Anwesa Banerjee
email: anwesabanerjee91@gmail.com

Nathan Cogné

Nicole Sequeira

Abhijit Bhattacharya

Dynamics of Early Neoproterozoic accretion, west-central India: I. Geochronology and Geochemistry

Keywords: Aravalli-Delhi Fold Belt, Central Indian Tectonic Zone, Archean granites and Paleoproterozoic gneisses, Early Neoproterozoic accretion, syn-collisional granitoids

The Godhra-Chhota Udepur (GC) sector (west-central India) is the zone of convergence between two crustal-scale accretion zones, i.e. the N/NNE-striking Aravalli Delhi Fold Belt (ADFB) against the E-striking Central Indian Tectonic Zone (CITZ). In this study, we demonstrate the two orogens welded during the Early Neoproterozoic.

In the GC sector, recumbently folded basement gneisses, shallow-dipping granitoid mylonites and a suite of allochthonous supracrustal rocks experienced top-to-the south thrusting and nappe formation (D2 deformation). The shallow-dipping crustal domain was modified by the superposition of a network of WNW/W-striking transpressional shear zones and related folds (D3 deformation). The D2-D3 deformations occurred due to oblique crustal convergence marked by the emplacement of pre-D2, post-D2 and syn-D3 granitoids. The post-D2, syn-D3 granite-granodiorites are weakly peraluminous, calc-alkalic, having ferroan to magnesian affinity, and characterised by LREE-enriched moderately fractionated REE patterns with variable negative Eu anomalies. Trace element geochemistry and whole rock Sr-Nd systematics suggest the granitoids were derived from dominantly meta-greywacke precursors. In South-GC, U-Pb zircons in the basement gneisses yield upper intercept/Concordia dates at 1.65-1.60 Ga for high-grade metamorphism. The lower intercept/Concordia dates in the gneisses coincide with the 0.95-0.93 Ga emplacement age of post-D2/syn-D3 granitoids throughout GC. However, the pre-D2 granitoids in South-GC are older, ~1.03 Ga. By contrast, pre-D2 granitoids in North-GC yield Late Neoarchean (2.5 Ga) Concordia/upper intercept emplacement ages, identical to the emplacement age of the Archean granites in the ADFB; the lower intercept/Concordia age is 0.95-0.93 Ga. The 2.5 Ga granites did not experience the 1.65-1.60 Ga high-grade metamorphism, but both the lithodemic units shared the 0.95-0.93 Ga D2-D3 deformation-metamorphism and the emplacement of post-D2 and J o u r n a l P r e -p r o o f Journal Pre-proof syn-D3 0.95-0.93 Ga granitoids. The juxtaposition of the ~2.5 Ga granitoids and the 1.65-1.60 Ga gneisses is attributed to the 1.03-0.93 Ga ADFB-CITZ oblique accretion that involved contemporaneous emplacement of syn-collisional S-type granitoids. (

INTRODUCTION

The dynamics of accretion-induced processes of superposed deformation, shear zone nucleation, magma generation and emplacement, and thermal perturbations are best understood at juxtapositions and terminations of orogenic belts [START_REF] Goscombe | Deformation correlations, stress field switches and evolution of an orogenic intersection: The Pan-African Kaoko-Damara orogenic junction, Namibia[END_REF].

These key locales are a storehouse of natural processes, and analyses of these processes are crucial for understanding the dynamical aspects of accretion of disparately evolved crustal blocks at a global scale vis-à-vis Supercontinent assembly. Granitoid suites from such key locales have been extensively used as proxies to understand crustal evolutionary histories [START_REF] Hinchey | Lithogeochemical and Nd isotopic constraints on felsic magmatism in the Makkovik Orogen, Labrador, Canada: Implications for assembly of the supercontinent Nuna[END_REF].

The Great Indian Proterozoic Fold Belt (GIPFOB; [START_REF] Leelanandam | Proterozoic mountain building in Peninsular India: an analysis based primarily on alkaline rock distribution[END_REF]) is considered to be a crustal-scale (~1600 km long) tectonic zone. The highly-tectonized zone seemingly -bends‖ around the North India Block (NIB) which comprises the crescent-shaped Archean Bundelkhand Craton (Fig. 1). The E-striking southern arm of the GIPFOB, also termed as the Central Indian Tectonic Zone (CITZ) [START_REF] Sharma | Cratons of the Indian Shield[END_REF] is sandwiched between the NIB and the South India Block (SIB) consisting of the Archean Cratons of Singhbhum and Bastar. This arm consists of the coherently evolved Late Paleoproterozoic to Early Neoproterozoic crustal domains of the Chottanagpur Gneiss Complex (CGC) and the southern and central domains of the Satpura Mobile Belt (SMB), extending west up to the Godhra-Chhota Udepur sector [START_REF] Banerjee | Tectonics of the Greater India Proterozoic Fold Belt, with emphasis on the nature of curvature of the belt in west-central India[END_REF](Banerjee et al., , 2022a)). On the other hand, the N/NNEstriking western arm of the GIPFOB comprises the Neoarchean to Early Neoproterozoic Aravalli Delhi Fold Belt (ADFB) juxtaposed between the Marwar Craton (MC) in the west, and the NIB in the east (Fig. 1). [START_REF] Banerjee | Tectonics of the Greater India Proterozoic Fold Belt, with emphasis on the nature of curvature of the belt in west-central India[END_REF]Banerjee et al. ( , 2022a) ) demonstrate that the curvilinear geometry of the GIPFOB is not due to the bending of a single accretion zone around an -indentor‖ (cf. [START_REF] Weil | Classification of curved orogens based on the timing relationships between structural development and vertical-axis rotation[END_REF]) such as the Bundelkhand Craton. Instead the broad -bend‖ in the J o u r n a l P r e -p r o o f southern parts of the ADFB is the result of the juxtaposition of two Early Neoproterozoic accretion zones, with the older N/NNE-striking ADFB terminating against the E-striking southern arm or the CITZ with sinistral kinematics [START_REF] Banerjee | Tectonics of the Greater India Proterozoic Fold Belt, with emphasis on the nature of curvature of the belt in west-central India[END_REF](Banerjee et al., , 2022a)), similar to the ones reported elsewhere (cf. [START_REF] Macedo | Controls on the geometry of fold -thrust belt salient[END_REF][START_REF] Velandia | Present-day structural frame of the Santander Massif and Pamplona J o u r n a l P r e -p r o o f Journal Pre-proof Wedge: The interaction of the Northern Andes[END_REF]. But the dynamics of the Early Neoproterozoic accretion of the two orogens are unexplained primarily due to the lack of robust geochronological data of the lithodemic units and geochemical data of the expansive Early Neoproterozoic granitoids that partly obscure the accretion zone. We aim to address this issue in a set of two articles in sequel, of which this manuscript is the first part. In this part, we present the results of the analyses of (i) mesoscale structures, (ii) Laser Ablation Inductively Coupled Plasma Mass Spectrometric (LA-ICP-MS) U-Pb zircon dating, (iii) electron probe microanalysis (EPMA) monazite dating, (iv) whole rock major and trace element geochemistry and (v) Rb-Sr and Sm-Nd isotope compositions in granitoids. The Godhra-Chhota Udepur (GC) sector, where the two accretion zones converge [START_REF] Banerjee | Tectonics of the Greater India Proterozoic Fold Belt, with emphasis on the nature of curvature of the belt in west-central India[END_REF](Banerjee et al., , 2022a)), has thus been adopted for this study.

GEOLOGICAL BACKGROUND

Four lithodemic units constitute the Precambrian crystalline rocks in the Godhra-Chhota Udepur sector (Fig. 2). The sector is dominated by variably deformed (massive, foliated, mylonitic) blastoporphyritic granitoids, collectively termed as the -Godhra granite‖ [START_REF] Gupta | Stratigraphy and structure of Delhi Supergroup of rocks in central part of Aravalli Range[END_REF]. Some of the granitoids are intrusive into poly-deformed anatectic quartzofeldspathic gneisses [START_REF] Mamtani | Granite emplacement and its relation with regional deformation in the Aravalli Mountain Belt (India)-inferences from magnetic fabric[END_REF]. The next dominant lithodemic unit comprises greenschist/epidote-amphibolite facies white mica-chlorite schists, micaceous quartzite, foliated and gneissose meta-carbonates, Mn-rich horizons, meta-arenites, deformed oligomict conglomerates and amphibolites of the Champaner Group of the Aravalli Supergroup (Fig. 2a). The Champaner Group of metasediments [START_REF] Gupta | Stratigraphy and structure of Delhi Supergroup of rocks in central part of Aravalli Range[END_REF][START_REF] Joshi | Evidence of syndeformational granitoid emplacement within Champaner Group, Gujarat[END_REF] J o u r n a l P r e -p r o o f Journal Pre-proof [START_REF] Joshi | Evidence of syndeformational granitoid emplacement within Champaner Group, Gujarat[END_REF] were previously thought to share an erosional contact with the anatectic gneisses and granitoids but some units of the Godhra granite were however inferred to be intrusive into the supracrustal unit [START_REF] Joshi | Evidence of syndeformational granitoid emplacement within Champaner Group, Gujarat[END_REF]. Some ultramafic rocks (pyroxenite, serpentinite) of unknown association also occur in the eastern part of the GC Sector near Jobat (Fig. 2a). The Lunavada Group of the Aravalli Supergroup consisting of greenschist facies quartzite, phyllite, schist and minor carbonates [START_REF] Gupta | Stratigraphy and structure of Delhi Supergroup of rocks in central part of Aravalli Range[END_REF] occur to the north of the Godhra-Chhota Udepur Sector (Fig. 2a). The Precambrian crystalline rocks in the southern part of the GC sector are obscured by the Upper Cretaceous Deccan volcanics, the infratrappean Lameta Formation and the intertrappean Bagh beds (terminology after [START_REF] Sahni | Upper Cretaceous dinosaur eggs and nesting sites from the Deccan-volcano sedimentary province of peninsular India[END_REF] (Fig. 2a).

The emplacement ages of the Godhra granite vary between Late Mesoproterozoic to Early Neoproterozoic, e.g. 955 ± 20 Ma, (Rb-Sr, [START_REF] Gopalan | Rb-Sr age of Godhra and related granites, Gujarat, India[END_REF], 1168 ± 30 Ma (Rb-Sr, [START_REF] Srimal | On the tectonic affinity of the Champaner Group of rocks, Eastern Gujarat[END_REF], 965 ± 40 Ma, (Rb-Sr, Goyal et al., 2001), and 1050 ± 50 Ma, (Sm-Nd, ShivKumar et al., 1993). The 955 Ma age of [START_REF] Gopalan | Rb-Sr age of Godhra and related granites, Gujarat, India[END_REF] is the most cited age for the emplacement of the Godhra granite (Mamtani and Greiling, 2005 and references therein). Recently Banerjee et al. (2022a) carried out U-Pb LA-ICP-MS zircon dating of an anatectic gneiss and a blastoporphyritic granite. The high-grade anatexis-metamorphism in the anatectic gneiss occurred at ~1.65 Ga, and the emplacement age of the granitoid was 0.95-0.90 Ga, consistent with the existing Early Neoproterozoic Rb-Sr and Sm-Nd isochron dates in the Godhra granite.

The lithological, field relation and analysis of mesoscale to regional structures and deformation kinematics are discussed by [START_REF] Banerjee | Tectonics of the Greater India Proterozoic Fold Belt, with emphasis on the nature of curvature of the belt in west-central India[END_REF]Banerjee et al ( , 2022aBanerjee et al ( , and 2022b, accompanying article), accompanying article). In this section, we highlight the structural aspects vis-à-vis stages of granitoid emplacement relevant to this article (Fig. 3a). The most significant feature in the GC sector is a shallowly-dipping to gently-inclined structural domain (D2 deformation) J o u r n a l P r e -p r o o f composed of mylonitic to foliated granitoids, recumbently folded anatectic gneisses and the Champaner group of greenschist to amphibolite facies supracrustal rocks (Fig 3b,c) inferred to be an allochthonous unit (Banerjee et al., 2022a). The W/WNW-plunging D2 recumbent folds in the gneisses formed on D1a, b metatexite layers; limited syn-D2 anatexis (<2 vol% of rock) was observed in a couple of biotite-rich gneiss outcrops. By contrast, the W/WNWplunging D2 folds in the supracrustal rocks formed on a pre-D2 axial planar fabric defined by the shape preferred aggregates of white mica-chlorite assemblages in mica schists, talctremolite-antigorite in meta-carbonate, and amphibole-plagioclase-clinozoisite-chlorite in amphibolites (details in accompanying article; [START_REF] Banerjee | Dynamics of Early Neoproterozoic accretion, west-central India: II Early Neoproterozoic LT-HP and Early Paleoproterozoic HT-LP metamorphism at Godhra-Chhota Udepur, and a tectonic model for accretion[END_REF]. The hinges of D2 folds in the gneisses and rocks in the supracrustal unit are broadly collinear with the D2 stretching lineation in the pre-D2 granitoids (Fig. 3b,c).

