Oldest rocks from Peninsular India: Evidence for Hadean to Neoarchean crustal evolution

    Oldest rocks from Peninsular India: Evidence for Hadean to Neoarchean crustal evolution M. Santosh, Qiong-Yan Yang, E. Shaji, M. Ram Mohan, T. Tsunogae, M. Satyanarayanan PII: DOI: Reference:

S1342-937X(14)00326-8 doi: 10.1016/j.gr.2014.11.003 GR 1360

To appear in:

Gondwana Research

Received date: Revised date: Accepted date:

20 August 2014 29 October 2014 2 November 2014

Please cite this article as: Santosh, M., Yang, Qiong-Yan, Shaji, E., Mohan, M. Ram, Tsunogae, T., Satyanarayanan, M., Oldest rocks from Peninsular India: Evidence for Hadean to Neoarchean crustal evolution, Gondwana Research (2014), doi: 10.1016/j.gr.2014.11.003

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Oldest rocks from Peninsular India: Evidence

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for Hadean to Neoarchean crustal evolution

M. Santosh1*, Qiong-Yan Yang1, E. Shaji2, M. Ram Mohan3, T.

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Tsunogae4,5, M. Satyanarayanan3 1

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School of Earth Sciences and Resources, China University of Geosciences

Beijing, 29 Xueyuan Road, Beijing 100083, China Department

of

Geology,

3

of

Kerala,

Kariyavattom

Campus,

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Trivandrum, 695 581, India

University

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2

4

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CSIR-National Geophysical Research Institute, Hyderabad, India-500007 Graduate School of Life and Environmental Sciences, University of Tsukuba,

Ibaraki 305-8572, Japan 5

Department of Geology, University of Johannesburg, Auckland Park 2006, South Africa

*Corresponding author E-mail: [email protected]; Tel. and Fax: + 86-1082323117

ACCEPTED MANUSCRIPT Page |2 Abstract The evolution of continental crust during Hadean and Archean and related

Here we report evidence for Hadean and Eoarchean crust from the

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history.

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geodynamic processes provide important clues to understand the early Earth

fringe of the Coorg Block, one of the oldest crustal blocks in Peninsular India. We

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present geological, petrological, and geochemical data, together with zircon U-Pb

charnockite,

metavolcanics)

and

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ages and Lu-Hf isotopes from a suite of metaigneous (granitoids, diorite, metasedimentary

(quartz

mica

schist,

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calcareous schist, ferruginous quartzite and BIF) rocks. Petrological and geochemical studies indicate that the igneous suite formed from subduction-

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related arc magmatism, and that the sedimentary suite represents an imbricated accretionary package of continental shelf sequence and pelagic components.

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Mineral thermometry suggests metamorphism under temperatures of 710-730C and pressures up to 8kbar. Magmatic zircons in the metaigneous suite show oscillatory zoning and high Th/U contents (up to 3.72) and record multiple pulses of magmatism at ca. 3.5, 3.2, 2.7 and 2.5-2.4 Ga.

The metasedimentary rocks

accreted along the margins of the Coorg Block show multiple zircon population with mean

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Pb/206Pb ages at 3.4, 3.2, 3.1, 2.9, 2.7, 2.6, 2.5, 2.2, 2.0, and 1.3

Ga, and overprinted by younger thermal event at ca. 0.8-0.7 Ga. Zircons in the 3.5 Ga dioritic gneiss show positive εHf (t) values ranging from 0.0 to 4.2 and Hf crustal model ages (TDMC) of 3517 to 3658 Ma suggesting that the parent magma was derived from Eoarchean juvenile sources. The zircons in the 3.2 Ga charnockite display εHf(t) values in the range of -3.0 to 2.9 and Hf crustal model

ACCEPTED MANUSCRIPT Page |3 ages (TDMC) of 3345 to 3699 Ma. The Neoarchean metagranites, diorites and felsic tuff show both positive and negative εHf (t) values and a range of TDMC 2904 to 3609 Ma suggesting magma derivation from Meso- to

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values from

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Eoarchean juvenile and reworked components. The TDMC values of the dominant zircon population in the metasedimentary suite range from 3126 to 3786 Ma, with

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the oldest value (4031 Ma) recorded by zircon grain in a ferruginous quartzite.

with a dominant crustal source.

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The εHf(t) values of detrital zircons also show both positive and negative values, Our zircon U-Pb and Lu-Hf data suggest

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vestiges of Neohadean primordial continental crust in Peninsular India with episodic crustal growth during Eoarchean, Mesoarchean and Neoarchean

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building the continental nuclei. The results contribute to the understanding of

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crustal evolution in the early history of the Earth.

Key words: Petrology and geochemistry; Zircon U-Pb geochronology; Lu-Hf isotopes; Early Earth; southern India.

ACCEPTED MANUSCRIPT Page |4 1. Introduction

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The formation and evolution of continental crust in the early Earth have been

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topics of prime interest among geoscientists, with potential clues in earlier studies provided by continental sediments (Allègre and Rousseau, 1984; Taylor

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and McLennan, 1995). Episodic crust formation events on the globe have been

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addressed in several recent studies from the ages of magmatic rocks which show peaks at 3.3-3.2, 2.7, 2.5 1.9 and 1.2 Ga (McCulloch and Bennett, 1994; Condie,

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2000; Kemp et al., 2006; Condie and Kröner, 2012; Condie and Aster, 2013; Zhai and Santosh, 2011; Santosh et al., 2015). However, the volume and composition

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of the Hadean crust during early Earth history, and the nature of source as depleted or enriched mantle remain contentious (Amelin et al., 1999; Bennett et

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al., 2007; Davis et al., 2005). Popular hypotheses include the basaltic “protocrust” (Kamber et al., 2005) or voluminous recycled felsic crust (Armstrong, 1981; Harrison et al., 2005). Some models consider that silicate Earth differentiation during the Hadean generated the same volume of continental crust as that of present day, but that the older crust was recycled back into the mantle by the onset of Archean, as argued from evolved isotopic signature (Bennett et al., 2007; Kemp et al., 2010).

Prolonged subduction of continental crust is

speculated to have generated stagnant „second continents‟ in the mantle transition zone (Kawai et al., 2013).

Although debates surround the nature and timing of initiation of plate tectonics on

ACCEPTED MANUSCRIPT Page |5 Earth, the formation of early Achaean tonalite-trondhjemite-granodiorite suites (TTG) and greenstones, and the interleaving of arc-plume sequences as

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observed in many ancient terranes are considered to indicate that subduction initiation events might have been common in the early Hadean-Eoarchean Earth

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(O‟Neill and Debaille, 2014). In a review addressing the role of detrital zircon in

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Hadean crustal evolution, Nebel et al. (2014) noted that regional scale TTG

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suites mark granitoid-generating processes in the Eoarchean, along with the first appearance of low-Ca (s-type) granites at around 3.9 Ga. The global detrital

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zircon record also coincides with the first addition of juvenile crust and that this age might probably mark the onset of Archean-style tectonics which was likely

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associated with subduction activity. Only limited information is available on Hadean crust from zircons with ages over 4.0 Ga that include reports from the

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Jack Hills of the Yilgarn Craton in Western Australia (Wilde et al., 2001; Valley et al., 2014), and the Acasta gneisses in the Wopmay orogen, Canada (Izuka et al., 2006). Detrital or xenocrystic grains in some of the Proterozoic and Phanerozoic orogenic belts also carry rare ancient zircons (e.g., He et al., 2011; Diwu et al., 2013; Cui et al., 2013). Although these reports suggest that the primodial continental crust might have formed in the Hadean, its extent of preservation remains unknown. A recent study combining Hf and O isotopes of Eoarchean zircons from Jack Hills suggest simultaneous loss of ancient crust accompanied by juvenile crust addition suggesting that subduction tectonics operated at this time, similar to the process on modern Earth (Bell et al., 2014).

ACCEPTED MANUSCRIPT Page |6 The growth of continental crust through time is debated with endmember models on episodic growth versus continuous growth. Crustal evolution history as

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studied in detail from one of the largest Phanerozoic orogens on the globe, the

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Central Asian Orogenic Belt, shows substantial addition of juvenile crust and continental building through arc-arc and arc-continental collision with ancient

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microcontinents caught in between (Xiao and Santosh, 2014 and references

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therein). Rino et al. (2008) reported detrital zircon data from sediments in major river mouths of the globe and provided robust evidence for the episodic growth of

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continental crust through time. Although their zircon population covers a wide time range from 4.2 Ga to the present, the data clearly identify discontinuous and

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episodic growth of continental crust during four peaks at 2.6–2.7 Ga, 2.0–2.2 Ga, 1.0–1.2 Ga, and 0.5–0.8 Ga. They also noted that the minor peaks in some

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cases, such as in the Mesoarchean, are possibly due to data bias arising from the lack of adequate information on these terranes.

Peninsular India assembles a collage of continental blocks which were part of various supercontinents in Earth history starting from Ur at 3.0 Ga through Columbia at 1.9 Ga, Rodinia at 1.0 Ga and Gondwana at 0.54 Ga (Rogers and Santosh, 2003; Meert et al., 2010; Nance et al., 2014). The Southern Granulite Terrane (SGT) to the south of the Dharwar Craton is composed of continental blocks ranging in age from Mesoarchean (3.2 Ga; Santosh et al., 2015) through Neoarchean and Paleoproterozoic to late Neoproterozoic – Cambrian (Santosh et al., 2009, 2003; Plavsa et al., 2012; Collins et al., 2014; Praveen et al., 2014;

ACCEPTED MANUSCRIPT Page |7 Shaji et al., 2014; Samuel et al., 2014; Kröner et al., 2014). In a previous study, our group reported Mesoarchean juvenile crust formation in the Coorg Block, an

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exotic crustal block that does not bear any imprints of the later Neoarchean,

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Paleoproterozoic and Neoproterozoic tectonothermal events that are widely represented in the surrounding crustal blocks in the SGT (Santosh et al., 2015).

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In this study, we focus on the margins of the Coorg Block, and the bounding

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suture zones where we carried out detailed field investigations and sample collection (Fig. 1). We present systematic geologic, petrologic, geochemical and

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zircon U-Pb and Lu-Hf data from a suite of metaigneous and metasedimentary rocks which provide new insights into Neohadean and Eoarchean crustal

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evolution history in Peninsular India as well as multiple magmatic pulses and

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episodic continental growth through the Archean Earth history.

2. Geological setting and sampling

2.1 Geological background

The Coorg Block is bound to the north by the E-W trending Mercara Shear Zone (MRSZ) and to the south by the WNW-ESE trending Moyar Shear Zone (MOSZ) (Figs .1, 2a)

(Chetty et al., 2012; Santosh et al., 2015) . The Mercara Shear

Zone welds the Coorg Block with the Dharwar Craton to the north and is marked by steep gravity gradients (Sunil et al., 2010) interpreted to suggest the presence of underplated high-density material in the lower crust. The Coorg–Nilgiri–Biligiri

ACCEPTED MANUSCRIPT Page |8 Rangan–Salem–Madras

Blocks

were

previously

grouped

together,

and

considered to have witnessed a common Neoarchean (ca. 2500 Ma) granulite

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facies metamorphism (Bernard-Griffiths et al., 1987; Bhaskar Rao et al., 1992;

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Bhaskar Rao et al., 2003; Clark et al., 2009; Devaraju and Janardhan, 2004; Ghosh, 2004; Janardhan et al., 1994; Peucat et al., 1993; Raith et al., 1990;

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Raith et al., 1999; Sato et al., 2011). Our recent geochronological and isotopic

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studies (Santosh et al., 2015) revealed that the Coorg Block is an exotic crustal domain within the SGT, in the absence of any records of the 2.5 Ga pervasive

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regional metamorphism widely represented in the surrounding blocks.

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Mesoarchean charnockites and TTG are the dominant rock types in the Coorg Block. Mafic-ultramafic rocks are volumetrically less abundant, and occur as the Metasedimentary units

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dismembered and altered tremolite-actinolite schists.

such as the psammites, pelites and carbonates are rare or absent within the central domain, but several tens of meters thick bands of granulite facies metapelites (khondalites) occur along the northern and northeastern peripheries of the block. The depositional and metamorphic ages of these rocks (our unpublished data) indicate that these passive margin sediments developed in Proterozoic

continental

Mesoproterozoic.

rifts

and

were

metamorphosed

during

latest

From the dominant lithological constituents comprising

charnockite-mafic granulite-TTG-porphyritic syenogranite suites, the Coorg Block can be considered as an eroded continental arc. In this study, we carried out field investigations and sampling in the southern and south eastern margin of the

ACCEPTED MANUSCRIPT Page |9 Coorg Block along the Irikkur – Thalipararmba – Nadukani – Periya sector of Kannur district and Tirunelli

– Appapara – Manandavadi sector of Wyanad

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district. The WNW-ESE trending Moyar Shear Zone, extending from Payyannur

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in the west to Sulthan Bathery in the east for about 150 km marks the southern suture of the Coorg Block. This zone merges with the northern Mercara Suture

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Zone around Padamala, Kartikulam, Tirunelli areas (Fig. 2).

Many workers have studied the geology and structure of the Waynad – Kannur

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sector (Asoka Kumar and Soney Kurien, 2011; Jain et al., 2003; Kurian et al., 1999; Meißner et al., 2002; Naha and Srinivasan, 1996; Nair et al., 1975;

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Nambiar, 1985; Nambiar et al., 1997; Pillay and Bhutia, 2010; Pillay and Khipra, 2012; Praveen, 2013; Rao and Varadan, 1967; Soney Kurien and Behera, 2012;

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Vidyadharan, 1981). These studies have classified the rock types in the region into four groups, namely the Archean Wyanad Group (equivalent to the Sargur Group of Dharwar Craton), the Peninsular Gneissic Complex (PGC), the Charnockite Group, and the younger basic and acid intrusives. The Wyanad Group comprises older supracrustals represented by the metasedimentary and metaultramafic units occurring as enclaves and rafts within the PGC and the Charnockite Group. The PGC comprises hornblende-biotite gneiss and granite gneiss. The Charnockite Group is represented by charnockites and mafic granulites. The Neoproterozoic younger intrusives are mainly granitoids.

Previous studies contended that the Sargur equivalent rocks (low-grade schists

ACCEPTED MANUSCRIPT P a g e | 10 and associated quartzites, and the high-grade metasedimentary-metaultramafic rocks) lie unconformably over the Wyanad gneissic complex. Based on

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lithostratigraphy and grade of metamorphism, these units were correlated with

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the Neoarchean Lower Bababudan Group of the Dharwar Supergroup (Nair et al., 1975). The gneiss-supracrustal association in the region is comparable to

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those other Archean terrains. The gneissic complex comprises tonalitic gneiss

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with amphibolite bands, hornblende-bearing tonalite gneiss and migmatitic gneiss. The rocks continue into the Peninsular Gneissic Complex (Older Gneissic

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Complex) of the Dharwar Craton. The rafts and enclaves of metasedimentary and metaultramafic rocks in Wynad were considered as remnants of the ancient

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supracrustals and categorised as the oldest rocks of Kerala (Nair et al., 1975; Geological Survey of India, 2014). This assumption was based on the

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stratigraphic and field relationships of the rock units of the area and not from isotope geochronologic data.

The N-S trending Sargur Schist Belt of southern Karnataka swings SW and continues as the Wyand Schist Belt extending WNW-ESE from Sulthan Bathery of Wyanad district in the east and Payyannur of Kannur district in the west. Minor exposures of this belt are seen in the Bandadka sector of Kasaragod district (Adiga, 1979) and in the Attappadi and Nilambur areas in the Palakkad and Malappuram districts (Nambiar, 1982; Nambiar and Rao, 1980; Praveen et al., 2013; Santosh et al., 2013; Shaji et al., 2014).

ACCEPTED MANUSCRIPT P a g e | 11 2.2 Geology of the sample locations

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Our sampling localities are shown in Fig. 2a and in a detailed geological map in

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Fig. 2b (modified after Geological Survey of India, 1995). Representative field photographs from these localities are shown in Figs. 3 and 4. A summary of the

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locations, co-ordinates, rock types and general mineralogy of the samples used

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for geochronology is presented in Table 1. A brief description of the various rocks types sampled in this study, grouped under metaigneous and metasedimentary,

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2.2.1 Metaigneous rocks

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is given below.

