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RESEARCH ARTICLE
Metamorphic evolution of the pelitic and mafic granulites from
Daltonganj, Chhotanagpur Granite Gneiss Complex, India:
Constraints from zircon U–Pb age and phase equilibria
modelling
Ravi Ranjan Kumar
1
| Kenta Kawaguchi
2,3
| Shyam Bihari Dwivedi
1
|
Kaushik Das
2,4
1
Department of Civil Engineering, Indian
Institute of Technology (BHU), Varanasi, India
2
Department of Earth and Planetary Systems
Science, Hiroshima University,
Higashihiroshima, Japan
3
Department of Earth and Environmental
Sciences, Jeonbuk National University, Jeonju,
Republic of Korea
4
Hiroshima Institute of Plate Convergence
Region Research, Hiroshima, Japan
Correspondence
Shyam Bihari Dwivedi, Department of Civil
Engineering, Indian Institute of Technology
(BHU), Varanasi 221005, India.
Email: sbd.civ@iitbhu.ac.in
Handling Editor: M. Santosh
The Daltonganj region is located on the northwestern extension of the Chhotanagpur
Granite Gneiss Complex in the eastern Indian Peninsula, which is characterized by
pelitic and mafic assemblages of granulite facies rock. The pelitic granulites contain
garnet, cordierite, biotite, plagioclase, K-feldspar, sillimanite, and quartz. Petrographi-
cal interpretations divulge prograde and retrograde metamorphic events within mafic
granulites, which consist of clinopyroxene, orthopyroxene, amphibole, plagioclase,
biotite, and quartz. Field observation, petrography, phase equilibrium modelling, and
U–Pb zircon geochronology of the pelitic granulites reveal two stages of metamor-
phic events along the clockwise P–Tpath. Laser Ablation Inductively Coupled Plasma
Mass Spectrometry (LA-ICP-MS) zircon U–Pb age dating of pelitic granulites shows
the detrital zircon ages from ~1,734 Ma to 1,677 Ma, and the possible metamorphic
domains show the weighted mean age of 1,638 ± 22 Ma, which represents the
timing of metamorphism. Subsequently, the magmatic emplacement of mafic granu-
lites was recorded at 1,629 ± 6 Ma age by Laser Ablation Inductively Coupled Plasma
Mass Spectrometry (LA-ICP-MS) zircon U–Pb dating which coincide with the timing
of metamorphism of the pelitic granulite. Phase equilibrium modelling in the
NCKFMASHTO system divulges the pre-peak metamorphic stage at ~3.2 kbar and
~620C and the first stage which is characterized by a peak metamorphic condition
that ranges from 7.40 to 9.10 kbar and from 815 to 835C during ~1,638 Ma with
the mineral assemblage of garnet +sillimanite +biotite +plagioclase +K-feldspar +
melt +quartz +ilmenite. Sequentially, the retrograde metamorphism is observed by
a nearly isothermal decompression stage at ~4.0 kbar/~790C after 1,638 Ma, due to
the appearance of garnet +cordierite +biotite +plagioclase +K-feldspar +melt +
quartz +ilmenite +magnetite. The formation of cordierite is due to the decompres-
sion and dehydration melting phases. The Nb, Sr, and Ti negative anomalies suggest
their generation from crustal sources. The geochemical analyses constrain that the
sedimentation of pelitic sediments was recorded along the convergent margin and
encountered by a subduction-related tectonic setting. The geochemical interpreta-
tion provides significant evidence that the protoliths of pelitic granulites were
derived from the Singhbhum Mobile Belt, Mahakoshal Supracrustal Belt, and
Received: 5 July 2021 Revised: 8 November 2021 Accepted: 9 November 2021
DOI: 10.1002/gj.4340
Geological Journal. 2021;1–27. wileyonlinelibrary.com/journal/gj © 2021 John Wiley & Sons Ltd. 1
Bundelkhand Craton, while their metamorphism was processed by the continent–
continent collision and followed by exhumation.