The shallow-dipping tectonic mélange formed by top-to-the-south thrusting of the supracrustal rocks over the basement rocks leading to the folding and interleaving of the rock units (Fig. 3a). The tectonic mélange is traversed by a network of W/WNW-striking steepdipping transpressional shear zones (D3) with sinistral and dominantly N-down kinematics (Fig. 3a); S-down movement along the D3 shears occur in a few outcrops. In the vicinity of these D3 shears (Fig. 3d,e) the gneisses and the supracrustal rocks exhibit upright folds and the granitoids evolve into steep-dipping L and L-S tectonites (Fig. 2b). Locally-developed steep-dipping conjugate shear zones (D4) striking NNE (dextral) and ENE (sinistral) in the D4 high-strain zones are melt-hosted within the granite mylonites, and are deemed to be coeval with the D3 deformation (Fig. 2a). As with the D2 deformation event, the D3 stretching lineations and broadly collinear D3 fold axes plunge at low to moderate angles to the W and WNW (Banerjee et al., 2022a). The thrust-dominated (D2) and wrench-dominated (D3) deformations are inferred to be a part of the progressive NNE-SSW crustal shortening that caused orogen-parallel stretching (Banerjee et al., 2022a).

J o u r n a l P r e -p r o o f

The granitoids in the area are dominantly post-D2 to syn-D3; the granitoids occur as lens-shaped bodies, exemplified by the Sanada granitoid pluton (Fig. 2a; Banerjee et al., 2022a). The pre-D2 granitoids cover a smaller area. Post-D3 granites are lacking in the Godhra-Chhota Udepur sector. All structural types of granitoids are blastoporphyritic, foliated and dynamically recrystallized. The pre-D2 granitoids possess a prominent tectonic foliation (D2) and contain cm-sized elliptical to round K-feldspar porphyries that constitute <2 vol% of the rock (Fig. 4a). Some of the pre-D2 granitoids are found to be interleaved with the anatectic gneisses, and the D2 foliation in the granitoid is axial planar to the D2 folds in the gneisses (Fig. 4b). In the post-D2 granitoids, K-feldspar porphyries are euhedral to subhedral, large (long axes up to 6 cm) and constitute up to 50 vol% of rock in the interiors of E-W striking plutons (Fig. 4c). In these granitoids, trains of euhedral K-feldspar porphyries and imbrications among euhedral porphyries are inferred to be magmatic flow textures; tectonic fabrics in these granitoids are weakly developed or lacking. But towards the pluton margins, the flow-textured and massive granitoids grade into intensely foliated (steep-dipping D3) varieties (Fig. 4d). In the syn-D3 granitoids, K-feldspar porphyries constitute up to 75% of the rock, and trains and imbrications among large euhedral K-feldspar porphyries dominate the rocks. Some of these porphyries develop asymmetric tails (sinistral sense) that are drawn out sub-parallel to quartz lentils and aggregates of shape-preferred biotite flakes forming the warping D3 foliation (Fig. 4e). The pre-D2 granitoids are sometimes preserved as small relicts within the post-D2 and the syn-D3 granitoids that exhibit intrusive margins; at other places mineralogically different types of granitoids share sharp contacts (Fig. 4f).

Deformation microstructures in granitoids

The granitoids within the D2 shallow-dipping domains are fine to medium grained, wellfoliated and contain porphyries of subhedral feldspar (Fig. 5a). The D2 foliation in the rocks J o u r n a l P r e -p r o o f is primarily defined by the shape-preferred biotite flakes (Fig. 5a; hornblende is rare), and xenoblastic mono-and poly-crystalline quartz lentils, commonly exhibiting strain wavy extinction and sub-grains (Fig. 5b); the mosaic of dynamically recrystallized alkali feldspar (microcline), plagioclase and internally-strained quartz grains share serrated (high energy) grain and phase boundaries (Fig. 5b,c), and are anchored to the D2 biotite and quartz lentils (Fig. 5c). Triple junctions among feldspar are rare. Coarse porphyries of magmatic Kfeldspar and plagioclase within the finer grained mineral mosaic exhibit patchy chemical zoning and core-mantle structures; the margins of these feldspar grains exhibit serrated to lobate-cuspate margins against the quartz grains (Fig. 5d). By contrast, the post-D2 granitoids are invariably coarse-grained, weakly foliated, and blastoporphyritic (Fig. 5e). The D3 fabric in the granitoids is defined by trains and imbrications among euhedral feldspar grains (Fig. 5f), crude alignment among flaky biotite, and internally strained quartz lentils; the quartz lentils have smaller aspect ratio (length/width) relative to those in the pre-D2 granitoids. The foliation is somewhat sinuous and wraps around coarser microcline phenocrysts within the mosaic of recrystallized minerals. The feldspar grains are weaklystrained internally and largely preserve their magmatic shapes (Fig. 5f). But within the mosaic, these feldspar grains share lobate-cuspate margins against the quartz lentils which in turn commonly show chess-board sub-grain structures (Fig. 5g). Intensely sheared post-D2 granitoids exhibit mylonitic fabric defined by internally strained quartz ribbons, and coremantle structured dynamically recrystallized feldspars that share lobate-cuspate grain and phase boundaries against other minerals (Fig. 5h).

Overall, the post-D2 granitoids are weakly strained relative to the pre-D2 granitoids in the shallow-dipping carapace; this is manifested by the finer grain size and the paucity of relic magmatic porphyries in the pre-D2 granitoids. But the common occurrences of chess-board microstructures in quartz suggest the post-D2 granitoids were hot (T> 650 ºC; [START_REF] Kruhl | Prism-and basal-plane parallel subgrain boundaries in quartz: a microstructural geothermobarometer. Prism-and basal-plane parallel subgrain J o u r n a l P r e -p r o o f Journal Pre-proof boundaries in quartz: a microstructural geothermobarometer[END_REF] J o u r n a l P r e -p r o o f during D3 deformation. Chess-board microstructures in quartz in the post-D2 granitoids are highlighted by several authors [START_REF] Mamtani | Granite emplacement and its relation with regional deformation in the Aravalli Mountain Belt (India)-inferences from magnetic fabric[END_REF]Banerjee et al., 2022a); by contrast the pre-D2 granitoids lack this deformation microstructure. If we therefore combine the mesoscale field relations with the deformation microstructures, the emplacement of the post-D2 granitoids appears to be broadly synchronous with the D3 deformation induced by the N-S convergence, but this deformation outlasted the solidification of the post-D2 granitoids.

GEOCHRONOLOGY

In this section, we present Laser Ablation ICP-MS U-Pb zircon dates in nine structurally constrained samples (2 anatectic gneisses, and 7 granitoids) and chemical dates from monazite in four samples (2 anatectic gneisses, and 2 granitoids) obtained from different parts of the Godhra-Chhota Udepur sector (locations in Fig. 2b). A brief summary of mineral assemblages, texture, zircon and monazite morphology in the 13 samples used in geochronology are presented in Table 1. The results are designed to constrain the age of the different magmatic, metamorphic and deformation events crucial for a tectonic restoration of the dynamics of accretion between the ADFB and the CITZ orogenic belts. In the nine samples, cathodoluminescence (CL) images of representative zircons along with the analyzed spots and corresponding 207 J o u r n a l P r e -p r o o f

Zircon geochronology

LA-ICP-MS U-Pb zircon dating was performed on two gneisses (AW 161, AW 114) and seven pre-D2 to syn-D3 granitoids (AW 98,AW 145,AW 127,AW 18,AW 73,AW 8,AW 9A). The zircon grains were analyzed at the Plateforme GeOHeLiS, Géosciences Rennes, University of Rennes, France. The analytical procedure and instrument operating conditions are detailed in the Appendix A. Zircons from both the gneiss and granite samples are large (~200-300 μm long), well-faceted, prismatic to square in shape, and pink to honey-yellow in colour (details of individual samples are in Table 1a). Plots of Th/U vs. 207 show prominent core-rim structures in the CL images (Fig. 6b). Th/U ratios of the grains vary in the range 0.04-1.60 (Fig. 6a); the values <0.1 (4 points) correspond to CL-dark zones.

J o u r n a l P r e -p r o o f

Two spots from the same grain (CL-dark zone, Th/U ~ 0.04) furnish concordant age of 909 ± 11 (±36) Ma (MSWD = 0.51; Fig. 7a). On the other hand, 33 of the 35 analyzed spots describe a well-defined Discordia with the upper intercept at 2485 ± 15 (± 96) Ma and the lower intercept at 932 ± 15 (± 39) Ma (MSWD = 1) (Fig. 7a). The younger date (~0.93 Ga) is inferred to be the age of deformation-metamorphism in the rock; the older date (~2.5 Ga) corresponds to either the age of formation of the rock or the age of inherited zircons in the rock.

Sample AW 114 is an anatectic gneiss from a D3 high-strain domain in the southern part of the GC sector (Fig. 2b). The metatexite gneiss comprising alternate biotite-rich and leucosome layers describe prominent D2 recumbent folds. The metatexite layers are pre-D2.

The recumbent folds are wrapped by locally penetrative isoclinal to tight folds forming a ramp and flat structure related to the D4 dextral shears. A total of 25 spots were analyzed in 24 grains in the sample. Most of the grains show core-rim textures, although some grains are homogenous, recrystallized and appear dark in CL images (Fig. 6c). The Th/U ratios of the zircon grains vary from 0.04-1.25 (Fig. 6a), the values <0.2 correspond to CL dark domains and are mostly from the recrystallized and homogenous grains. All the 25 spots define a Discordia with upper intercept date of 1742 ± 20 (± 69) Ma and a lower intercept date of 470 ± 30 (± 35) Ma (MSWD = 0.41; Fig. 7b). We consider that the Pan African lower intercept date (~0.5 Ga) has no physical significance in view of the fact that monazites which are especially susceptible to fluid-induced alteration even at greenschist facies condition does not yield dates younger than Early Neoproterozoic in the diverse lithodemic units (including anatectic gneisses) from the GC sector examined by [START_REF] Banerjee | Tectonics of the Greater India Proterozoic Fold Belt, with emphasis on the nature of curvature of the belt in west-central India[END_REF] and in this study (see later).

J o u r n a l P r e -p r o o f 3.1.2 Granitoids: Two samples, AW 18 and AW 145, are post-D2 blastoporphyritic granitoids sampled from D3 high strain domains (Fig. 2b). Sample AW 18 is the northernmost dated sample of pink blastoporphyritic granitoid neighboring Godhra; the alignment of euhedral K-feldspar porphyries defines N110° striking magmatic fabric. Sample AW 145 is a weakly foliated pink granitoid consisting of K-feldspar porphyries and biotite defining the N110° steep fabric. Sample AW 98 is a granite phyllonite with steep NNE-trending fabrics corresponding to the D4 shears.

Thirty spots were analyzed in 15 grains from the sample AW 18. The zircon grains show well developed core-rim structures with oscillatory zoning (Fig. 6d). Th/U ratios in these grains vary from 0.3-1.91 (Fig. 6a), except for 2 spots with Th/U ratio of 0.16 and 0.18 corresponding to two CL-dark rims of zircon grains. Seven concordant analyses yield a concordia age of 946 ± 6 (± 37) Ma (MSWD = 0.54; Fig. 7c). These seven points lie at the upper intercept of a Discordia defined by seventeen other spots from both cores and rims of zircon grains (Fig. 7c). The lower intercept of the Discordia does not have significance. No difference in dates could be deciphered between the core and rims of the zircon grains.

In the sample AW 145, 35 spots were analyzed in 19 grains (Fig. 6d). The Th/U ratios of the analyzed spots range from 0.37-2.52 (Fig. 6a), with only three spots marked by Th/U ratios <0.1. These three spots pertain to CL-dark domains within the zircon grains and yield highly discordant ages and have not been considered. Twelve concordant spots yield a concordia age of 955 ± 7 (± 37) Ma (MSWD = 1.2) and define a Discordia with 8 other points with an upper intercept at 2525 ± 46 (± 106) Ma and lower intercept at 944 ± 15 (± 39) Ma (MSWD = 1; Fig. 7d). The overlapping concordia and lower intercept dates correspond to the post-D2 emplacement age of the granitoid, whereas the Neoarchean upper intercept date possibly represents the age of the protolith.