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The metaigneous rocks comprise hornblende-biotite gneiss, dioritic gneiss, felsic orthogneiss, metadiorite, hornblende schist, migmatitic biotite gneiss and charnockites.

Hornblende-biotite gneiss (TTG) is the most extensive rock type of the area. The rock shows migmatitic texture with compositional variation from hornblende gneiss to biotite-rich gneiss. Enclaves and rafts of amphibolites are common and those of metaultramafics and minor metasedimentary rocks are also observed. Medium-grained leucocratic hornblende-biotite gneiss is exposed in a working quarry at Ondayangadi. The rock shows migmatitic structure with alternating leucocratic and mesocratic bands. Amphibolite bands varying in width from 10

ACCEPTED MANUSCRIPT P a g e | 12 cm up to 2m are seen in the gneiss. Migmatitic biotite gneiss with deformed compositional banding is observed in several abandoned quarries near Dioritic enclaves of different dimensions within these rocks

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Manandavadi.

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resemble those resulting from the intrusion of mafic magma into felsic magma

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chambers and consequent magma mixing and mingling.

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Dioritic gneiss is another major rock unit of the study area and fresh exposures of these rocks occur at Nedumpoyil quarry, Peruva and Irikkur (see Table 1). The

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rocks exhibit alternating light and dark bands, and also show compositional variation as diorite gneiss, diopside gneiss, and orthogneiss. Stretched and

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elongated boudins of hornblendite and amphibolite occur as enclaves. Pockets of metatonalites, metatrondhjemites with minor amphibolites and meta-ultramafic

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hornblende-rich rocks are seen within the dioritic gneiss. The tabular or lensoid bodies are deformed and are concordant with the metamorphic banding of the tonalitic and trondhjemitic gneisses. In high strain zones, the gneisses exhibit mylonitic deformation. At Periya, a large working quarry exposes TTG gneiss with bands and boudins of cumulate rocks (mainly hornblendites). enclaves of metadiorite are also common.

Large

Sheath folds are the prominent

structure in this exposure.

Charnockite and associated rocks are exposed in the north-western part of the study at Nadukani and Thaliparamba. The quarries in these locations fall within the southern margin of the Coorg Block. The charnockite are medium to coarse

ACCEPTED MANUSCRIPT P a g e | 13 grained and shows typical greasy green appearance. Bands and boudins of

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mafic granulites occur within the charnockite in some places.

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Gneissose granites trending WNW-ESE to E-W are exposed in Tirunelli and Appapara areas along the southern part of the Coorg Block.

Patches of

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hornblende gneiss occur as relicts within the metagranitoids at some places.

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Coarse to medium-grained light pink and grey granite gneisses are exposed in the Bavali region, with local shearing and mylonitisation. Similar rocks are also

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exposed near Kartikulam.

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The metaultramafic rocks, metapyroxenites and talc-tremolite schist occur either as thin conformable bands or as linear and lensoid bodies in the south-eastern

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part of the study area. Most of the meta-ultramafic exposures are seen in the Kenichera – Sulthan Bathery area of Wyanad district and in the Irikkur sector of Kannur district. Talc tremolite schist exposed north of Sulthan Bathery shows spinifex texture and have been interpreted as komatiitic flows (Pillay, 2010). Mappable units of amphibolite are very few in the study area.

2.2.2 Meta-sedimentary rocks

Quartz-mica schist ± kyanite and quartz-sericite schist, calcareous schist and banded magnetite quartzites (metamorphosed Banded Iron Formation) are the dominant metasedimentary units and are exposed mainly in the Iritty, Irikkur and

ACCEPTED MANUSCRIPT P a g e | 14 Kottiyoor areas of Kannur district and in the Padamala, Thirunelli, Talapuzha-

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Manandavadi areas of Wyanad district.

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Thin bands of meta BIF occurring together with quartzite, quartz mica schist and fine grained felsic gneisses are exposed in several localities. Banded magnetite as 1 to 2 km long and 10-30 m wide WNW-ESE

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quartzite (BMQ) occurs

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trending bands at Padamala and along the Kartikulam – Tirunelli Road. Thin bands of oxide and sulphide facies of BMQ are present to the west of (Praveen, 2013) and Padamala area near to the St. Alphonsa

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Padinjarathara

Church. Sulphidic meta BIF occurs in close association with thinly laminated

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orthogneiss and quartz sericite schist at Padamala (our sample number PDM-2,

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Table 1) and at „Thazhe 54‟ on Kartikulam – Manathawady road (sample no

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KTMR-2, Table 1). Several meta BIF bands occur seen associated with metaultramafics in Munnankuzhi and Kenichera, in the Manandavadi - Sulthan Bathery sector.

Quartz mica schist is the voluminously abundant metasedimentary rock exposed in the area. Two roughly E-W trending fine- grained, finely laminated, pale red to white quartz mica schist bands, 100 to 500 m wide,

are exposed

along

Kartikulam – Tirunelli road (TNL-1, Table 1). The rock corresponds to ferruginous sandstone. Another exposure of schistose rock with thinly laminated quartz, muscovite, and sillimanite occur near the stream section at Tirunelli (sample TNL3-1). Close to Tirunelli temple, several exposures of medium to fine- grained,

ACCEPTED MANUSCRIPT P a g e | 15 finely laminated, pale green to yellowish white quartz mica schist with calcareous schist are seen (sample TNL-4-1)

Weathered quartz mica schist interbanded

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with fuchsite quartzite is exposed on the western side of Mambaram (sample

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MBM-1) and continues in the Kuppadi reserve forest NW of Vengur. A small hillock with fine laminated garnet-bearing brownish quartz mica schist occurs at

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Neduvaloor along the Irikur –Thaliparamba road (samples -NDV-1 &2). Quartz

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mica schist is also exposed south-east of Manadavadi where the rock occurs in association with fuchsite and micaceous quartzite, talc-tremolite schist, meta BIF,

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and amphibolite. Pale greenish fuchsite quartzite and medium grained white quartzites are also exposed in many parts of the study area at Tirunelli,

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Manandavadi and Sulthan Bathery areas.

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3. Analytical techniques

3.1 Petrography and mineral chemistry

Polished thin sections were prepared for petrographic study at the State Key Laboratory of Geological Processes of Mineral Resources of China University of Geosciences Beijing, and at the Tsukuba University, Japan. Mineral chemical analyses were carried out using an electron microprobe analyzer (JEOL JXA8530F) at the Chemical Analysis Division of the Research Facility Center for Science and Technology, the University of Tsukuba. The analyses were performed under conditions of 15 kV accelerating voltage and 10 nA sample current, and the data were regressed using an oxide-ZAF correction program

ACCEPTED MANUSCRIPT P a g e | 16 supplied by JEOL.

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3.2 Whole-rock geochemistry

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Eight representative magmatic rocks, having the mafic, intermediate and felsic affinities are chosen for the whole-rock geochemical analyses, and the data are

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compared with the first set of magmatic rocks from Coorg Block (Santosh et al.,

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2015) to understand the tectonic setting in which the Archean magmatic rocks of Coorg are derived. Care has been taken to avoid the samples of any surface

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alteration or weathering. The bulk samples were initially reduced in a jaw crusher,

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and then manually fine powdered in agate mortars to avoid any contamination.

Major oxides were analyzed using a Phillips® MagiX PRO Model 2440 X-ray

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fluorescence (XRF) spectrometer (Philips, Eindhoven, The Netherlands) at the CSIR-National Geophysical Research Institute, Hyderabad. Pressed pellets of the samples and geochemical reference materials were prepared separately and loaded into XRF for analysis. Preparation of pressed pellets involved weighing one gram of finely powdered (-200 mesh ASTM) sample/standard in collapsible aluminium cups (Krishna et al., 2007) filled at the bottom with ~2.5 gm of boric acid, which was later pressed under a hydraulic pressure of 25 t to obtain the pellet. International rock reference materials from the USGS, Geological Survey of Japan, Natural Resources Canada, International Working Groups (France) and National Geophysical Research Institute (India) were used to prepare calibration curves for major elements, and to check the accuracy of analytical

ACCEPTED MANUSCRIPT P a g e | 17 data. The precision and accuracy of the analysis was ~2% RSD for almost all the oxides.

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major

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For trace elements including rare earth (REE) and high field strength elements (HFSE), the homogenized sample powder was dissolved in reagent grade

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HF:HNO3 acid mixture in Savillex® screwtop vessels. A test portion (0.05 g) of

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the sample was added to 25 ml Savillex Teflon pressure decomposition vessels. To each sample, 10 ml of an acid mixture (containing 7:3:2 HF-HNO3–HCl) was 103

Rh solution was added as an internal

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added. Subsequently, 5 ml of 1 ng/ml

standard to each Savillex vessel. After thorough swirling, the vessels were tightly

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closed and kept on a hot plate at ~140 °C for 48 h. Following this, the vessels were opened and the contents were evaporated at 200 °C to near dryness with a

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few drops of HClO4 to ensure complete removal of HF and HCl from the mixture. The remaining residues were dissolved by adding 10 ml of 1:1 HNO 3 and the volume was made to 250 ml with Milli Q® de-ionized water (18 MO), and the solution was stored finally in HDPE bottles. Matrix matching certified reference materials JG-2, JG-3, JB-2 from Geological Survey of Japan and G-1A, G-2 from USGS along with couple of procedural blanks were also prepared with the sample batch by adopting the same protocol described above to negate errors due to reagent and handling. In the present investigation, very clear solutions were obtained for all the samples and calibration standards. Solutions were analyzed by PerkinElmer® Model ELAN® DRC™ II ICP mass spectrometer (PerkinElmer, Inc., Shelton, CT, USA) at the CSIR National Geophysical

ACCEPTED MANUSCRIPT P a g e | 18 Research Institute (NGRI), Hyderabad. The sample introduction consisted of a standard Meinhard® nebulizer with a cyclonic spray chamber. All quantitative

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measurements were performed using the instrument software (ELAN v. 3.1). This

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software uses knowledge-driven routines in combination with numerical calculations (quantitative analysis) to perform an automated interpretation of the

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spectrum of interest. Several well-known isobaric interferences are programmed 103

Rh

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and the corrections are automatically applied (Balaram and Rao, 2003).

was used as an internal standard and external drift was corrected by repeated

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analyses of a 1:5000 solution of JG-2, JG-3 and JB-2, which were also used as calibration standards accordingly. Instrument response was corroborated

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relative to two independent digestions of G-1 and G-2. Precision and accuracy are better than RSD 5% for the majority of trace elements. Anomalies of HFSE

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relative to neighboring REE are given as Nb/Nb*, Zr/Zr*, Hf/Hf* and Ti/Ti*. Mg# is calculated as Mg/(Mg + Fet)*100. Chondrite and primitive mantle normalization values are taken from Sun and McDonough (1989).

3.3 Zircon U-Pb and Lu-Hf isotopes

Zircon grains were separated by gravimetric and magnetic separation from crushed rock samples, and then purified by hand picking under a binocular microscope at the Yu‟neng Geological and Mineral Separation Survey Centre, Langfang city, Hebei Province, China. The grains were mounted in epoxy resin discs and polished to reveal mid-sections, followed by gold sputter coating.

ACCEPTED MANUSCRIPT P a g e | 19 Zircons were imaged under both transmitted and reflected light, and were imaged using cathodoluminescence (CL) to identify internal structures and choose

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potential target sites for U-Pb analyses. The CL imaging was carried out at the Beijing Geoanalysis Centre. Individual grains were mounted along with the 206

Pb/238U age of 417 Ma (Black et al., 2003), onto

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standard TEMORA 1, with

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double-sided adhesive tape and enclosed in epoxy resin discs. The discs were

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polished to a mid depth and gold coated for cathodoluminescence (CL) imaging and U-Pb isotope analysis. Zircon morphology, inner structure and texture were

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examined by using a JSM-6510 Scanning Electron Microscope (SEM) equipped with a backscatter probe and Chroma CL probe. The zircon grains were also

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examined under transmitted and reflected light images using a petrological microscope. Zircon U-Pb dating and in-situ Hf isotopic analyses were conducted

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by a Neptune MC-ICP-MS equipped with a 193 nm Geolas Q Plus ArF excimer laser ablation at the Tianjin Institute of Geology and Mineral Resources, with spot sizes of 35 μm and 50 μm, respectively. In situ zircon Hf isotopic analyses were conducted on the same spots which were analyzed for U-Pb dating. Zircon GJ-1 was used as an external standard for U-Pb dating and In-situ zircon Hf isotopic analyses. Common-Pb corrections were made using the method of Andersen (2002). Data were processed using the GLITTER and ISOPLOT (Ludwig, 2008) programs. Errors on individual analyses by LA-ICP-MS are quoted at the 95% (1σ) confidence level. Details of the technique are described by Li et al. (2009) and Geng et al. (2011).

ACCEPTED MANUSCRIPT P a g e | 20 4. Petrology and mineral chemistry

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4.1 Petrography

The samples discussed in this study are classified into nine rock types; dioritic to gneiss,

metadiorite

and

metagranite,

charnockite,

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granitic

amphibolite,

magnetite quartzite (meta

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hornblende schist, quartz-mica schist, migmatitic biotite gneiss, banded BIF), and calcareous schist. A summary of the

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petrographic features of the each rock types analyzed in this study is given

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below. Representative photomicrographs are shown in Figs. 5 and 6.

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4.1.1. Dioritic and granitic gneiss

Sample NDPL-1 is a typical dioritic gneiss that contains hornblende (45-55%), plagioclase (35-45%), epidote (2-5%), titanite (1-2%), and quartz (1-2%) with accessory ilmenite, apatite, and zircon. Gneissosity defined by alternation of plagioclase-rich and hornblende-rich layers is obvious in outcrop and in hand specimen. The rock shows weak foliation defined by aligned subhedral hornblende (0.2-1.8 mm) (Fig. 5a). Plagioclase (0.1-1.1 mm) is subhedral and rounded. Quartz is present as aggregates of a few fine grains only in the plagioclase-rich layer. Titanite (<0.2 mm) is subhedral and occurs along the grain margin of hornblende. Epidote is euhedral to subhedral, fine to medium grained (0.05-0.4 mm), and rectangular to thin needle-like grains mostly occurring along

ACCEPTED MANUSCRIPT P a g e | 21 the grain boundaries of plagioclase and hornblende. Some coarse epidote grains show optically concentric zoning. Epidote and titanite are also present as

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inclusions in plagioclase and hornblende. These textures suggest that the

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protolith of the rock is a diorite which underwent epidote-amphibolite- to

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amphibolite-facies metamorphism.

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Sample PRV-2 shows textures and mineral assemblage similar to sample NDPL1. The rock is composed of hornblende (30-40%), plagioclase (30-40%), quartz

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(10-20%), and ilmenite (2-5%) with accessory apatite, epidote, and zircon. Foliation is not obvious in this sample as hornblende occurs as randomly

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oriented flakes of various grain sizes (0.1 to 2.2 mm) (Fig. 5b). The hornblende is often intergrown with ilmenite (Fig. 5b), the latter carrying thin exsolution lamellae

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of hematite. Plagioclase is medium to coarse grained (0.2-1.5 mm), but is highly coarse grained (~3 mm) in plagioclase-rich domains of the rock where the mineral shows irregular grain margins probably related to metamorphic overgrowth. Rare epidote occurs along the grain boundaries of plagioclase and hornblende as metamorphic/hydrothermal products. The protolith of the rock may be diorite or andesite.

Sample IRK-1 is a dark grayish migmatitic rock with obvious gneissosity defined by hornblende-rich melanocratic (mafic) layers and quartz-rich leucocratic (felsic) layers. The mineralogy of the felsic layer is quartz (35-45%), plagioclase (3040%), biotite (10-20%), K-feldspar (10-20%), opaque minerals (ilmenite and

ACCEPTED MANUSCRIPT P a g e | 22 pyrite; 1-2%), and accessory hornblende and epidote (Fig. 5c), whereas the mafic layer is composed of plagioclase (30-40%), hornblende (20-30%), biotite

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(15-25%), quartz (1-2%), and ilmenite (1-2%) (Fig. 5d). Foliation defined by

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aligned biotite (~0.3 mm) and hornblende (~1.9 mm), and elongated plagioclase (~1.5) is obvious in the mafic layer. Mylonitic textures such as fine-grained

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aggregates of plagioclase, hornblende, and biotite around the coarse-grained

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porphyroblastic minerals, and wavy extinction of plagioclase suggest the effect of deformation after the peak amphibolite-facies metamorphism. The leucocratic

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layer is characterized by subhedral plagioclase grains surrounded by fine-grained aligned biotite and quartz aggregates (Fig. 5c) possibly formed by the

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mylonitization.