KEYWORDS
Chhotanagpur Granite Gneiss Complex, Columbia assembly, mafic granulites, pelitic granulite,
pseudosection modelling, U–Pb zircon dating
1|INTRODUCTION
Granulites are known to represent the lower crust to upper mantle
part of the lithosphere and provide important information regarding
heat transfer between the lithosphere and asthenosphere during the
process of orogenesis; thus, granulites are attracting a lot of attention
in recent times (Wang, Song, Allen, Su, & Wei, 2019 and references
therein). High-grade pelitic granulites have been found extensively
around the world and serve as an essential component of the orogenic
belt (Harley, 1989; Kohn, 2014; O'Brien, 2008), whereas the clock-
wise P–T–tpath of pelitic granulites is indeed a representative feature
of an orogenic setting. They were formed by the sedimentary
protoliths when they metamorphosed up to the granulite facies at
middle-lower crustal depth with subduction tectonism (Harley, 1989;
Liu et al., 2019; O'Brien & Rötzler, 2003). The Indian Peninsular shield
has acquired its present geological feature after encountering various
tectonic activities that occurred during the formation of three super-
continents in different periods: Columbia, Rodinia, and Gondwana
(Bhowmik, Wilde, Bhandari, Pal, & Pant, 2012; Dalziel, 1991; Dwivedi,
Theunuo, & Kumar, 2020; Li et al., 2008; Meert, 2003; Rogers &
Santosh, 2002; Sengupta et al., 2015; Zhao, Li, Sun, & Wilde, 2015).
The Central India Tectonic Zone (CITZ) is the main suture zone of the
Greater Indian landmass located between the northern and southern
Indian blocks. The CITZ is aligned between the two primary tectonic
settings, namely, the Central Indian Shear Zone (CIS) along the south-
ern boundary and the Son Narmada North Fault (SNNF) on the north-
ern side. The CITZ has three prominent components: the Mahakoshal
Supracrustal Belt (MSB) (~2,400–1,700 Ma), the Betul Supracrustal
Belt (~1,500 Ma), and the Sausar Mobile Belt (SMB) (~1,400–
900 Ma), and all lie in a north to south direction (Roy & Prasad, 2003).
The CITZ is located in the central part of the Indian Peninsula and
was formed by the Indo-Antarctica collision during the Columbia
Supercontinent (Acharyya, 2003; Bhandari, Pant, Bhowmik, &
Goswami, 2011; Bhowmik et al., 2012). The CITZ is an extensive
suture zone formed during ~1,500 Ma due to the collision of the
North Indian Block (NIB) and the South Indian Block (SIB), where the
SIB was subducted under the NIB to form the Indian Peninsular
shield (Bhowmik et al., 2012; Bhowmik, Wilde, Bhandari, &
Sarbadhikari, 2014). However, D. C. Mishra, Singh, Tiwari, Gupta, and
Rao (2000) and Yedekar, Jain, Nair, and Dutta (1990) recommended
that the NIB underwent the SIB, whereas the double-sided subduc-
tion model was proposed by Naganjaneyulu and Santosh (2010). The
CITZ preserves Palaeoproterozoic (~1,800 Ma) orogenic events in the
northern part, although Palaeoproterozoic–Mesoproterozoic (1,600–
1,500 Ma) collision activity is recorded in the southern region. These
were followed by crustal expansion, and eventually, the last collision
recorded in the late Mesoproterozoic to early Neoproterozoic age
(1,040–930 Ma) led to the final stitching of the Northern and South-
ern Indian blocks (Chattopadhyay, Bhowmik, & Roy, 2020).
The Chhotanagpur Granite Gneiss Complex (CGGC) belongs to
the eastern part of the east–west trending CITZ. The age of pelitic
rocks is ~1,900–1,700 Ma, obtained from detrital zircon, which
reflects that the protoliths of pelitic granulites were derived from a
sedimentary provenance located nearby (Dey, Mukherjee, Sanyal,
Ibanez-Mejia, & Sengupta, 2017; Rekha et al., 2011). The MSB lies at
the northern boundary of the CGGC with the Vindhyan Supergroup
(~1,640 Ma; M. Mishra, Bickford, & Basu, 2019) and is aligned as a
narrow linear belt. The Singhbhum Craton (SC) is located on the
southern boundary of the CGGC and has an age of >1,800 Ma (Das,
Karmakar, Dey, Karmakar, & Sengupta, 2017). The SMB and CGGC
have not established any contact relationship due to the thick sedi-
mentation of Gondwana rocks. However, Verma (1985) suggested
that the SMB was a western extension of the CGGC based on geo-
physical data. Instead, the CGGC was associated with various super-
continents in different periods. The CGGC was a part of the Columbia
Supercontinent in the Palaeoproterozoic (~1,800–1,600 Ma), and
again it assembled with the Rodinia supercontinents during the
Mesoproterozoic to Neoproterozoic (~1,100–900 Ma) (Mukherjee,
Dey, Sanyal, & Sengupta, 2019). The Columbia Supercontinent
attained its peak strength during ~2,100–1,600 Ma, and successively
their rifting began after ~1,500 Ma age; consequently, the fragmented
portion of the Columbian Plate accreted to form the Rodinia Super-
continent during the Grenvillian Orogeny (~1,000–900 Ma) (Li
et al., 2008; Rogers & Santosh, 2002). The chemical age shows
972 Ma, revealing that the CGGC was part of the Rodinia Superconti-
nent, which amalgamated with East Antarctica (Prydz Bay)
(Chatterjee & Ghose, 2011; Kumar & Dwivedi, 2019).
