Spatio-Temporal Evolution of the Satpura Mountain

GEOSCIENCE FRONTIERS 3(3) (2012) 241e267

available at www.sciencedirect.com China University of Geosciences (Beijing) GEOSCIENCE FRONTIERS

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GSF FOCUS Spatio-temporal evolution of the Satpura Mountain Belt of India: A comparison with the Capricorn Orogen of Western Australia and implication for evolution of the supercontinent Columbia

S. Mohanty

Department of Applied Geology, Indian School of Mines, Dhanbad 826 004, India

Received 5 August 2011; accepted 26 October 2011 Available online 9 December 2011

KEYWORDS Abstract Reconstruction of the Neoproterozoic supercontinent Rodinia shows near neighbour positions of Paleoproterozoic; the South Indian Cratons and Western Australian Cratons. These cratonic areas are characterized by extensive Supercontinent; Paleoproterozoic tectonism. Detailed analysis of the spatio-temporal data of the Satpura Mountains of India Capricorn Orogeny; indicates presence of at least three episodes of Proterozoic orogeny at w2100e1900 Ma, w1850 Ma Satpura Orogeny and w1650 Ma, and associated basin development and closing. A subdued imprint of the Grenville orogeny (w950 Ma) is also found in rock records of this Mountain Belt. The Capricorn Orogen of Western Australia also shows three episodes of orogeny: OpthalmianeGlenburgh Orogeny (2100e1950 Ma), Capricorn Orogeny (w1800 Ma) and Mangaroon Orogeny (w1650 Ma), and basin opening and closing related to these tectonic movements. These broad similarities suggest their joint evolution possibly in a near neighbour position during Paleoproterozoic Era. In view of juxtaposition of the Western Australia along the east coast of India, at the position of the Eastern Ghats, during Archean, it is suggested that the breaking of this Archean megacraton at w2400 Ma led to northward movement of the broken components and formation of the SatpuraeCapricorn Orogen (at w2100 and w1800 Ma) due to the collision of cratonic blocks with the pre- existing northern cratonic nuclei of India and Western Australia. This is also the time of formation of the

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supercontinent Columbia. A phase of basin opening followed the w1800 Ma event, followed by another phase of collisional event at w1600 Ma at the site of the SatpuraeCapricorn Orogen. Subsequent evolutions of the Satpura and the Capricorn Orogens differ slightly, indicating separate evolutional history. ª 2011, China University of Geosciences (Beijing) and Peking University. Production and hosting by Else- vier B.V. All rights reserved.

1. Introduction fundamental implications for understanding the making and breaking of Columbia. The concept of the Neoproterozoic supercontinent Rodinia Attempts at the reconstruction of the supercontinent Gond- (Dalziel, 1991; Hoffman, 1991; Moores, 1991) has initiated interest wanaland suggested matching the east coast of India with the west to understand the nature of changes in the tectonic processes at the coast of Australia (Crawford and Oliver, 1969; King, 1973). This ArcheaneProterozoic boundary and related atmospheric and reconstruction model changed in favour of matching coastline biospheric evolutions. It is believed that the supercontinent configuration of India and East Antarctica (Crawford, 1974; assembly and disruption have a 500e600 Ma cycle possibly related Powell et al., 1988). However, analysis of the paleomagnetic to the mantle convection. Common histories of cratonic develop- and spatio-temporal data for Paleoproterozoic age indicates ment of spatially related groups of cratons apparently indicate juxtapositions of South India, West Australia and Napier Complex w relatively small intracratonic movement (w1 cm/y) and small-scale of East Antarctica at 2400 Ma (Fig. 4; Mohanty, 2010b, tectonic regimes during late ArcheanePaleoproterozoic times 2011a,b). The paleogeographic and geologic links provide (Piper, 2003). This has led to make a model of supercontinent support for this configuration (Fig. 5). The breaking and dispersal assemblies during Paleoproterozoic (Piper, 1976). From geological of the constituent elements were followed by the formation of the and paleomagnetic data it is now established that three proto- Satpura Mountains of India and the Capricorn Orogen of Western w continental nuclei: “Ur” (central South Africa, India and Australia. The Satpura Mountain Belt developed at 1800 Ma Australia), “Nena” (Fenoscandia, Laurasia and Siberia) and when the amalgamation of the North Indian Block and the South “Atlantica” (South America and Northwest Africa) had stabilised by Indian Block took place during Proterozoic time (Mohanty, w2500 Ma (Rogers, 1996; Aspler and Chiarenzelli, 1998; Condie, 2010a). This is also the time when the Pilbara and the Yilgarn 2002; Piper, 2003). Several reorganisations during the Early Pale- Cratons of Western Australia collided to form the Capricorn oproterozoic possibly formed a supercontinent “Columbia” (Rogers and Santosh, 2002) during the time period 1900e1500 Ma (Fig. 1). Lack of good quality paleomagnetic data raises several alternative possibilities of the configuration of Columbia and its dispersal to form Rodinia during the worldwide Grenvillian orogenic cycle at w1100 Ma based on geological and geochronological data (Figs. 2, 3; Condie, 2002; Zhao et al., 2002, 2004). Therefore, the transition from Paleoproterozoic to Mesoproterozoic marks an important part of the earth’s history for our understanding of Paleoproterozoic supercontinent dynamics. Early Paleoproterozoic (2100e1900 Ma) tectonism and magmatism are restricted to South America, Africa (Doumbia et al., 1998; Hartmann et al., 1999), Canada (De et al., 2000), Baltic shield (Daly et al., 2001), Gawler craton (Daly et al., 1998), Western Australia, (Page, 1988; Windley, 1993; Sheppard et al., 2004), China and India. The correlation of some of these Paleo- proterozoic orogenic belts has the potential of generating a better picture of understanding the development of the Paleoproterozoic supercontinent Columbia. The Indian craton is divided into two blocks (the North Indian Block and the South Indian Block) by a prominent orogenic belt (the Satpura Orogen) with wENE-WSW trend in the central part of India. This orogen was earlier considered to be of Grenville (w1000 Ma) age (Bhowmik et al., 1999; Acharyya, 2001; Roy et al., 2006), and was subsequently revised to be of 1600e1500 Ma (Acharyya, 2003; Bhandari et al., 2011; Bhowmik et al., 2011). However, Mohanty (2003, 2010a) has questioned the basis of such an inference, and has shown that this mountain belt had the first orogenic imprint of w2100e1900 Ma and a second event at w1800 Ma. These orogenic trends and age data match with those of the Capricorn Orogen of Western Australia, when reconstructed for the configuration of Columbia (Zhao et al., 2002). Therefore, the formation Figure 1 Configuration of the supercontinent Columbia (modified and evolution history of these two orogenic belts have from Rogers and Santosh, 2002). S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267 243

Figure 2 Conﬁguration of the pre-Rodinia supercontinent Columbia (modiﬁed from Zhao et al., 2002).

Orogen. In this paper an attempt is made to synthesise the Pale- for 800e1000 Ma that comprises repeated basin formation, oproterozoic tectonic evolution of the Satpura Mountains and the magmatism and orogeny in the Wilson cycle of Paleoproter- Capricorn Orogen for understanding the events associated with the ozoiceMesoproterozoic age (Tyler and Thorne, 1990). Four discrete supercontinent Columbia. Paleoproterozoic orogenic events at 2215e2145 Ma (Opthalmian Orogeny), 2005e1960 Ma (Glenburgh orogeny), 1830e1780 Ma (Capricorn Orogeny) and 1680e1620 Ma (Mangaroon orogeny) 2. The Capricorn Orogenic Belt of Western and a single Mesoproterozoic to Neoproterozoic Edmundian Australia and its adjacent cratons orogeny (1070e755 Ma) have been recorded from the Capricorn Orogen (Cawood and Tyler, 2004; Sheppard et al., 2004, 2007). The Capricorn Orogen between the Archean Yilgarn and Pilbara The oldest identiﬁed rock in Australia is the Meeberrie Gneiss Cratons of Western Australia (Fig. 5) has a history of evolution (Myers and Williams, 1985), which yields igneous zircon ages

Figure 3 Conﬁguration of the Paleoproterozoic supercontinent (modiﬁed from Condie, 2002). 244 S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267