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Sample PDM-2 is a fine-grained felsic gneiss composed of aligned paragonite (60-70%), quartz (30-40%), and minor rutile and kyanite. All the minerals are finegrained (<0.7 mm) except for some rutile grains (~1.5 mm), suggesting that the protolith of the rock may be felsic tuff.

4.1.2. Metadiorite and metagranite

Sample PRY-1 is a gneissose dioritic rock, and contains scapolite with higher modal abundance of epidote than the other dioritic rocks. The rock is composed of plagioclase (35-45%), hornblende (25-35%), epidote (10-15%), scapolite (2-

ACCEPTED MANUSCRIPT P a g e | 23 5%), biotite (2-5%), and titanite (1-2%) (Fig. 5e). A well-defined foliation is observed by the weakly aligned subidioblastic hornblende (0.2-0.8 mm) and

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biotite (0.02-0.2 mm). The biotite shows intergrowth with rim of the hornblende.

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Plagioclase (0.2-1.1 mm) crystals are not aligned along the foliation. The grain boundaries of the minerals are defined by aggregates of epidote and titanite.

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Scapolite occurs as aggregates of medium-grained subidioblasdic (0.3-1.1 mm)

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grains forming scapolite-rich domains. Titanite occurs as subidioblastic prisms. These textures suggest that the rock underwent epidote-amphibolite-facies

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metamorphism.

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Sample TNL-2-1 is a coarse-grained granitic rock composed of K-feldspar (4555%), quartz (15-25%), hornblende (10-15%), plagioclase (2-5%), biotite (2-5%),

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and minor titanite, epidote, ilmenite, apatite, and zircon (Fig. 5f). The rock is characterized by coarse-grained (~8 mm) porphyroblastic perthite (representing relict phenocryst) composed of about 80% K-feldspar and 20% thin plagioclase lamellae. Quartz is also coarse grained (~4.2 mm) and elongated along the rock foliation. The matrix of the rock is composed of aggregates of medium-grained hornblende (~2.1 mm), biotite (~2.4 mm), fine-grained quartz (0.1-1.1 mm), and plagioclase (0.1-0.5 mm), which are aligned and form dominant foliation of the rock. The coarse-grained nature of the rock and mineralogy suggests porphyritic granite as the protolith.

4.1.3. Charnockite

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Sample NDK-1 is a dark greenish-gray massive rock composed of plagioclase

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(50-60%), quartz (20-30%), K-feldspar (10-20%), orthopyroxene (1-2%), and

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accessory magnetite, apatite, and zircon (Fig. 5g). This is the only granulitefacies lithology examined in this study and comes from the margin of the Coorg

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Block. The rock displays medium-grained granoblastic texture without any

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obvious foliation. Orthopyroxene (0.2-0.6 mm) is subhedral to anhedral, and scattered randomly along the grain boundaries of quartz and feldspars.

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Plagioclase (0.2-0.7 mm) is antiperthitic and contains thin lamellae of K-feldspar. K-feldspar is also present as fine-grained interstitial minerals between the

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antiperthitic plagioclase and rounded quartz (0.1-0.6 mm). These textures are nearly identical with those reported from massive magmatic charnockite in the

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Coorg Block (e.g., Santosh et al., 2015).

4.1.4. Amphibolite

Sample APP-1 is a typical medium-grained massive amphibolite, which corresponds to metamorphosed mafic magmatic enclave (MME) within host dioritic rock. The rock is composed of hornblende (50-60%), plagioclase (2030%), and biotite (10-15%) with accessory quartz (2-3%), apatite, and zircon (Fig. 5h). The rock shows crystalloblastic texture of semi-equigranular aggregates of medium-grained (0.2-0.6 mm) hornblende (50-60%) and

ACCEPTED MANUSCRIPT P a g e | 25 plagioclase (20-30%) with accessory biotite (5-10%), quartz (2-3%), apatite, and zircon. Grain size of the minerals increases toward the margin of the MME near

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the host dioritic rock. Biotite occurs around hornblende probably as a retrograde

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mineral. Quartz is present only as fine-grained (~0.15 mm) rounded minerals

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along the grain boundaries of plagioclase and hornblende.

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4.1.5. Hornblende schist

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Sample KTMR-1 is a coarse-grained hornblendite-rich schistose rock. It is composed mainly of calcic amphibole (40-50% greenish hornblende and 10-20%

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colorless actinolite) and cummingtonite (30-40%) with accessory chlorite (2-5%) and rutile (<1%). All the minerals are aligned along the foliation (Fig. 6a). Both

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calcic amphibole and cummingtonite are coarse grained (~4.5mm) and subidioblastic. The greenish hornblende is often surrounded by colorless actinolite, probably reflecting decreasing P-T during the amphibole growth. Chlorite occurs as an interstitial mineral around the amphiboles, possibly as a retrograde mineral.

4.1.6. Quartz-mica schist

Sample TNL-1-1 is a typical well-foliated quartz-mica schist. The rock is composed of muscovite/paragonite (80-90%) and quartz (10-20%) with accessory chlorite (altered biotite) and rutile (Fig. 6b). The rock exhibits strong

ACCEPTED MANUSCRIPT P a g e | 26 foliation both in hand specimen and in thin section defined by nematoblastic aggregates of white mica (<0.15 mm) and chlorite (<0.2 mm), and elongated

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ribbon quartz (0.1-1.9 mm) with width:length ratio of 1:3 to 1:5.

Sample TNL-3-1 is a moderately-foliated quartz-mica schist. The mineral

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assemblage is similar to that of sample TNL-1-1, although this sample shows

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abundant quartz (60-70%) (Fig. 6c). Foliation is defined by fine-grained muscovite + sillimanite aggregates, although quartz (0.2-2.6 mm) and chlorite

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(0.05-0.7 mm) are relatively coarse-grained and randomly oriented.

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Sample MBM-1 is weakly foliated quartz-mica schist with >90% quartz and ~10% muscovite (Fig. 6d). The grain size of quartz (~3.9 mm) and muscovite (~2.3 mm)

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are coarser than the above two samples. The width:length ratio of most quartz grains ranges approximately from 1:1 to 1:2, and therefore foliation is not obvious in the sample.

Samples NDV-1 and NDV-2 are garnet-bearing quartz-mica schist that comprises quartz (40-50%), muscovite (15-25%), chlorite (10-20%), garnet (5-10%), and rutile (~1%) (Fig. 6e). The foliation of the rock is defined by aligned flakes of muscovite and chlorite grains, and elongated ribbon quartz. All the minerals are fine grained (<0.3 mm), while some coarse-grained garnet (~1.1 mm) and quartz (~2.2 mm) are also present.

ACCEPTED MANUSCRIPT P a g e | 27 4.1.7. Migmatitic biotite gneiss

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Sample MNT-1, which corresponds to melanocratic (restitic) portion of the

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migmatitic gneiss, is a medium-grained foliated rock with quartz (20-30%), biotite (20-25%), plagioclase (15-20%), epidote (5-10%), Fe-Ti oxide (~1%), and calcite

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(~1%) (Fig. 6f). Brownish biotite (0.1-0.9 mm) is present as aligned flakes and

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defines foliation of the rock. Epidote (0.1-0.3 mm) is also aligned together with the biotite. Plagioclase occurs as medium-grained (~1.9 mm) subhedral spots in

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fine-grained matrix, and contains numerous fine-grained inclusions of epidote. Quartz is fine-grained (0.1-0.4 mm), not well oriented, and fills the matrix of

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biotite and epidote.

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4.1.8. Banded magnetite quartzite (meta BIF)

Sample KTMR-2 (Fig. 6g) is composed of nearly equal amounts of quartz and magnetite. No other ferromagnesian and aluminous minerals are present in the rock. The rock is characterized by thin alternation of quartz and magnetite layers, probably reflecting original sedimentary structure of banded iron-formation. The quartz layers are composed of aggregates of medium-grained (~0.6 mm) quartz probably formed by metamorphic crystallization.

4.1.9. Calcareous schist

ACCEPTED MANUSCRIPT P a g e | 28 Samples TNL-4-1 (Fig. 6h) and TNL-4-2 are calcareous schist comprising carbonate (dolomitic; 50-60%), quartz (20-30%), chlorite (5-15%), and muscovite

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(2-5%). Opaque minerals are absent. The rock is characterized by euhedral to

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subhedral dolomite (0.2-1.4 mm) surrounded by fine-grained quartz (0.05-0.3 mm), chlorite (0.2-0.5 mm), and muscovite (0.1-0.6 mm). Quartz and muscovite

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are also present as inclusions in the dolomite, while chlorite occurs only in the

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matrix. Weak foliation of the rock is defined by aligned muscovite and chlorite,

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whereas the quartz and dolomite are not aligned.

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4.2. Mineral Chemistry

Representative compositions of minerals from electron microprobe analyses are

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given in Tables 2 to 5 (Supplementary Data), plotted in Figure 7, and briefly discussed below.

4.2.1. Calcic amphibole

Calcic amphibole in dioritic gneiss (samples NDPL-1, PRV-2, and IRK-1), metadiorite (sample PRY-1), metagranite (sample TNL-2-1), amphibolite (sample APP-1), and hornblende schist (sample KTMR-1) shows notable compositional variation depending on its occurrence (Table 2, Fig. 7a). The mineral is characterized by high Ca and (Na+K)A contents (1.76-1.91 pfu and 0.54-0.78 pfu, respectively), except in sample KTMR-1 (hornblende schist) where the

ACCEPTED MANUSCRIPT P a g e | 29 amphibole shows (Na+K)A of 0-0.26. Calcic amphibole in the sample shows obvious core-rim texture with greenish core (magnesio-hornblende; Si = 7.23-

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7.28, XMg = Mg/(Fe+Mg) = 0.76-0.79) surrounded by colorless rim (actinolite; Si =

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7.89-7.63, XMg = 0.82-0.83). Sample KTMR-1 also contains cummingtonite (not shown in Fig. 7a) which is characterized by high XMg (= 0.81-0.83) and Si (7.97-

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7.99 pfu), and low Al (0.11-0.16 pfu).

Most calcic amphiboles in dioritic gneiss, metadiorite, and amphibolite are

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classified as edenite or pargasite with Si = 6. 31-6.75 and XMg = 0.5-0.6. Those in sample PRV-2 (dioritic gneiss) are slightly Fe-rich as ferro-pargasite (Si = 6.31-

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6.40 and XMg = 0.46-0.49). Calcic amphibole in sample TNL-2-1 (metagranite)

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shows the lowest XMg of 0.26-0.27 as ferro-edenite.

4.2.2. Plagioclase

Plagioclase in the examined rocks shows significant compositional variations depending on lithologies (Table 3). Plagioclase in dioritic gneiss (samples NDPL1, PRV-2, and IRK-1) and metadiorite (sample PRY-1) shows nearly consistent anorthite contents of An20-32, although core of the plagioclase in sample NDPL-1 is slightly anorthite rich as An40 compared to its rim (An32). Plagioclase with a similar composition occurs in amphibolite (sample APP-1, An36-38). On the other hand, plagioclase in migmatitic biotite gneiss (sample MNT-1) and charnockite (sample NDK-1) is slightly albite rich as An17-18 and An15-16, respectively.

ACCEPTED MANUSCRIPT P a g e | 30 Plagioclase in metagranite (sample TNL-2-1), which occurs as exsolution lamella in K-feldspar, shows the lowest anorthite content of An 4-12.The host K-feldspar in

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the metagranite is orthoclase-rich and compositionally nearly homogeneous as

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Or94-96.

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4.2.3. White mica

White mica in the examined rocks shows wide compositional variations including

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muscovite, phengite, and paragonite (Fig. 7b, Table 4). Most white micas in the quartz-muscovite schist (sample TNL-3-1, MBM-1, NDV-1, and NDV-2) are

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muscovite-phengite series, but some white micas in sample TNL-1-1 is significantly Na-rich as paragonite (Na/(Na+K) ~0.88). White mica in sample

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MBM-1 shows the highest Fe+Mg content of ~0.97 pfu as phengitic mica. Composition of white mica in calcareous schist (sample TNL-4-2) is also phengitic as Fe+Mg = 0.37-0.43 pfu.

4.2.4. Biotite

Biotite in metagranite (sample TNL-2-1), migmatitic biotite gneiss (sample MNT1), metadiorite (sample KDG-1), amphibolite (sample APP-1), and quartz-mica schist (samples TNL-3-1 and NDV-1) exhibits moderate TiO2 content of 1.7-3.4 wt.% (Fig. 7c, Table 4). Biotite in amphibolite and quartz-mica schist is Mg-rich as XMg = 0.51-0.62, while that in metagranite and migmatitic biotite gneiss is Fe-rich

ACCEPTED MANUSCRIPT P a g e | 31 as 0.33-0.34 and 0.37-0.38, respectively, probably related to Fe-rich character of

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the host rock.

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4.2.5. Garnet

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Garnet occurs only in garnet-bearing quartz-mica schist (sample NDV-1), and it is

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essentially almandine-rich with minor pyrope, grossular, and spessartine components (Table 5). There is no obvious compositional variation between core

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(Alm62-63 Prp32-33 Grs4-5 Sps0-1) and rim (Alm62-63 Prp32-33 Grs4-5 Sps0-1) of single

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4.2.6. Orthopyroxene

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grains.

Orthopyroxene occurs only in the charnockite. The mineral shows moderate XMg of 0.61-0.64 and low Al content of 0.05-0.06 pfu (1.2-1.4 wt.% Al2O3, Table 5). These are nearly consistent with the orthopyroxene compositions reported from charnockites in the Coorg Block (XMg =0.55-0.62, Al = 0.03-0.05; Santosh et al., 2015)

4.2.7. Epidote

Epidote is a dominant mineral in migmatitic biotite gneiss (sample MNT-1), and an accessory mineral in dioritic gneiss (samples NDPL-1 and IRK-1) and

ACCEPTED MANUSCRIPT P a g e | 32 metadiorite (sample PRY-1). Its composition is close to the ideal composition of epidote, and its Fe3+ content varies from 0.61-0.62 pfu (sample PRY-1), 0.63-

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0.65 pfu (sample NDPL-1), 0.80-0.82 pfu (sample IRK-1), and 0.79-0.80 pfu

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(sample MNT-1) (Table 5). The replacement of Ca by Mn is very minor, only ~2.1

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% (up to 0.042 pfu of Mn in sample MNT-1).

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4.2.8. Chlorite

Chlorite is a common mineral in quartz-mica schist (samples TNL-1-1, TNL-3-1,

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NDV-1, NDV-2), and also a minor retrograde mineral in dioritic gneiss (sample

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IRK-1) and hornblende schist (sample KTMR-1). Its XMg varies depending on samples from 0.51-0.63 (quartz-mica schist), 0.63-0.64 (dioritic gneiss), to 0.72

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(hornblende schist) (Table 5). Chlorite in sample IRK-1 (dioritic gneiss) contains up to 1.4 wt.% Cr2O3 and up to 0.12 wt.% MnO. Up to 0.9 wt.% K2O in chlorite in sample TNL-3-1 (quartz-mica schist) suggests the chlorite is an alteration product from biotite.

4.3. Geothermometry

The peak metamorphic temperature of the metaigneous rocks in our study area was estimated using hornblende + plagioclase geothermometer, as these minerals coexist in dioritic rocks and amphibolite. Based on hornblende solidsolution models and well-constrained natural and experimental studies, two

ACCEPTED MANUSCRIPT P a g e | 33 geothermometers were calibrated by Holland and Blundy (1994) based on the edenite-tremolite reaction, which is applicable to quartz-bearing rocks, and

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edenite-richterite reaction, which is applicable to both quartz-bearing and quartz-

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free rocks. As quartz is present in the samples, the two thermometers were used for the calculation of temperature. The calculated results for dioritic gneisses are

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680720C for sample NDPL-1, 640-690C for sample PRV-2, and 660-690C for

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sample IRK-1 at 6 kbar. Metadiorite (sample PRY-1) shows slightly lower but nearly consistent temperature range of 620-670C, whereas the temperatures

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estimated for the amphibolite (sample APP-1) are slightly higher but also nearly

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consistent as 690-730C. The amphibolite-facies temperatures obtained from

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dioritic gneiss, metadiorite, and amphibolite are consistent with the common

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occurrences of calcic amphibole and lack of pyroxenes.