The present study has investigated detailed petrological informa-
tion, mineral chemistry, geochemistry, phase equilibrium modelling,
and U–Pb zircon (LA-ICP-MS) geochronology of pelitic and mafic
granulites from the northwestern part of the CGGC. We have used
conventional and phase equilibria modelling to estimate the metamor-
phic P–Tconditions of pelitic granulites. The quantitative constraints
in phase equilibrium modelling are calculated from bulk rock composi-
tions by consistent thermodynamic datasets (Holland & Powell, 1998).
In the context of phase equilibrium modelling, we have adopted
the NCKFMASHTO (Na
2
O–CaO–K
2
O–FeO–MgO–Al
2
O
3
–SiO
2
–H
2
O–TiO
2
–O
2
) system. The major, trace, and rare earth elements (REE)
geochemical data will characterize pelitic granulites and help unravel
the geodynamic evolution. We have documented the age of pelitic
2KUMAR ET AL.
granulites and mafic granulites, including the early stage of the
magmatism and metamorphism from the Daltonganj region.
2|GEOLOGICAL SETTING
The CITZ lies within two parallel east–west trending belts in central India:
the SMB and the MSB (Figure 1). The CGGC is an eastward extension of
the CITZ and covers a large area (80,000 km
2
) of the Proterozoic conti-
nental crust (Acharyya & Roy, 2000; Mazumdar, 1988; Sarkar, 1988)
(Figure 1). At the eastern extension of the CITZ, the MSB is located at the
northern periphery of the CGGC, whereas the SC is to the south and is
separated by the North Singhbhum Mobile Belt. The Daltonganj lies on
the NW margin of CGGC, and their basement rocks are mainly composed
of granitic gneiss, in which pelitic and mafic granulites are present as
enclaves. At some places, it is present in the form of an isolated outcrop.
However, few of the mafic granulites are in boulder form. The CGGC
consists of amphibolite to granulite facies rocks, while porphyritic granit-
oid and granitic gneisses are situated as basement rock, with a variety of
other rock types present such as migmatites, quartzo-feldspathic gneisses,
metasedimentary, and metabasic rocks as well as mafic to ultramafic rocks
(Ghose, 1992).
The complex metamorphic evolutionary history influenced the
CGGC with the CITZ; four stages of metamorphism (M
1
–M
4
) have
been recognized between the Palaeo- to Neoproterozoic age
(Chattopadhyay et al., 2020; Mukherjee et al., 2017; Sanyal &
Sengupta, 2012). (a) The significant metamorphic evidence has been
recorded in pelitic granulites at ~1,600 Ma with U–Pb zircon dating
(Dey et al., 2017, 2020; Rekha et al., 2011) as well as the electron
microprobe analysis (EPMA) chemical dating (Chatterjee, Banerjee,
Bhattacharya, & Maji, 2010). It is considered that the oldest basement
of CGGC came into existence during the Palaeoproterozoic period in
~1,750–1,660 Ma (Chatterjee & Ghose, 2011; Saikia et al., 2017). This
same age has been recorded from the MSB, indicating that the gran-
ites from the northern portion of CGGC were an extension of the
MSB (Chatterjee & Ghose, 2011; Yadav, Ahmad, Kaulina, Bayanova, &
Bhutani, 2020). The protolith of metapelites rocks was obtained from
adjacent continental masses, which belonged to the Eastern Ghats
Belt, the Aravalli Craton, and the Lesser Himalayas of ~1,900 to
1,700 Ma (Dey et al., 2017; Rekha et al., 2011); further deposited sed-
iments experienced the first metamorphic event M
1
during ~1,680–
1,580 Ma, in which the garnet +plagioclase +K-feldspar +quartz +
sillimanite +ferrian-ilmenite mineral assemblages occurred under
high-temperature (>850C) condition (Dey et al., 2020). (b) The M