Figure 4 Configuration of the Paleoproterozoic supercontinental nuclei SIWA (modified from Mohanty, 2010b, 2011a). AFB Z Aravalli Fold Belt; BC Z Bastar Craton; CB Z Cuddapah Basin; NIB Z North Indian Block; SC Z Singhbhum Craton; SMB Z Satpura Mountain Belt; and NC Z Napier Complex. from 3750 to 3600 Ma (Kinny and Nutman, 1996; Pidgeon and Orogen, has abundance of medium-K I-type tonalite and granodi- Wilde, 1998). These oldest units constitute a part of the Narryer orite similar to Phanerozoic Andean-type batholiths (Sheppard Terrane on the northwestern margin of the Yilgarn Caton and the et al., 2004). The emplacement of this suite took place in a conver- southern margin of the Capricorn Orogen. Layered mafic intru- gent margin setting over a northwest dipping subduction zone which sions forming the Manfred Complex (Myers, 1988) have zircons gave rise to the collision of the Glenburgh Terrane and the Yilgarn as old as 4404 8Ma(Wilde et al., 2001). The Narryer Terrane is Craton (Sheppard et al., 2004). composed of granitic gneisses interlayered with minor amounts of Along the northern margin of the Yilgarn Craton occurs a belt metamorphosed banded iron formation (BIF), metasedimentary of (w700 km long and 100 km wide) Paleoproterozoic basins of rocks (cherts), mafic and ultramafic intrusions (Myers, 1988, 2200e1800 Ma age. Complex history of evolution of Yerrida, 1990, 1993; Pidgeon and Wilde, 1998). Prior to the deposition Bryah, Padbury and Earaheedy basins is not completely resolved, of supracrustal rocks of Jack Hills greenstone belt the terrane had but possibly includes an intracratonic sag, collision and accretion deformation, amphibolite-granulite facies metamorphism and of juvenile crust and orogenic uplift. granitic magmatism at w3300 Ma and further felsic magmatism The Rudall Complex located along the northern margin of the at w3100 Ma. Widespread intrusions of Neoarchean monzonite West Australia craton is characterized by a medium pressure granites, deformation and amphibolite facies metamorphism took metamorphism (12 kPa, 800 C), which took place during the place between 2750 and 2600 Ma (Myers, 1990, 1993; 2654 7 collision of the West Australian craton and the North Australia and 2643 7 Ma age by Pidgeon and Wilde, 1998). A number of craton ca. 1790 and 1765 Ma (Yapungku orogeny; Betts and Giles, granite-greenstone complexes constitute a major part of the 2006; Betts et al., 2008). Archean succession of the Yilgarn and Pilbara Cratons. The Glenburgh Terrane (w2540e2000 Ma) was accreted to the Yilgarn Craton during the Glenburgh orogeny (w2005e1960 Ma; 3. The Satpura Orogenic Belt of India and its Occhipinti et al., 2004). The Capricorn Orogeny (1830e1780 Ma) adjacent cratons produced dextral transpressional structures at greenschist facies conditions (Occhipinti and Reddy, 2004) in the Glenburgh Terrane The Satpura Orogen of Central India is a Proterozoic mountain belt that and the Narryer Terrane. The Dalgaringa Supersuite, a dominant has amalgamated the Bundelkhand protocontinent in the north India component of the Glenburgh Terrane in the Southern Capricorn (NIB) and the Deccan protocontinent (SinghbhumeBastareDharwar) S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267 245

Figure 5 Terrane elements of the Western Australian Shield juxtaposed with the Eastern Indian and Central Indian Shields for reconstruction of SIWA. AB Z Ashburton Basin; B Z Bryah Basin; BC Z Bastar Craton; CB Z Cuddapah Basin; CGC Z Chhotanagpur Gneissic Complex; COB Z Collier Basin; D Z Dumka; EB Z Edmund Basin; EGF Z Eastern Goldﬁelds; EHB Z Earaheedy Basin; GC Z Gascoyne Complex; GT Z Glenburgh Terrane; J Z Lake Johnson; M Z Murchison; N Z Narryer Gneiss; OFB Z Opthalmian Fold Belt; P Z Padbury; SC Z Southern Cross; SG Z Singhbhum Granite; SW Z South West; T Z Toodyay Lake Grace; VB Z Vindhyan Basin; Y Z Yeelirrie; and YB Z Yerrida Basin.

in the south (SIB). The structural trend of the lithological units and their orogenic belts have a complex evolutionary history through multiple dominant fabric are wE-W, referred as “Satpura Trend”. The orogen cycles. The comparative evolution pattern will be analysed in this paper continues eastward on to the Chhotanagpur plateau and the Meghalaya to explain their role in global supercontinent assembly. (Shillong) plateau (Fig. 5). The composite Satpura orogenic trend was reported to extend into the AlbanyeFraser orogenic belt of Western 3.1. The western domain of the Satpura Mountains Australia in the supercontinent assembly of Rodinia (Harris, 1993). Mohanty (2010a) has carried out critical analysis of the recent studies The western domain of the Satpura Orogen is represented by the in the Satpura Orogen and has shown that the Satpura Orogen is Satpura Mountains of Central India. Although the axial regions of correlatable with the Capricorn Orogen of Western Australia. Both the the Satpura Mountains are occupied by the Deccan Traps of 246 S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267

CretaceouseTertiary age, the flanking regions on the north and The Sausar belt adjoining the Satpura Mountains consists of an south and several inliers in the axial region have Precambrian Archean basement complex (Tirodi Gneiss) overlain by a volcano- rocks with dominantly E-W to ENE-WSW trend, referred as sedimentary succession of Paleoproterozoic age containing “Satpura Trend” in Indian geological literature. Banded Iron Formation (BIF) and Banded Manganiferous The northern flank of the Satpura Mountains is occupied by the Formations (BMF) exposed in three basins: Sausar, Betul and Mahakoshal belt of Paleoproterozoic age and its Archean basement Harda. The basement and cover succession were affected by three (Sidhi Complex and Dudhi Complex). The northern boundary of phases of Proterozoic regional deformations and low- to medium- these rocks is marked by a regional fault (Sone-Narmada fault) grade metamorphism (Mohanty, 1988, 1993, 2010a; Mohanty and which separates the Vindhyan Range of Paleoproterozoic to Neo- Mohanty, 1996; Mohanty et al., 2000). Two belts of granulite proterozoic age, GwalioreBijawar Groups and the Bundelkhand facies metamorphism are present on either side of the low-grade Complex on the northern side from the Precambrian Terranes of the rocks of the Sausar belt: Ramakona Granulite Belt on the north Satpura Mountains (Fig. 6). The evolution of this northern domain is and the BhandaraeBalaghat Granulite Belt in the south. The linked to the evolution of the Satpura Mountains, during the basement gneisses have Archean ages (cf. Sm-Nd age of amalgamation of the NIB and SIB and in the subsequent phases of 2325e2494 Ma for the Tirodi Gneiss, Ahmad et al., 2009; U-Pb evolution (Table 1). The Bundelkhand Complex has TTG suite of zircon ages of 2378 17 and 2432 5 Ma of the Amgaon Gneiss, rocks of w3500 Ma age and younger components of Archean age Ahmad et al., 2009; and 2478 9 Ma Re-Os age by Stein et al., up to w2500 Ma. The Mahakoshal Group, the Bijawar Group and 2004; 2480 3 Ma U-Pb zircon age by Panigrahy et al., 2002 the Gwalior Group were deposited in different basins of the Bun- reported for the Malanjkhand Granite). The unconformable rela- delkhand Craton during Early Paleoproterozoic. The amalgamation tionship between the Tirodi Gneiss and the Sausar Group is of the Bundelkhand Craton and the associated Paleoproterozoic marked by the presence of polymictic conglomerates at the basins with the southern domain of the Bastar Craton took place in contacts of the two units (Mohanty, 1993). Granites and migma- two/three phases: Mahakoshal/Sausar Orogeny (2100e2200 Ma tites later than the Sausar Group have two age clusters. The and 1950e2050 Ma) and Satpura Orogeny (1750e1850 Ma). The earliest of these were developed syn-kinematically with the first amalgamation was followed by the deposition of the Vindhyan deformation of the Sausar Group and have 2100e2200 Ma ages Supergroup during several cycles of basin opening and closing (e.g., 2106 Ma Sm-Nd age for Tirodi Gneiss by Ahmad et al., (Table 1). 2009; 2170 70 Ma Rb-Sr age for the thermal overprint on the The southern flank of the Satpura Mountains is occupied by the Amgaon Gneiss reported by Sarkar et al., 1981 and Sausar belt, the Amgaon belt and the Bastar Craton (Fig. 7). The 2199 178 Ma Rb-Sr age for the Malanjkhand pink granite Bastar Craton and the Amgaon belt have evolutionary history determined by Panigrahy et al., 1993). The later granites and from w3500 Ma to the end ArcheaneEarly Paleoproterozoic. migmatites have ages between 1618 and 1415 Ma (U-Pb zircon Several generations of granites, gneisses and migmatites and age of 1618 8 Ma reported for Tirodi Gneiss by Bhowmik et al., associated metamorphism have created difficulty in establishing 2011; 1553 19 Ma U-Pb zircon age for metamorphism of Tirodi the stratigraphic relations in this region (Table 1). Gneiss suggested by Ahmad et al., 2009; 1525 70 Ma Rb-Sr age

