fold Belt pelitic granulites also (Bhowmik and Spiering 2004), (SFB), the associated granulites (RKG and BBG indicating an overall collisional setting for the RKG belts), and the GTSZ, and a cogent picture on the granulites (Bhowmik, 2019 and references therein). Proterozoic orogenesis in the CITZ is gradually emerging. Therefore, only this part of the CITZ is In the last few years, the work on Sausar Fold taken up in the present review. belt (including RKG) mostly concentrated on the timing of the tectonothermal events. While a late Sausar Fold Belt and Ramakona-Katangi (RKG) Mesoproterozoic to early Neoproterozoic (ca. 1063- Granulites 993 Ma) age of prograde and retrograde metamorphism respectively has been established by The 300 km long and 70 km wide arcuate (southward Electron Microprobe (EMP) dating of monazites from convex) Sausar Fold Belt (SFB) is the southernmost Sausar Group metasediments, the metapelitic supracrustal belt of the CITZ, lying between the GTSZ granulites from RKG belt yielded weighted mean and the CIS (Fig. 1). SFB consists of the monazite age of ca.1043 Ma and 955 Ma for peak metasedimentary Sausar Group (SSG) - a typical and retrograde metamorphism. SHRIMP U-Pb zircon platformal assemblage of metamorphosed quartzite- age of magmatic charnockite from the RKG domain pelite-carbonate with stratabound Mn-ore, which has yielded an age of ca. 938 Ma (Bhowmik et al., structurally overlies a vast expanse of gneissic rocks 2012). Chattopadhyay et al. (2015) have reported (dominantly TTG, migmatites and granite gneiss) EMP monazite ages of ca. 945 Ma from syntectonic known as the Tirodi Biotite Gneiss (TBG). TBG is (syn-D2) granites and ca. 928 Ma from post-tectonic presently considered as the basement to the Sausar granites intrusive into the Sausar Group. From the Group (Bhowmik et al., 1999; Chattopadhyay et al., similarity of peak (syn-D2) metamorphism of SSG and Proterozoic Orogenesis in the CITZ 101 Fig. 1: Simplified geological map of the CITZ in central India showing all the supracrustal belts and tectonic lineaments. Selected geochronological data from different parts of CITZ are shown in the boxes (modified after Yedekar et al. 1990; Acharyya and Roy 2000; Chattopadhyay and Khasdeo 2011). Geochronological data taken from Bhowmik et al. (2012), Bhowmik (2019), Chattopadhyay et al. (2015), Chattopadhyay et al. (2017). See the text for more details age of retrograde metamorphism in RKG, they argued Another major controversy has recently for a slightly younger tectonothermal history of the surfaced, regarding the glaciogenic origin of Sausar SSG than that of the RKG. rocks. This issue is also intertwined with the 102 Anupam Chattopadhyay Paleoproterozoic vis-a-vis Meso-Neoproterozoic age 2011). The eastern part of this linear structure is of the Sausar Group. Mohanty et al. (2015) have expressed as a ductile shear zone comprising sheared argued that a major diamictite horizon present in the Precambrian gneisses and granitoids, while the lower part of the Sausar Group (Nayakund western part is mainly observed as a brittle fault zone Formation), and the presence of ‘dropstones’ and rock affecting Gondwana sandstone and Deccan Trap fragments within dolomitic marble (Potgowari basalt flows, within which slivers of the sheared Formation) characterize it as a glacial deposit with a gneissic basement rocks are also found. Repeated cap-carbonate horizon. Isotopic analyses (δ13C and reactivation of the fault/shear zone from Proterozoic δ18O) of the cap carbonate indicates strong negative to Quaternary has been established (Bhattacharjee δ13C excursion, similar to other Paleoproterozoic et al., 2016; Chattopadhyay and Bhattacharjee, 2019).