2
event has been reported in pelitic granulites, preserved as enclaves in
the host felsic orthogneiss during ~1,470–1,400 Ma (Dey et al., 2019,
2020). The M
2
event of pelitic granulites is equivalent to the first-
phase metamorphism of felsic orthogneiss, where pelitic granulites
have mineral assemblages (Garnet +sillimanite +biotite +K-feldspar
+plagioclase +quartz +rutile +melt). However, the first metamor-
phism in mafic granulites was recorded at ~1,450 Ma under peak
metamorphic conditions with 12 kbar and 800C (Dey et al., 2020). In
contrast to these metamorphic events, few magmatic emplacements
also occurred in the CGGC, where the anorthositic magmatic activity
was recorded in older metasedimentary granulites during ~1,550 Ma
(Chatterjee, Crowley, & Ghose, 2008). The U-Th-total Pb EPMA mon-
azite dating reveals that the age of protolith of garnet–hypersthene
gneiss is ~1,424 Ma (Kumar & Dwivedi, 2019). Zircon U–Pb dating
and geochemical analysis revealed that A-type felsic magma
crystalized at ~1,447 Ma (Mukherjee et al., 2017), and other granitoid
rocks were emplaced at ~1,470–1,450 Ma in the NE portion of the
CGGC (Mukherjee, Dey, Ibanez-Mejia, Sanyal, & Sengupta, 2018).
(c) A major metamorphic event (M
3
) occurred in the CGGC during the
Grenvillian Orogeny (1,100–900 Ma), where the majority of continen-
tal crusts (host rocks and enclaves) underwent a granulite facies meta-
morphism (Chakraborty, Upadhyay, Ranjan, Pruseth, & Nanda, 2019;
Chatterjee & Ghose, 2011; Dey et al., 2017; Karmakar, Bose,
Sarbadhikari, & Das, 2011; Kumar & Dwivedi, 2019; Maji et al., 2008).
The EPMA monazite dating of felsic orthogneiss and pelitic
(khondalite) rock enclaves from the northeastern CGGC region was
shown to be ~1,100–930 Ma as an age of metamorphism (Chatterjee
et al., 2008, 2010; Sanyal, Sengupta, & Goswami, 2007). (d) Finally,
the M
4
metamorphic event is referred to as retrograde metamor-
phism, where the granulitic rocks were retrograded to the amphibolite
facies condition around ~870–780 Ma (Chatterjee, 2018; Mukherjee,
Dey, Sanyal, & Sengupta, 2018; Ray, Sanyal, & Sengupta, 2011;
Sanyal & Sengupta, 2012). In contrast, monazite dating provided a
high-pressure metamorphic event that occurred at ~880–830 Ma
(Chatterjee et al., 2010), and also regional metamorphism within the
Dumka-Jamua-Ghormara sector was recorded around ~850–780 Ma
(Sanyal et al., 2007). This metamorphic event has been considered the
last significant metamorphism and deformation of the CGGC.
2.1 |Local geology
The study area around Daltonganj lies in the northwestern margin of
the CGGC (Figure 2) within the Daltonganj (North Palamau)–
Hazaribagh–Dumka Belt. The investigated area falls between latitude
23550Nto23
5803000N and longitude 84020Eto84
0603000Einthe
Survey of India Toposheet number 73A/1. The study area extends up
to Renukoot, and it is separated from the Mahakoshal Belt by the Son–
Narmada South Fault. In the NNW direction, it extends to Japala of Gar-
hawa district. A thrust separates it to Vindhyan Supergroup, which lies
in the Sasaram. The study area consists of quartzo-feldspathic gneisses,
granitoid, and migmatites with enclaves of high-grade metasedimentary
rocks, as well as metabasic rocks, and basic to intermediate intrusive
rocks (Ghose, 1983, 1992). The CGGC is crucial terrain not only for
understanding the assembly of the Greater Indian Landmass, but also
for transcontinental correlation involving India, East Antarctica, and
Western Australia during the later part of the Proterozoic era.