Figure 6 Geological units on the northern margin of the Satpura Orogen. Table 1 Proterozoic events stratigraphy of the Satpura Mountain Belt (India), the Capricorn Orogen (Western Australia), and adjacent cratons. Time (Ma) Western Domain (South) Western Domain Eastern Domain (North) Eastern Domain (South) Northeast Domain Western Australia (BastareSausar) (North)(Bundelkhande (Chhotanagpur) (Singhbhum) (Shillong Plateau) Mahakoshal) 500e550 Mafic dykes of Boyagin dyke swarm Arunachal Arunachal biotite granite (non-foliated) 500 19 (E-1) Thermal imprint on Sonapahar metapelites 500 14 (E-2) Nongpoh Granite 241 (2012) 3(3) Frontiers Geoscience / Mohanty S. 550 15 (E-3) 550e600 Upper Bhander Subgroup: D4 of Shillong Pinjarra Orogeny: 540e590 siliciclastics and carbonate Group (W-1) Centralian Superbasin Sequence 3 þ 4 600e750 Thermal imprints on Khasi Granite Mundine Well dyke swarm: Bundelkhand mafic dykes 690 19 (E-3) 755 3 (W-2) 692 11, 711 17, 715 7, Mylliem Granite 729 11, 753 6 (B-1) 607 13 (E-4) Goalpara Granite 647 122 (E-5) 750e800 Lower Bhander Subgroup: Edmundian Orogeny siliciclastics and carbonate Ends w750 (W-3) Centralian Superbasin Sequence 1 800e1000 Low intensity deformation Thermal imprints on Munger Orogeny Ends Thermal overprint on Low intensity Edmundian Orogeny: e of Sausar Group (SD3) Majhgawan kimberlite MD2 of Munger Group Barabazar granite deformation of 1075e750 (W-3) 267 Thermal imprints on Sausar 974 30 (B-2) KD3 of Kodarma Group 971 58 (D-1) Dirang Formation amphibolite 834 21, Raigarh Granite II D2 of Shillong Group 929 85 (A-1); 830 90, (Kunkuri) 972 114 (C-1); Sindhuli Granite 847 65, (A-2); 803 49, 815 47, 881 39 (E-6) metamorphic overprint on 1005 51 (C-2) Sausar metasediments Sushina Nepheline Syenite w950 Ma (A-3) 922 10 (C-3) Bhandara granulite ITD and Post-CD3eCM4 800 171, 967 72, thermal overprint on Bengal 973 63 (A-1) Anorthosite 947 27 Betul Granite II (C-5); metapelites (Navegaon) 850 15 950 20; 995 24 (C-6); (A-4) 818 11, 825 26, 247 (continued on next page) 248 Table 1 (continued) Time (Ma) Western Domain (South) Western Domain Eastern Domain (North) Eastern Domain (South) Northeast Domain Western Australia (BastareSausar) (North)(Bundelkhande (Chhotanagpur) (Singhbhum) (Shillong Plateau) Mahakoshal) 981 26 (C-7); 921 18 (C-8); foliated granite 967 11, 992 11, 977 15, 1021 26 (C-7); 928 23, 923 3 (C-8), 910 9, 944 9, 945 17 (C-9) 1000e1075 Low intensity deformation Thermal imprints on Munger Orogeny MD1 Thermal overprint on Low intensity Edmundian Orogeny .Mhny/Gocec rnir ()(02 241 (2012) 3(3) Frontiers Geoscience / Mohanty S. of Sausar Group (SD3) Bundelkhand mafic dykes KD2 of Kodarma Group Arkasani Granophyre deformation and low- begins w1075 (W-3) Thermal imprints on Sausar 1002 39, 1062 87 (B-1) CD3 deformation of CGC 1052 84 (D-2) grade metamorphism of amphibolite 1009 18 (A-1) Purulia Granite 1071 64 Ekma granite (Gangpur) Shillong Group/Dirang (C-10) ITD; Mica belt 1025 11 (D-3) Formation granite III (Meromako) Thermal imprint on 1021 46 (C-11); Gumla Sonapahar metapelite granite 1051 272 (C-1); 1078 31 (E-2) Marme granite 1065 74 Granite (biotite augen (C-12) gneiss) intrusion into ITD e M3 thermal resetting Dirang Formation (?) age of Ranchi Granite 1025 36, 1072 17 (C-8); metapelite 1009 24 (C-8) Chhatisgarh Supergroup Rewa Formation: Munger Group: Deposition (?) of Dirang Bangemall Supergroup Conglomerate, felsic flows, Conglomerate, black/gray Formation (Arunachal) 1070 6 (W-4) tuffs, shale and quartzite, and soft shale volcaniclastics (phyllite) e 267 1075e1200 Dolerite dykes in Sausar Decompression event: Meta-dolerite dykes, ITD Newer Dolerite-VII w1069 Khasi Greenstone: Warakurna LIP mafic Group 1116 58, Kimberlite intrusion path of MPR granulite belt (D-4), 1100 200 (D-5) Mafic intrusions intrusion and dykes 1112 77 (A-2) Majhgawan pipe 1073 14 Rapakivi granites Thermal imprints on Anatectic event/ w1078 (W-5) Expansive granite intrusion (B-3); 1067 31 (B-4), Expansive granite intrusion metapelites 1149 46 migmatisation Albany-Fraser Orogeny II: Nainpur-Lalbara (Mandla) 1044 22 (B-5); 1140 12 Jajawal Granite 1100 20 (D-6) 1150 26 (E-7) 1214e1140 Ma granite 1147 16 (A-5) (B-6); 1120 45 (B-2) (C-13); Chianki granite (1154 15 Ma) (W-6) Hinota pipe 1170 45 (B-2) 1119 24 (C-12), Raigarh diorite 1138 193 (C-13); alkali syenite 1054 104 (C-1); Thermal imprint on metapelite of CGC 1176 9 (C-7), 1168 53 (C-14), 1190 26 (C-15); Purulia Migmatites ITD 1178 61 (C-10) Chhatisgarh Supergroup Upper Kaimur Subgroup: Munger Group: Quartzite, Dirang Formation Deposition of Collier/ sandstone, shale and ferruginous hard shale, and (Arunachal): Salvation Group volcaniclastics mafic flows (amphibolite?) Conglomerate, (1200e1100) (W-3) quartzite, limestone and shale 1200e1300 Dolerite dyke (intruding Dolerite (amphibolite) Newer Dolerite-VI Marnda Moorn LIP: Abujhmar Group, Bastar) dykes 1241 25, 1264 25 w1210 (W-7) 1229e1259 (A-6) Mica belt granite II (D-5, D-7) Crustal extension: Fraser Decompression (intrusion of 1238 33, 1284 409 Thermal imprints on dike swarm 1212 10 241 (2012) 3(3) Frontiers Geoscience / Mohanty S. gabbro) in BBG 1422 104 (C-11) metapelites 1241 25 (W-8); Darling range dyke (A-1) Binda granite 1242 34 (D-6) swarm 1214 5 (W-9) (C-15); Thermal imprints on metapelites 1272 35 (C-14); 1270 19 (C-8); granite 1239 66 (C-8) 1300e1450 Thermal resetting ages of Bundelkhand mafic dykes Post-CD2 granites: Raigarh Syn-S3 greenschist facies Norite enclave of Khasi Deformation of Edmund mafic granulites of Bhandara 1407 11 (B-1) I M3 of Dalma w1300 Ma batholith 1462 Ma (E-8) Group: 1400e1220 (W-3) Craton 1403 99, Nagam granite 1331 42 (D-8) Thermal imprint on Albany-Fraser Orogeny I: 1407 11, 1408 81, (C-12); Thermal imprints Thermal overprint on soda Sonapahar metapelite 1345e1260 (W-6) 1416 59 (A-2); 1450 9 on CGC 1305 74, granite 1420 17 (D-9); 1472 38 (E-2) Deformation, granulite (1437e1501) 1442 80 (C-14); Chandil tuff 1484 44 facies metamorphism (A-7); Terminal metamorphic 1333 27, 1435 26 (C-8) (D-10) (1321 11 Ma) (W-6) event of Sausar Group 1480 9 (C-9) Ankro felsic volcanics 1415 23 (A-8); Tirodi 1487 34 Gneiss (?) 1454 5 (A-9); (D-11) Amgaon Gneiss (thermal e

resetting) age 1450 50 267 (A-10) 1450e1500 Chhatisgarh Supergroup Lower Kaimur Subgroup: Munger Group: Quartzite, Shillong Group (?): Deposition of Edmund/ conglomerate, sandstone, ferruginous hard shale, and Conglomerate, shale Scorpion Group shale, volcaniclastic, felsic mafic flows (amphibolite?) and carbonaceous shale flow and tuff 1550 (E-9) 1500e1600 SD2b deformation, Syn-MD3 granite (Dudhi) Chhotanagpur/Simultala Syn-D2 M2 of metapelites Ziro high-Ca granite Basic dyke 1600 Ma amphibolite facies 1576 76 (B-7) Orogeny KD1b of Dalma w1520 Ma 1536 60 (E-10) metamorphism 1525 70 Bundelkhand mafic dykes Syn-CD2 Dumka granulite (D-8); metamorphic Thermal imprint on (A-11); Sausar granulite 1491 29, 1585 58, 1331 125 (C-10) and imprints on Chaibasa mafic rocks of Garo 1553 19; 1569 15, 1587 11, (B-1) Dumka syenite 1457 63 metabasics 1546 46 Hills 1596 15 (E-2) 1577 89 (A-9), (C-10) (D-12) (Peak of monazite age metamorphic overprint on Mor valley hypersthene Newer Dolerite-V 1500e1650) (E-2)