J o u r n a l P r e -p r o o f

A total of 30 spots in 14 grains were analyzed in sample AW 98. The analyzed spots mostly have high common lead and their Th/U ratios range from 0.09-1.82. No alignment is found in the Wetherill plot (Fig. 7e). However, two concordant spots (shown in pink colour in Fig. 7e), with no common lead, and Th/U ratio of 0.39 and 0.43 (Fig. 6a) are obtained with 207 Pb/ 206 Pb dates of 2418 ± 30 Ma and 2384 ± 30 Ma respectively (Fig. 6f) that possibly correspond with the age of emplacement (~2.4 Ga) of the granitoid. Sample AW127 is pink granitoid collected from a large outcrop in the Orsang river bed south of Bodeli in the southern GC sector (Fig. 2b). The granitoid is very coarse-grained and studded with end-to-end touching and imbricate grains of large (> 6cm long crystals), euhedral to subhedral, un-recrystallized K-feldspar laths exhibiting zoning and Carlsbad twins. An ill-defined steep E-striking D3 fabric in the rock is described by trains of feldspar laths. The weak planar fabric, the coarse-grained nature of the granites, and the unrecrystallized feldspar laths suggest that the rock represents the last episode of granite emplacement in the region. Twenty-five spots have been analyzed in 21 zircon grains (Fig. 6g). Seven of the 25 spots furnished a concordant date of 951±10 (± 37) Ma (MSWD = 1.2; Fig. 7f). All the seven spots are from the rims of the zircon grains while the cores yield discordant dates. This date is inferred to correspond to the emplacement age of the syn-D3 granitoid.

Sample AW 9A is a massive (no mesoscale fabric) post-D2 white coloured granitoid impoverished in ferromagnesian minerals. The sugary appearance of the rocks is due to dynamic recrystallization of feldspars. The granite is apophytic into an ensemble of multiplydeformed quartzofeldspathic and interleaved calc-silicate gneisses that experienced multiple deformation events. A total of 30 spots were analyzed in 13 grains (Fig. 6h). Although most of the analyzed spots are discordant and have some amount of common lead, 2 spots from the J o u r n a l P r e -p r o o f CL-dark core of a zircon grain yield a concordant date of 1607 ± 24 Ma (MSWD = 0.40) while a single concordant analysis with 206 Pb/ 238 U date of 951 ± 17 Ma is obtained from the CL-dark core of another zircon grain. A Discordia is defined with four spot ages (no common lead, Th/U ratios between 0.26-0.79, all from cores of zircon grains, with an upper intercept age of 2544 ± 82 (± 127) Ma and a lower intercept age of 958 ± 26 (± 45) Ma (MSWD = 0.88; Fig. 7g). The youngest dates (951 ± 17 Ma, 958 ± 26 Ma) in the deformed and recrystallized granite with no mesoscale fabric possibly correspond with the age of emplacement of the intrusive. The older date at ~1.61 Ga closely corresponds to the age of high-grade metamorphism in the anatectic gneisses [START_REF] Banerjee | Tectonics of the Greater India Proterozoic Fold Belt, with emphasis on the nature of curvature of the belt in west-central India[END_REF]; the ~2.54 Ga date is coeval with the emplacement age of the granite or the protolith age of the gneisses in the northern part of the GC sector. Notably though no Discordia exists between 2.54 Ga and 1.61 Ga.

Two pre-D2 grey-coloured granitoids were dated from the southern domain, AW 8 and AW 73 (Fig. 7h). The sample AW 73 is from a large hillock, whereas AW 8 was sampled from a hummocky sheeted outcrop. Both samples are characterized by low proportions (< 2 vol%) of cm-sized circular-shaped K-feldspar phenocrysts and high modal amounts of biotite.

The rocks possess biotite-defined weak shallowly-dipping D2 fabrics in a mosaic of dynamically recrystallized feldspars and quartz.

For AW 73 (Fig. 6i), 40 spots were analyzed in 18 grains and no concordant spots were obtained. However, 29 spots define a Discordia with upper and lower intercepts at 1026 ± 17 (± 43) Ma and 111 ± 40 (± 40) Ma (MSWD = 1.4; Fig. 7h). In sample AW 8 (Fig. 6j), 40 spots were analyzed in 22 grains. Three spots from the rims of three zircon grains yield a concordant date of 983 ± 11 (± 39) Ma (MSWD = 1.4; Fig. 7i). These three spots along with 21 other spots corresponding to both cores and rims of zircon grains define a Discordia with upper and lower intercepts at 1020 ± 22 (± 45) Ma and 186 ± 35 (± 36) Ma (MSWD = 0.95) J o u r n a l P r e -p r o o f respectively (Fig. 7i). For both the foliated granitoids, the upper intercept dates are inferred to correspond with the emplacement ages of the granitoids. The significance of the slightly younger concordant dates (~0.98 Ga) obtained from the rims of the zircon grains may correspond with thrusting and associated shallow-dipping fabric formation. The lower intercept dates are not considered to be significant.

Monazite chemical dating:

Two samples each of anatectic gneisses (AW 7, AW 9B) and grey granitoids (AW 12, AW 163) with steep E-striking D3 fabrics were analyzed for monazite chemical dating following the procedure of [START_REF] Montel | Electron microprobe dating of monazite[END_REF] at the Department of Earth Sciences, Indian Institute of Technology Bombay (Powai). A brief description of the methodology is provided in Appendix B. The locations of the analyzed samples are shown in Fig. 2b and the data is presented in Supplementary Material 2 . A brief description of the rocks, textural chemical characteristics, and summary dates in monazite are provided in Table 1b. The monazite grains mostly occur within biotite-rich aggregates, and only few monazites are hosted within quartz-feldspar aggregates (Fig. 8a,c,e,g). The grains are ellipsoidal to prismatic, xenoblastic to sub-idioblastic and chemically zoned in Th, Y and U (rarely Pb) (Fig. 8a,c,e. g). Based on X-ray element maps for Th, U, Pb and Y and back-scattered electron images, 58 spot dates were obtained in chemically distinct domains in the four samples. The monazite spot ages in the four samples (Fig. 8b,d,f,h) taken together yield dates between 863 ± 50 Ma to 969 ± 47 Ma, with an average age of around ~ 918 Ma; one outlier spot is dated at 1020 ± 32 Ma. The mean dates obtained for the samples are identical at 2 level. Anatectic gneisses AW 9B and AW 7 yield mean dates of 923 ± 13 Ma (MSWD = 1.8, n = 11) and 905 ± 16 Ma (MSWD = 3.7, n = 14) respectively (Fig. 8b,d). The granitoid AW 163 yields a J o u r n a l P r e -p r o o f mean date of 908 ± 19 Ma (MSWD = 2.7, n= 12), and 21 spots in the granitoid AW 12 yield a mean date of 926 ± 11 Ma (MSWD = 3.3) (Fig. 8f,h).

Summary of age data:

The LA-ICP-MS U-Pb zircon dates obtained in the nine samples, combined with two zircondated samples in Banerjee et al (2022a), may be grouped into four age populations, e.g. 2.5-2.4 Ga, 1.7-1.6 Ga, 1.03-1.02 Ga and 0.95-0.93 Ga (Fig. 9). The monazite chemical dates in this study and those in Banerjee et al. (2022a) in gneisses, granitoids, and greenschist/amphibolite facies supracrustal rocks overlap with the youngest population of U-Pb zircon dates. The youngest age population (0.95-0.93 Ga) corresponds to the emplacement of the post-D2 granitoids including the syn-D3 granitoids. The age population (1.03-1.02 Ga) corresponds to the emplacement of the younger set of pre-D2 granitoids. Pre-D2 high-grade metamorphism-anatexis in the anatectic gneisses occurred at 1.65-1.6 Ga (cf. [START_REF] Banerjee | Tectonics of the Greater India Proterozoic Fold Belt, with emphasis on the nature of curvature of the belt in west-central India[END_REF]Banerjee et al., , 2022a[START_REF] Banerjee | Dynamics of Early Neoproterozoic accretion, west-central India: II Early Neoproterozoic LT-HP and Early Paleoproterozoic HT-LP metamorphism at Godhra-Chhota Udepur, and a tectonic model for accretion[END_REF]. The oldest Concordant and upper intercept Discordia dates (2.5-2.4 Ga) in zircons are obtained from pre-D2 foliated granites and non-anatectic gneisses located in the northern part of the GC sector based on the results of LA-ICP-MS zircon U-Pb analysis from a total of 11 samples (Fig. 2b). There is no evidence to suggest that these Neoarchean/Early Paleoproterozoic rocks, lacking in the southern part of the GC sector, experienced the 1.65-1.60 Ga high-grade metamorphism recorded in the anatectic gneisses (Fig. 2b). The consequences of these observations are discussed in section 5.

GEOCHEMISTRY OF 1.03-0.93 Ga GRANITES

Whole rock major and trace element geochemistry

Whole rock geochemical analyses were performed on 9 pink granitoids, 10 grey granitoids and 5 anatectic gneisses (locations in Fig. 2b). The details of sample processing and protocols

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Journal Pre-proof for analyses done by Inductively Coupled Plasma Emission Spectrometry (ICP-ES) for major elements, and Inductively Coupled Plasma Mass Spectrometer (ICP-MS) for trace elements at the ACME Lab, Bureau Veritas, Vancouver, Canada are described in the Appendix C. The results are provided in Table 2 andused The major element oxide contents in the pre-D2 ~1.03 Ga granitoids and post-D2 0.95-0.93 Ga granitoids are variable, e.g. SiO 2 (63.27-75.74 wt%), Al 2 O 3 (10.15-15.48 wt%), Fe 2 O 3 total (0.54-6.17 wt%), MgO (0.32-1.82 wt%), K 2 O (2.59-6.88 wt%), Na 2 O (0.68-4.8 wt%), CaO (0.24-3.31 wt%), and TiO2 (0.06-1.22 wt%) (Table 2). The Fe# (molar FeO/FeO+MgO) of these granitoids lie between 0.40 and 0.77 (Table 2). The granitoids are granite-granodiorite in composition (Fig. 10a), with the exception of AW 155 which plots in the field for monzonite. The alumina saturation index (ASI) in the granitoids, calculated as molar Al 2 O 3 /(CaO+Na 2 O+K 2 O), lies in the range 0.98-1.24; the granitoids therefore are weakly peraluminous (Fig. 10b), with AW 155 (ASI value: 0.86) being the only exception.

The granitoids plot in the field of S-type granitoid (Fig. 10c). Within the granitoids, Fe 2 O 3 (total), MgO and CaO decrease with increasing SiO 2 ; Al 2 O 3 exhibits a weak negative correlation with SiO 2 , and K 2 O exhibits the opposite trend (Supplementary Material 3 ). The compositions of the anatectic gneisses overlap with those in granitoids; however MgO contents in the gneisses are higher and Fe# are lower relative to the granitoids in the GC sector (Supplementary Material 3 ).

The ∑REE in the pink granitoids vary between 108 ppm and 751 ppm; the corresponding value for the grey granitoids range between 84 and 424 ppm (Fig. 10d, Table 2). Sample AW 155 has the highest REE abundance, 1008 ppm (Fig. 10d, Table 2). The chondrite normalized REEs in the granitoids are LREE enriched [(La/Yb) CN = 11-89] and the

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HREEs exhibit relatively flat patterns [(Gd/Yb) CN = 1.54-4.67] (Fig. 11). The granitoids are characterised by small but variable negative Eu anomalies (computed as (Eu CN /Eu*; Fig. 11), where Eu* is calculated as (√Sm CN *Gd CN ) for the pink granitoids and range between 0.08 and 0.83; a grey granitoid (AW 63) has a Eu anomaly value of 1.00 (Table 2; Fig. 10d).

The Nb/Ta values for the GC granitoids (5.2-21.6) are typical for peraluminous granites unmodified by hydrothermal activity (> 5; [START_REF] Ballouard | Nb-Ta fractionation in peraluminous granites: A marker of the magmatichydrothermal transition[END_REF]. The negative trend of Nb/Ta versus Ta (Fig. 10e) is attributed to mica fractionation [START_REF] Ballouard | Nb-Ta fractionation in peraluminous granites: A marker of the magmatichydrothermal transition[END_REF]. In the Nb/Ta versus Zr/Hf diagram (Fig. 10f), the GC granitoids plot in the field for peraluminous -barren‖ granites [START_REF] Ballouard | Nb-Ta fractionation in peraluminous granites: A marker of the magmatichydrothermal transition[END_REF]. On the Th/Ta versus Yb plot [START_REF] Gorton | From continents to island arcs: a geochemical index of tectonic setting for arc-related and within-plate felsic to intermediate volcanic rocks[END_REF] (Fig. 10g), some of the pink granites lie in the field of active continental margins; the rest of the granitoids plot in the field of oceanic arcs.