3|SAMPLING, FIELD RELATIONSHIPS,
AND ANALYTICAL TECHNIQUES
During geological mapping, 30 rock specimens were collected from
the Daltonganj area during various fieldwork sessions. We have found
KUMAR ET AL.3
various rock types along with pelitic granulite, mafic granulite, and
granitic gneiss. The mapping was carried out by the Global Positioning
System instrument (Garmin GPSMAP 78s) to record the collected
samples' location (latitude/longitude). Granitic gneisses are dominated
as basement rock, whereas pelitic and mafic granulites are present as
patches (Figure 3a), or somewhere both granulites are found as out-
crops. Rock thin sections of all samples were prepared, and their pet-
rographic observation was performed with a petrological microscope
(LEICA DM 2500 P). Mineral assemblages and reaction texture rev-
ealed that pelitic granulites and mafic granulites were present in the
study area. Pelitic granulites' fabric typically contains gneissose tex-
ture with minor foliation texture, which is due to parallel orientation
of biotite and sillimanite flakes alternating with a fine mosaic of
garnet, quartz, and cordierite. A coarse-grained variety of garnet
(2–4 cm) is seen on the outcrop of pelitic granulites (Figure 3b). The
mafic granulites are characterized by medium- to coarse-grained gran-
ulite texture, and they show dark black to greenish-black colour. It
appears as discontinuous, scattered, lenticular patches throughout the
area (Figure 3c,d). The strike of the foliation in mafic granulites
throughout the region is NE–SW trending. Granitic gneisses typically
FIGURE 1 (a) Inset map showing the location of CGGC in India. The NIB and SIB contain the Archean nuclei of Bundelkhand (BN) and
Singhbhum (SN)-Bastar (BN)-Karnataka (KN), respectively (ADMB, Aravalli-Delhi Mobile Belt; CGGC, Chhotanagpur granitic gneissic complex;
CITZ, Central Indian Tectonic Zone; EGMB, Eastern Ghats Mobile Belt; SMGC, Shillong-Meghalaya gneissic complex) (after Bhowmik et al., 2014).
(b) The geological map shows different lithological units and tectonic elements of the CITZ (after Acharyya, 2003; Hossain, Tsunogae, Rajesh,
Chen, & Arakawa, 2007; Hossain, Tsunogae, Tsutsumi, & Takahashi, 2018). BBG, Balaghat-Bhandara Granulite; BC, Bastar Craton; BG, Betul
Group; BGB, Barapukuria Gondwana Basin; BN, Bundelkhand Craton; CGGC, Chhotanagpur Granite Gneiss Complex; CH, Chhattisgarh; CIS,
Central Indian Shear Zone; DGB, Damodar Gondwana basins; DS, Darjeeling-Sikkim Himalaya; DT, Deccan Trap; GTSZ, Gavligarh Tan Shear
Zone; M, Mohakoshal and equivalents; R, Rajmahal Trap; RKG, Ramakona-Katangi Granulite; SC, Singhbhum Craton; SG, Sausar Group; Si,
Singhbhum (Palaeoproterozoic); SMGB, Son Mahanadi Gondwana basins; SONA, Son Narmada Lineament; V, Vindhyan. The rectangle represents
the Shillong-Meghalaya gneissic complex located in the western part of NE India. (c) Geological map of the Chhotanagpur granite-gneiss complex
(modified after Acharyya, 2003; Chatterjee & Ghose, 2011; Maji et al., 2008). EITZ, Eastern Indian Tectonic Zone; D, Dudhi; MGB, Makrohar
Granulite Belt; R, Rihand-Renusagar area
4KUMAR ET AL.
consist of a gneissose texture with a well-defined foliation due to the
parallel orientation of biotite flakes and hornblende alternating with a
granular mosaic of K-feldspar and plagioclase.
3.1 |Electron microprobe analysis
We have selected representative samples for the EPMA based on the
petrological study. Various minerals of the D-3 (pelitic granulite) and
RP-1 (mafic granulite) were chosen for EPMA mineral chemistry,
which was carried out at the Department of Geology, Banaras Hindu
University (CAMECA SX five EPMA), with operating conditions of
15 kV accelerating voltage and 10 nA beam current. Some of the min-
erals like cordierite and biotite (included and matrix phases for both)
of D-3 (pelitic gneiss) were measured using the electron probe
microanalyzer (JEOL JXA-iSP100) at the Natural Science Center for
Basic Research and Development (N-BARD) Facility of Hiroshima Uni-
versity, Hiroshima, Japan, with an accelerating voltage of 15 kV and
10 nA beam current.