(continued on next page) 249 250 Table 1 (continued) Time (Ma) Western Domain (South) Western Domain Eastern Domain (North) Eastern Domain (South) Northeast Domain Western Australia (BastareSausar) (North)(Bundelkhande (Chhotanagpur) (Singhbhum) (Shillong Plateau) Mahakoshal) Tirodi Gneiss 1534 15 granite 1522 71 (C-16); 1540 16 (D-7) (A-9), 1584 17 (A-12), charnockite 1489 67 1572 7 (A-12); spot (C-16); granulites chemical ages of monazite 1515 5 (C-17) rims in BBG 1525 13 Bengal Anorthosite (A-7); 1582 13; 1603 12 1550 12 (C-18); Mica (A-13); UHT; M4 overgrowth belt granite I 1590 30 of monazite 1238e1654 (C-15); Makrohar granulite (A-7) 1700e1580 (N-31); Mor 241 (2012) 3(3) Frontiers Geoscience / Mohanty S. Betul granite I (Morkha) Valley migmatite 1580 33 1550 50 (A-4) (C-19) CGC metapelite 1547 18 (C-9) Semri Group (Upper): Kodarma Group (Upper): Shillong Group: (?) Deposition of Edmund/ sandstone, limestone, shale Quartzite, carbonaceous Conglomerate, shale Scorpion Group 1640 (W-3) and felsic tuff shale, shale, amygdular and carbonaceous shale Limestone 1599 48 (B-8) flow and felsic tuff Tuff 1602 10 (B-9) 1600e1750 Tirodi Gneiss 1603 23, Bundelkhand mafic dykes Chhotanagpur/Simultala Dalma Orogeny BD2b deformation Mangaroon Orogeny 1620 1618 8 (A-12); Dongargarh 1613 80, 1670 11, Orogeny KD1b SD2 deformation; Syn-S2 Ziro biotite granite e1670 (W-10) granite (thermal imprint) 1680 20, 1713 267, CD2 folding, medium amphibolite facies M2; gneiss 1644 40, Durlacher Supersuite 1640 60 (A-14) 1721 3, 1733 34 (B-1) pressure, high T, Thermal imprint on Soda 1676 122 (E-1) granites 1620e1670 (W-10) Majhgaon Kimberlite 1630 amphibolite facies Granite 1633 6, Migmatisation/ (B-10) Kersentite 1610 55 metamorphism IBC 1677 11 (D-13); Arkasani Patharkang granite (B-11); Barambaba granite Hypersthene gneiss of Mor granophyre 1721 142 1714 44 (E-8) 1690 70 (B-11); Mirgarani Valley 1624 5 (C-17); (D-14); 1677 80 (D-15); Tonalite of Dinajpur e 267 granite 1635 67 (B-12); Post peak IBC low-K metapelites 1617 41 1722 6 (E-11) Rihand granite 1731 36 Tholeiite dike Kirwil- (D-6) (B-7); Muirpur granite Sagobandh 1648 112 Gabbro-pyroxenite 1709 102 (B-7); Dubha (C-20); Thermal imprint on intrusion in Dalma granite 1754 16 (B-13) CGC 1691 69, 1720 31 1619 38 (D-16) (C-21); 1649 13 (C-8); Kuilapal Granite in Dalma Hazaribagh granite volcanics 1638 38 (D-17) 1718 102 (C-22) Semri Group (Lower): Kodarma Group (Middle): Dalma Group (Upper): Shillong Group: Pooranoo Metamorphics: Foreland basin deposition of Quartzite, carbonaceous Pillow basalt, volcaniclastic Conglomerate, shale Coarse clastics and flood shale-limestone; felsic shale, shale, amygdular conglomerate, komatiitic and carbonaceous shale basalts 1680 13 (W-10) volcanics 1631 5 (B-14); flow and felsic tuff vitric tuff and rhyolite Foreland basin deposition 1628 8 (B-9); limestone Chandil rhyolite 1629 5 (Yerrida Basin) 1721 90 (B-8); coarse (D-19) clastics 1750e1850 Mafic dyke (BD2) of Bastar Sidhi Trachyte 1789 50 Chhotanagpur/Simultala Dalma Orogeny BD2a deformation, Capricorn Orogeny 1776 13 (A-15) (B-11); Sidhi Alkali gabbro Orogeny KD1a M1 (pre-S2) High-grade porphyritic and biotite 1780e1830 (W-11) Satpura Orogeny (MD2); 1760 43 (B-11); Bari CD1b deformation, granites, metamorphism; granite Greenschist facies SD2a; Spot chemical ages syenite 1800 55 (B-11); migmatisation, and Kuilapal Granite 1863 80 metamorphism of monazite cores in BBG Jhirgadandi granite granulite event; Daltonganj (D-20); 1718 40 (D-21) Moorarie Supersuite 1794 44 (A-13) 1813 65 (B-7); 1860 180 granite 1741 65 Ma Romapahari (Mayurbhanj- granites 1780 e1810 (B-15); Sidhi granite (C-22); Barra Bazar granite II) granite 1895 46 (W-12) 1850 40 (B-7); 1771 210 (C-23); (D-22) Bundelkhand mafic dykes Tatapani gray migmatite 1795 50, 1844 8 (B-1) 1787 72 (C-24); CGC gneiss 1870 74 (C-14) e 1850 1900 Mafic dykes of Bastar Gwalior/Bijawar Group Kodarma Group (Lower): Dalma Group (Lower): Deposition of Earaheedy/ 241 (2012) 3(3) Frontiers Geoscience / Mohanty S. (BD2) 1883 2; (Upper): Siliceous- Conglomerate, quartzite, Mafic and ultramafic flows, Blair Basin 1891 1 (A-16) ferruginous shale, chert, BIF, clacitic/dolomitic vitric tuff, shale and Upper Yerrida/Wyloo limestone, tuffaceous limestone, BIF, shale, mafic carbonaceous shale Basin sandstone with 5 basaltic volcanics, and felsic tuff Chlorite schist of Dalma flows. Gwalior Traps (? Sillimanite schist) w1825 Ma (D-8) 1830 200 (B-6); 1854 7 (B-17); Kurrat Lava 1691 180 (B-16); Dargawan mafic rocks 1789 71 (B-16); Hindoli Tuff 1729 23; 1854 7 (B-17); Sediments 1800 (B-18); Bundelkhand mafic dykes 1863 9, 1895 8 (B-1) 1900e1950 Post-SD1 Harda granite Gwalior Group (Lower): Intrusion of ultramafic Newer Dolerite-IV Bomdila augen gneiss Basic dyke 2000e1600 1856 68 (A-17) Conglomerate, phosphoritic and mafic bodies 1960 40 (D-4); Gabbro- 1914 25 (E-10) Post-orogenic granite e

dolomite, shale and basic CGC metapelites Anorthosite-Ultramafics Meta-ultramafic bodies (1945e1950) (W-12) 267 volcanic 1925 110 (C-8) Detrital core of monazite and dykes Deposition of Padbury Bundelkhand mafic dykes 1906e2085 (D-8) foreland basin: 1960 1918 6, 1939 17, Dalma Group (Lower): (W-3) 1939 30 (B-1) Mafic and ultramafic flows, vitric tuff, shale and carbonaceous shale 1950e2000 Sausar Orogeny II Mahakoshal Orogeny II CD1a deformation, Singhbhum Orogeny-IIb BD1bdeformation Glenburgh Orogeny granites, migmatisation, Mayurbhanj granite e I 2005e1960 (W-12) and granulite event (?) 2084 74 (D-23) High-grade metamorphism Newer Dolerite-III D2,M2 1956 9 (W-12) 2004 35; 2068 38 Dalgarina supersuite (D-5) intrusions w1975 (W-12)

(continued on next page) 251 252 Table 1 (continued) Time (Ma) Western Domain (South) Western Domain Eastern Domain (North) Eastern Domain (South) Northeast Domain Western Australia (BastareSausar) (North)(Bundelkhande (Chhotanagpur) (Singhbhum) (Shillong Plateau) Mahakoshal) Basic dyke 2000 2000e2030 SD1b deformation; M1 UHT Mahakoshal Orogeny II: Singhbhum Orogeny-IIa Glenburgh Orogeny D1, EPMA age of monazite rim MD1 SD1b; Soda granite II High-grade metamorphism in felsic granulite 2299-1924, 2017 (D-13) M1 2003 8; 1997 8 average 2040 17 (A-7); (W-12) monazite core 1995-2104, average 2048 14 (A-7) 2030e2100 Chilpi Group: conglomerate, Mahakoshal Group (Upper): Deposition of protoliths Kolhan Group w2100 Tenga Formation of EGP Kimberlite 2025 10 .Mhny/Gocec rnir ()(02 241 (2012) 3(3) Frontiers Geoscience / Mohanty S. slate, quartzite, greywacke Conglomerate, coarse arenite, of pelitic schists and Coarse clastics, carbonate, Bomdila Group: (W-13); Rifting: eruption and limestone purple shale, carbonate, gneisses (?) shale Deposition of of Narracoota Volcanics High-Mg mafic dyke of porcellanite and basaltic Dhalbhum Group: siliciclastics, mafic Deposition of Bryah Basin Bastar 2100 11 (A-18) flows Quartzite, and mica schist. volcanics, and thick 2100 Ma Pb-Pb model age Newer Dolerite-II carbonate of galena (B-18); 2105 38; 2144 39 Bundelkhand mafic dykes (D-5, D-7) 2063 45 (B-1) 2100e2250 Sausar Orogeny I Mahakoshal Orogeny I Singhbhum Orogeny I: Singhbhum Orogeny I Deformation BD1a Opthalmian Orogeny (amalgamation of NIB and (amalgamation of NIB metamorphism and SD1a; Soda granite I Metamorphism of felsic 2215e2145 (W-14) SIB): SD1a deformation and and SIB) migmatisation 2220 54 (D-13) gneiss of Meghalaya Deposition of Lower migmatisation; Tirodi Gneiss Amalgamation of Chaibasa Group: 2230 13 Ma (E-12) Yerrida/Wyloo Basin: II 2106 Ma (A-19); Bastar Singhbhum Craton and Polymictic conglomerate, 2200e2100 (W-3) granite 2095 118 (A-20); Chhotanagpur Craton mafic tuffaceous rocks, Paliam-Darba granite kyanite quartzite, 2275 80 (A-21); Burugum amphibolite, magnetite granite 2237 70 (A-21); quartzite, and mica schist Amgaon Gneiss (thermal Detrital core of monazite e 267 imprint) 2170 60 (A-10); 2202e2316 (D-8) Bijli rhyolite (thermal Jagannathpur volcanics imprint) 2180 25 (A-10); 2250 81 (D-24) Dongargarh granite 2270 90 (2222) (A-10); Malanjkhand granite II 2243 217; 2106 102 (A-22); Malanjkhand pink granite 2199 178 (A-22); Abujhmar metalava (thermal imprint) 2217 38 (A-23); BBG monazite 1958-2208, average 2086 16 (A-7); 1970e2177, average 2089 14 (A-7) 2250e2400 Sausar Group: siliciclastics, Mahakoshal Group (Lower): Deposition of siliciclastic, Koira Group: Coarse Khetabari Formation of Turee Creek Group: volcanics, glacial diamictite, Deposition of BIF-bearing carbonate and calcareous- clastics, glacial diamictite? Bomdila Group: 2200e2445 (W-15) carbonate, Mn-bearing volcano-sedimentary units argillaceous sediments dolomite, chert, black shale, Deposition of Deposition of siliciclastics, clastics BIF and Mn-bearing siliciclastics, felsic and BIF, glacial diamictite and TDM (Hf) age of juvenile clastics mafic volcanics, evaporites 2449 3 (W-16) source of Tirodi Gneiss (?) carbonate, carbonaceous 2379 Ma (A-24); TDM and graphitic sediments (Sm-Nd) 2118e2503 Ma (A-25) 2400e2600 Amgaon gneiss 2378 17; Bundelkhand Mafic dykes Newer Dolerite-I Widgiemooltha dyke 2432 5 (A-9); 2549 (A-19); 2420 77 (B-1); 2613 177 (D-25) 2410 2 (W-17); e Tirodi gneiss I 2325 2494 Bundelkhand granite TDM (Sm-Nd) age of Jimberlana dyke 2411 5 241 (2012) 3(3) Frontiers Geoscience / Mohanty S. (A-19); Dongargarh granite 2492 10 (B-19), juvenile source of Soda (W-18); 2465 22 (A-26); Bundelkhand Diorite granite 2460e2610, Deposition of Hamersley Malanjkhand Grey Gneiss 2563 6 (B-19); average 2520 Ma (D-26); Group 2445e2630 (W-15) 2405 63 (A-22), Bundelkhand Gneiss Nilgiri granite 2366 126 Malanjkhand granite I 2467 22 (B-20) (D-22); 2467 38 (A-22), 2478 9, Dhanjori-Simlipal Group 2477 10 (A-27); 2490 8 (Upper) (auriferous) (A-28); Katekalyan Conglomerate, arkose, migmatite (Bengpal) mafic-ultramafic volcanics, 2530 89 (A-17) basaltic flows (pillowed), Markampara Granite and BIF 2480 3 (A-29) Abujhmar/Sonakhan Group (auriferous): Coarse clastics, volcanics, and BIF Maspur Trap 2490 48 (A-30) e