Chondrite normalized REE diagrams and bulk continental crust normalized trace element spider diagrams for the granitoids and gneisses in the GC sector are presented in Figs. 11 and 12 respectively. The trace element abundances of the S-type granitoids normalized to the bulk continental crust composition [START_REF] Rudnick | Composition of the continental crust[END_REF] show an overall enrichment of incompatible elements in the granitoids (Fig. 12a-b). Similar trace element enrichment is also observed in the gneisses with respect to the bulk continental crust (Fig. 12c). An average gneiss composition (blue bold line in Fig. 12c) for the GC samples also mimics the enriched trend of the gneisses relative to the bulk crust. Assuming the anatectic gneisses were the source rocks for the granitoids (see Discussion), we normalized the granitoid trace element abundances to the average composition of the 5 basement gneisses (Fig. 12d-e). Relative to the average gneiss (Fig. 12c), the pink granitoids are enriched in Ba, Th and LREEs and depleted in P, Eu, Ti and HREEs (Fig. 10d); the grey granitoids on the other hand show enrichment of Rb, Ba, Th, U, K, Nb, Ta and LREEs, and depletion of P, Ti Zr, Hf, Sm, Eu, Y and HREEs (Fig. 12e).

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The Zr concentrations of the granitoids were used to calculate the zircon saturation temperature (T Zr ) [START_REF] Clemens | S-type granitic magmas-petrogenetic issues, models and evidence[END_REF] which may be used as a proxy for obtaining crystallization temperature of the melts [START_REF] Watson | Zircon saturation revisited: temperature and composition effects in a variety of crustal magma types[END_REF]). The T Zr was calculated for the GC granitoids (Table 2) using the formulation of [START_REF] Watson | Zircon saturation revisited: temperature and composition effects in a variety of crustal magma types[END_REF] and [START_REF] Boehnke | Zircon saturation re-revisited[END_REF]. The average temperature estimate obtained for the pink granitoids is 840 °C and 800 °C by the [START_REF] Watson | Zircon saturation revisited: temperature and composition effects in a variety of crustal magma types[END_REF] and [START_REF] Boehnke | Zircon saturation re-revisited[END_REF] formulations respectively; while the T Zr for the grey granitoids vary between 800°C and 760 °C.

Whole rock Sr-Nd systematic in granitoids

Whole rock Rb-Sr and Sm-Nd isotopic analyses were performed on 4 pink and 3 grey granitoids (Table 3). The methodology is described in Appendix D. The granitoids have a wide range of 87 Sr/ 86 Sr ratios (0.7156-0.7950). The 143 Nd/ 144 Nd ratios for these granitoids are tightly constrained between 0.511033 and 0.511407 (Table 3). The ƐNd(0) for these granitoids are strongly negative (-23.9 to -31.2) (Fig. 13a; Table 3). The ƐNd(t) at t=1030Ma for pre-D2 granitoids and at t=950 Ma for post-D2 granitoids range from -11.1 to -18.6 (Fig. 13b, Table 3). In the ƐNd(t) versus T 2DM plots (Fig. 13c), the GC granitoids also have negative ƐNd(t) values. The ranges of T CHUR , T DM and T 2DM estimates for the GC granitoids are 1.65-2.18 Ga, 2.05-2.53 Ga and 2.43-3.05 Ga respectively. The T DM and T 2DM are better approximations relative to CHUR for most post-Archean rocks since significant amounts of crust formed in the Archean by repeated melt extractions from the mantle [START_REF] Patchett | Radiogenic Isotope Geochemistry of Rare Earth Elements[END_REF].

The ƐNd(t) versus the 87 Sr/ 86 Sr initial ratios for the GC granitoids (Fig. 13b) also show crustal values ( 87 Sr/ 86 Sr > 0.706, ƐNd negative; [START_REF] Winter | Chemical Petrology II: Trace elements and isotopes[END_REF].

DISCUSSION

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In Table 4, the important mesoscale structural features and the gamut of age data generated in this study and in Banerjee et al. (2022a) are integrated to highlight the significant tectonic features in the Godhra-Chhota Udepur Sector.

Tectonic interleaving at 1.03-0.95 Ga

The spatial distribution (Fig. 2b) of LA-ICP-MS U-Pb zircon dates obtained in this study (Fig. 7a-i) and by Banerjee et al. (2022a) in the Godhra-Chhota Udepur sector (Fig. 9) reveal intriguing features unknown earlier. First, the Late Neoarchean Discordant upper intercept ages and the Concordant ages in the pre-D2 granitoids are restricted to the northern parts of the sector (Fig. 2b). By contrast, the Late Paleoproterozoic (1.7-1.6 Ga) age of pre-D2 high-grade metamorphism in the anatectic gneisses and the younger Late Mesoproterozoic (~1.03 Ga) pre-D2 granitoids occur exclusively in the southern part. And second, the Discordia lower intercept and the Concordant ages for the emplacement of the post-D2 granitoids (including syn-D3 granitoids) across the north-south divide are tightly constrained between 0.95 and 0.93 Ga. These ages are identical to the ones obtained from the existing Rb-Sr and Sm-Nd isochron ages [START_REF] Gopalan | Rb-Sr age of Godhra and related granites, Gujarat, India[END_REF][START_REF] Srimal | On the tectonic affinity of the Champaner Group of rocks, Eastern Gujarat[END_REF][START_REF] Shivkumar | Proterozoic rift in lower Champaners and its bearing in uranium mineralisation in Panchmahals district, Gujarat[END_REF][START_REF] Goyal | Geochemistry and Rb-Sr age of the late Proterozoic Godhra granite of central Gujarat, India[END_REF]. In view of the large variations in the emplacements ages of the granitoids, the term -Godhra granite‖ coined by [START_REF] Gopalan | Rb-Sr age of Godhra and related granites, Gujarat, India[END_REF] and adopted by later workers [START_REF] Srimal | On the tectonic affinity of the Champaner Group of rocks, Eastern Gujarat[END_REF][START_REF] Shivkumar | Proterozoic rift in lower Champaners and its bearing in uranium mineralisation in Panchmahals district, Gujarat[END_REF][START_REF] Goyal | Geochemistry and Rb-Sr age of the late Proterozoic Godhra granite of central Gujarat, India[END_REF] for the gamut of felsic intrusives in the sector is a misnomer, and needs to be discontinued. It may be recalled that several researchers [START_REF] Mamtani | Granite emplacement and its relation with regional deformation in the Aravalli Mountain Belt (India)-inferences from magnetic fabric[END_REF] based on field investigations had also suggested that the -Godhra granite‖ is a composite unit [START_REF] Banerjee | Tectonics of the Greater India Proterozoic Fold Belt, with emphasis on the nature of curvature of the belt in west-central India[END_REF](Banerjee et al., , 2022a; this study). The Late Neoarchean granitoids are unlikely to be the basement for the younger Late Paleoproterozoic gneisses, for it would be impossible for the Neoarchean granitoids to escape the pervasive 1.65-1.60 Ga metamorphism-anatexis at T ≥750 °C (accompanying article: [START_REF] Banerjee | Dynamics of Early Neoproterozoic accretion, west-central India: II Early Neoproterozoic LT-HP and Early Paleoproterozoic HT-LP metamorphism at Godhra-Chhota Udepur, and a tectonic model for accretion[END_REF]. It therefore is reasonable to assume that the 2.5-2.4 Ga granitoids are slivers of crustal domains that are tectonically interleaved with the Late Paleoproterozoic gneisses and the younger (~1.03 Ga) granitoids of the CITZ. These chronologically diverse lithodemic units experienced a shared syn to post-D2 history, and were intruded by 0.95-0.93 Ga post-D2 granitoids. We infer, therefore, that the tectonic interleaving of the lithodemic units occurred between ~0.93 Ga (age of post-D2 granitoids) and the 1.03-1.02 Ga pre-D2 granitoids in the tectonic melange.

1.03-0.93 Ga granitoids: Petrogenesis

Large volumes of S-type magmas maybe generated from melting of metasedimentary protoliths of metagreywacke, metapelitic or metatonalitic compositions [START_REF] Clemens | S-type granitic magmas-petrogenetic issues, models and evidence[END_REF]. Zhu (2020) argue that turbidite sequences in accretionary prisms comprising banded shale and greywackes undergo melting towards the end of orogenic cycles following initial continent-J o u r n a l P r e -p r o o f continent collision and accretionary prism development to generate S-type magmas. The GC granitoids show high molar CaO/MgO+FeO T (0.42-0.74) and CaO/Na 2 O (0.3-2.5) ratios (Fig. 14a,b) indicating they were mostly derived from plagioclase-rich greywackes; however, a few samples also show relatively low molar CaO/MgO+FeO T (0.15-0.32) and CaO/Na 2 O (<0.1) ratios which are interpreted to be derived from metapelitic melts [START_REF] Sylvester | Post-collisional strongly peraluminous granites[END_REF].

Two granitoids (AW 9A, AW 21) have a high molar CaO/MgO+FeO T ratio (1.62, 1.54). The post-D2 white-coloured granitoid AW 9A has the highest molar CaO/MgO+FeO T ratio (1.62) and high molar Al 2 O 3 /MgO+FeO T (12.5). The corresponding values for the other granitoid AW-21 are 1.54 and 4.18 respectively. These samples may be derived from source rocks having meta-tonalite affinity [START_REF] Sylvester | Post-collisional strongly peraluminous granites[END_REF]. The GC granitoids thus appear to be melting products of heterogeneous metasedimentary protoliths, dominated by metagreywackes.

The spread in the 87 Sr/ 86 Sr (0.71564-0.79103) and 143 Nd/ 144 Nd (0.511033 to 0.511407) ratios (Fig. 13) may also be attributed to this heterogeneity of the protolith characters [START_REF] Clemens | Chemical structure in granitic magmas-a signal from the source?[END_REF] or may have been caused by mixing with other crustal melts [START_REF] Collins | S-and I-type granites of the eastern Lachlan fold belt: products of threecomponent mixing[END_REF]. Strongly negative ƐNd (-23.9 to -31.2) values suggest the derivation of the granitoids from recycled crustal sources. The 87 Sr/ 86 Sr i ratios (0.7074-0.7217) and the negative ƐNd(t) (-11.1 to -18.6) calculated at ~1.03 Ga for pre-D2 granitoids and 0.95 Ga post-D2 granitoids (Fig. 13b) also imply that crustal protoliths were the source rocks for the granitoids, and preclude significant contributions from mantle-derived melts (Allègre and Ben Othman, 1988).

The anatectic gneisses in the GC sector plot in the field for greywacke in the lithochemical classification diagrams (Basei et al., 2011) (Fig. 14c, d); the gneisses in the GC sector are thus considered to be majorly metagreywackes. The higher MgO abundances and the lower Fe# of the gneisses relative to the granitoids (Supplementary material 3 , Table 2) suggest a restitic character for these gneisses. The mesocratic biotite ± hornblende gneisses J o u r n a l P r e -p r o o f interleaved with minor amounts of garnet-free amphibolites are the dominant basement rocks exposed in the Godhra-Chhota Udepur sector, followed by the garnetiferous biotitecordierite-sillimanite bearing melanocratic gneisses. In the granitoids, sporadic grains of mmsized garnet porphyroblasts are noted only in a couple of outcrops, and sillimanite and cordierite are lacking. Assuming the gneisses continue to the depth where the granitoids originated, the mineralogical evidence and the geochemical signatures (Fig. 10111213) suggest that the mesocratic gneisses chemically resembling metagreywacke (Fig. 14) were the likely protolith for the S-type syn-collisional granitoids. The expansive granitoids are likely to have formed by partial melting via the model congruent melting reaction quartz + plagioclase + Kfeldspar + biotite + garnet → melt (cf. Patiňo [START_REF] Patiňo Douce | Effects of P, f(O 2 ) and Mg/Fe ratio on dehydration melting of model metagreywackes[END_REF]. The melting of the metagreywacke dominated protoliths [START_REF] Vielzeuf | Melting relations in hydrous systems revisited: application to metapelites, metagreywackes and metabasalts[END_REF]) possibly occurred at 800-840 °C for the pink granitoids and 760-800 °C for the grey granitoids, inferred from zircon saturation temperature (T Zr ).