3.2 |X-ray fluorescence and ICP-MS
Seven representative samples were collected from the fresh outcrop
surface of the pelitic granulites. Special care was taken to mitigate the
possible effects of local contamination before the samples were sub-
jected to geochemical analysis. Since this rock type was metamor-
phosed and occurred in enclaves (K-1, K-10, and D-12) as well as
massive outcrop (S-9, K-4, D-7, and D-3), samples were collected from
both identities to extract the genetic information. Analysis of pelitic
FIGURE 2 Local geological map of the study area around the south-west part of Daltonganj, District Palamau (Jharkhand), India (after
Kumar & Dwivedi, 2021)
KUMAR ET AL.5
granulites for major oxide, trace, and REE were carried out at Birbal Sahni
Institute of Palaeosciences Lucknow, India. The fine rock powder was
prepared from fresh sample chips using a jaw crusher and agate mortar to
prevent contamination. Samples were prepared by the pressed powder
method using boric acid as a binder (boric acid: sample ratio, 2:3). Major
oxides were analysed by X-ray fluorescence (XRF) using wavelength dis-
persive (WD-XRF AXIOS MAX) machine with power: 4KW, 60 kV–
160 mA analytical, on pressed powder pellet machine used “kameyo”at
pressure 15–20 ton, with 4 mm pallet thickness. REE were analysed by
ICP-MS (Make: Agilent, Model: ICP-MS 7700). All solutions were pre-
pared using ultrapure water (18.2 MX). All the samples were digested by
taking 30 mg (300 mesh) sediment powder by using supra pure acid (HF,
HClO
4
,HNO
3
); four solutions (10, 40, 100, 200, and 300 ppb for all ele-
ments) were prepared by 71A and 71B multi-element calibration standard
solutions (Inorganic ventures) as external calibration. All the data set will
be below 5% error with a right calibration curve.
3.3 |LA-ICP-MS zircon dating
Zircon separation and mount-making processes are the same as those
described in Kawaguchi, Minh, Hieu, Cuong, and Das (2021). Zircon sepa-
ration was accompanied by the panning method using the whole-rock
powder with water. Magnetic minerals were removed from the heavy
mineral concentration using an Nd magnet. All the separated heavy and
non- to less-magnetic mineral fractions were mounted within the epoxy
resin without hand-picking to avoid human bias. The zircon mount was
polished until the full widths of the majority of zircon grains were
exposed at the surface. Cathodoluminescence (CL) images of the zircon
grains were captured using a scanning electron microscope (SEM: JEOL
7500F) installed at Hiroshima University, Japan. CL images of the zircon
grains were used to check the internal texture and to select the measured
point. Zircon FC1 (
207
Pb/
206
Pb age of 1,099.0 ± 0.6 Ma; Paces &
Miller, 1993) was used as a standard sample for correction of U–Pb ratio,
and glass standard NIST SRM 610 was used for correction of Th/U ratio.
During the analyses, zircon YO1 (TIMS
206
Pb/
238
U age of 279.3 Ma,
leached zircon; Herzig, Kimbrough,&Hayasaka,1997)wasmeasuredasa
consistency standard sample to evaluate the data quality. Zircon U–Pb
isotope analysis was performed using a 213 nm Nd-YAG Laser (New
Wave Research UP-213) combined with an inductively coupled plasma
ionization mass spectrometer (Thermo Fisher X-Series-II) (LA-ICP-MS)
housed at Hiroshima University, Japan. Throughout the analysis
179
Hf,
202
Hg,
204
(Pb +Hg),
206
Pb,
207
Pb,
208
Pb,
232
Th, and
238
U were monitored.
Before every analysis, pre-ablation was conducted by the laser spot diam-
eter of 32 μm to clean the surface of zircon grains. Each analysis was con-
ducted by the laser spot diameter of 25 μm with the repetition of 4 Hz.
Common Pb correction was performed by the
204
Pb that cancelled the
204
Hg isobaric interference using the
202
Hg. Data reduction and age cal-
culation processes are the same as those described in Kimura
et al. (2021). Statistical data plotting was conducted by Isoplot/EX version
3.00 (Ludwig, 2003). The weighted average
206
Pb/
238
Uageforthemea-
sured YO1 zircon grains yield 273 ± 19 Ma (95% confidence interval,
MSWD =3.1, probability =0.044) which is closely tallying with the
previously reported value.