2600e2700 Bailadila Orogeny: Granulite Jabalpur Metabasalt Granulite grade Newer Dolerite-I Granulite grade Granulite metamorphism of 267 metamorphism and 2686 83 (B-21); Bijawar metamorphism and 2613 177 (D-25) metamorphism and Narryer Terrane 2654 7 migmatisation of basement Dolerite Dyke 2780 365 migmatisation migmatisation (W-19) gneisses 2672 54 (A-2) (2721) (B-6) CGC metapelites Granitoid intrusion of 2569 18 (C-8) Yilgarn Craton 2620e2750 (W-12) 2700e2900 Bailadila/Sakoli Group: Bundelkhand Gneiss Dhanjori-Simlipal Group Older Metamorphic Granite Greenstone Coarse clastics, volcanics, 2733 30 (B-20); (Lower) (auriferous) Group of Meghalaya: successions (Fortescue and BIF 2780 64, 2785 49 QPC, Coarse clastics, felsic quartz-sillimanite Group): (auriferous) (B-22) volcanics, mafic/ultramafic schist, calc-silicate, 2630e2775 (W-15) flow, and tuffaceous amphibolite and BIF Komatiitic basalts, felsic phyllite Felsic gneiss volcanics, BIF, clastics, 2787 270 (D-27) 2637 55 Ma (E-12) dolomite, turbidite

(continued on next page) 253 254 Table 1 (continued) Time (Ma) Western Domain (South) Western Domain Eastern Domain (North) Eastern Domain (South) Northeast Domain Western Australia (BastareSausar) (North)(Bundelkhande (Chhotanagpur) (Singhbhum) (Shillong Plateau) Mahakoshal) 2858 17 (D-24); Se La Group Tamperkola granite (Arunachal): Quartzite, 2809 12 (D-28), acid kyanite-sillimanite- volcanics 2822 67 (D-28) staurolite gneiss, calc- silicate, marble, mafic and felsic gneiss 2900e3050 Amgaon Gneiss 2709, 2862, De Grey Supergroup 2974 Ma (A-19) 2930e3020 (W-20) .Mhny/Gocec rnir ()(02 241 (2012) 3(3) Frontiers Geoscience / Mohanty S. 3050e3200 Amgaon/Bengpal Orogeny Fundamental Gneiss: Iron-Ore Orogeny Pinsep Orogeny: Elizabeth Sukma Granite III Tonalite gneiss and Mayurbhanj granite Hill granites (Ambhibole/Biotite granite) granulites 3080 8, 3092 5 (D-29) Soansville Group: 3018 61 (A-31) SBG e III 3130 28 3000e3200 (W-21) Amgaon Gneiss 3072, 3106, (D-30); Bonai granite II 3396 Ma (A-19) 3163 126 (D-31) 3200e3350 Granulite metamorphism Bundelkhand Gneiss Metamorphism of OMG Sulphur Springs Group: Mafic dykes (amphibolite) 3270 3 (B-19) and OMTG 3244 6, 3240 Ma (W-21) TDM (Hf) model age of 3241 7 (D-29); Deformation (D3); juvenile source of Tirodi Epidiorite; Champua Granulite metamorphism Gneiss (?) 3218 (range amphibolite 3305 56 3300e3350 (W-22) 3051e3630) Ma (A-24) (D-31) Kelly Group: 3315e3350 Kaptipada granite (W-21) 3292 51 (D-32), 3294 50 (D-33) SBG-II 3302 13 (D-19); Bonai granite I 3328 7 (D-29); 3308 38 (D-33); e 267 3369 57 (D-31); 3380 6 (D-31) 3350e3500 Bengpal/Amgaon Group: Iron-Ore Group (IOG-I) Deposition of sediments, Fine clastics, BIF, dolomite, Fine clastics, BIF, dolomite, greenstone and ovoid volcanics, Coarse clastics volcanics, Coarse clastics granites (Pilbara Craton): Dacite lava of Daitari coarse clastics, BIF, pelite; 3508 2 (D-34) Basic/ultramafic dykes Older Metamorphic Group Warrawoona Group: (OMG): xenoliths 3520e3427 (W-21) 3369 57 (D-32), amphibolite 3378 98 (D-31), 3420 9 (D-29) Sukma Granite II (K-rich) Singhbhum Granite-I Dugel Gneiss 3509 14 (A-29) (SBG-I) Tonalite gneiss (syenogranite) 3400 (W-22) 3437 9 (D-29) Deformation (D2) >3500 Sukma Gneiss: Sukma Babina TTG Gneiss Older Metamorphic Meeberrie Gneiss w3680 Granite I (TTG) High-grade 3503 99 (B-23) Tonalite Gneiss (OMTG): (W-22) gneisses 3561 11 (A-32); TTG basement 3457 35 Deformation (D1) 3585 10; 3582 4 (A-33); (D-29); 3715 73 (D-35); Manfred Complex w3780 Markampura TTG Gneiss 3775 85 (D-36) (W-22); Zircon 4404 8 3511 155 (A-34) (W-23) References for age data Western Domain (South) A-1: Rb-Sr internal isochron age Roy et al., 2006; A-2: Sm-Nd internal isochron age Roy et al., 2006; A-3: Ar-Ar cryptomelane age Lippolt and Hautmann, 1995; A-4: Rb-Sr age Mahakud et al., 2000; A-5: Rb-Sr WR age Pandey et al., 1998; A-6: K-Ar age Sarkar et al., 1986c; A-7: EPMA monazite age Bhowmik et al., 2005; A-8: Monazite spot age Bhowmik et al., 2011; A-9: U-Pb zircon age Ahmad et al., 2009; A-10: Rb-Sr age Sarkar et al., 1981; A-11: Rb-Sr WR age Sarkar et al., 1986a; A-12: SHRIMP U-Pb zircon age Bhowmik et al., 2011; A-13: Monazite spot

age Bhandari et al., 2010; A-14: Rb-Sr WR age Sarkar et al., 1991; A-15: U-Pb age Srivastava et al., 2000; A-16: U-Pb baddeleyite age French et al., 2008; A-17: Rb-Sr WR age Bandyopadhyay 241 (2012) 3(3) Frontiers Geoscience / Mohanty S. et al., 1990; A-18: U-Pb baddeleyite age French, 2007; A-19: Sm-Nd age Ahmad et al., 2009; A-20: Rb-Sr WR age Sarkar and Gupta, 1990; A-21: Rb-Sr WR age Pandey et al., 1989; A-22: Rb-Sr WR age Panigrahy et al., 1993; A-23: K-Ar WR Sarkar and Gupta, 1989; A-24: TDM (Hf) age Bhowmik et al., 2011; A-25: TDM (Sm-Nd) age Mishra et al., 2009; A-26: Rb-Sr WR age Krishnamurthy et al., 1988; A-27: Re-Os age Stein et al., 2004; A-28: U-Pb zircon age Panigrahy et al., 2002; A-29: U-Pb zircon Sarkar et al., 1993; A-30: Rb-Sr WR Sarkar and Gupta, 1989; A-31: Pb-Pb age Sarkar and Gupta, 1989; A-32: U-Pb zircon age Ghosh, 2004; A-33: U-Pb zircon age Rajesh et al., 2009; A-34: Pb-Pb WR age Sarkar et al., 1993 Western Domain (North) B-1: Ar-Ar age Mallikharjuna Rao et al., 2005; B-2: K-Ar age Paul et al., 1975; B-3: Ar-Ar phlogopite age Gregory et al., 2006; B-4: Rb-Sr Phlogopite age Smith, 1992; B-5: Rb-Sr phlogopite age Anil Kumar et al., 1993; B-6: Rb-Sr WR age Crawford, 1970; Crawford and Compston, 1969; B-7: Rb-Sr WR age Sarkar et al., 1998; B-8: Pb-Pb WR age Sarangi et al., 2004; B-9: SHRIMP U-Pb zircon age Rasmussen et al., 2002; B-10: Rb-Sr WR age Paul, 1979; B-11: Rb-Sr age Jain et al., 1995; B-12: Rb-Sr WR age Pandey et al., 1998; B-13: Rb-Sr WR age Dhurandhar et al., 2003; B-14: TIMS U-Pb zircon age Ray et al., 2002; B-15: Rb-Sr WR age Pandey et al., 1995; B-16: Rb-Sr age Sarkar et al., 1997; B-17: U-Pb zircon Concordia age Deb et al., 2002; B-17: Rb-Sr WR age Sarkar et al., 1997; B-18: Pb-Pb model age of galena Hansen et al., 2003; B-19: SIMS Pb-Pb zircon age Mondal et al., 2002; B-20: Monazite spot age Saha et al., 2011; B-21: K-Ar age Jain et al., 1995; B-22: U-Pb discordia age Saha et al., 2011; B-23: Rb-Sr WR Sarkar et al., 1998 Eastern Domain (North) C-1: Rb-Sr WR age Pandey et al., 1998; C-2: Rb-Sr WR Singh et al., 1989; Singh and Krishna, 2009; C-3: SHRIMP U-Pb zircon age Mazumder et al., 2010; C-5: ID-TIMS U-Pb zircon lower discordia age Chatterjee et al., 2008; C-6: ID-TIMS U-Pb monazite age Chatterjee et al., 2008; C-7: EPMA CHIME age of monazite Maji et al., 2008; C-8: LA-ICPMS Pb-Pb zircon spot ages Rekha et al., 2011; C-9: LA-ICPMS U-Th-Pb monazite spot ages Rekha et al., 2011; C-10: Rb-Sr WR age Ray Barman et al., 1994; C-11: Mallik, 1993; C-12: Rb-Sr WR age Krishna et al., 1996; C-13: Rb-Sr WR age Pandey et al., 1986b; C-14: ID-TIMS monazite ages Chatterjee et al., 2010; C-15: Rb-Sr WR age Pandey et al., 1986a; C-16: Mazumdar, 1996; C-17: U-Pb zircon upper intercept age Sarkar et al., 1998; C-18: ID-TIMS U-Pb zircon upper intercept age Chatterjee et al., 2008; C-19: Rb-Sr WR age Sarkar et al., 1998; C-20: Rb-Sr WR isochron age e