The peak metamorphic temperature of metasediments was estimated using garnet-muscovite (phengite) geothermometry. Wu and Zhao (2006) calibrated a new garnet-muscovite geothermometer under conditions of T = 450-760C and P = 0.8-11.1 kbar using a large number of metapelitic samples. Application of the method to garnet-bearing quartz-mica schist (sample NDV-2) yielded a temperature range of 710-760C. The results are slightly higher than those from the metaigneous rocks (620-730C), but also confirm the peak amphibolite-facies metamorphism.

5. Geochemistry

ACCEPTED MANUSCRIPT P a g e | 34 The major and trace element compositions of representative samples from Coorg Block and surrounding sutures are given in Table 6 (Supplementary Data). In

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conjunction with the petrographic observations and the similarities in the major

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elemental compositions, the magmatic rocks of present study from the margin of the Coorg Block and bounding suture zones are broadly grouped into:

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charnockite (NDK-1), dioritic gneiss (IRK-1, NDPL-1and PRY-1), gneissic diorite

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(MNT-1, PDM-2 and PRV-2) and hornblende schist (KTMR-1). The hornblende schist represents near primitive magma composition, whereas the charnockite

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and granitoids might represent the more differentiated members, with the remaining rocks in the suite corresponding to intermediate compositions. The

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charnockite in our study shows the highest SiO2 content (71.50 wt.%) and in the TAS diagram (Cox et al., 1979) this sample falls in the field of granite, which is in

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accordance with the available geochemical data for the Coorg charnockites (Santosh et al., 2015) (Fig. 8a). The diorites are distributed within the fields of diorite and granodiorite, whereas the gneissic rocks are confined to the syenodiorite field, and the hornblende schist possess low silica and alkalis (Fig. 8a). Other major elemental features of these rocks include broadly metaluminous nature (<15 wt% Al2O3) (Fig. 8b) (Shand, 1943), and higher sodic compositions over potassium (Table 6). The hornblende schist possess low alumina (5.63 wt% Al2O3), high MgO (24.71 wt.%) (Table 6). There are subtle variations in the trace elemental systematics. The charnockite sample shows the highest REE fractionation ((La/Yb)cn=25.15), with the LREE enrichment ((La/Sm)cn=6.90 (Table 6) similar to charnockites from other parts of the Coorg Block, along with +ve Eu

ACCEPTED MANUSCRIPT P a g e | 35 anomaly (Fig. 9a). The diorites also display fractionated REE patterns (Fig. 9b), although the extent of fractionation and LREE enrichment are less than that of

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the Coorg charnockites. These rocks exhibit mild positive Eu anomalies (Fig. 9b)

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suggesting the plagioclase accumulation during melting. The gneisses are variably fractionated with mild LREE enrichment, but these rocks display slightly

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negative Eu anomalies (Fig. 9c and Table 6) suggesting plagioclase fractionation.

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The hornblende schist shows slightly fractionated REE pattern, having low REE abundances when compared to other magmatic rocks of the Coorg block (Fig. 9).

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Other common characteristics include consistently negative Nb anomalies in the primitive mantle normalized multi element variation diagrams (Sun and

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McDonough, 1989) for all the rock types of Coorg block (Fig. 9d-f), and the relative enrichment of LILE (large ion lithophile elements) over HFSE (high field

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strength elements) (Table 6). These features are generally ascribed to magmas generated in convergent margin setting (Pearce and Peate, 1995). The subduction-derived magmatism is also confirmed by the confinement of these rocks within the field of volcanic arc granites (VAG) in the tectonic discrimination diagram (Fig. 10a), and further substantiated by immobile elemental systematics (Fig. 10b).

6. Zircon U-Pb geochronology and Lu-Hf isotopes

6.1 U-Pb Geochronology A summary of the location and salient features of the samples analyzed for

ACCEPTED MANUSCRIPT P a g e | 36 geochronology are given in Table 1, and the zircon U-Pb results are given in Supplementary Table 7 and 8. Zircon Lu-Hf data for the metaigneous and

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metasedimentary rocks are given in Tables 9 and 10 respectively. Representative

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11-15, and the age data are plotted in Figs. 16-22.

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CL images of the zircons from different rock types in this study are shown in Figs.

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6.1.1 Metaigneous rocks

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IRK-1 [dioritic gneiss]

Zircons from the sample IRK-1 are mostly colorless, and some grains are light

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brown. Most of the zircons are transparent or translucent euhedral crystals and display prismatic morphology, with few of them showing grain margin dissolution

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leading to sub-rounded morphology. The grains range from 100-200×30-80μm in size with aspect ratios of 3:1 to 2:1, and rarely up to 6:1. In CL images, the zircons display clear oscillatory zoning typical of magmatic origin with very thin and light rims (Fig. 11).

A total of 30 spots were analyzed on 30 zircon grains (Table 7). The results show Pb content in the large range of 72 to 629 ppm, U content in the range of 82 to 817 ppm and Th in the range of 16 to 198 ppm, with Th/U ratios of 0.15 to 0.53 (except one spot with Th/U ratio of 0.09). In the concordia diagram (Fig. 16a), all the 30 spots cluster as a coherent group (concordance of 91%–100%) with 207

Pb/206Pb spot ages ranging from 3408 to 3525 Ma and weighted mean age of

ACCEPTED MANUSCRIPT P a g e | 37 3502±11 Ma (MSWD=1.02, N=30).

PT

NDPL-1 [dioritic gneiss]

RI

Zircons in this sample are colorless or light brownish and transparent to translucent. Some are euhedral crystals and show prismatic morphology,

SC

whereas others are stumpy or sub-rounded. The grains range from 100-250×50-

NU

200μm in size with aspect ratios of 3:1 to 1:1 (mostly around 120×100μm 100×50μm in size with aspect ratios of 2:1 to 1.2:1). In CL images, most of the

MA

zircons display core-rim texture (Fig. 12). A total of 27 spots were analyzed on 27 zircon grains (Table 7). The results show low Pb, U, Th contents in the range

TE

D

of 3 to 49 ppm, 6 to 96 ppm and 0.4 to 39 ppm, respectively, with Th/U ratios of 0.1 to 0.5 (except few grains with < 0.1). Among the 27 spots, most are

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concordant, with few grains showing Pb-loss. The data define an upper intercept age of 2503±11 Ma (MSWD=1.4, N=27), and is similar to the

207

Pb/206Pb

weighted mean age of the concordant group of zircons at 2500±11 Ma (MSWD=1.3, N=27) (Fig. 16c,d).

MNT-1 [migmatitic biotite gneiss] Zircons from this metagranite sample are colorless or light brownish and transparent to translucent. Most of the grains are euhedral with prismatic morphology, and few grains are stumpy. They range from 100-300×50-100μm in size with aspect ratios of 3:1 to 1.2:1 (mostly around 120×60μm in size with aspect ratios of 2:1). In CL images, most of the zircons display core-rim texture,

ACCEPTED MANUSCRIPT P a g e | 38 with few grains showing clear oscillatory zoning surrounded by metamorphic rims (Fig. 11). However, the rims with bright luminescence are too thin to for U-Pb

PT

dating. A total of 24 spots were analyzed on 24 zircon grains (Table 7). The

RI

results show Pb content in the large range of 12 to 103 ppm, U content in the range of 16 to 195 ppm and Th in the range of 3 to 153 ppm, respectively, with

SC

high Th/U ratios of 0.29 to 3.29 (except one spot with Th/U ratio of 0.06). All the

NU

24 spots cluster as a concordant group (concordance 96%–100%). The 207

Pb/206Pb spot ages range from 2482 to 2611 Ma and yield a weighted mean

MA

age of 2554±13 Ma (MSWD=2.5, N=24) (Fig. 17a,b).

TE

D

NDK-1 [charnockite]

Zircons from the charnockite sample are light brownish and transparent or

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translucent. Some zircons are euhedral crystals and show prismatic morphology, the others are stumpy or partly rounded. The grains range from 50-200×50100μm in size with aspect ratios of 3:1 to 1:1. In CL images, many of the zircons display dark luminescence, and some display clear oscillatory zoning with slightly brighter luminescence (Fig. 12). A total of 30 spots were analyzed on 30 zircon grains (Table 7). The results show Pb content in the large range of 108 to 1186 ppm, U content in the range of 154 to 1731 ppm and Th in the range of 14 to 309 ppm, respectively, with Th/U ratios of 0.11 to 0.40 (except few grains with Th/U values < 0.1). 29 spots of the 30 spots fall along a discordia line and define an upper intercept age of 3172±8 Ma (MSWD=0.76, N=29), which is similar to the 207

Pb/206Pb weighted mean age of 3172±6 Ma (MSWD=1.11, N=29) computed for

ACCEPTED MANUSCRIPT P a g e | 39 this sample (Fig. 17c,d). The remaining one spot (spot 17) is a xenocryst and

PT

yield the 207Pb/206Pb age of 3284±16 Ma with a concordance of 99%.

RI

PRY-1 [metadiorite]

Zircons from this sample are colorless or light brownish and translucent. Most of

SC

the grains are euhedral and show prismatic morphology and only few zircons are

NU

slight rounded or stumpy. The grains range from 100-300μm×80-150μm in size with the aspect ratios of 3:1 to 2:1. In CL images, the zircons display the unclear

MA

zoning and some of them show core-rim texture (Fig. 13). A total of 25 spots were analyzed on 25 zircon grains (Table 7). The results show relatively low Pb,

TE

D

U, Th contents in the large ranges of 4 to 165 ppm, 8 to 331 ppm, 2 to 109 ppm, respectively, with Th/U ratios of 0.21 to 0.49. All the 25 spots are concordant and

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cluster as a coherent group on concordia (except spot 26 which shows Pb loss). The data define an upper intercept age of 2518±13 Ma (MSWD=0.85, N=25), closely comparable with the

207

Pb/206Pb weighted mean age of 2501±11 Ma

(MSWD=2.0, N=25) (Fig. 18a,b).

PDM-2 [metamorphosed felsic tuff] Zircons in this rock are light brownish and transparent or translucent. Most of the grains are euhedral and show long prismatic morphology, ranging in size from 50-150μm×30-60μm with the aspect ratios of 4:1 to 2:1. In CL images, many of the zircons display unclear zoning with only few grains showing oscillatory zoning (Fig. 12).

ACCEPTED MANUSCRIPT P a g e | 40

A total of 31 spots were analyzed on 31 zircon grains (Table 7). The results show

PT

Pb content in the large range of 100 to 369 ppm, U content in the range of 212 to

RI

778 ppm and Th in the range of 2 to 194 ppm, respectively, with low Th/U ratios mostly less than 0.29 (except one spot with Th/U ratio up to 0.53). All the 31

207

Pb/206Pb ages ranging from 2413 to

NU

coherent group on the concordia with

SC

spots are concordant and can be divided into two groups. 29 spots cluster as a

2570 Ma (concordance of 97%-100%) and yield

207

Pb/206Pb weighted mean age

MA

of 2452±9 Ma (MSWD=2.5, N=29) (Fig. 18c,d). The remaining two spots (spots

PRV-2 [dioritic gneiss]

TE

D

22 and 30) show 207Pb/206Pb spot ages of 2570±16 Ma and 2527±15 Ma.

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Zircons from this sample are colorless or light brownish and transparent to translucent. Most of the grains are euhedral and show prismatic morphology. The grains range from 100-300μm×100-150μm in size with aspect ratios of 3:1 to 2:1. In CL images, all the zircon grains display bright luminescence. Many of the zircons show core-rim texture, and some grains show clear oscillatory zoning (Fig. 13), suggesting magmatic crystallization. A total of 33 zircon spots were analysed on 33 grains (Table 7) and the results show Pb content in the range of 6 to 181 ppm, U content in the range of 10 to 339 ppm and Th in the range of 15 to 116 ppm, with high Th/U ratios (up to 3.72). The 33 analysed spots can be divided into 3 groups. Spots 5 and 28 are concordant and show

207

Pb/206Pb ages

of 2706±16 Ma and 2737±17 Ma, respectively. Spot 22 is also concordant and

ACCEPTED MANUSCRIPT P a g e | 41 yields

207

Pb/206Pb age of 2627±15 Ma. Among the remaining 30 spots, most of

the data are concordant but few are discordant and show Pb loss. The 30 spots

PT

define an upper intercept age of 2485±13 Ma (MSWD=1.00, N=30), similar to the Pb/206Pb mean age of 2475±12 Ma (MSWD=1.6, N=30) from this sample (Fig.

RI

207

SC

19a,b).

NU

KTMR-1 [hornblende schist]

Zircons from this sample are light brownish or colorless, transparent or

MA

translucent. Some of the grains are euhedral crystals and show prismatic morphology, but most of them are subhedral or anhedral. The grains are very

TE

D

small ranging from 30-80×20-60μm in size with aspect ratios of 2:1 to 1:1 (except few with aspect ratios of 3:1).

In CL images, the zircons display unclear

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oscillatory zoning or lack any zoning (Fig. 11). A total of 30 spots were analyzed on 30 zircon grains (Table 7). The results show Pb content in the range of 382 to 1643 ppm, U content in the range of 725 to 3072 ppm and Th in the range of 111 to 1624 ppm, respectively, with Th/U ratios of 0.14 to 0.57 (except one spot with Th/U ratio of 0.06). All the 30 spots are concordant (concordance 96%–100%). The

207

Pb/206Pb spot ages range from 2427 to 2549 Ma and yield a weighted

mean age of 2495±12 Ma (MSWD=4.5, N=30) (Fig. 19c,d).

6.1.2 Metasedimentary rocks

MBM-1 [quartz mica schist]

ACCEPTED MANUSCRIPT P a g e | 42 Zircons from this rock are light brownish and few grains are colorless. They are transparent or translucent, and most of the grains are euhedral crystals showing

PT

prismatic morphology. The grains range from 50-200×30-80μm in size with

RI

aspect ratios of 3:1 to 1:1 (mostly around 100×50μm in size with aspect ratios of 2:1).

In CL images, most of the zircons display clear oscillatory zoning

SC

corresponding to magmatic crystallization whereas some show unclear zoning or

NU

lack any zoning, with dark or bright luminescence (Fig. 14), suggesting metamorphic origin. A total of 23 spots were analysed on 23 grains. The results

MA

show Pb content in the large range of 10 to 136 ppm, U content in the range of 24 to 298 ppm and Th in the range of 7 to 210 ppm, respectively, with Th/U ratios

TE

D

of 0.22 to 1.41 (except one spot with Th/U ratio of 0.06). The data can be divided into 4 groups: the first group including 3 spots (spots 15, 18, 29) is concordant 207

Pb/206Pb spot ages of 3273±16 Ma, 3141±22 Ma, and 2901±22 Ma. The

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with

second group of concordant zircons include 5 grains (spots 4, 11, 14, 23, 24) with 207

Pb/206Pb weighted mean age of 2659±31 Ma (MSWD=1.5, N=5) (Fig. 20a,b,c).

The third group includes two concordant spots (spots 6, 16) with

207

Pb/206Pb

ages of 1855±38 Ma and 1953±18 Ma. The fourth group has 13 spots which fall along a discordia and define an upper intercept age of 2589±39 Ma and a lower intercept age of 1688±58 Ma (MSWD=0.36, N=13) (Fig. 20a,b,c).

TNL-3/1 [quartz mica schist]

Zircons in this sample are colorless or light brownish, and transparent or

ACCEPTED MANUSCRIPT P a g e | 43 translucent. Most of them are slightly rounded or stumpy and only few of them are euhedral and show prismatic morphology. The grains are small (the length

PT

and width are less than 100μm in size with the aspect ratios are around 1.5:1 to 1:1) and few of them that show prismatic morphology have a size range of 100In CL images, some

RI

200μm×30-50μm with the aspect ratios are up to 4:1.

SC

zircons show unclear oscillatory zonings, suggesting magmatic source (Fig. 15).

NU

Many grains display core-rim texture with thin metamorphic rims yielding bright luminescence. A total of 36 zircon spots were analysed on 36grains for U-Pb

MA

dating. The results show Pb content in the large range of 35 to 425 ppm, U content in the range of 50 to 297 ppm and Th in the range of 23 to 386 ppm,

D

respectively, with Th/U ratios up to 1.35. All the 36 spots are concordant, and can 207

TE

be divided into 5 groups with

Pb/206Pb mean ages of 3.4 Ga (n=1), 3.1 Ga

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(n=2), 2.9 Ga (n=2), 2.7 to 2.2 Ga (n=19) and 2.0 to 1.35 Ga (n=12) (Fig. 20 d,e).