Based on the crystal-melt partition co-efficient of elements compiled by [START_REF] Rollinson | Using geochemical data: To understand geological processes[END_REF]Table 4.3 therein), the molar proportion of garnet in the model reaction should be small to account for the slight depletion of Y and HREEs in the granitoids relative to the gneisses; the enrichment of Nb, Ta, Th and U in the granitoids on the other hand precludes the involvement of Fe-Ti oxide phases (ilmenite) in the congruent melting reaction.

Given the compatible nature of Nb (4-9.5) and Ta (1.2-1.9) [START_REF] Rollinson | Using geochemical data: To understand geological processes[END_REF], the modal proportion of biotite in the melting reaction is unlikely to be high. The Nb/Ta ratio is a measure of the degree of fractionation of the granitic magmas (Nb/Ta<5 indicating fractionation; [START_REF] Ballouard | Nb-Ta fractionation in peraluminous granites: A marker of the magmatichydrothermal transition[END_REF] whereas the Zr/Hf ratio is a measure of fertility of the magma in terms of metallogenic minerals like Sn, W, Mo, Be and Ta [START_REF] Ballouard | Nb-Ta fractionation in peraluminous granites: A marker of the magmatichydrothermal transition[END_REF]; the melts producing the GC granitoids were unfractionated (Fig. 10e) and -barren‖ in terms of metallic content (Fig. 10f) [START_REF] Ballouard | Nb-Ta fractionation in peraluminous granites: A marker of the magmatichydrothermal transition[END_REF]. The SMB and CGC granitoids also J o u r n a l P r e -p r o o f show similar unfractionated and barren characteristics although the CGC granitoids originated as A-type magmas. S-type granites may exhibit geochemical characteristics similar to A-type granites [START_REF] Whalen | A-type granites: geochemical characteristics, discrimination and petrogenesis[END_REF].

According to the Th/Ta versus Yb plot (Fig. 10g), these granitoids are from oceanic arcs and active continental settings. S-type granites are common in syn to post-collisional settings [START_REF] Chappell | Two contrasting granite types: 25 years later[END_REF][START_REF] Sylvester | Post-collisional strongly peraluminous granites[END_REF]. The syn-collisional nature of the granitoids is supported by the high-T deformation microstructures (Fig. 5f,g) and the magmatic flow textures (Fig. 4e) in these granitoids hosted within D3 shears. The field relations, the microstructures and the geochemical characteristics together suggest that the granitoids originated as a part of the Neoproterozoic accretion event in a syn-collisional setting. These granitoids are typical of the global Grenvillian-age felsic magmatism during Rodinia assembly [START_REF] Chen | Ca. 1050 Ma intra-continental riftrelated A-type felsic rocks in the southwestern Yangtze Block, South China[END_REF].

~2.5 Ga granitoids: the ADFB connection

A brief summary of the lithological, structural and chronological aspects of the Aravalli-Delhi Fold Belt is presented below to understand the Early Neoproterozoic accretion tectonics between the ADFB and the CITZ. The 700 km long N/NNE-striking Aravalli Delhi Fold Belt (ADFB) comprises Proterozoic Aravalli and Delhi supracrustal successions overlying an older basement referred to be the Banded Gneissic Complex (BGC) (Heron, 1953). The Archean nucleus in central and southern ADFB is known as BGC-I [START_REF] Sharma | Cratons of the Indian Shield[END_REF]. Archean granitoid bodies as in Untala, Gingla, Jagat, Berach and Ahar River areas, dated between 2.6 Ga and 2.4 Ga (Roy and Kroner, 1996;[START_REF] Wiedenbeck | Stabilization of the Aravalli Craton of northwestern India at 2.5 Ga: an ion microprobe zircon study[END_REF][START_REF] Sivaraman | Zircon geochronology of Berach granite of Chittorgarh, Rajasthan[END_REF][START_REF] Kaur | Origin of trondhjemite and albitite at the expense of A-type granite, Aravalli orogen, India: Evidence from new metasomatic replacement fronts[END_REF] constitute a major lithologic component in BGC-I. On the other hand, BGC-II is a more reworked component mantling the northern fringes of BGC-I [START_REF] Sharma | Cratons of the Indian Shield[END_REF]. BGC-II comprising the Sandmata-Mangalwar Complex J o u r n a l P r e -p r o o f and the basement rocks underlying the Eastern Aravalli Terrane yield Late Paleoproterozoic dates, 1.8-1.75 Ga [START_REF] Buick | The Proterozoic magmatic and metamorphic history of the Banded Gneiss Complex, central Rajasthan, India: LA-ICP-MS U-Pb zircon constraints[END_REF][START_REF] Buick | Constraints on the Proterozoic evolution of the Aravalli-Delhi Orogenic belt (NW India) from monazite geochronology and mineral trace element geochemistry[END_REF][START_REF] Bhowmik | Grenvillian age high-pressure upper amphibolite-granulite metamorphism in the Aravalli-Delhi Mobile Belt, Northwestern India: New evidence from monazite chemical age and its implication[END_REF][START_REF] Kaur | Origin of trondhjemite and albitite at the expense of A-type granite, Aravalli orogen, India: Evidence from new metasomatic replacement fronts[END_REF], deemed to represent the age of high-grade metamorphism in the ADFB. The poly-deformed Aravalli and Delhi Supergroups are Proterozoic in age [START_REF] Bhowmik | Grenvillian age high-pressure upper amphibolite-granulite metamorphism in the Aravalli-Delhi Mobile Belt, Northwestern India: New evidence from monazite chemical age and its implication[END_REF][START_REF] Buick | The Proterozoic magmatic and metamorphic history of the Banded Gneiss Complex, central Rajasthan, India: LA-ICP-MS U-Pb zircon constraints[END_REF]2010;[START_REF] Souza | Mesoarchaean to Neoproterozoic (3.2-0.8 Ga) crustal growth and reworking in the Aravalli Craton, northwestern India: Insights from the Pur-Banera supracrustal belt[END_REF][START_REF] Kaur | Paleoproterozoic continental arc magmatism, and Neoproterozoic metamorphism in the Aravalli-Delhi orogenic belt, NW India: New constraints from in-situ zircon U-Pb-Hf isotope systematic, monazite dating and whole rock geochemistry[END_REF][START_REF] Mckenzie | New age constraints for the Proterozoic Aravalli-Delhi successions of India and their implications[END_REF]. Archean dates obtained from detrital zircons in these rocks [START_REF] Wang | Zircon U-Pb age and Hf isotope evidence for an Eoarchaean crustal remnant and episodic crustal reworking in response to supercontinent cycles in NW India[END_REF][START_REF] Souza | Mesoarchaean to Neoproterozoic (3.2-0.8 Ga) crustal growth and reworking in the Aravalli Craton, northwestern India: Insights from the Pur-Banera supracrustal belt[END_REF] suggest inherited components from an older basement.

The 2.5 Ga granitoids and gneisses are lacking in the CGC (Sequeira and Bhattacharya, 2021;Sequeira et al., 2020Sequeira et al., , 2021)), in the southern and central domains of the SMB [START_REF] Banerjee | Tectonics of the Greater India Proterozoic Fold Belt, with emphasis on the nature of curvature of the belt in west-central India[END_REF], and the southern part of the Godhra-Chhota Udepur sector (Fig. 7b). It appears, therefore, that the ~2.5 Ga granitoids in the northern domain of the Godhra-Chhota-Udepur sector correspond to the BGC-I ~2.5 Ga granitoids identified in several areas including Berach in the Aravalli-Delhi Fold Belt. These ~2.5 Ga foliated granitoids of the ADFB were tectonically juxtaposed with the Late Paleoproterozoic gneisses in the tectonic mélange in the GC sector (Fig. 2b). It is however unclear if the ~2.5 Ga granitoids occurred as tens-of meters to couple-of-hundreds of meters wide slivers inter-leaved with the 1.7-1.6

Ga anatectic gneisses of the CITZ or these granitoids (and gneisses) constitute tens-ofkilometre wide disparately evolved crustal segments juxtaposed with the Late Paleoproterozoic CITZ gneisses along the broken line in Fig. 2b. Nevertheless the gamut of evidence points to an accretion between the ADFB and the CITZ in the Godhra-Chhota Udepur sector. This accretion was contemporaneous with Early Neoproterozoic oblique D2-D3 crustal convergence (Banerjee et al., 2022a) and the coeval emplacement of 1.03-0.93 Ga S-type granites that originated by partial melting of sedimentary protoliths dominated by metagreywacke.

APPENDIX A. LA-ICP-MS U-Pb zircon dating

For separating zircons, the rocks were crushed, sieved and followed by panning to remove the lighter fractions. The heavier fractions were then passed through a column of bromoform to retrieve the heavy mineral fraction, and magnetic separation. The zircons were handpicked from the non-magnetic sample using a stereomicroscope. Araldite mounts were prepared for the embedded zircon grains; the mounts were polished to expose the internal structures of the grains.

The CL imaging of the zircon grains were done using the RELION CL instrument at the Plateforme GeOHeLiS, Géosciences Rennes, University of Rennes as well as with the Cameca SX-100 electron probe microanalyzer at the Department of Earth Sciences, Indian Institute of Technology Bombay, Mumbai. LA-ICP-MS U-Pb analyses of zircons were performed at the Plateforme GeOHeLiS, Géosciences Rennes, University of Rennes. A summary of instrumentation and analytical protocols are provided in Supplementary Material 4 . The analytical data for the zircon standard GJ-1 during the five analytical sessions is provided in the Supplementary Material 1 . The long-term uncertainty (1.9%) is only applied to population age and is quoted in italics between brackets in the text. All uncertainties are quoted at ± 2σ. Concordia diagrams are generated using IsoplotR [START_REF] Vermeesch | IsoplotR: a free and open toolbox for geochronology[END_REF], and the reported MSWD are for concordance and equivalence.

No common Pb correction has been applied to the data as the measurement of 204 Pb is not precise enough on a Q-ICP-MS instrument. However, the presence of common lead has been qualitatively assessed using the f206c indicator which is calculated as follow:

J o u r n a l P r e -p r o o f

B. Monazite chemical dating

Monazite dating [START_REF] Montel | Electron microprobe dating of monazite[END_REF] was carried out in the Department of Earth Sciences, Indian Institute of Technology Bombay (Powai). The protocol for monazite analyses is detailed in [START_REF] Deshmukh | Late Paleoproterozoic clockwise P-T history in the Mahakoshal Belt, Central Indian Tectonic Zone: Implications for Columbia supercontinent assembly[END_REF] and only a brief summary is presented here. U-Th-total Pb monazite dating was performed using a CAMECA SX-FIVE electron probe microanalyzer (EPMA). Monazite analyses were determined with a 15 kV accelerating voltage, 200 nA beam current and 1 µm beam diameter. Pb M a , Th M a , and U M b spectral lines were calibrated using crocoite (PbCrO 4 ), Th-glass (ThO 2 = 5 wt.%) and U-glass (UO 2 = 5 wt.%) standards, and were simultaneously measured in two LPET crystals for 240 s, 160 s, and 160 s, respectively. The peak and background intensities of Pb M a , Th M a , and U M b were acquired with a five-cycle sub-counting methodology [START_REF] Prabhakar | Resolving poly-metamorphic Paleoarchean ages by chemical dating of monazites using multi-spectrometer U, Th and Pb analyses and sub-counting methodology[END_REF][START_REF] Deshmukh | Late Paleoproterozoic clockwise P-T history in the Mahakoshal Belt, Central Indian Tectonic Zone: Implications for Columbia supercontinent assembly[END_REF]. The Pb M a counts were determined using an exponential background fit to precisely define the distinctly located background positions (cf. [START_REF] Jercinovic | Analytical perils (and progress) in electron microprobe trace element analysis applied to geochronology: back-ground acquisition, interferences, and beam irradiation effects[END_REF][START_REF] Spear | Limitations of chemical dating of monazite[END_REF]. The matrix effects (ZAF) were reduced using the X-PHI approach (Merlet, 1992). The overlapping X-ray lines of Th M2-O4, Th Mζ1, Th Mζ2, YL C2 , YL C3 , La L a on Pb M a and Th M c , Th M3-N4 on U M b were corrected using the CAMECA Peak Sight software (version 6.1). Monazite dates were verified by analysing the Steenkampskraal monazite standard (SHRIMP age: 1030 ± 6 Ma; [START_REF] Knöper | The Steenkampskraal monazite vein: a subhorizontal stretching shear zone indicating extensional collapse of Namaqualand at 1033 Ma?[END_REF] during quantification.