Dhurandhar et al., 2005, 2006; C-21: ID-TIMS U-Pb zircon age Chatterjee et al., 2010; C-22: GSI Rec. 125(2), 19-21 (1992); C-23: Pb-Pb WR age Dwivedi et al., 2011; C-24: Rb-Sr WR age 267 Hansoti and Deshmukh, 1990 Eastern Domain (South) D-1: Rb-Sr WR age Dwivedi et al., 2011; D-2: Rb-Sr WR age Sengupta et al., 1994; D-3: Rb-Sr WR Pandey et al., 1998; D-4: K-Ar age Sarkar and Saha, 1977; D-5: K-Ar age Mallik and Sarkar, 1989; D-6: ID-TIMS monazite ages Chatterjee et al., 2010; D-7: K-Ar age Mallik and Sarkar, 1994; D-8: EPMA CHIME age of monazite Mahato et al., 2008; D-9: Rb-Sr WR age Pandey et al., 1986c; D-10: Rb-Sr Sengupta and Mukhopadhyay, 2000, Sengupta et al., 2000; D-11: Rb-Sr WR age Sarkar and Ghosh Roy, 1999; D-12: K-Ar age Sarkar et al., 1969; D-13: Rb-Sr WR age Sarkar and Saha, 1986; D-14: Pb-Pb WR age Pandey et al., 1996; D-15: Rb-Sr WR age Pandey et al., 1996; D-16: Rb-Sr WR age Roy et al., 2002; D-17: Rb-Sr WR age Sengupta et al., 1994; D-19: SHRIMP U-Pb zircon age Mazumder et al., 2010; D-20: Pb-Pb age ERAC 2011; D-21: Rb-Sr age ERAC 2011; D-22: Rb-Sr WR age Vohra et al., 1981; D-23: Rb-Sr WR age Iyengar et al., 1981; D-24: Pb-Pb WR age Misra and Johnson, 2005; D-25: Rb-Sr WR age Roy et al., 2004; D-26: TDM (Sm-Nd) age Pandey et al., 1986c; D-27: Sm-Nd WR age Misra and Johnson, 2005; D-28: in situ Pb-Pb zircon age Bandyopadhyay et al., 2001; D-29: Pb-Pb zircon age Misra et al., 1999; D-30: Pb-Pb age Ghosh and Lambert in Saha, 1994; D-31: Pb-Pb WR age Sengupta et al., 1991; 1996; D-32: Pb-Pb age Moorbath et al., 1986; D-33: Pb-Pb age Manton in Saha, 1994; D-34: U-Pb SHRIMP age of zircon Mukhopadhyay et al., 2008; D-35: Sm-Nd age (continued on next page) 255 256 S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267

determined for Tirodi Gneiss by Sarkar et al., 1986a; 1415 23 Ma monazite overgrowths in Tirodi Gneiss reported by Bhowmik et al., 2011). These two age clusters are considered to ; W-7; ; W-12: the ages of the ﬁrst and second deformation of the Sausar Group (Mohanty, 2010a). ; E-9: Chimote et al., On the basis of metamorphic and geochronological studies

Bidyananda and Bhowmik et al. (1999, 2000, 2005)andBhowmik and Roy (2003) interpreted the Satpura trend to be the effect of Gen-

Clark et al., 2000 villean orogeny at w1000 Ma. Detailed structural studies

Western Australia carried out in several parts of the Sausar belt in the southern

; W-6: part of the Satpura Mountains, and the Chhotanagpur regions on Ghosh et al., 1994

; E-4: Rb-Sr WR age the eastern continuity of the Satpura Mountains, combined with the available geochronological data led Mohanty (2003) to identify four phases of evolution of the Satpura Mountains

; E-12: Pb-Pb zircon age (w1800, w1500, w1000 and w600 Ma). The dominant E-W trend of the region (referred as the Satpura trend) was considered to be the result of the deformation at w1500 Ma Wingate et al., 2004 Ghosh et al., 1991 Northeast Domain (Shillong Plateau) (Mohanty, 2003). ; E-8: Rb-Sr WR age It may be noted that a two-phase evolution of the Satpura

; W-5: Mountain Belt was proposed Acharyya (2003). The Satpura

Ameen et al., 2007 Orogeny I was considered to be the collisional event of the North Indian Block (NIB) and the South Indian Block (SIB) at 1500e1600 Ma, and development of a back-arc basin of the Dalma Volcanic Belt of the Singhbhum Craton and granulites Ghosh et al., 2005 ; E-3: Rb-Sr WR age along the suture. This event was associated with the sedimentation

Tyler and Thorne, 1990; Evans et al., 2003; Occhipinti and Reddy, 2004 in the Vindhyan Basin, Sausar Basin and Gangpur Basin, and

Eastern Domain (South) (Singhbhum) exhumation of granulites (Acharyya, 2003). The closure of the

Martin and Thorne, 2004 Sausar Basin was thought to occur during the Satpura Orogeny II ; W-11: at w1000 Ma (Acharyya, 2003). However, Acharyya (2003) had

; W-4: overlooked high precision SHRIMP U-Pb zircon age data of the lower Vindhyan which suggest the initiation of Vindhyan sedi- ; E-7: Rb-Sr WR age Chatterjee et al., 2007 mentation at w1700 Ma (Ray et al., 2002; Rasmussen et al., ; E-11: SHRIMP Pb-Pb zircon age 2002), and Rb-Sr whole rock age of 1525 70 Ma reported for the migmatisation and metamorphism of the rocks of the Sausar

Sheppard et al., 2005 Group (Sarkar et al., 1986a). Eastern Domain (North) (Chhotanagpur) Pirajno et al., 2004 A critical analysis of the evolution of the Sausar fold belt by

Ghosh et al., 2005 Sharma (2007) does not support the hypothesis of Bhowmik et al. ; W-10: (1999), Acharyya (2001, 2003) and Roy et al. (2006) that the ; W-3: w

e Satpura Orogeny is of Grenvillean age ( 1000 Ma). Mohanty Dikshitullu et al., 1995 (2006) and Sharma (2007) have raised questions about the

; E-2: EPMA monazite rim age timing of the granulite facies metamorphism in the RKG belt and the isothermal decompression after the peak metamorphic condi- tion of the belt suggested by Bhowmik et al. (1999, 2000). The w ; E-6: Rb-Sr WR age massive granite emplaced at 1147 16 Ma (Rb-Sr WR age, Pandey et al., 1998) during the terminal stage of the third defor- Pidgeon and Cook, 2003 Basu et al., 1981 Western Domain (North)(Bundelkhand Mahakoshal) mation of the Sausar Group is interpreted to be syn- to post-

; E-10: Rb-Sr WR age tectonic with respect to the last tectonic event of the region, ; W-9: Wingate and Giddings, 2000 followed by intermittent thermal (cooling and heating) events at 800e900 Ma (Sharma, 2007). Isolated occurrences of granulites

; W-2: within the Tirodi Gneiss and identical ages of Tirodi Gneiss (1450 50 Ma) and granulites are explained by a dehydration-

Van Breemen et al., 1989 melting model by Sharma (2007). The emplacement of maﬁc dykes of the RKG belt took place during the cooling event after Wingate et al., 2000 ; D-36: Sm-Nd WR age

Mitra and Mitra, 2001 the main orogeny as suggested by the development of coronal ) Bhalla and Bishui, 1989; Bhalla et al., 1990 garnet at the interface of orthopyroxene and plagioclase during the (Bastar e Sausar) ; W-8: subsolidus cooling (Sharma, 2007). The Sm-Nd age of 1416 Ma (Roy et al., 2006) put the time limit of the main orogeny (the Saha, 1994 continued ( second deformation of the Sausar Group) at ca. 1500 Ma (Sharma, Collins and Pisarevsky, 2005

; E-5: Rb-Sr WR age 2007). On the basis of these observations Sharma (2007) has questioned the proposition of Bhowmik et al. (1999, 2000) and Manton in E-1: Rb-Sr WR age 1988 Deomurari, 2007 W-1: Spaggiari, 2007 Pb-Pb age of galena Acharyya (2001, 2003) that the Satpura orogenic event I at Table 1 Time (Ma) Western Domain (South) Northeastern India Australia 1500e1600 Ma is pre-Sausar in age. S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267 257

Figure 7 Geological units on the southern margin of the Satpura Orogen.