NDV-1 [quartz mica schist with garnet]

Zircons from the sample NDV-1 are colorless or light brownish and transparent or translucent. Most of the zircons are rounded and only few of them are euhedral and show prismatic morphology. The grains are very small and the length and width are less than 100μm (mostly less than 60μm), the aspect ratios are around 1.2:1 or 1:1 (few of them up to 2:1). In CL images, many of the zircons display unclear zoning with very thin metamorphic rims showing bright luminescence. Some of them show clear oscillatory zoning (Fig. 14), suggesting the magmatic

ACCEPTED MANUSCRIPT P a g e | 44 source. A total of 29 spots were analyzed on 29 zircon grains. The results show Pb

PT

content in the large range of 102 to 673 ppm, U content in the range of 135 to

RI

963 ppm and Th in the range of 1 to 184 ppm, respectively, with Th/U ratios of 0.15 to 0.87 (except few of them less than 0.1). Among the 29 spots, most of

SC

them are concordia plots and only few of them are slightly discordant with Pb-

N=29), similar to the

NU

loss. The data show define an upper intercept age of 3122±11 Ma (MSWD=0.71, 207

Pb/206Pb weighted mean age of 3120±7 Ma (MSWD=1.5,

TE

D

MA

N=29) (Fig. 21a,b).

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NDV-2 [quartz mica schist with garnet]

Zircons from this sample are light brownish and transparent or translucent. Most of the grains are rounded and only few are euhedral and show prismatic morphology. The grains are very small with length and width around 50μm and aspect ratios of 1.2:1 or 1:1. A few grains show prismatic morphology and magmatic oscillatory zoning have size range of 60-80μm and aspect ratios up to 2:1 (Fig. 14). In CL images, many of the zircons display unclear zoning with variably thick metamorphic rims showing bright luminescence and clear core-rim texture. A total of 25 spots were analyzed on 25 zircon grains (Table 3). The results show Pb content in the large range of 58 to 351 ppm, U content in the range of 78 to 460 ppm and Th in the range of 2 to 372 ppm, respectively, with

ACCEPTED MANUSCRIPT P a g e | 45 Th/U ratios of 0.10 to 1.32 (except few of them less than 0.1). Twenty four of the 25 spots fall along a discordia line and define an upper intercept age of 3160±14

PT

Ma (MSWD=1.4, N=24). Among these many are concordant and only few show slight discordance and Pb-loss. Thus, the upper intercept age (3160±14 Ma) is 207

Pb/206Pb weighted mean age of 3146±12 Ma

RI

closely comparable with the

207

Pb/206Pb spot age of 3270±17 Ma with 99%

NU

20) is a xenocryst and yield

SC

(MSWD=2.4, N=24) from this sample (Fig. 21c,d). The remaining one spot (spot

MA

concordance (Fig. 21c,d).

TNL 4/2 [calcareous schist]

TE

D

Zircons from this sample are light brownish, and transparent to translucent. Some of them are euhedral and show prismatic morphology whereas a few

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grains are slightly rounded or stumpy. The grains are small with size around 5080μm and aspect ratios are around 2:1 to 1:1. A few grains show long prismatic morphology (up to 150μm length and aspect ratios up to 4:1 or 3:1). In CL images, some zircons show clear oscillatory zoning, suggesting magmatic provenance (Fig. 15). However they also show clear core-rim texture with bright luminescent rims resulting from metamorphism. Some of the grains are unzoned with dark luminescence. A total of 27 spots were analysed on 27 grains. The results show Pb content in the large range of 30 to 2439 ppm, U content in the range of 108 to 3943 ppm and Th in the range of 16 to 1455 ppm, respectively, with Th/U ratios <1.11. The age data from the 27 spots can be divided into 4 groups. The first group includes 2 concordant spots (spots 20, 22) with

ACCEPTED MANUSCRIPT P a g e | 46 207

Pb/206Pb ages of ca. 2.6 Ga (Fig. 22); the second group (spot 2) shows

207

Pb/206Pb age of 3175±16 Ma (N=1) (Fig. 22); the third group comprises 2 206

Pb/238U ages of ca. 3.0; the last group

PT

concordant spots (spots 29, 31) with

RI

includes 22 spots which fall along a discordia and define an upper intercept age of 2831±12 Ma and lower intercept age of 834±78 Ma (MSWD=5.4, N=22) (Fig.

NU

SC

22).

MA

TNL-1/1 [ferruginous quartz mica schist]

Zircons from sample TNL-1-1 are colorless or light brownish and transparent to

TE

D

translucent. Most of grains are slightly rounded or stumpy and only few show euhedral prismatic morphology. The grains are very small and the length and

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width are around 50μm with the aspect ratios of 1.2:1 or 1:1. A few grains show prismatic morphology with a size range of 60-100μm and aspect ratios of 2:1. In CL images, all the zircons show dark luminescence. Many grains display unclear zoning with core-rim texture and carry a very thin metamorphic rim with bright luminescence (Fig. 15). A total of 23 zircon spots were analysed for zircon U-Pb dating on 23 grains. The results show Pb content in the large range of 9 to 353 ppm, U content in the range of 277 to 775 ppm and Th in the range of 13 to 186 ppm, respectively, with low Th/U ratios up to 0.56. The age data can be divided into 3 groups. Spots 01, 03, 10, 13 and 21 are old zircons with concordant 207

Pb/206Pb ages of 2.9 to 3.0 Ga (n=5). Spots 09, 16 and 27 are also concordant

with

207

Pb/206Pb ages of 2.0 to 2.1 Ga (n=3). The remaining 15 spots fall along a

ACCEPTED MANUSCRIPT P a g e | 47 discordia line and define an upper intercept age of 2492±28 Ma (MSWD=2.3,

PT

N=15) (Fig. 23a,b).

RI

KTMR-2 [meta- BIF, banded magnetite quartzite]

SC

Zircons from this banded magnetite quartzite (meta BIF) are light brownish and

NU

only few of them are colorless. They are transparent or translucent, and some of them are euhedral crystals with prismatic morphology, while others are subhedral

MA

or anhedral. The grains are very small ranging from 30-100×20-80μm in size with aspect ratios of 2:1 to 1:1 (except few of them with aspect ratios of 3:1 to 4:1). In

TE

D

CL images, few zircons display clear oscillatory zoning and manly of them possess unclear oscillatory zoning or are unzoned with dark luminescence (Fig.

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14), carrying thin metamorphic rims yielding bright luminescence. Only 11 grains were analyzed due to the scarcity of zircons and their very small size. The results show Pb content in the large range of 22 to 515 ppm, U content in the range of 112 to 736 ppm and Th in the range of 26 to 397 ppm, respectively, with Th/U ratios of 0.11 to 1.56. The age data can be divided into 4 groups. The first group including 5 spots (spots 1, 4, 8, 11, 15) are discordant and define an upper intercept age of 3129±41 Ma and lower intercept age of 1614±63 Ma (MSWD=0.36, N=5) (Fig. 23c,d). The second group includes 4 concordant spots (spots 2, 3, 9, 13) with

207

Pb/206Pb ages of 2445±23 Ma, 2563±23 Ma, 2477±24

Ma, and 2707±23 Ma, respectively. The third group (spot 14) is a xenocryst with 207

Pb/206Pb age of 3255±22 Ma and the last group is represented by spot 12 with

ACCEPTED MANUSCRIPT P a g e | 48 206

Pb/238U age of 703±5 Ma (Fig. 23c).

RI

PT

6.2 Zircon Lu-Hf isotopes

SC

In situ Hf isotope analyses have been carried out on zircons on the same spots or immediately adjacent domains from where the U-Pb dating was done. A total

NU

of 135 zircon grains were analyzed for Lu-Hf isotopes and the results are

MA

presented in Table 9 and 10 and plotted in Figs. 24 and 25. The salient features

IRK-1

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TE

6.2.1 Metaigneous rocks

D

from the metaigneous and metasedimentary suites are briefly evaluated below.

Nine zircons were analyzed from sample IRK-1 for Lu-Hf isotopes. The results show initial

176

Hf/177Hf ratios in the range of 0.280570 to 0.280658 and positive

εHf(t) values ranging from 0.0 to 4.2 with mean at 2.6. The

207

Pb/206Pb ages of

individual zircon spots (3441-3517 Ma) were used for calculation. The Hf depleted model ages (TDM) are between 3504 Ma and 3619 Ma (mean 3554 Ma), and Hf crustal model ages (TDMC) varies from 3517 to 3658 Ma (mean 3599 Ma). The data suggest that the parent magma was derived from the Paleoarchean juvenile mantle sources (Fig. 24a).

NDPL-1

ACCEPTED MANUSCRIPT P a g e | 49 Eleven zircons were analyzed from this sample for Lu-Hf isotopes. The results show initial

176

Hf/177Hf ratios of 0.281192 to 0.281299 and positive εHf (t) values in 207

Pb/206Pb mean

PT

the range of 0.2 to 4.0 with an average value of 1.6, when the

RI

age of 2500 Ma was used for calculation. The Hf depleted model ages (T DM) are between 2660 Ma and 2799 Ma (mean 2749 Ma), and Hf crustal model ages

SC

(TDMC) vary from 2757 to 2990 Ma (mean 2904 Ma). The data suggest that the

NU

magma was sourced Neoarchean to Mesoarchean juvenile sources (Fig. 24a).

MA

MNT-1

D

Ten zircons were analyzed from this sample and the results show initial Hf/177Hf ratios of 0.280904 to 0.281008. The εHf (t) values are negative and in

TE

176

AC CE P

the range of -8.8 to -5.1 with an average value of -6.8 when the 207Pb/206Pb mean age of 2554 Ma was used for calculation. The Hf depleted model ages (T DM) are between 3050 Ma and 3199 Ma (mean 3116 Ma), and Hf crustal model ages (TDMC) range from 3355 to 3581 Ma (mean 3456 Ma). The data suggest that the source material was derived from Paleoarchean reworked crust (Fig. 24a).

NDK-1 Seven zircons were analyzed from this sample for Lu-Hf isotopes and the results show initial

176

Hf/177Hf ratios of 0.280665 to 0.280829 and both negative and

positive εHf(t) values ranging from -3.0 to 2.9 with a mean at -0.5, when the 207

Pb/206Pb mean age of 3172 Ma was used for calculation. The Hf depleted

ACCEPTED MANUSCRIPT P a g e | 50 model ages (TDM) are between 3280 Ma and 3496 Ma (mean 3404 Ma), and Hf crustal model ages (TDMC) varies from 3345 to 3699 Ma (mean 3548 Ma). The

PT

results suggest the parent magma came from a mixed Paleoarchean source of

RI

both juvenile and crustal components (Fig. 24a).

SC

PRY-1

176

Hf/177Hf

NU

Ten zircons were analyzed in this sample and the results show initial

ratios of 0.281106 to 0.281233. The data also show both positive and negative

MA

εHf(t) values in the range of -2.9 to 1.7 with an average value of 0.2, when the 207

Pb/206Pb mean age of 2501 Ma was used for calculation. The Hf depleted

D

model ages (TDM) are between 2747 Ma and 2915 Ma (mean 2801 Ma), and Hf

TE

crustal model ages (TDMC) vary from 2901 to 3177 Ma (mean 2989 Ma). The data

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indicate a mixed Mesoarchean source involving both juvenile mantle and reworked crustal components (Fig. 24a).

PDM-2

Six zircons were analyzed from this sample and the results show initial

176

Hf/177Hf

ratios of 0.281016 to 0.281087 and negative εHf (t) values in the range of -7.2 to 4.7 with an average value of -5.9, when the

207

Pb/206Pb mean age of 2452 Ma

was used for calculation. The Hf depleted model ages (T DM) are between 2946 Ma and 3039 Ma (mean 2994 Ma), and Hf crustal model ages (T DMC) vary from 3250 to 3403 Ma (mean 3327 Ma). The data suggest that the magma was sourced from Paleoarchean reworked crustal components (Fig. 24a).

ACCEPTED MANUSCRIPT P a g e | 51

PT

PRV-2

Eighteen zircons were analyzed from sample PRV-2 for Lu-Hf isotopes. The 176

Hf/177Hf ratios of 0.280803 to 0.281047. The εHf (t) values

RI

results show initial

SC

are in the range of -14.0 to -3.9 with an average value of -10.0, when the Pb/206Pb mean age of 2475 Ma was used for calculation. The Hf depleted

NU

207

model ages (TDM) are between 2998 Ma and 3321 Ma (mean 3183 Ma), and Hf

MA

crustal model ages (TDMC) vary from 3322 to 3834 Ma (mean 3609 Ma). The data indicate that the magma from which the zircons crystallized was derived by the

TE

D

reworking of Eoarchean-Paleoarchean crustal components (Fig. 24a).

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KTMR-1

Due to the small size of zircons, only three grains were analyzed from sample KTMR-1 for Lu-Hf isotopes, others are too small to be analysed. The results 176

Hf/177Hf ratios range from 0.281091 to 0.281123 and display

show initial

negative εHf(t) values in the range of -3.6 to -1.9 with an average value of -2.5 , when the

207

Pb/206Pb age of individual zircon spots (2495-2531 Ma) were used

for calculation. The Hf depleted model ages (TDM) are between 2893 Ma and 2935 Ma (average 2910 Ma), and Hf crustal model ages (TDMC) varies 3136-3214 Ma (average 3163 Ma). The negative εHf (t) values suggest that the magma source was derived from the Mesoarchean reworked crustal component (Fig. 24a).

ACCEPTED MANUSCRIPT P a g e | 52

PT

6.2.2 Metasedimentary rocks

RI

MBM-1

Only four zircons were analyzed for Lu-Hf isotopes from this sample because of

SC

the small size of the zircon grains. The results show initial

176

Hf/177Hf of

average value of -1.6, when the

NU

0.280808 to 0.281270. The εHf (t) values are in the range of -5.2 to 6.0 with an 207

Pb/206Pb ages of 2178-2901 Ma from

MA

individual zircon spots were used for calculation. The Hf depleted model ages (TDM) are between 2697 Ma and 3307 Ma (mean 2900 Ma), and Hf crustal model

TE

D

ages (TDMC) range from 2739 to 3566 Ma (mean 3126 Ma). The data indicate a mixed source from both Mesoarchean-Neoarchean juvenile and reworked crustal

TNL -3/1

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components (Fig. 24a).

Four zircons were analyzed from sample TNL-3-1 for Lu-Hf isotopes. The results show initial

176

Hf/177Hf ratios of 0.280586 to 0.280853 and mainly negative εHf(t)

values in the range of -17.4 to 0.0 (mean -7.1), when the

207

Pb/206Pb ages of

2360-3420 Ma from individual zircon spots were used for calculation. The Hf depleted model ages (TDM) range from 3248 Ma to 3602 Ma with the average of 3386 Ma, and the Hf crustal model ages (TDMC) are between 3496 Ma and 3956 Ma with the average of 3714 Ma. The data suggest a reworked Eoarchean and Paleoarchean crustal source (Fig. 24a).

ACCEPTED MANUSCRIPT P a g e | 53

NDV-2

PT

Six zircons were analyzed from this sample and the results show initial

176

Hf/177Hf

ratios in the range of 0.280701 to 0.280754 and with both positive and negative

RI

εHf(t) values in the range of -2.7 to 0.9 (mean -1.2), when the

207

Pb/206Pb ages of

SC

3118-3203 Ma from individual zircon spots were used for calculation. The Hf

NU

depleted model ages (TDM) are between 3377 Ma and 3446 Ma (mean 3415 Ma), and Hf crustal model ages (TDMC) vary from 3490 Ma to 3623 Ma (mean 3580

MA

Ma). The predominantly negative εHf(t) values with one positive εHf(t) value suggest that the magma sources are mainly derived from the reworked

24a).

TNL-4/2

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TE

D

Paleoarchean crust together with the limited juvenile mantle components (Fig.