J o u r n a l P r e -p r o o f

Also, samples were chosen such that the abundances of the elements ThO 2 (2.96-20.65 wt%), UO 2 (0.01-1.72 wt%), PbO (0.19-0.83 wt%) and Y 2 O 3 (0.5-3.09 wt%) were high to keep errors in background measurement low; only spots with 2σ errors <6% error [100x 2σ errors/total age in Ma] (Prabhakar, 2013) were considered. Based on X-ray element maps Th, U, Pb and Y (Fig. 6) and back-scattered electron images, 58 spot in chemically distinct domains were analyzed. The mean age population were statistically resolved using Isoplot 3.0 [START_REF] Ludwig | Isoplot/Ex version 4.15, a geochronological toolkit for Microsoft Excel[END_REF]. Monazite analytical data and spot ages (±2σ errors) are presented in the Supplementary Material 2 .

C. Whole rock major and trace element geochemistry

About 3-4 kg of rocks were broken into chips and crushed to less than 8 mm diameter in a Fritsch jaw crusher. The internal parts of the jaw crusher and the plastic collector was cleaned by ethyl alcohol and air dried before and after sample insertion. Sample contamination was avoided by flushing the channel by passing crushed rock chips and emptying the collector several times before starting the final crushing stage. After several rounds of cone and quartering, the representative fractions of the crushed rocks were powdered to less than 200mesh in a puck and ring Fritsch pulveriser. For the samples, at each step, both equipments were cleaned with water and soap, air dried, and wiped clean by ethyl alcohol. The samples were analyzed at ACME Lab, Bureau Veritas, Vancouver, Canada. Sample digestion was done by lithium borate fusion method. Analysis was done by Inductively Coupled Plasma Emission Spectrometry (ICP-ES) for major elements (package code: LF300), and Inductively Coupled Plasma Mass Spectrometer (ICP-MS) (package code: LF100) for trace elements. For the packages, the detection limits are 0.01 wt% for all major elements (detection limit is 0.002 wt% for Cr 2 O 3 ). For trace elements, the detection limits are 0.01 to 0.1 ppm for REEs, 0.1-0.5 ppm for the other elements, except Ba , Be and Sn (1ppm) and V (8 ppm). The

J o u r n a l P r e -p r o o f

Journal Pre-proof analytical accuracy was controlled using the internal geological reference materials STD SO-19. The accuracy was better than ± 5%. The precision was verified by duplicated samples in each analytical set and the 2SD% (2SD/average*100) was also within ± 5%.

D. Sr and Nd isotope analysis

A set of seven granitoid samples were analysed to determine for Sr and Nd isotopic ratios at the Radiogenic Isotope Laboratory, IIT Kharagpur. The analysis was performed following protocols as in [START_REF] Mukherjee | Constraining paleoproterozoic (∼ 1.7 Ga) collisional orogenesis between the Eastern Dharwar and Bastar cratons: New Sm-Nd garnet isochron and Th-U-total Pb monazite chemical ages from the Bhopalpatnam orogen, central India[END_REF]. About ~80 mg of whole rock powders (as in Appendix C) from each of the samples and one rock standard BCR2 (Columbia River Basalt, U.S. Geological Survey) were weighed, dissolved in screw capped Teflon vials with HF+HNO3 for three days and evaporated to bone dryness, followed by aqua regia attack steps for complete digestion. These digested samples were then evaporated to dryness and dissolved in 1M HCl and 0.1M HF solution for cation separation by ion exchange chromatography. Sr from the samples was eluted with 1.5 N HCl and LREE factions were collected in 6 N HCl on Teflon columns packed with 2mL BioRad AG50W x 8, 200e400 mesh cation exchange resin. All fractions were made to ~2 mL in 0.2% HNO3 to obtain <1mV background intensity for their respective pilot masses. Determination of isotope compositions was carried out in static mode on a Thermo Fisher Neptune Plus MC-ICPMS. [START_REF] Tanaka | JNdi-1: a neodymium isotopic reference in consistency with LaJolla neodymium[END_REF] for Nd isotopes. The precision and accuracy of the data is checked on the reference material BCR-2 which was run along with the samples; values of 87 Sr/ 86 Sr = J o u r n a l P r e -p r o o f 0.70475±0.00006 (2σ) and 143 Nd/ 144 Nd = 0.512795±0.000030 (2σ) were obtained which is well within the accepted limits. For all calculations, 147 Sm-143 Nd decay constant (λ = 6.54 × 10 -12 year -1 ) is used after [START_REF] Lugmair | Lunar initial 143 Nd/ 144 Nd: differential evolution of the lunar crust and mantle[END_REF]. The εNd(T) and Nd model ages (T DM ) were calculated using 143 Nd/ 144 Nd = 0.512630, 147 Sm/ 144 Nd = 0.1960 of CHUR [START_REF] Bouvier | The Lu-Hf and Sm-Nd isotopic composition of CHUR: constraints from unequilibrated chondrites and implications for the bulk composition of terrestrial planets[END_REF] and for depleted mantle 143 Nd/ 144 Nd = 0.513151 and 147 Sm/ 144 Nd = 0.2136 [START_REF] Goldstein | Nd and Sr isotopic systematics of river water suspended material: implications for crustal evolution[END_REF], respectively. The value for 87 Rb-86 Sr decay constant (λ = 1.42 × 10 -11 year -1 ) is used after [START_REF] Steiger | Subcommission on geochronology: convention on the use of decay constants in geo-and cosmochronology[END_REF]. 2016). Data for granitoids in CGC (Sequeira et al., 2021;[START_REF] Mukherjee | Geochemistry, U-Pb geochronology and Lu-Hf isotope systematics of a suite of ferroan (A-type) J o u r n a l P r e -p r o o f Journal Pre-proof granitoids from the CGGC: Evidence for Mesoproterozoic crustal extension in the east Indian shield[END_REF] and SMB [START_REF] Chattopadhyay | Syn-and post-tectonic granite plutonism in the Sausar Fold Belt, central India: age constraints and tectonic implications[END_REF][START_REF] Chattopadhyay | Neoproterozoic transpression and granite magmatism in the Gavilgarh-Tan Shear Zone, central India: Tectonic significance of U-Pb zircon and U-Th-total Pb monazite ages[END_REF] are added for comparison (e-g). (g) Th/Ta versus Yb after [START_REF] Gorton | From continents to island arcs: a geochemical index of tectonic setting for arc-related and within-plate felsic to intermediate volcanic rocks[END_REF]. McDonough and Sun, 1995) bulk crust composition [START_REF] Rudnick | Composition of the continental crust[END_REF] is plotted for comparison.

Figure Captions

Figure 12: Bulk crust normalized [START_REF] Rudnick | Composition of the continental crust[END_REF] trace element patterns for (a) pink granitoids, (b) grey granitoids and (c) gneisses from the GC sector. An average gneiss composition calculated for the GC gneisses is shown with the bold blue line in (c).

The GC average gneiss normalized trace element patterns for (d) pink granitoids and (e) grey granitoids. 2.

Table Captions

Table 1: Summary of lithology and mineral assemblage, morphology/texture of (a) zircon and (b) monazite, composition and dates in the 13 samples used for geochronology. Zircon grains are prismatic to square shaped; some prismatic grains are fragmented (Fig. 6c). Width (60-80 µm) and length (100-300 µm). CL images exhibit core-rim textures; the zircon cores mostly have a CL dark response, faint traces of oscillatory zoning is preserved in some of these cores.

Granitoids

Syn-D3 pink blastoporphyritic granitoid; Kfs+Pl+Qz+Bt; Sph, Zrn and Opq grains occur as accessory minerals.

Zircon grains are prismatic: width (60-100 µm), length (100-150 µm). In CL (Fig. 6d) the grains display well-defined oscillatory zoning; some of the grains have xenocrystic cores surrounded by new magmatic overgrowths.

15 grains/30 spots 0. J o u r n a l P r e -p r o o f

W - 5 A W - 1 8 A W - 2 1 A W - 9 8 A W - 1 0 A W - 1 2 7 A W - 1 4 5 A W - 1 5 5 A W - 8 A W - 7 3 A W - 1 4 A W - 1 5 A W - 1 6 A W - 3 8 A W - 6 3 A W - 1 1 A A W - 7 7 A A W - 9 A A W - 7 A W - 1 1 B A W - 2 2 A W - 1 6

  Pb/ 206 Pb dates are shown in Fig. 6. Throughout the text, figures and tables, the uncertainties are shown at 2 level. The concordia plots are shown in Fig. 7. Representative monazite X-ray elemental images with embedded spot dates in Ma, BSE images depicting textural setting of the monazite grains and probability-density plots showing mean populations dates (in Ma) are shown in Fig. 8. Fig. 2b provides the spatial distribution of the zircon dates obtained in this study and those in the two samples analyzed by Banerjee et al. (2022a).

  Pb/ 206 Pb ages in zircons are shown in Fig. 6a. CL images of the zircons show oscillatory zoning (alternating light and dark bands surrounding a core), patchy zoning (localized clusters of bright domains in a homogenous dark grain), overgrowths truncating earlier zoning or completely recrystallized textures (dark CL response, no texture) (Fig. 6b-i). Age spots were analyzed in each of these domains. The U-Pb analysis and the age data obtained from the individual samples are provided in Supplementary Material 1 and a brief description of each sample is provided in Table 1a and discussed below. All uncertainties are quoted at 2 level; see Appendix for details about propagation of uncertainties. 3.1.1 Gneisses: Sample AW 161 is a quartzofeldspathic gneiss. The prominent mineral segregation banding in the rock bears one set of prominent D3 tight to open folds with steep dipping E-W striking axial planes and moderate plunge to the WNW. Pre-D3 folds are rare, but metatexite layers are lacking. A total of 35 spots were analyzed in 23 zircon grains. The zircon grains do not

  in various discrimination plots in Fig. 10. Chondrite normalized REE diagrams and bulk continental crust normalized trace element spider diagrams for the granitoid and gneiss samples are presented in Figs. 11 and 12 respectively.

  The pre-D2 Neoarchean granitoids with single shallow-dipping tectonic foliation do not exhibit the multiple folds and imprints of the younger Late Paleoproterozoic high-grade metamorphism and anatexis typical of the basement gneisses in the different crustal domains J o u r n a l P r e -p r o o f of the CITZ that extends eastwards from the Godhra-Chhota Udepur sector into the central and southern domains of the Satpura Mobile Belt (SMB) in central India, and the Chottanagpur Gneiss Complex (CGC) further to the east (Banerjee et al., 2021). Also the Late Paleoproterozoic basement gneisses in the Godhra-Chhota Udepur sector do not provide evidence of Neoarchean or older inheritance in the analyzed zircon grains. Yet zircon U-Pb systematics show that both the Neoarchean granitoids and the Late Paleoproterozoic gneisses bear Early Neoproterozoic imprints either as lower intercept Discordia and/or concordant dates, identical to the emplacement ages (0.95-0.93 Ga) of the post-D2 and syn-D3 granitoids (Figs. 7-9).

  J o u r n a l P r e -p r o o f6. CONCLUSIONSThe gamut of evidence from field studies, LA-ICP-MS U-Pb (zircon) geochronology, chemical monazite dating and granite geochemistry indicates that the Archean (2.5-2.4 Ga) lithodemic units of the N/NNE-striking Aravalli-Delhi Fold Belt and the Late Paleoproterozoic (1.65-1.60 Ga) high-grade anatectic gneisses of the E-striking Central Indian Tectonic Zone were juxtaposed during oblique crustal accretion between the two terranes. The N-S crustal accretion involving top-to-the-south thrusting (D2 deformation) and nucleation of transpressional steep-dipping shear zones (D3 deformation) occurred between 1.03 and 0.93 Ga. Mesoscale structures (Figs.2, 3 and 4) and deformation microstructures (Fig.5) indicate that the D3 contractional deformation was broadly contemporaneous with the expansive emplacement of S-type syn-collisional granites formed by the partial melting of basement rocks dominated by metagreywacke, but the deformation outlasted the emplacement of the granitoids. handling of the manuscript and Editorial corrections by Greg Shellnutt are greatly appreciated.