3.2. The eastern continuation of the Satpura Orogen and granite-granophyre (w1000 Ma). On the other hand, the Kodarma Basin has three phases of deformation and is intruded by 3.2.1. The Chhotanagpur Gneiss granites of w1600 Ma (Singh, 2000). The Chhotanagpur Gneiss Complex (CGC) is the northern crustal The CGC is intruded by massif anorthosite plutons (1550 Ma age), segment of the Eastern Indian Shield (Fig. 8). This complex porphyroblastic hypersthene granite/charnockites (1599 33 Ma covers an arcuate belt with wEW trend and northward convexity, Rb-Sr age), granite gneiss (1522 71 Ma) and migmatites having a length of w500 km and breadth of w200 km. This (1580 33 Ma). These isotopic studies apparently suggest a high- complex is on the eastward continuity of the Satpura Mountain grade event at ca. 1600 Ma (Ray Barman et al., 1994). Belt. The region was involved in polyphase deformation, metamorphism and migmatisation over a period of w2000 Ma from 3.2.2. The Shillong Plateau Archean to the end of Mesoproterozoic. The Precambrian rocks of AssameMeghalaya are mainly exposed The CGC is dominantly composed of a high-grade (amphibolite- in the Shillong Plateau, south of the Brahmaputra River (Fig. 9). granulite facies) terrane of granites, metasediments and meta- The northern and southern margins of the plateau are marked by volcanics of varied composition. Two major sedimentary basins two major fault systems, the Brahmaputra fault system and the (Kodarma Basin and Munger Basin) of relatively lower grade of Dauki fault system, respectively. The Precambrian rocks of the metamorphism are located on the northern margin of the CGC. Shillong Plateau were subdivided into the lower “Gneissic Series” These basins are characterized by a thick pile of psammopelitic- and the upper “Shillong Series” (Medlicott, 1869). Detailed calcareous sediments, intruded by granites and maﬁc rocks, and mapping of the region distinguished three periods of igneous have unconformable relationship with the high-grade gneisses. Two activities in these two units (Barooah et al., 1981). less known belts to the south (Parasnath belt in the center and The Older Gneissic Group comprises quartz-sillimanite schist, PuruliaeRanchi on the south) are considered to be equivalents of the Mg-Al pelite, cordierite-biotite-sillimanite gneiss, calc-silicate, Kodarma belt (Mukherjee and Kumar, 2000). The shape and spatial BIF, amphibolite, pyroxene granulite and charnockite of distributions of these basins are controlled by the regional 2637 55 Ma age (Bidyananda and Deomurari, 2007). These ENE-WSW trending fabric of the basement (“Satpura trend”). metasedimentary rocks occur as enclaves within the next unit Therefore, these are interpreted to be rapidly subsiding ensialic rift (Augen Gneiss) of w1700 Ma age. The banded supracrustal basins (Ghose and Mukherjee, 2000). The sedimentary basins show assemblages of the Gneissic Group show polyphase deformation medium- to high-grade (upper amphibolite facies) assemblages in and poly-metamorphism. The earliest (F1) folds are isoclinal, the Kodarma Basin (also known as “Bihar Mica Belt”) and associated with granulite facies metamorphism. The second- low-grade (greenschist facies) assemblage in the Mungere generation folds (F2) are most dominant and responsible for the RajgireGaya belt. The metasedimentary assemblage of the Munger present structural conﬁguration. These folds are upright with Group has two phases of deformation and is intruded by late- to post- NE-SW trend. The rocks were retrograded from granulite to tectonic basic dykes, massive (non-foliated) gabbro-anorthosite, amphibolite facies during this event. The third phases of folds (F3) 258 S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267

Figure 8 Geological units on the eastern continuation of the Satpura Orogen. are open to isoclinal, upright with E-W to ESE-WSW trend. 3.2.3. The Arunachal Domain A second event of retrograde metamorphism of epidote- The contact of the Shillong Plateau with the rocks of the Hima- amphibolite facies took place during this deformation. The older laya Mountain in Arunachal Pradesh is concealed. The presence Gneissic Group and the Augen Gneiss are intruded by maﬁc dykes of polyphase deformed metasediments of greenschist to amphib- followed by porphyritic granites. The Shillong Group comprising olite facies (migmatites, Kyanite-Sillimanite-Staurolite gneiss and basal conglomerate, phyllite, and carbon phyllite, are feebly schist, quartzite, calc-silicate, marble, graphitic schist, amphibo- metamorphosed and weakly deformed. Pb-Pb age of galena from lite) forming the Se La Group in Arunachal Pradesh is considered these rocks indicates an age of 1550 Ma (Mitra and Mitra, 2001). to be Archean. The Se La Group is overlained by the Bomdila The Shillong Group has intrusions of metabasic rocks and Group, consisting of lower Khetabari Formation (maﬁc volcanic Neoproterozoic granite. and riftogenic to unstable platformal sediments quartzite, acidic

Figure 9 Geological units on the northeastern margin of the Satpura Orogen. S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267 259 tuff, carbonaceous and graphitic phyllite, marble, calc-silicate and 3.3. The Singhbhum Craton garnet mica schist) and upper Tenga Formation (quartzite, vesicular to amygdaloidal mafic volcanic, phyllite, and marble/ The Singhbhum Craton of Eastern India (Fig. 10) is one of the proto- dolomite) and Chilliepam Formation (interbedded phyllite, continental nuclei of India. The oldest rocks of India (3775 85 Ma quartzite and thick dolomite/limestone). Mafic dykes, mica- gneisses) were reported from this craton (Basu et al., 1981), but peridotite and pyroxenites intrude these metasedimentary units. debated later (Moorbath et al., 1986). Subsequent geochronological The presence of acidic intrusions (Ziro Gneiss) of 1914 25 Ma works have confirmed the antiquity of the craton (Table 1). The and 1676 122 Ma age, two phases of deformation (D1 and D2), geological evolution of the craton was first described by Dunn (1929, and two metamorphic episodes (M1 and M2) in the Bomdila 1940),andDunn and Dey (1942) and was updated by Saha (1994) and Group indicate the upper limit of the Bomdila Group. The D1 is summarized by Mukhopadhyay (2001). The summary presented here found in the Khetabari Formation only and not in Tenga Forma- takes into account the geochronological analysis of key units. tion, indicating a break in sedimentation (Gopendra Kumar, The Singhbhum Craton comprised the Archean nucleus of 1997). Presence of 2300e2100 Ma acidic magmatism and Singhbhum and the Proterozoic fold belts to the north and west of 2510 Ma mafic volcanic in similar setup in the Himalayas can be the nucleus. The principal units of the nucleus are: (a) the Older considered to be the lower limit of Bomdila Group (Gopendra Metamorphic Tonalite Gneiss (OMTG), (b) the Older Meta- Kumar, 1997). The Ziro Gneiss is unconformably overlain by morphic Group (OMG), (c) the older granite-greenstone belt oligomictic conglomerate, quartzite, calc-silicate, tremolite- (3400e3500 Ma age) containing Banded Iron Formation (BIF) of actinolite marble, phyllite and garnet-muscovite-biotite schist of the GorumahisanieBadampahareDaitari Iron-Ore Group, (d) the Dirang Formation. The Dirang Formation is intruded by ovoid granite (3100e3300 Ma age) plutons, (e) two units of biotite augen gneiss of w1000 Ma and non-foliated biotite younger greenstone belt with BIF of 2700e2900 Ma and granites of 500 19 Ma age (Bhalla and Bishui, 1989; Bhalla 2400e2600 Ma age (DhanjorieSimplipal Group), (f) younger et al., 1990). granites, and (h) mafic dyke swarms (Newer Dolerite).

Figure 10 Geological units on the southeastern margin of the Satpura Orogen. 260 S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267