Eight zircons were analyzed from this sample Lu-Hf isotopes. The results show initial

176

Hf/177Hf ratios of 0.280794 to 0.281053. Their εHf(t) values are in the

range of -5.7 to -0.6 with an average value of -2.8, when the

207

Pb/206Pb ages of

2619-2986 Ma from individual zircon spots were used for calculation. The Hf depleted model ages (TDM) are between 2989 Ma and 3332 Ma (mean 3197 Ma) and Hf crustal model ages (TDMC) vary from 3217-3594 Ma with a mean at 3416 Ma. The data suggest that the source protoliths from which the zircons were sourced involved Paleoarchean reworked crust (Fig. 24a).

ACCEPTED MANUSCRIPT P a g e | 54

TNL-1/1

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Six zircons were analyzed from this sample and the results show initial 176Hf/177Hf of 0.280671 to 0.280882 and negative εHf (t) values in the range of -18.5 to -4.1

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with an average value of -10.8, when the 207Pb/206Pb ages of 2256-2981 Ma from

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individual zircon spots were used for calculation. The Hf depleted model ages

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(TDM) are between 3209 Ma and 3485 Ma (mean 3348 Ma), and Hf crustal model ages (TDMC) range from 3576-4031 Ma (mean 3786 Ma). The data suggest that

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the source rocks were generated from a magma derived by the melting of

KTMR-2

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Eoarchean and early Paleoarchean reworked crust (Fig. 24a).

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Pb/206Pb ages of 2284 Ma,

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Only four zircons (spots No.1, 2, 9, 14 with the

2445 Ma, 2477 Ma and 3255 Ma), were analyzed this sample for Lu-Hf isotopes because most of the zircons are too small in size. The data show initial 176Hf/177Hf ratios in the tight range of 0.280815 to 0.281211. The spots 1, 2 and 9 display negative εHf(t) values of -8.0, -0.4 and -4.9, whereas spot 14 with

207

Pb/206Pb age

of 3255 Ma shows positive εHf(t) value of 4.3. The Hf depleted model ages (TDM) are between 2780 Ma and 3300 Ma (mean 2995 Ma), and Hf crustal model ages (TDMC) vary from 2985 to 3325 Ma (mean 3229 Ma). The data indicate that the zircons were sourced from rocks generated through the melting of PaleoarcheanMesoarchean crustal and juvenile mantle components (Fig. 24a).

ACCEPTED MANUSCRIPT P a g e | 55 7. Discussion

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7.1 Rock types and metamorphic P-T conditions

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The samples analyzed in this study are petrographically classified as dioritic and granitic gneiss (e.g., sample NDPL-1; hornblende + plagioclase ± epidote ±

SC

quartz ± titanite ± biotite), metadiorite (sample PRY-1; plagioclase + hornblende +

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epidote + scapolite + biotite + titanite), metagranite (sample TNL-2-1; K-feldspar + quartz + hornblende + plagioclase + biotite + titanite + epidote), charnockite

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(sample NDK-1; plagioclase + quartz + K-feldspar + orthopyroxene + magnetite), amphibolite (sample APP-1; hornblende + plagioclase + biotite + quartz),

cummingtonite

+

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hornblende schist (sample KTMR-1; magnesio-hornblende + actinolite + chlorite),

quartz-mica

schist

(e.g.,

sample

TNL-1-1;

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muscovite/paragonite + quartz ± chlorite ± garnet ± sillimanite ± rutile), migmatitic biotite gneiss (sample MNT-1; quartz + biotite + plagioclase + epidote), and banded magnetite quartzite (sample KTMR-2; quartz + magnetite).

The

metaigneous suite corresponds to arc magmatic rocks where as the metasediments

represent

both

pelagic

and

volcano-sedimentary

trench

sequences accreted onto the continent. The metamorphic conditions were estimated based on conventional geothermobarometry on dioritic gneiss, metadiorite, amphibolite, and garnet-bearing quartz-mica schist. The peak temperature was estimated for hornblende + plagioclase ± quartz assemblages in samples NDPL-1, PRV-2, IRK-1, PRY-1, and APP-1 as 620-730C. Slightly higher but nearly consistent temperature range of 710-760C was obtained for

ACCEPTED MANUSCRIPT P a g e | 56 garnet-muscovite

assemblage

in

sample

NDV-2.

Therefore,

the

peak

metamorphic temperature of this region is inferred as ca. 710-730C, which is

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consistent with the common occurrences of amphibolite-facies mineral

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assemblages. Although the pressure conditions could not be estimated from the

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available mineral assemblage, the occurrence of sillimanite in some quartz-

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muscovite schists suggests pressures up to 8 kbar (at 710-730C).

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7.2 Tectonic setting and petrogenetic Implications

The petrogenesis of magmatic suites generally depends on the tectonic regime in

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which the parent magmas are generated. Charnockites represent the metamorphosed equivalent of granitic protoliths (Newton et al., 1980; Rajesh and

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Santosh, 2006, 2012), despite contentions about the igneous (basaltic) (Condie and Allen, 1984; Peucat et al., 1989) or sedimentary parentage (Raith et al., 1999) of these rocks. The igneous parentage for the protoliths of the Coorg magmatic rocks is evident from their metaluminous nature (Fig. 8b), their disposition in the K2O/Al2O3 vs. Na2O/Al2O3 diagram (Fig. 8c), and lower K2O/Na2O ratios (Table 6). The near unity of Eu anomalies and the nearly flat HREE patterns for all the magmatic rocks (Fig. 9) indicate the role of plagioclase in the source residue and implies melting at shallow depths. Moderate La/Yb (>20) and Sr/Y (>40) ratios (Fig. 8d) (Moyen, 2009) for the charnockites and dioritic samples further corroborate the variable depths of melting, probably as deep as the garnet

ACCEPTED MANUSCRIPT P a g e | 57 stability field (for those samples with Sr/Y >40 and La/Yb >20) and as shallow as to bear the amphibole± plagioclase as source components.

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The available information on the Mesoarchean charnockites from the

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Biligiri Rangan hills in southern India suggest their formation in active continental margin setting as part of the initial crustal accretion event in the Dharwar Craton

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(Tomson et al., 2013). Recent integrated studies on major lithologies of

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Mesoarchean Coorg block clearly indicate magma derivation in an active convergent margin setting (Santosh et al., 2015). The available geochemical

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studies on Mesoarchean TTG rocks from the Holenarsipur area of Dharwar Craton suggest their derivation in a subduction-related setting (Mohan et al.,

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2008; Naqvi et al., 2009). The Neoarchean charnockites from the adjacent Nilgiri Block have also been correlated to subduction-accretion tectonics, with the

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magmatic suite in the Nilgiri Block accreted together with imbricated ocean plate stratigraphy (Samuel et al., 2014a). Further south, in the Nilambur region, the charnockites and associated magmatic rocks have been correlated to subduction-related magmatism (Shaji et al., 2014). In the traditional tectonic discrimination diagram of Pearce et al. (1984), the magmatic rocks of present study are confined to the field of volcanic arc granites (VAG) (Fig. 9a), and their subduction affinity is further confirmed by immobile elemental systematics (Fig. 9b) (Thieblemont and Tegyey, 1994).

South of the present study area is the Nilgiri Block from where Samuel et al. (2014) reported geochemical evidence for volcanic arc affinities for most of the

ACCEPTED MANUSCRIPT P a g e | 58 magmatic suites. They suggested that the magmatic suite in the Nilgiri Block formed in a Neoarchean convergent margin setting. From the southern flank of

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the Nilgiri Block, Santosh et al. (2013) reported a well-preserved suprasubduction

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zone ophiolite suite in the Agali Hills. The lithological association here represents a 2.6 to 2.5 Ga old ocean plate stratigraphy, imbricated and accreted onto the

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continent during the subduction-collision tectonics. They correlated the supra-

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subduction zone ophiolites with the arc and exhumed sub-arc mantle material toward the northwest in the Nilgiri Block. The southern periphery of the Dharwar

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Craton is straddled by several Archean crustal blocks including Coorg, Nilgiri, Salem and Madras. Several suprasubduction suites including the anorthosites

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and related rock suites of Sittampundi, Bhavani and Gopichettipalayam, and the Devannur-type dismembered ophiolites are distributed along the margins of

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these blocks. Thus, Santosh et al. (2013) proposed a scenario of arc accretion within an oceanic realm to the southern periphery of the Dharwar Craton during Neoarchean-earlier Paleoproterozoic. They envisaged multiple subduction systems with northward accretion of arcs and microcontinents with final closure of the ocean (termed as Dharwar Ocean) by late Neoarchean – earliest Paleoproterozoic. In the Coorg Block to the north, zircon

207

Pb/206Pb ages from

magmatic suites reported in Santosh et al. (2015) and those presented in this study reveal voluminous Mesoarchean magma emplacement during 3.5 to 3.1 Ga, followed by metamorphism at ca. 3.0 to 2.9 Ga.

These data suggest

Eoarchean – Mesoarchean subduction-related crust building. The majority of zircons from the magmatic suites within the Coorg rocks show Hf isotope

ACCEPTED MANUSCRIPT P a g e | 59 features typical of crystallization from magmas derived from juvenile sources. Their Hf crustal model ages suggest that the crust building might have also

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involved partial recycling of basement rocks as old as ca. 3.8 – 4.0 Ga (Santosh

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et al., 2015, and this study).

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7.3 Meso-Neoarchean crustal evolution in Peninsular India

7.3.1 Magmatic Rocks surrounding Coorg Block

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Zircon U-Pb age data, in conjunction with Lu-Hf isotopic systematics help in deciphering the crustal growth history, timing of the major episodes of crust

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generation, and the source region(s) of the magmas. Among the data presented here for eight magmatic rocks (Figs. 24a, 25a) from the margins of the Coorg

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Block and adjacent suture, the crystallization ages range between 3517 and 2452 Ma. The Mesoarchean ages reported in our present study from the magmatic suite along the margins of the Coorg Block are

comparable with

similar ages reported from widely spaced localities in this block in a previous study (Santosh et al., 2015), although the oldest weighted mean age of 3.5 Ga obtained in this study is the first report. The Neoarchean ages from the suture belt surrounding the Coorg Block in this study are comparable to similar ages reported in a number of recent studies from the adjacent Nilgiri Block and its southern flanks (Samuel et al., 2014; Shaji et al., 2014, Praveen et al., 2014). A compilation of the age data from the magmatic suites of present study from the margins of the Coorg Block and the surrounding suture shows clear pulses at

ACCEPTED MANUSCRIPT P a g e | 60 3.5, 3.2 and 2.5 Ga (Figure 26), suggesting episodic magmatism and crust building events during Eoarchean, Mesoarchean and Neoarchean. On a global

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scale, the dominant magmatic activities that built the exposed global continental

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crust show major pulses at 2.7, 2.5 Ga, 1.9 and 1.2 Ga (Condie, 2000; Condie and Kröner, 2012; McCulloch and Bennett, 1994, Zhai and Santosh, 2011). In

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addition, 3.3 and 1.9 Ga peaks have also been recorded from the Nd and Hf

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model ages of detrital zircons (Kemp et al., 2006). The felsic magmatic activity in the adjacent Dharwar Craton shows a different pattern, with the oldest

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magmatism (3358± 66 Ma, Gorur gneiss, Rb-Sr whole rock; Beckinsale et al., 1980) being younger than that of Coorg Block. The available geochronological

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data show that the felsic magmatic activity in Western Dharwar Craton is broadly continuous, with major peaks at 3.3, 3.1, 2.9 and 2.5 Ga (Bhaskar Rao et al.,

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1983; Monrad, 1983; Peucat et al., 1993; Taylor et al., 1984). In contrast, the ~2.5 Ga granitic magmatism predominates in the central and eastern Dharwar Cratons, wherein Neoarchean short-lived episodic crustal growth is envisaged with the episodic crustal growth during Archean correlated to

subduction

magmatism (Mohan et al., 2014). Within the Coorg Block, however, there is no record of the 2.9 and 2.5 Ga magmatic events, suggesting the exotic nature of this block within the SGT collage (Santosh et al., 2015 and this study).

It has been established that

176

Lu/177Hf isotopic ratios provide robust tools

to differentiate the source reservoirs, with the range of 0.022-0.026 representing mafic magmas (Rudnick and Gao, 2003), and 0.01 suggesting felsic source

ACCEPTED MANUSCRIPT P a g e | 61 (Blichert-Toft and Albarède, 2008). Zircons with different crystallization ages, but derived from the crust of the same composition and mantle extraction age form a

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linear array in the ɛHft vs. age plots (Fig. 24). Nearly 18 orders of variation in the

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ɛHft values as displayed in the range of -14 and +4.2 in the present case clearly indicate variable sources (Table 9). The sample IRK-1, a dioritic gneiss from

ɛHft values ranging from 0.0 to 4.2 with mean at 2.6,

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this sample show

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Irikkur, shows the oldest U-Pb crystallization age of 3517 Ma, and the zircons in

essentially lying within the CHUR and depleted mantle domains (Fig. 24a),

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suggesting juvenile magmatic additions at ~3.5 Ga, with possible derivation from depleted mantle. The next oldest rock is represented by sample NDK-1

D

(charnockite from Nadukani) with a weighted mean age at 3172 Ma, and showing

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both +ve and –ve ɛHft values (Fig. 24a and Table 9) suggesting a mixed

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signatures with both juvenile and evolved nature of the source magma, derived from recycled ancient crust, similar to the data from magmatic suites reported in our earlier study from the Coorg Block (Fig. 24b, Santosh et al., 2015). The remaining magmatic rocks all crystallised at ~2.5 Ga, wherein, zircons from sample NDPL-1 (dioritic gneiss from Nedumpoil quarry) shows + ve ɛHft values (Fig. 24a and Table 9), suggesting juvenile crustal additions during Neoarchean. In contrast, four samples (KTMR-1, MNT-1, PDM-2 and PRV-2) essentially have ve ɛHft values, and they extend up to the Neohadean isotopic evolution line (Fig. 24a and Table 9), highlighting the role of recycled older crust. Mesoarchean arc magmatic rocks of Coorg Block were derived from juvenile crustal additions, as well as through recycled Neohadean felsic crust. In the T DMc vs. crystallization

ACCEPTED MANUSCRIPT P a g e | 62 age plot for the igneous suite (Fig. 25a), it is evident that the magmatic suite surrounding the Coorg Block that formed during the Neoarchean had

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incorporated substantial volumes of Eoarchean crustal components (ranging up

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SC

7.3.2 Metasediments surrounding Coorg Block

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to 3834 Ma).

Mesoarchean ages are well-documented from detrital zircons in the

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Dharwar Craton (Bidyananda et al., 2011; Nutman et al., 1992; Sarma et al., 2012). So far, the oldest known metasedimentary rocks in southern India are

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from the Sargur Group (3580-3130 Ma) of the western Dharwar Craton (WDC), and their detrital zircons have a prolonged provenance history confined to the

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Archean (Nutman et al., 1992). The metasediments of eastern Dharwar Craton (EDC) are relatively younger (3348±10 Ma) as compared to those of the WDC (Bidyananda et al., 2011). Although the metasedimentary rocks surrounding the Coorg Block are substantially younger than the magmatic suite (with sedimentation continuing up to Mesoproterozoic (Fig. 27), the oldest detrital zircons (as old as 3517 Ma) have ages similar to those of the WDC.

In

conjunction with Lu-Hf isotopic systematics, our geochronological data on zircons from these metasediments suggest the existence of very old crustal sources, of Eoarchean and up to Neohadean (Fig. 24a and 25b). The Lu-Hf systematics also indicates that the extent of the involvement of older crust increased with time, i.e. the younger sedimentary rocks were derived from the recycling of older

ACCEPTED MANUSCRIPT P a g e | 63 crust (Figs. 24a, 25b). In contrast to the prominent episodic magmatic history of Coorg and surrounding regions that culminated by Neoarchean, sedimentation

closure

is

marked

by

high

grade

metamorphism

during

late

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ocean

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appears to have continued in the intervening ocean until Mesoproterozoic. The

Mesoproterozoic (our unpublished age data from garnet and kyanite bearing

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SC

granulite facies metapelites accreted along the fringes of the Coorg Block).