Figure 1 :

 1 Figure 1: Generalized geological map of the northern part of India (see inset) showing the

Figure 2 :

 2 Figure 2: (a) Simplified lithological map of the Godhra-Chhota Udepur sector -compiled

Figure 3 :

 3 Figure 3: (a) A 3-D block diagram depicting the litho-structural elements in the GC sector.

Figure 4 :

 4 Figure 4: Field photographs showing mesoscale textures and structures of granitoids in the

Figure 5 :

 5 Figure 5: Crossed polars photomicrographs of deformation microstructures in the pre-D2

Figure 6 :

 6 Figure 6: (a) Th/U versus 207 Pb/ 206 Pb age (in Ma) plot for analyzed zircon spots in granitoids

Figure 7 :

 7 Figure 7: U-Pb Concordia and Discordia plots for gneisses (a-b) and granitoids (c-i). In the

Figure 8 :

 8 Figure 8: Y and Th zoning maps and embedded spot dates (±2σ) in Ma of representative

Figure 10 :

 10 Figure 10: Geochemical plots and discrimination diagrams for the granitoids in the GC sector

Figure 11 :

 11 Figure 11: Chondrite normalized REE patterns for (a) pink granitoids (b) grey granitoids and

Figure 13 :

 13 Figure13: Plots (data in Table3) for GC sector granitoids. (a) ϵ Ndt=0 versus 87 Sr/ 86 Sr t=0 for all

Figure 14 :

 14 Figure 14: (a) Molar (Al 2 O 3 /MgO + FeO T ) versus molar (CaO/MgO + FeO T ) plot

Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7A Figure 7B Figure 8 Figure 9 Figure 10 Figure 11 Figure 12 Figure 13

 1234567A7B8910111213 Figure 1

Figure 14

 14 Figure14

Journal Pre-proof f206c

  = ( 207 Pb/ 206 Pb m -207 Pb/ 206 Pb*)/( 207 Pb/ 206 Pb c -207 Pb/ 206 Pb*)x100 where 207 Pb/ 206 Pbm is the measured ratio, 207 Pb/ 206 Pb* is the radiogenic expected ratio given a defined age ( 206 Pb/ 238 U age if it is < 1000 Ma, 207 Pb/ 206 Pb age if not) and 207 Pb/ 206 Pbc is the common Pb ratio based on the Stacey and Kramers (1975) Pb evolution model. As this factor relies on assumptions made on the age and on the Pb model it is only indicative, however we are confident that the data used for date calculation do not show high level of common Pb.

  Typical operating parameters during isotope measurement are given in the table:For Sr measurements, the isobaric interferences of Kr on 84 Sr and 86 Sr, and of Rb on 87 Sr were corrected using 83 Kr and85 Rb, respectively; for correction of interfering 144 Sm on 144 Nd, both 147 Sm and 149 Sm were measured and 144 Nd corrected using an exponential law. Finally

		Journal Pre-proof
	Cool gas flow	16 L min -1
	Interface
	Sample cone	Nickel
	Skimmer cone	Nickel
	Data acquisitions conditions
	Wash (OPZ) meas. time	16 min (4-7 blocks of 10 cycles each)
	Sampling meas. mode Integration time Idle time the blank On Peak Zero (OPZ) voltage intensities were subtracted from the sample intensities 20 min (6-10 blocks of 10 cycles each) 4.194 s cycle -1 3 s following the protocol of Thirlwall and Anczkiewicz (2004) for intensity correction. The isotope analysis per sample consisted of a single sequence measuring 8 blocks, with each block consisting of 10 cycles having an integration time of 4.194 s per cycle/sequence. The J o u r n a l P r e -p r o o f blank OPZ analyses consisted of 4 blocks, with 10 cycles per block. For IC measurements in
	MC-ICP conditions samples, in-run mass bias was calculated from individual measurements using normalization
	RF forward power to 88 Sr/ 86 Sr ratio = 8.37521 and 146 Nd/ 144 Nd = 0.7219 by exponential mass fractionation 1200 W
	correction. The mass fractionation correction factors were calculated from the sample-
	Torch	Quartz torch
	standard bracketing method using 20210226 Sr standard for Sr and JNdi 20210302 standard
	Sample gas flow	1.01 Lmin -1
	Auxiliary gas flow	0.8 L min -1

Table 1a : Summary of lithology and mineral assemblage, zircon morphology, Th/U ratio in zircon, and concordant and discordant dates. Isotope ratios and spotwise dates in zircons are in Supplementary Material 1 .

 1a

				Journal Pre-proof
							Concordan
							t date: 909
							± 11 (±36)
							Ma
				Zircon grains are long			(MSWD:
				prismatic, width			0.51);
			Quartzofeldspathic gneiss.	(80-100 µm), length			Discordia
			D1 fabric defined by	(200-300 µm). The CL			dates:
	AW		alternate layers of Hbl-Bt-	images exhibit core-rim	23 grains/ 35	0.04-	Upper
	161		Ms and Pl+Kfs-Qz; Rt, Opq	textures; cores exhibit	spots	1.60	intercept
			and Zrn are accessory	oscillatory or convolute			2485 ± 15
			phases.	zoning; rims appear to			(±96) Ma,
				be recrystallized			Lower
				overgrowths (Fig. 6b).			intercept
							932 ± 15
							(±39) Ma
							(MSWD:
	AW 114	Gneiss	Anatectic gneiss with alternate Hbl+Bt and Pl+Qz+Kfs layers; Rut, Zrn and Ilm are accessory J o u r n a l P r e -p r o o f phases.		1)
	Sam ple No.		Rock type and mineral assemblage	Zircon morphology	Number of analyzed grains and spots	Th/U ratios	Concordan t and discordant dates (Ma)
							(±2σ)

Table 1b : Brief summary of lithology, mineral assemblage and summary of monazite textures, composition and chemical dates. Spot wise chemical composition, age, and 2σ errors (in Ma) of monazites are provided in Supplementary Material 2 .

 1b

					(0.50-2.48)
					Zoning is
					patchy-
	AW 7		Coarse grained quartzofeldspathic gneiss (Kfs-Pl-Qz-Ms-Bt); Cpx occurs as an accessory phase with Hbl, Chl and Mnz.	Long and short prismatic grains of 60-100 µm (long axes); occur associated with the Bt grain aggregates	nebulous. ThO 2 (6.06-9.70 wt%), UO 2 (0.14-1.69 wt%), PbO (0.23-	5 grains/ 14 spots	876 ± 26 to 1020 ± 32 Ma; 911 ± 22 (MSWD: 7.1)
					0.62), Y 2 O 3
					(1.11-2.62)
	AW 163 AW 12	Granitoids	Post D2 granitoid with fine grained mosaic of Bt-Ms-Hb-Qz-Pl-Kfs-Grt. Zrn-Rt-Mnz-Opq occur as accessory phases. Post-D2 blastoporphyritic granitoid comprising Bt-Ms-Kfs-Qz-Pl assemblage. Mnz is an accessory phase. J o u r n a l P r e -p r o o f Short prismatic grains with long axis >50 µm; associated with foliated Bt, and also in the recrystallized quartz-feldspar mosaic. Zoning is patchy-nebulous; rarely concentric. ThO 2 (2.96-10.64 wt%), UO 2 (0.24-1.25 wt%), PbO (0.21-0.47), Y 2 O 3 (1.69-3.09) Sub-rounded to elliptical grains (long axis 100-150 µm) occur within aggregates/individual Bt grains; monazite alignment Zoning is patchy-nebulous. ThO 2 (4.48-14.07 wt%), UO 2 (0.15-1.02 wt%), 0.83), Y 2 O 3 (0.88-2.56) exhibits no preferred PbO (0.19-	5 grains/ 12 spots 5 grains/ 21 spots	872 ± 47 to 959 ± 27 Ma; 908 ± 19 (MSWD: 2.7) 863 ± 50 to 969 ± 47 Ma; 926 ± 11 (MSWD: 3.3)
	Sam ple No.		Rock type and mineral assemblage	Textural setting of monazites	Zoning pattern and chemical variations in monazites	No. of analyze d grains and spots	Range of spot dates (±2σ) and mean dates (±2σ) in Ma
					Zoning is
	AW 9B	Gneiss	Basement anatectic gneiss comprising coarse-grained mosaic of Kfs-Qz-Pl-Bt-Hbl; calcite veins occur in the rock at places. Mnz is accessory mineral	Rounded to short prismatic grains of 60-80 µm (long axes)occur associated with Bt	patchy-nebulous. ThO 2 (5.37-12.64 wt%), UO 2 (0.01-0.65 wt%), PbO (0.25-	3 grains/ 11 spots	878 ± 28 to 940 ±38 Ma; 923 ± 13 (MSWD:1 .8)
					0.59), Y 2 O 3

Mineral abbreviations: Biotite (Bt), chlorite (Chl), garnet (Grt), hornblende (Hb), ilmenite (Ilm), K- feldspar (Kfs), monazite (Mnz), muscovite (Ms), opaque phase (Opq); plagioclase (Pl), quartz (Qtz); rutile (Rt), zircon (Zrn).

Table 2 :

 2 Major and trace element compositions of granitoids and gneisses in the GC sector.

				Pink Granitoids	Grey Granitoids	Gneiss
		pre-		pre-
		D2	post-D2	D2	post-D2
	S e pl m a	1 -W A	A