The OMTG contains Tonalite Trondhjemite Granodiorite 1638 38 Ma (Sengupta et al., 1984) and 1619 38 Ma (Roy (TTG) suite of juvenile material (>3500 Ma). These are referred et al., 2002). Therefore, the age of Dalma Group is considered here as Singhbhum Granite-I. The OMG consists of metasedi- here to be 1850e1900 Ma for the lower part and 1750e1650 Ma for mentary and orthoamphibolites as enclaves in older granites. The the upper part. The older ages of zircon population possibly reflect reported ages range from w3800 Ma (Basu et al., 1981)to ages of country rocks engulfed in the magma chamber. The younger w3370 Ma (Moorbath et al., 1986; Sengupta et al., 1991). The ages are effects of zircon overgrowth during later metamorphism. mafic enclaves represent materials derived from a pre-existing The Dalma Basin which was possibly very narrow closed at mafic crust. The principal units of the older greenstone sequence w1800 Ma during the Dalma Orogeny. This event is identified from (3350e3500 Ma) are coarse clastics, BIF, fine clastics, mafic the third peak of monazite ages at 1800e1850 Ma and intrusion of volcanic and carbonates. The dacite lava of this unit has U-Pb Kuilapal granite and Rompahari granite (1895 46 Ma Rb-Sr age; SHRIMP zircon age of 3508 2Ma (Mukhopadhyay et al., Vohra et al., 1981). Eruption of mafic and felsic volcanic of the 2008). The ovoid granite plutons emplaced during the green- Dalma Group possibly continued during this basin evolution phase. stone belt development (3437 9 Ma age; Misra et al., 1999) are The closing of the Dalma Basin took place during the Dalma termed here as Singhbhum Granite-II. All these older sequences Orogeny (1633e1677 Ma), which was associated with the thermal were involved in deformation, metamorphism and migmatisation imprints on Soda Granite (1633 6, 1677 11 Ma Rb-Sr age; at 3300e3350 Ma (Iron-Ore Orogeny), followed by stretching and Sarkar et al., 1986b), emplacement of Arkasani Granophyre emplacement of mafic dykes (epidiorites). About 12 ovoid granite (1721 142 Pb-Pb age, 1677 80 Ma Rb-Sr age; Chavan et al., intrusions (Singhbhum Granite-III) took place during the time 1996), and gabbro-pyroxenite intrusions (1638 38 Rb-Sr age; period 3100e3300 Ma. The Singhbhum Granite, Bonai Granite Sengupta et al., 1984; 1619 38 Ma; Roy et al., 2002). The second and Kaptipada granite are the known major phases of this suite. deformation (SD2) and syn-S2 amphibolite facies metamorphism Later thermal stretching gave rise to the development of a sedi- (M2) possibly continued up to 1500 Ma (second peak of monazite mentary basin and the younger greenstone sequence (Dhanjori- age between 1500 and 1600 Ma). This has given rise to thermal Simlipal Group) and associated granite intrusion (Tamperkola resetting of age of Newer Dolerite-V (1540 16 Ma K-Ar age). granite). There was possibly w100 Ma hiatus and emplacement of mafic dykes (Newer Dolerite-Ia) before the deposition of the 4. Synthesis of tectono-thermal events upper part of the younger greenstone sequence. The end Archean events of the Singhbhum nucleus are intrusions of granite pluton On the basis of available geochronological data from the Satpura (Nilgiri granite) and mafic dyke swarms (Newer Dolerite-Ib). Mountain Belt of India, the Capricorn Orogen of Western Australia, The Proterozoic evolution of the Singhbhum protocontinent has and adjacent cratonic areas is a spatio-temporal model of evolution a punctuated history of basin development and orogeny in three was synthesized (Table 1). It is observed that the tectonic evolution phases, and of one phase of crustal extension. The oldest basin of the Satpura Mountains and the adjacent cratons has broad simi- developed at the northern and western margin of the Singhbhum larity with that of the Capricorn Orogen and its environs. The nucleus and was marked by the deposition of coarse clastics, BIF cratonic nuclei on the southern and northern side of both the and fine clastics (Koira Group) and associated basic volcanic orogenic belts have Archean TTG gneisses of >3500 Ma as the (Jagannathpur Volcanics), followed by a hiatus and deposition of basement over which Archean granite greenstone belts were dominantly pelitic-arenaceous sediments (Chaibasa Group). The developed. The end ArcheaneEarly Paleoproterozoic time is first phase of the orogenic activity at w2200 Ma (Singhbhum characterized by high-grade metamorphism and high-K granite Orogeny-I) gave rise to the amalgamation of the Singhbhum nuclei intrusions, followed by an extensional event marked by intrusion of on the south and the Chhotanagpur nuclei on the north. The second high-Mg mafic dyke swarms, development of sedimentary basins in phase of basin development (2100e2050 Ma) is marked by crustal extension, emplacement of Newer Dolerite-II (2105 38 Ma K-Ar age Mallik and Sarkar, 1994) and deposition of coarse clastics, carbonate and shale (Kolhan Group). The second orogenic episode at w1970e2030 Ma (Singhbhum Orogeny-II) was possibly associated with the development of the Singhbhum Shear Zone. This event is represented by the emplacement of Soda Granite-II (2017 Ma Pb-Pb age; Sarkar et al., 1986b) and Mayurbhanj Granite (2084 74 Rb-Sr age; Iyengar et al., 1981), and thermal imprint on the Newer Dolerite-III (2004 35 Ma and 2068 38 Ma). The phase of crustal extension of the Singhbhum Craton was associated with the emplacement of ultramafic-mafic- anorthosite plutons and Newer Dolerite-IV (1960 40 K-Ar age; Sarkar and Saha, 1977). The thermal expansion possibly gave rise to the development of Dalma Basin. It may be noted that the U-Pb zircon age of Dalma volcanic is 2396 110 Ma (Misra and Johnson, 2005) which is debatable (Roy and Sarkar, 2006). U-Pb age cluster between 1740 and 1630 Ma for the Dalma volcanic and between 1500 and 2900 Ma (mean of 2467 9 Ma) for the Chandil Formation has been reported by Mazumder et al. (2010). The Kuilapal granite intruding the Dalma Volcanics has Pb-Pb age Figure 11 Gaussian probability plot of concordant Pb-Pb ages of of 1863 63 Ma and Rb-Sr age of 1718 40 Ma. Gabbro- zircon and monazite from the northwestern Yilgarn Craton and pyroxenite intrusions in the Dalma Volcanics have ages between southern Gascoyne Complex (from Nelson, 2001). S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267 261

Figure 12 Distribution of Precambrian age data from the Satpura Mountains and adjoining cratons.

which BIF/BMnF and associated volcanic rocks were deposited. domains of the Satpura Mountains, but has maximum effect on the This period is marked by the presence of glaciogenic sediments in northern (Chhotanagpur) domain as the Munger orogeny. The the Turee Creek Group on the northern domain of the Capricorn effect of Pinjarra orogen is found in the northeast (Shillong) Orogen, and in the Sausar Group on the southern domain of the domain only and absent in all other domains of India. Satpura Mountains. At w2100e2200 Ma the northern and southern High precision Pb-Pb ages of zircon and monazite grains from cratonic domains collided to form the first stage of formation of the the Gascoyne Complex and the northwestern Yilgarn Craton show Satpura Mountains (the Sausar Orogeny I/Mahakoshal Orogeny peaks at w3500 Ma, w3300 Ma, 2750e2500 Ma, 2100e1950 Ma, I/Singhbhum Orogeny I) and the Capricorn Orogen (Opthalmian w1800 Ma and w1650 Ma (Fig. 11; Nelson, 2001). Synthesis of all Orogeny). An extensional event between 2030 Ma and 2100 Ma available geochronological data from the Satpura Mountains and gave rise to the development of sedimentary basins, which was the adjacent cratons (Fig. 12) also shows similar pattern, with age involved in orogenic movement, high-grade metamorphism and probability peaks at w3500 Ma, w3300 Ma, w2500 Ma, granitisation at w1950e2030 Ma (the Sausar Orogeny II/Maha- w2100 Ma, w1850 Ma, w1650 Ma and w950 Ma. Broad patterns koshal Orogeny II/Singhbhum Orogeny II) of the Satpura Range, of age probability data of both these areas are apparently similar up and the Glenburgh orogeny of Western Australia. Subsequent to w1650 Ma. Slight difference in detail possibly results from use evolution of the cratons is characterized by an extensional regime at of low to high precision age data (U-Pb, Pb-Pb, Sm-Nd, Rb-Sr, w1850e1950 Ma and development of basins of deposition Ar-Ar and K-Ar) for the synthesis of geochronological data for (BijawareGwalior, Kodarma Basins, and Dalma Basin of India, and India and/or local diachronous nature of the orogenic movements. Padbury, Earaheedy/Blair Basin, Upper Yerrida/Wyloo Basin of The probability peaks in the Proterozoic time are related to the Western Australia). The effect of Satpura Orogeny marked a major Opthalmian e Glenburgh e Singhbhum e Mahakoshal e Sausar deformation and development of regional folds with EW striking Orogeny (2100e1950 Ma), Capricorn e Satpura Orogeny axial planes at w1750e1850 Ma. This orogeny is contempora- (1800e1850 Ma) and Mangaroon e Dalma e Chhotanagpur neous with the Capricorn Orogeny. The marginal parts of both these Orogeny (1650 Ma). The apparent similarity of evolution of the orogens developed foreland basins where deposition continued up Capricorn Orogen and the Satpura Mountains possibly results from to w1700 Ma. Subsequent evolution of the Satpura Orogenic Belt is their near neighbour position. More detailed and precise age data for characterized by a series of orogenic movements, granitisation, these pre-Rodinia orogenic movements will be useful in under- decompression, and basin development from 1600 Ma to 1300 Ma, standing the formation and dispersion of the supercontinent but the Western Australian craton was involved in the Mangaroon Columbia. orogeny at 1500e1600 Ma. Thus, the Satpura Mountains and the Capricorn Orogen show common evolutionary history up to 1500 Ma, subsequent developments of both of these orogenic belts 5. Conclusions differ from each other. A major phase of extensional tectonics is marked by intrusions The paleomagnetic and spatio-temporal attributes indicate that the of mafic dyke swarms and expansive granites at 1238e1243 Ma Precambrian terranes of South India (Dharwar Craton, Bastar and again at 1073e1138 Ma and basin development on the Craton and the Singhbhum Craton), Western Australia (Yilgarn northern margin of the Satpura Orogen. These events are Craton) and the Napier Complex of East Antarctica formed contemporaneous with the Marda Moon Large Igneous Province a contiguous megacraton (SIWA) at w2400 Ma (Mohanty, 2010b, (LIP) and Warakurna LIP, respectively. The Edmundian orogeny 2011a,b). This megacraton underwent breaking and dispersion of Western Australia is contemporaneous with a low intensity during the Early Paleoproterozoic. The Yilgarn Craton was deformation and thermal overprint on the western and southern possibly first separated from the SIWA, followed by the Napier 262 S. Mohanty / Geoscience Frontiers 3(3) (2012) 241e267

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