In the ɛHft vs. crystallization age plot (Fig. 24a), the sample (KTMR-2,

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banded magnetite quartzite) with Mesoarchean detrital zircon grain (3255 Ma) shows +ve ɛHft value (4.3), whereas the remaining three grains with Neoarchean

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age possess -ve ɛHft values (up to -8 ɛHft) (Table 10). The positive ɛHft values in Mesoarchean detrital zircons suggest the existence of depleted mantle domains

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that comprised fraction of the silicate Earth, formed in response to the extraction of a voluminous primordial crust (Harrison et al., 2005). Similar isotopic systematics are noted for the sample MBM-1 (quartz mica schist), with 10 orders of ɛHft values, and a prominent signature of recycled crustal component (Fig. 24 a and Table 10). The remaining samples exhibit systematically increasing evolved isotopic signatures (up to -18.5 ɛHft) with time and their distribution is mainly defined by Eoarchean (and even extending up to Neohadean) isotopic evolution line (Fig. 24 a), thus confirming the role of older recycled crust for the evolution of these rocks. The zircons that plot along the Eoarchean evolution line corresponds to the

176

Lu/177Hf ratio 0.015, which in turn suggests the source as

intermediate-felsic crust.

ACCEPTED MANUSCRIPT P a g e | 64 The plot of zircon crystallization age against Hf model age demonstrates model ages up to ca. 4.1 Ga (Fig. 25b and Table 10), revealing, for the first time,

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the existence of Neohadean protocontinental crust in southern India. The Hf

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model ages for the detrital zircons are clustered at ca 3.2, 3.5 and 3.8 Ga (Fig. 25 b). The first two clustered model ages are synchronous with the abundant

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felsic-intermediate arc magmatic rocks of the Coorg Block (Santosh et al., 2015).

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Therefore we consider that these rocks in the Coorg Block might have provided the potential source for the deposition of the shelf sequences in the

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metasedimentary suite which were later subducted, metamorphosed, exhumed, and incorporated with the marginal suture. These results have important bearing the involvement of crustal

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D

on the crustal growth mechanism, suggesting

recycling processes, and thus reiterating the episodic subduction-accretion

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processes in the SGT extending up to Meso- and Neoproterozoic (Santosh et al., 2009). The subduction-related history of Archean and Proterozoic magmatic suites have been widely reported from the SGT (Mohan et al., 2013; Samuel et al., 2014a; Santosh et al., 2009; Santosh et al., 2013; Sato et al., 2011; Shaji et al., 2014; Yellappa et al., 2012).

7.3.3 Regional implications

In a recent work, Lancaster et al. (2014) reported U-Pb-Hf analyses of detrital zircons from the Dharwar Craton. Their data indicate significant juvenile crustal extraction events at ca. 3.3 and 2.7 Ga, with continuous extraction from 3.7-3.3

ACCEPTED MANUSCRIPT P a g e | 65 Ga. They suggested that modern style plate tectonics had already started by ca. 3.0 Ga, associated with the onset of cratonization in Dharwar. Evidence for

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Mesoarchean crust formation is also emerging from the other cratonic domains of

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Peninsular India. In a recent study, Nelson et al. (2014) reported geochemical and SHRIMP U–Pb data from the Singhbhum Craton where detrital zircons in

SC

sandstone enclave within tonalitic gneiss show maximum time of deposition as

NU

3375. They also reported magmatic crystallization ages between 3380 and 3299 Ma from tonalite and trondhjemite gneisses. In another study, Upadhyay et al.

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(2014) recorded granitoid emplacement in two pulses at 3.45–3.44 Ga and 3.35– 3.32 Ga in the Singhbhum Craton. They identified major felsic crust formation in

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a narrow time interval between 3.4 and 3.3 Ga with minor contributions of material as old as 3.6 Ga.

The nuclei of several old cratons on the globe such

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as the Yilgarn Craton, Western Australia, and the Slave Craton, Canada, carry Eoarchean–Paleoarchean (3.8 Ga, 3.6 Ga and 3.4 Ga) magmatic records with evidence for reworking of Hadean crust. In a recent study, Zhang et al. (2014) reported Hf and O isotope data on detrital zircons from Paleoproterozoic quartzites in the southern part of the North China Craton which reveal episodic magmatism during the Eoarchean, Paleoarchean, Mesoarchean, Neoarchean and Paleoproterozoic. Their data show that the Eoarchean–Paleoarchean (3.8 Ga, 3.6 Ga and 3.4 Ga) phase involved substantial reworking of the Hadean crust. Significant crustal growth also occurred during Mesoarchean to early Neoarchean in the North China Craton.

ACCEPTED MANUSCRIPT P a g e | 66 8. Conclusions

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Our integrated study on the geology, petrology, geochemistry, zircon U-Pb

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geochronology and Lu-Hf isotopes of metamorphosed magmatic sedimentary suites from the fringes of the Coorg Block and surrounding suture leads to the

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following conclusions.

The magmatic suites within the Coorg Block show features typical of subduction-

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related arc magmas and are proposed to have formed in an Eoarchean –

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Mesoarchean convergent margin.

Episodic magmatism during Eoarchean, Mesoarchean and Neoarchean built the

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ancient continental crust in southern Peninsular India.

The negative to strongly negative ɛHft values of zircons in the sedimentary suite suggest the formation of their igneous protoliths by remelting of older crustal components. These source reservoirs were heterogeneous in age and isotopic composition.

Magmatic zircons plot above the Hf evolutionary trend defined by the Eoarchean detrital zircons and overlap with the Hf isotopic fields of the younger detrital zircon populations. This suggests that the Mesoarchean detrital populations were derived from the magmatic rocks in the Coorg Block.

ACCEPTED MANUSCRIPT P a g e | 67

Evidence exists in southern India for a Hadean felsic continental crust, expanding

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our knowledge on the crustal evolution in the early history of the Earth.

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Acknowledgments

We thank Editor Dr. Shoujie Liu and two anonymous referees for constructive

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and helpful comments. We are grateful to Tang Li and Xueming Teng at China University of Geosciences Beijing for help with zircon U-Pb and Lu-Hf analysis.

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This study contributes to the Talent Award to M. Santosh under the 1000 Plan of the Chinese Government. Partial funding for this project was produced by a

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Grant-in-Aid for Scientific Research (B) from Japan Society for the Promotion of Science (JSPS) to Tsunogae (Nos. 22403017 and 26302009).

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Figure Captions

Figure 1

Generalised geological and tectonic framework of southern India

showing the study area (after Collins et al., 2014 and Santosh et al., 2015).

Fig 2

(a) Geological map of the Coorg Block and surrounding sutures

(modified from Chetty et al.2013), showing the sample locations. (b) Detailed geological map of the study area (after Geological Survey of India, 2005),

ACCEPTED MANUSCRIPT P a g e | 77 showing the sample localities.

Representative field photographs of the metaigneous suites from

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Fig. 3

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the margins of Coorg block and bordering suture investigated in the present study. (a) Dioritic gneiss with amphibolite/hornblendite enclaves at NDPL. (b)

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Felsic meta-tuff at PDM. (c) Dioritic gneiss at PRV. (d) Dioritic gneiss at IRK. (e)

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Hornblende schist at KTMR. (f) Charnockite at NDK. For details of the localities,

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see Table 1.

Fig. 4 Representative field photographs of the metasedimentary suites from the

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margins of Coorg block and bordering suture investigated in the present study. (a) Garnet-bearing quartz mica schist at NDV. (b) Quartz mica schist at TNL-3.

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(c) Sulfidic meta BIF at KTMR. (d) Calcareous schist at TNL-4. (e) Ferruginous quartz mica schist at TNL-1. (f) Quartz mica schist at MBM. For details of the localities, see Table 1.

Fig. 5. Photomicrographs of representative thin sections discussed in this study. Polarized-light photographs except (d) to (f) (crossed polars). (a) Foliated hornblende + plagioclase + epidote + titanite assemblage in dioritic gneiss (sample NDPL-1). (b) Less foliated hornblende + plagioclase assemblage in dioritic gneiss (sample PRV-2). (c) Plagioclase + quartz + biotite assemblage in felsic layer of dioritic gneiss (sample IRK-1). (d) Hornblende + plagioclase +

ACCEPTED MANUSCRIPT P a g e | 78 biotite assemblage in melanocratic layer of dioritic gneiss with mylonitic texture (sample IRK-1). (e) Plagioclase + hornblende + epidote assemblage in

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metadiorite (sample PRY-1). (f) Coarse-grained perthite (Pth) in the matrix of

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quartz, plagioclase, biotite, and hornblende in metagranite (sample TNL-2-1). (g) Granoblastic texture of plagioclase, quartz, and orthopyroxene in massive

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charnockite (sample NDK-1). (h) Medium-grained massive amphibolite with

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hornblende, plagioclase, and biotite (sample APP-1).

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Fig. 6. Photomicrographs of representative thin sections discussed in this study. Crossed-polars photographs except (a) and (g) (polarized light). (a) Elongated

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coarse-grained hornblende and cummingtonite in hornblende schist (sample KTMR-1). (b) Well-foliated quartz-mica schist with muscovite/paragonite and

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quartz (sample TNL-1-1). (c) Moderately-foliated quartz-mica schist (sample TNL-3-1). (d) Least-foliated and massive quartz-mica schist with >90% quartz and ~10% muscovite. (e) Garnet-bearing quartz-mica schist that comprises quartz, muscovite, chlorite, and garnet (sample NDV-1). (f) Well-foliated biotite + epidote + quartz + plagioclase assemblage in the melanocratic portion of migmatitic biotite gneiss (sample MNT-1). (g) Alternation of magnetite- and quartz-rich layers in banded magnetite quartzite (sample KTMR-2). (h) Subhedral dolomite in the matrix of fine-grained quartz, chlorite, and muscovite in calcareous schist (sample TNL-4-1).

ACCEPTED MANUSCRIPT P a g e | 79 Figure 7. Compositional diagrams showing chemistry of representative minerals. (a) Si (pfu) versus XMg diagram showing compositions of calcic amphibole. (b) Al

Geochemical differentiation diagrams to depict the intermediate

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Figure 8

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versus TiO2 (wt.%) diagram showing biotite chemistry.

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(pfu) versus Na/(Na+K) diagram showing compositions of white micas. (c) XMg

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nature of Coorg charnockites.

Total Alkalis-Silica diagram after Cox et al. (1979)

(b)

Metaluminous nature of Coorg rocks in the Shand (1943) index

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(a)

diagram.

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K2O/Al2O3 vs. Na2O/Al2O3 diagram (after Tarney, 1976) to show the

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(c)

magmatic parentage for the Coorg rocks. Sr/Y vs.La/Yb plot wherein the lower ratios of these elements (<40 and

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(d)

<20 respectively) are indicative of shallow melting conditions.

Figure 9

Chondrite- normalized REE plots (a, b and C) and primitive mantle

normalized multi element variation diagrams (d, e and f) for the magmatic rocks of Coorg Block. Normalisation values are from Sun and McDonough (1989). The Nb, Ta and Zr (HFSE) depletions in the samples are in accordance with arc signature.

Figure 10

(a)

Granites discrimination diagram of Pearce et al. (1984),

wherein the Coorg magmatic rocks are confined to the volcanic arc granite (VAG)

ACCEPTED MANUSCRIPT P a g e | 80 field. (b) Zr vs. Nb/Zr diagram showing the nature of tectonic setting. All the Coorg lithologies are confined to the subduction field. Discrimination fields are

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Figure 11 Cathodoluminescence (CL) images of representative zircons in

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Figure 12 Cathodoluminescence (CL) images of representative zircons in metaigneous samples NDK-1, NDPL-1, PDM-2. Small yellow circle: Pb/206Pb age in Ma; large red circle: εHf (t) value.

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Figure 13 Cathodoluminescence (CL) images of representative zircons in

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metaigneous samples PRV-2, PRY-1. Small yellow circle:

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Pb/206Pb age

in Ma; large red circle: εHf (t) value. Figure 14 Cathodoluminescence (CL) images of representative zircons in metasedimentary samples KTMR-2, MBM-1, NDV-1, NDV-2. yellow circle:

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Small

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Pb/238U age (<1000 Ma) in

Ma; large red circle: εHf (t) value. Figure 15 Cathodoluminescence (CL) images of representative zircons in metasedimentary samples TNL 1/1, 3/1, 4/2. 207

Pb/206Pb age (>1000 Ma) or

Small yellow circle:

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Pb/238U age (<1000 Ma) in Ma; large red

circle: εHf (t) value. Figure 16. Zircon U-Pb concordia plots and age data histograms with probability

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curves for samples MNT-1 (a and b) and NDK-1 (c and d).

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Figure 18. Zircon U-Pb concordia plots and age data histograms with probability curves for samples PRY-1 (a and b) and PDM-2 (c and d).

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Figure 19. Zircon U-Pb concordia plots and age data histograms with probability

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curves for samples PRV-2 (a and b) and KTMR-1 (c and d). Figure 20. Zircon U-Pb concordia plots and age data histograms with probability

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curves for samples MBM-1 (a, b and c) and TNL-3/1 (d and e). Figure 21. Zircon U-Pb concordia plots and age data histograms with probability

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curves for samples NDV-1 (a and b) and NDV-2 (c and d). Figure 22. Zircon U-Pb concordia plots and age data histograms with probability

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curves for sample TNL -4/2. Figure 23. Zircon U-Pb concordia plots and age data histograms with probability curves for samples TNL-1/1 (a and b) and KTMR-2 (c and d) Figure 24. εHf (t) versus

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Pb/206Pb age diagram of zircons from the

metaigneous and metasedimentary suite in this study (a) and for the metaigneous suite from the Coorg Block (b, after Santosh et al., 2015). Figure 25. Crystallization age versus TDMC diagram of zircons from the metaigneous (a) and metasedimentary (b) rocks in this study. Figure 26. Compiled zircon

207

Pb/206Pb age data histograms and probability plot

for metaigneous rocks in this study. Figure 27. Compiled zircon

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Pb/206Pb age data histograms and probability plot

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for metasedimentary rocks in this study.

Table 1

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Table Captions

Location, rock type and mineralogy of samples

Table 9

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geochronology and Lu-Hf isotope analyses.

used for U-Pb

Zircon Lu-Hf isotope data for the metaigneous suite from the Coorg

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Zircon Lu-Hf isotope data for the metasedimentary suite from the Coorg Block and surrounding sutures.

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Table 10

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Block and surrounding sutures.

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Sample No. Locality Metaigenous

Latitude

Longitude

NDPL-1

Nedumpoil quarry

11°50'51.2"

2

PDM-2

Padamala

11°49'15.4"

3

PRV-2

Peruva

11°50'33.9"

4

PRY-1

Periya (Mile 34)

5

IRK-1

6

KTMR-1

Irikkur Kartikulam-Manandavadi Road

7

MNT-1

Manandavadi

8

NDK-1 Nadukani Metasedimentary

75°46'55.9 " 76°04'37.3 " 75°41'35.5 " 75°49'51.8 " 75°32'55.5 " 76°02'47.5 " 76°00'43.7 " 75°24'06.2 "

PT ED

MA

NU

1

SC

No .

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Table 1. Location, rock type and mineralogy of samples used for U-Pb geochronology and Lu-Hf isotope analyses.