=Eu N /√(Sm N *Gd N ) WH88: Watson and Harrison, 1988; B13: Boehnke et al., 2013

											Journal Pre-proof
		.	.	.	6 .	. .	2 8 1 8	. .	. 7 5 1 7 4 2 . . . . 7		1 5 3	. 0		4 6 0	8
		8	0	6		5	7 5				8 6	7	0	2	0	3					3
	P r T h	2 3 . 5 3 5 . 1	3 2 . 9 3 8 . 1	2 0 . 4 3 8 . 3	5 . 1 1 4 . 1	1 9 . 7 6 2 . 0	1 5 . 4 3 2 . 7	3 5. 3 4 9. 0	1 2. 4 2 4. 4	4 9. 3 7 1. 3	2 0 . 5 6 3 . 4	1 4 . 4 3 4 . 6	2 0 . 2 1 9 . 3	1 4 . 4 3 7 . 9	1 6 . 0 4 6 . 1	1 2 . 5 2 9 . 1	3 . 8 1 2 . 3	7. 2 1 9. 9	1 1. 8 4 4. 5	5 . 7 2 9 . 2	1 1 . 2 3 9 . 7	9. 8 2 6. 0	5 . 1 8 . 6	2 1. 2 1 2. 4	1 3. 1 2 6. 4
	N d U	8 5 . 3 6 . 8 0	1 0 4 . 5 3 . 2 0	6 8 . 6 4 . 8 0	1 8 . 1 1 . 9 0	6 4 . 0 6 . 1 0	5 2 . 5 2 . 7 0	1 1 0. 0 2. 6 0	4 3. 3 4. 8 0	1 6 2. 1 2. 6 0	6 4 . 1 5 . 7 0	4 6 . 0 4 . 2 0	7 0 . 7 2 . 1 0	5 0 . 1 4 . 3 0	5 2 . 6 4 . 1 0	4 2 . 3 4 . 4 0	1 2 . 8 1 . 3 0	2 3. 7 2. 6 0	3 9. 6 6. 2 0	1 8 . 8 1 0 . 7 0	3 9 . 1 6 . 0 0	3 4. 0 5. 5 0	1 8 . 6 2 . 7 0	7 5. 8 1. 1 0	4 6. 5 3. 5 0
	S m Σ R E E	1 4 . 5 6 4 2 7 . 5	1 3 . 9 6 6 8 7 . 6	1 0 . 1 1 4 1 8 . 4	2 . 8 3 1 0 8 . 3	1 0 . 0 9 4 1 5 . 3	9 . 5 5 3 3 5 . 1	1 3. 7 5 7 5 5. 2	6. 5 8 2 5 3. 1	2 1. 5 9 1 0 0 8. 4	8 . 7 1 4 2 4 . 0	7 . 0 3 3 0 0 . 5	1 0 . 8 2 4 1 5 . 3	7 . 4 7 2 9 2 . 8	8 . 2 4 3 1 8 . 0	6 . 0 0 2 5 9 . 9	1 . 9 5 8 3 . 7	4. 1 0 1 5 1. 8	6. 2 7 2 5 6. 8	2 . 9 0 1 2 2 . 6	7 . 1 5 2 4 1 . 9	6. 2 9 2 0 9. 9	3 . 1 2 1 0 7 . 9	1 2. 0 1 4 0 4. 3	8. 5 3 2 7 1. 4
	J o u r n a l P r e -p r o o f 0 . 7 7 0 . 8 7 2. 2 9 0. 7 1 4. 4 9 0 . 8 8 0 . 7 3 2 . 1 2 1 . 3 3 0 . 8 9 1 . 2 3 0 . 5 4 0. 6 1 0. 6 4 7 . 0 1 9 . 3 8 8. 5 6 4. 6 1 1 2. 6 3 5 . 2 0 4 . 9 9 8 . 4 4 5 . 3 5 4 . 9 3 4 . 2 0 1 . 3 8 3. 1 8 5. 0 4 0 . 9 4 1 . 5 7 1. 0 7 0. 5 8 1. 4 5 0 . 5 4 0 . 6 4 1 . 1 2 0 . 7 1 0 . 5 8 0 . 5 5 0 . 1 9 0. 4 3 0. 7 5 4 . 7 3 9 . 3 6 5. 1 9 2. 6 7 6. 6 9 2 . 3 1 3 . 2 5 5 . 9 0 3 . 6 3 2 . 6 9 3 . 0 9 0 . 9 9 2. 4 9 4. 4 1 0 . 7 8 1 . 8 9 0. 9 1 0. 4 6 1. 1 2 0 . 3 5 0 . 5 4 1 . 1 1 0 . 6 9 0 . 4 4 0 . 5 8 0 . 1 9 0. 4 8 0. 9 3 1 . 9 5 5 . 0 2 2. 5 6 1. 1 7 2. 6 7 0 . 9 4 1 . 4 0 3 . 0 6 1 . 8 7 1 . 2 2 1 . 7 3 0 . 5 8 1. 3 4 2. 6 9 0 . 2 6 0 . 6 7 0. 3 6 0. 1 7 0. 3 9 0 . 1 3 0 . 1 7 0 . 4 2 0 . 2 6 0 . 1 7 0 . 2 5 0 . 0 7 0. 1 9 0. 3 9 1 . 5 7 4 . 0 3 2. 3 4 1. 3 4 2. 3 9 0 . 9 0 1 . 0 6 2 . 7 9 1 . 7 0 1 . 1 4 1 . 6 6 0 . 5 5 1. 4 2 2. 6 4 0 . 2 8 0 . 2 8 0 . 6 4 0 . 3 9 0 . 8 3 0 . 4 0 0 . 3 8 0 . 6 8 0 . 6 4 0 . 4 3 0 . 7 5 1 . 0 0 0. 5 1 0. 3 5 8 2 4 8 3 6 8 5 9 9 0 0 8 5 4 8 2 7 8 1 7 8 7 9 8 1 8 8 0 7 8 0 6 7 4 1 7 7 5 7 9 1 7 8 7 7 9 8 8 2 3 8 7 8 7 9 0 7 8 8 7 7 5 8 3 9 7 7 7 7 6 4 7 5 8 6 9 3 7 2 9 7 4 6 bdl: below detection limit E u 0 . 3 4 1 . 5 7 1 . 4 3 0 . 6 5 G d 1 2 . 8 2 8 . 8 6 7 . 1 8 2 . 0 1 T b 1 . 9 0 1 . 1 0 0 . 9 6 0 . 2 9 D y 1 1 . 0 6 5 . 3 4 5 . 1 1 1 . 6 0 H o 2 . 2 3 0 . 9 2 0 . 9 3 0 . 3 2 E r 6 . 2 7 2 . 2 0 2 . 6 4 0 . 9 3 T m 0 . 9 4 0 . 3 1 0 . 4 0 0 . 1 4 Y b 6 . 1 4 2 . 0 3 2 . 4 8 0 . 9 9 E u/ E u * 0 . 0 8 0 . 4 3 0 . 5 1 0 . 8 3 T Zr W H 8 8 8 4 6 8 7 2 8 3 1 7 4 1 T Zr B 1 3 8 1 9 8 3 6 7 8 6 6 8 5 A/CNK=molar AL2O3/CaO+Na2O+K2O Fe#=molar FeO/FeO+MgO J o u r n a l P r e -p r o o f Eu/Eu*	0 . 6 6 2 . 2 3 0 . 3 3 1 . 7 5 0 . 3 7 0 . 9 5 0 . 1 4 1 . 0 8 0 . 7 9 7 6 5 7 1 7	1 . 3 7 6 . 3 6 0 . 9 6 5 . 7 5 1 . 1 3 3 . 2 5 0 . 4 5 3 . 0 6 0 . 6 2	1. 2 4 5. 3 7 0. 7 6 4. 3 9 0. 8 6 2. 4 8 0. 3 3 2. 1 3 0. 6 5	1 . 0 9 2 . 7 0 0 . 3 4 1 . 9 6 0 . 3 7 1 . 0 2 0 . 1 5 1 . 9 0 1 . 1 4	2. 2 1 8. 3 9 0. 9 8 4. 8 7 0. 8 5 2. 2 5 0. 3 1 1 2. 0 0 . 6 7	1. 5 7 7. 3 5 1. 0 2 5. 6 0 0. 9 4 2. 4 1 0. 2 7 3 1. 6 0. 6 0
	L u	0 . 9 0	0 . 3 2	0 . 3 7	0 . 1 6	0 . 2 3	0 . 5 7	0. 3 4	0. 2 4	0. 3 5	0 . 1 3	0 . 1 5	0 . 4 3	0 . 2 6	0 . 1 7	0 . 2 2	0 . 0 8	0. 2 2	0. 3 8	0 . 1 5	0 . 4 4	0. 3 4	0 . 1 9	0. 2 9	0. 2 4
	H f	7 . 2 0	1 0 . 2 0	7 . 7 0	2 . 7 0	6 . 6 0	7 . 8 0	9. 2 0	1 2. 9 0	1 6. 6 0	7 . 2 0	6 . 4 0	1 4 7 2 1 2 . 3 0	9 8 8 6 . 0 0	6 4 0 5 . 9 0	1 4 8 5 6 . 2 0	1 2 5 9 2 . 1 0	7 2 4 4. 1 0	5 0 8 4. 9 0	5 5 8 3 . 3 0	2 4 8 1 0 . 2 0	1 2 4 0 1 0. 3 0	4 6 8 1 1 . 0 4	1 1 0 8 7. 8 0	4 3 4 5. 1 0
	L a T a	1 0 0 . 8 1 . 8 0 5	1 8 4 . 6 1 . 1 0 7	1 1 0 . 2 1 . 7 0 8	2 7 . 6 0 . 6 0 6	9 7 . 8 1 . 8 0 5	7 9 . 6 1 . 2 0 1	2 1 2. 3 1. 1 0 6	6 3. 1 0. 6 0 1	2 7 7. 1 1. 0 0 3	1 1 7 . 5 0 . 8 0 1	7 5 . 5 2 . 4 0 9	1 0 1 . 1 1 . 5 0 6	7 2 . 8 1 . 1 0 6	7 9 . 0 1 . 9 0 9	6 7 . 2 1 . 4 0 7	2 2 . 9 0 . 5 0 7	3 9. 7 1. 7 0 8	6 4. 1 2. 7 0 8	3 3 . 1 0 . 6 0 9	5 5 . 4 1 . 5 0 5	4 8. 5 1. 0 0 6	2 5 . 0 . 9 0 8 8	9 3. 6 0. 6 0 4	6 4. 4 1. 2 0 9
	C W e	1 6 5 2 0 .	3 2 1 1 9 .	1 8 4 2 7 .	4 7 4 7 . .	2 0 2 7 5 .	1 4 0 6 4 3	3 6 6 9. 0. 5	1 1 2 1 5. 0.	4 6 4 6. 6. 3	2 0 1 2 1 5	1 4 7 1 4 .	1 8 5 8 7 .	1 3 7 4 2 .	1 5 1 6 0 .	1 1 3 9 8 .	3 7 2 3 . .	6 6. 0 3. 8 5	1 1 1 4. 7. 3	5 4 2 9 . .	1 0 9 3 6 .	9 3. 9 4. 4 9	4 6 3 8 . .	1 7 9 2. 9. 6	1 1 2 4. 7. 6

Table 3 :

 3 Whole rock Sr and Nd isotopic data for granitoid samples from the GC sector. Nd/ 144 Nd=0.512630, 147 Sm/ 144 Nd=0.1960 of CHUR[START_REF] Bouvier | The Lu-Hf and Sm-Nd isotopic composition of CHUR: constraints from unequilibrated chondrites and implications for the bulk composition of terrestrial planets[END_REF] 143 Nd/ 144 Nd=0.513151, 147 Sm/ 144 Nd=0.2136 of Depleted Mantle (DM)[START_REF] Goldstein | Nd and Sr isotopic systematics of river water suspended material: implications for crustal evolution[END_REF] ʎ 147 Sm= 6.54*10 -12 yr -1[START_REF] Lugmair | Lunar initial 143 Nd/ 144 Nd: differential evolution of the lunar crust and mantle[END_REF] ʎ 87 Rb= 1.42*10 -11 yr -1[START_REF] Steiger | Subcommission on geochronology: convention on the use of decay constants in geo-and cosmochronology[END_REF])Abbreviations: CHUR=Chondrite Uniform Reservoir, DM= Depleted Mantle

	Sa mpl e A W 5 A W	Granite type Pink Grani te pre D2 Pink Grani pos t	87Sr /86S r 0.73 22 0.71 J o u r n a l P r e -p r o o f Sm (pp m) Nd (pp m) 147S m/144 Nd 143N d/144 Nd T DM T 2D M T CH UR 13.9 6 104. 5 0.0841 0.511 407 2.05 E+0 9 2.43 E+0 9 1.65 E+0 9 0.511 2.42 E+0 2.75 E+0 2.03 E+0	f(S m/N d) -0.6	εN d (0) -23. 9 -25.	εN d( T) -11. 1 -13.	Time T (Ma) 1030
	21	te	D2	56	2.83 18.1 0.0985	318	9	9	9	-0.5	6	7	950
	A	Pink	pos					2.30	2.89	1.96		-	-
	W	Grani	t	0.72	13.7		0.511	E+0	E+0	E+0		29.	15.
	127	te	D2	31	5	110 0.0787	110	9	9	9	-0.6	7	4	950
	A	Pink	pos					2.36	2.72	1.97		-	-
	W	Grani	t	0.75			0.511	E+0	E+0	E+0		25.	13.
	145	te	D2	62	6.58 43.3 0.0957	318	9	9	9	-0.5	6	4	950
	A	Grey						2.51	3.05	2.18		-	-
	W	Grani	pre	0.78			0.511	E+0	E+0	E+0		31.	18.
	8	te	D2	89	8.71 64.1 0.0856	033	9	9	9	-0.6	2	6	1030
	A	Grey	pos					2.53	2.89	2.16		-	-
	W	Grani	t	0.79			0.511	E+0	E+0	E+0		27.	15.
	16	te	D2	10	8.24 52.6 0.0987	235	9	9	9	-0.5	2	4	950
	A	Grey	pos					2.28	2.72	1.91		-	-
	W	Grani	t	0.71			0.511	E+0	E+0	E+0		26.	13.
	38	te	D2	85	6.00 42.3 0.0893	281	9	9	9	-0.5	3	3	950

143

Table 4 :

 4 Summary of pre-D2, D2 and D3 deformation features, age and tectonic significances in the three lithodemic units, e.g. the basement gneisses, the supracrustal unit, and pre-and post-D2 granitoids.

	Deformatio	Basement	Granitoids Supracrustal	Tectonic	U-Pb
	n events	gneiss	Unit	significanc	zircon and
		(autochthonous	(allochthonous	e	monazite
		)	)		ages

ACKNOWLEDGEMENTS

This work constitutes a part of the Doctoral dissertation of Anwesa Banerjee; the author acknowledges the financial support provided by the host Institute for her fellowship. The authors thank Ravikant Vadlamani (IIT Kharagpur) for helping with the whole rock Sm-Nd and Rb-Sr analyses, and his inputs in interpreting the data. N. Prabhakar (Department of Earth Sciences, IIT Bombay, India) kindly helped with X-ray element mapping and chemical dating of monazites. We acknowledge Debarun Dutta for his help in organising the fieldwork session at a difficult time during the pandemic. NS acknowledges the School of Earth, Ocean and Atmospheric Sciences, Goa University for permitting the collaborative work. The authors acknowledge the insightful comments of two anonymous journal reviewers; their comments went a long way in improving the clarity and presentation of the manuscript. The Editorial J o u r n a l P r e -p r o o f

Supplementary Materials

Supplementary Material 1 : U-Pb zircon analytical data for gneisses (AW161, AW 114) and granitoids (AW 18, AW 145, AW 127, AW 98, AW 9A, AW 73, AW 8) from the Godhra-Chhota Udepur sector. Lines in bold and italics are discordant analyses, lines in bold are concordant analyses. Analytical data for quality control material GJ-1 is also provided. Supplementary Material 2 : Electron probe microanalytical data of monazites, spot ages with 2σ errors in Ma, and error % computed following [START_REF] Prabhakar | Resolving poly-metamorphic Paleoarchean ages by chemical dating of monazites using multi-spectrometer U, Th and Pb analyses and sub-counting methodology[END_REF].