11°50'19.1" 11°59'29.0"

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11°49'55.5" 11°48'28.00 " 12°06'48.4"

9

NDV-1

Neduvaloor

12°03'16.7"

10

TNL-1-1

Tirunelli

11°52'25.9"

11 12

TNL-3-1 KTMR-2

Tirunelli Kartikulam-Manandavadi

11°53'19.6" 11°49'42.9"

75°27'33.9 " 76°04'22.4 " 76°04'27.8 " 76°02'32.3

Rock type

Mineral assemblage

Dioritic gneiss

Hbl Pl Ep Ttn

Felsic orthogneiss

Ms Qtz Ky Rt

Dioritic gneiss Metadiorite

Hbl Pl Ilm Qtz Pl Hbl Bt Ttn Ep Scp

Dioritic gneiss

Pl Hbl Bt Qtz Ep

Hbl schist

Hbl Act Cum

Migmatitic Bt gneiss Charnockite

Pl Qtz Bt Ep Pl Kfs Qtz Opx Mag

Qtz-mica schist with garnet

Qtz Grt Ms Chl Rt

Qtz-mica schist

Ms Qtz Rt Chl

Qtz-mica schist Banded magnetite

Qtz Ms Sil Chl Mag Qtz

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11°49'32.9"

14

NDV-2

Neduvaloor

12°03'16.7"

15

TNL-4-2

Tirunelli

11°54'34.4"

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quartzite

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Mambaram

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MBM-1

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13

" 75°30'28.2 " 75°27'33.9 " 75°59'53.2 "

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Road

Qtz-mica schist Qtz-mica schist with garnet

Qtz Ms

Calcareous schist

Qtz Dol Chl Ms

Qtz Grt Ms Chl

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177

Hf/ Hf 0.280756 0.280681 0.280651 0.280676 0.280740 0.280648 0.280721 0.280601 0.280702 0.281121 0.281131 0.281096 0.280959 0.281021 0.280983 0.280991 0.281065 0.281010 0.280956 0.281012 0.281037 0.281002 0.280731 0.280775 0.280815 0.280880 0.280689 0.280778 0.280701

2s 0.000025 0.000016 0.000015 0.000017 0.000016 0.000018 0.000019 0.000022 0.000023 0.000015 0.000021 0.000017 0.000018 0.000017 0.000019 0.000020 0.000020 0.000017 0.000018 0.000020 0.000018 0.000032 0.000010 0.000021 0.000025 0.000021 0.000017 0.000019 0.000015

PT

176

176

177

Hf/ Hfi 0.280593 0.280645 0.280617 0.280629 0.280619 0.280598 0.280652 0.280570 0.280658 0.281115 0.281123 0.281091 0.280904 0.280980 0.280939 0.280954 0.281006 0.280966 0.280909 0.280984 0.281008 0.280966 0.280715 0.280736 0.280761 0.280829 0.280665 0.280749 0.280691

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Lu/ Hf 0.0024 0.0005 0.0005 0.0007 0.0018 0.0007 0.0010 0.0005 0.0007 0.0001 0.0002 0.0001 0.0011 0.0008 0.0009 0.0008 0.0012 0.0009 0.0010 0.0006 0.0006 0.0007 0.0003 0.0006 0.0009 0.0008 0.0004 0.0005 0.0002

SC

176

NU

177

Yb/ Hf 0.1028 0.0196 0.0206 0.0277 0.0697 0.0301 0.0457 0.0200 0.0288 0.0038 0.0042 0.0039 0.0504 0.0335 0.0345 0.0301 0.0497 0.0415 0.0459 0.0249 0.0276 0.0321 0.0102 0.0285 0.0400 0.0404 0.0181 0.0233 0.0080

MA

176

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Age (Ma) 3478 3443 3475 3517 3495 3517 3499 3444 3441 2531 2508 2495 2554 2554 2554 2554 2554 2554 2554 2554 2554 2554 3172 3172 3172 3172 3172 3172 3172

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Spot No. IRK-1.1 IRK-1.5 IRK-1.10 IRK-1.12 IRK-1.20 IRK-1.24 IRK-1.27 IRK-1.30 IRK-1.35 KTMR-1.12 KTMR-1.13 KTMR-1.14 MNT-1.8 MNT-1.11 MNT-1.14 MNT-1.15 MNT-1.16 MNT-1.22 MNT-1.23 MNT-1.24 MNT-1.27 MNT-1.32 NDK-1.7 NDK-1.18 NDK-1.20 NDK-1.21 NDK-1.22 NDK-1.23 NDK-1.28

Lu-Hf isotope data for the metaigneous suite from the Coorg Block and surrounding sutures.

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Table 9 Zircon

eHf(0) -71.3 -74.0 -75.0 -74.1 -71.9 -75.1 -72.5 -76.8 -73.2 -58.4 -58.0 -59.3 -64.1 -61.9 -63.3 -63.0 -60.4 -62.3 -64.2 -62.2 -61.4 -62.6 -72.2 -70.6 -69.2 -66.9 -73.7 -70.5 -73.2

eHf(t) 1.6 2.7 2.4 3.8 3.0 2.7 4.2 0.0 3.1 -1.9 -2.1 -3.6 -8.8 -6.1 -7.6 -7.1 -5.2 -6.6 -8.6 -6.0 -5.1 -6.6 -1.2 -0.4 0.5 2.9 -3.0 0.0 -2.1

TDM (Ma) 3595 3520 3557 3541 3556 3582 3510 3619 3504 2902 2893 2935 3199 3091 3148 3125 3062 3111 3188 3081 3050 3108 3429 3404 3371 3280 3496 3385 3461

C

TDM (Ma) 3658 3568 3608 3555 3590 3621 3517 3728 3542 3138 3136 3214 3581 3416 3506 3472 3361 3446 3569 3407 3355 3446 3591 3546 3492 3345 3699 3518 3644

fLu/Hf -0.93 -0.98 -0.98 -0.98 -0.95 -0.98 -0.97 -0.99 -0.98 -1.00 -0.99 -1.00 -0.97 -0.97 -0.97 -0.98 -0.96 -0.97 -0.97 -0.98 -0.98 -0.98 -0.99 -0.98 -0.97 -0.97 -0.99 -0.99 -0.99

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0.281265 0.281204 0.281247 0.281216 0.281200 0.281265 0.281226 0.281216 0.281192 0.281223 0.281299 0.281087 0.281077 0.281025 0.281034 0.281070 0.281016 0.280951 0.280828 0.280892 0.280865 0.280803 0.280960 0.280883 0.280810 0.281047 0.281046 0.280871 0.280869 0.280877 0.280927 0.280994 0.280938

RI

SC

0.000017 0.000016 0.000016 0.000015 0.000013 0.000021 0.000019 0.000017 0.000016 0.000023 0.000026 0.000016 0.000013 0.000015 0.000017 0.000017 0.000015 0.000015 0.000020 0.000018 0.000018 0.000017 0.000018 0.000021 0.000015 0.000025 0.000020 0.000023 0.000024 0.000020 0.000033 0.000015 0.000024

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0.281293 0.281231 0.281257 0.281236 0.281221 0.281302 0.281254 0.281248 0.281196 0.281250 0.281335 0.281114 0.281099 0.281062 0.281068 0.281116 0.281039 0.280970 0.280844 0.280910 0.280881 0.280828 0.280983 0.280900 0.280834 0.281071 0.281064 0.280888 0.280886 0.280893 0.280945 0.281013 0.280957

MA

0.0006 0.0006 0.0002 0.0004 0.0005 0.0008 0.0006 0.0007 0.0001 0.0006 0.0008 0.0006 0.0005 0.0008 0.0007 0.0010 0.0005 0.0004 0.0003 0.0004 0.0003 0.0005 0.0005 0.0004 0.0005 0.0005 0.0004 0.0004 0.0003 0.0003 0.0004 0.0004 0.0004

PT ED

0.0261 0.0260 0.0093 0.0179 0.0189 0.0332 0.0262 0.0290 0.0037 0.0221 0.0397 0.0259 0.0234 0.0407 0.0339 0.0417 0.0213 0.0175 0.0145 0.0161 0.0144 0.0202 0.0196 0.0152 0.0220 0.0222 0.0188 0.0171 0.0169 0.0146 0.0162 0.0159 0.0171

CE

2500 2500 2500 2500 2500 2500 2500 2500 2500 2500 2500 2452 2452 2452 2452 2452 2452 2475 2475 2475 2475 2706 2475 2475 2475 2475 2475 2475 2475 2475 2475 2627 2475

AC

NDPL-1.1 NDPL-1.2 NDPL-1.6 NDPL-1.14 NDPL-1.15 NDPL-1.16 NDPL-1.17 NDPL-1.18 NDPL-1.20 NDPL-1.22 NDPL-1.24 PDM-2.2 PDM-2.4 PDM-2.6 PDM-2.20 PDM-2.21 PDM-2.28 PRV-2.1 PRV-2.2 PRV-2.3 PRV-2.4 PRV-2.5 PRV-2.7 PRV-2.10 PRV-2.12 PRV-2.13 PRV-2.15 PRV-2.17 PRV-2.18 PRV-2.20 PRV-2.21 PRV-2.22 PRV-2.23

-52.3 -54.5 -53.6 -54.3 -54.8 -52.0 -53.7 -53.9 -55.7 -53.8 -50.8 -58.6 -59.2 -60.5 -60.3 -58.6 -61.3 -63.7 -68.2 -65.9 -66.9 -68.7 -63.3 -66.2 -68.5 -60.2 -60.4 -66.6 -66.7 -66.4 -64.6 -62.2 -64.2

2.8 0.6 2.1 1.0 0.4 2.8 1.4 1.0 0.2 1.3 4.0 -4.7 -5.0 -6.9 -6.6 -5.3 -7.2 -9.0 -13.3 -11.1 -12.1 -8.9 -8.7 -11.4 -14.0 -5.6 -5.6 -11.8 -11.9 -11.6 -9.8 -3.9 -9.4

2705 2788 2728 2770 2793 2706 2758 2772 2799 2762 2660 2946 2957 3032 3019 2973 3039 3125 3286 3202 3238 3321 3113 3215 3314 2998 2999 3230 3232 3221 3156 3065 3141

2832 2965 2871 2938 2975 2832 2917 2938 2990 2923 2757 3250 3271 3384 3365 3286 3403 3530 3795 3657 3716 3702 3510 3677 3834 3322 3325 3702 3706 3689 3581 3339 3557

-0.98 -0.98 -0.99 -0.99 -0.99 -0.98 -0.98 -0.98 -1.00 -0.98 -0.98 -0.98 -0.99 -0.98 -0.98 -0.97 -0.99 -0.99 -0.99 -0.99 -0.99 -0.99 -0.99 -0.99 -0.98 -0.98 -0.99 -0.99 -0.99 -0.99 -0.99 -0.99 -0.99

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0.280853 0.280929 0.281198 0.281167 0.281186 0.281180 0.281202 0.281215 0.281221 0.281106 0.281233 0.281218

RI

SC

0.000021 0.000020 0.000014 0.000017 0.000017 0.000018 0.000016 0.000020 0.000020 0.000025 0.000027 0.000023

NU

0.280919 0.280945 0.281210 0.281185 0.281200 0.281208 0.281221 0.281232 0.281235 0.281115 0.281253 0.281233

MA

0.0014 0.0003 0.0002 0.0004 0.0003 0.0006 0.0004 0.0004 0.0003 0.0002 0.0004 0.0003

PT ED

0.0636 0.0146 0.0106 0.0180 0.0121 0.0240 0.0159 0.0171 0.0138 0.0088 0.0201 0.0145

CE

2475 2475 2501 2501 2501 2501 2501 2501 2501 2501 2501 2501

AC

PRV-2.24 PRV-2.29 PRY-1.3 PRY-1.5 PRY-1.9 PRY-1.12 PRY-1.13 PRY-1.23 PRY-1.25 PRY-1.26 PRY-1.27 PRY-1.28

-65.5 -64.6 -55.3 -56.1 -55.6 -55.3 -54.9 -54.4 -54.4 -58.6 -53.7 -54.4

-12.5 -9.8 0.4 -0.7 0.0 -0.2 0.5 1.0 1.2 -2.9 1.7 1.1

3276 3153 2793 2835 2809 2820 2789 2771 2763 2915 2747 2767

3742 3577 2977 3044 3003 3017 2969 2939 2927 3177 2901 2933

-0.96 -0.99 -0.99 -0.99 -0.99 -0.98 -0.99 -0.99 -0.99 -0.99 -0.99 -0.99

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177

Hf/ Hf 0.281103 0.281241 0.281117 0.280991 0.281325 0.281287 0.281181 0.280808 0.280732 0.280755 0.280703 0.280755 0.280716 0.280754 0.280797 0.280671 0.280742 0.280829 0.280750 0.280883 0.280872 0.280661 0.280788 0.280853 0.280949 0.281070 0.280903 0.281084 0.281030 0.280925

2s 0.000016 0.000017 0.000019 0.000028 0.000020 0.000037 0.000018 0.000017 0.000018 0.000014 0.000013 0.000015 0.000018 0.000015 0.000016 0.000020 0.000019 0.000019 0.000021 0.000016 0.000043 0.000023 0.000022 0.000017 0.000016 0.000022 0.000020 0.000018 0.000024 0.000022

PT

176

176

177

Hf/ Hfi 0.281102 0.281211 0.281065 0.280815 0.281271 0.281250 0.281152 0.280808 0.280715 0.280715 0.280701 0.280754 0.280714 0.280753 0.280796 0.280671 0.280730 0.280829 0.280749 0.280882 0.280773 0.280586 0.280787 0.280853 0.280893 0.280939 0.280817 0.281053 0.280940 0.280866

RI

177

Lu/ Hf 0.0000 0.0006 0.0011 0.0028 0.0011 0.0009 0.0006 0.0000 0.0003 0.0006 0.0000 0.0000 0.0000 0.0000 0.0000 0.0000 0.0002 0.0000 0.0000 0.0000 0.0016 0.0011 0.0000 0.0000 0.0010 0.0024 0.0016 0.0006 0.0017 0.0011

SC

176

NU

177

Yb/ Hf 0.0011 0.0251 0.0494 0.1176 0.0440 0.0407 0.0305 0.0010 0.0117 0.0240 0.0010 0.0005 0.0020 0.0006 0.0010 0.0005 0.0077 0.0007 0.0004 0.0006 0.0789 0.0498 0.0004 0.0008 0.0464 0.1129 0.0796 0.0326 0.0807 0.0554

MA

176

PT ED

Age (Ma) 2284 2445 2477 3255 2630 2178 2420 2901 3121 3186 3127 3118 3174 3203 2926 2981 2975 2475 2371 2256 3127 3420 2360 2552 2847 2855 2825 2619 2797 2804

CE

Spot No. KTMR-2.1 KTMR-2.2 KTMR-2.9 KTMR-2.14 MBM-1.11 MBM-1.21 MBM-1.27 MBM-1.29 NDV-2.7 NDV-2.17 NDV-2.18 NDV-2.19 NDV-2.25 NDV-2.26 TNL-1/1.1 TNL-1/1.10 TNL-1/1.13 TNL-1/1.22 TNL-1/1.24 TNL-1/1.31 TNL-3/1.12 TNL-3/1.18 TNL-3/1.26 TNL-3/1.34 TNL-4/2.6 TNL-4/2.11 TNL-4/2.19 TNL-4/2.20 TNL-4/2.24 TNL-4/2.25

Zircon Lu-Hf isotope data for the metasedimentary suite from the Coorg Block and surrounding sutures.

AC

Table 10

eHf(0) -59.0 -54.1 -58.5 -63.0 -51.2 -52.5 -56.3 -69.4 -72.1 -71.3 -73.2 -71.3 -72.7 -71.4 -69.9 -74.3 -71.8 -68.7 -71.5 -66.8 -67.2 -74.7 -70.2 -67.8 -64.5 -60.2 -66.1 -59.7 -61.6 -65.3

eHf(t) -8.0 -0.4 -4.9 4.3 6.0 -5.2 -3.1 -4.2 -2.4 -0.9 -2.7 -1.1 -1.2 0.9 -4.1 -7.2 -5.3 -13.3 -18.5 -16.5 -0.2 0.0 -17.4 -10.7 -2.4 -0.6 -5.7 -2.0 -1.9 -4.4

TDM (Ma) 2918 2780 2982 3300 2697 2736 2859 3307 3429 3432 3446 3377 3429 3378 3322 3485 3411 3279 3383 3209 3362 3602 3333 3248 3204 3152 3314 2989 3148 3242

C

TDM (Ma) 3325 2985 3282 3323 2737 3072 3129 3566 3623 3582 3650 3543 3592 3490 3576 3809 3686 3794 4031 3819 3496 3710 3956 3693 3417 3312 3594 3217 3347 3502

fLu/Hf -1.00 -0.98 -0.97 -0.92 -0.97 -0.97 -0.98 -1.00 -0.99 -0.98 -1.00 -1.00 -1.00 -1.00 -1.00 -1.00 -0.99 -1.00 -1.00 -1.00 -0.95 -0.97 -1.00 -1.00 -0.97 -0.93 -0.95 -0.98 -0.95 -0.97

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0.000021 0.000026

0.280903 0.280794

PT

0.280979 0.280848

MA

NU

SC

RI

0.0014 0.0009

PT ED

0.0686 0.0473

CE

2838 2986

AC

TNL-4/2.30 TNL-4/2.31

-63.4 -68.0

-2.3 -2.7

3194 3332

3401 3541

-0.96 -0.97

ACCEPTED MANUSCRIPT

SC

RI

PT

P a g e | 118

AC CE P

TE

D

MA

NU

Graphical abstract

ACCEPTED MANUSCRIPT P a g e | 119

PT

Research Highlights

 Episodic magmatism during Eoarchean, Mesoarchean and Neoarchean.

SC

 Evidence for Hadean felsic continental crust.

RI

 Magmatic pulses related to subduction tectonics in convergent margins

AC CE P

TE

D

MA

NU

 Heterogeneous source reservoirs involving juvenile and reworked components.