4|ROCK TYPES AND MINERAL
ASSEMBLAGES
The Daltonganj area has different rock types: pelitic granulites,
mafic granulites, charnockites, garnet-hypersthene-cordierite gneisses,
migmatites, garnet-biotite gneisses, amphibolites, and granitic gneisses
FIGURE 3 Outcrop photographs
showing field features of the studied
rocks. (a) Melanocratic pelitic granulites
present as enclaves within the granitic
gneisses country rock. (b) Porphyroblastic
garnet (size: 2–3 cm) present within the
pelitic granulites. (c) Outcrop represents
mafic granulite, and it is associated with
migmatitic rock. (d) Closer view of fresh
mafic granulites
6KUMAR ET AL.
(Dwivedi, Kumar, & Srivastava, 2019; Kumar & Dwivedi, 2021) (Figure 2).
The pelitic granulite (D-3) and mafic granulite(RP-1)wereselectedfor
detailed petrological investigations and P–Tcalculations based on their
mineral compositions, representing the granulite-facies metamorphism.
Granitic gneisses occupy the major part of the area as the dominant rock
type (D-10). The characteristics of these rocks are described in Sec-
tions4.1,4.2,and4.3.Thepeliticrockmainlyconsistsofgarnet,cordier-
ite, sillimanite, biotite, plagioclase, K-feldspar, quartz, and opaque minerals
(ilmenite and magnetite). However, the studied mafic granulites are domi-
nated by clinopyroxene, orthopyroxene, amphibole, plagioclase, quartz,
biotite, and ilmenite.
4.1 |Pelitic granulites
Pelitic granulites are massive and medium- to coarse-grained with grey to
pinkish colour (Figure 3a). The abundance of garnet gives a smooth
appearance and shows a granulitic texture. Microscopically, the pelitic
granulite consists of medium to large garnets with sub-rounded to sub-
hedral grains in a matrix of cordierite, biotite, plagioclase, K-feldspar, silli-
manite, and quartz (Figure 4a). Matrix forming cordierite is closely
associated with the biotite (Figure 4b); in localized domains, medium-sized
biotite flakes are wrapped around the garnet (Figure 4b). At some places,
minute biotite, sillimanite, cordierite, and plagioclase are incorporated into
the garnet porphyroblasts (Figure 4c,d). Oriented needle-like ilmenites are
included within the garnets (Figure 4d). The cordierite and garnet
porphyroblasts usually contain sillimanite needles. These inclusions are
much smaller, may represent relicts of a prograde stage of mineral growth,
resulting in a coarse-grained matrix. The garnet porphyroblasts contain
inclusions of sillimanite and biotite, and at some places, garnets are
embedded in the matrix which consists of feldspars, quartz, sillimanite,
cordierite, and biotite. Textural relations suggest that the garnets include
high-grade metamorphic minerals and that, on the other hand, the sur-
rounding matrix minerals are well recrystallized, and in chemical equilib-
rium, one may conclude that the deformation phases affected the garnets
of the metapelites took place under high-grade metamorphic conditions.
Cordierite (35%) exists as a dominant mineral in pelitic granulites (D-3)
with garnet (25%), biotite (15%), quartz (10%), plagioclase (7%), and silli-
manite (5%), whereas accessory mineral phases are present as minor
amounts: ilmenite, magnetite, zircon, apatite, monazite, etc. A Table S1
has been added to represent the summary of mineral assemblages and
textural features of pelitic granulite samples. Petrography and reaction
textures observed between different mineral assemblages reveal the fol-
lowing multistage metamorphic stages in the pelitic granulites: pre-peak
(M
0
), peak (M
1
), and post-peak (M
2
).
4.1.1 | Pre-peak assemblage (M
0
)
Fine-grained cordierite, biotite, plagioclase, quartz, and ilmenite are
included in porphyroblastic garnet cores (Figure 4d). These minerals
are present in the core portion of garnet, indicating that garnet has
evolved from the intake of these minerals. Therefore, we suggest that
these mineral phases are developed as pre-peak metamorphic assem-
blages (M
0
) (Currie, 1971).
Cordierite þbiotite !garnet þKfeldspar þH2Oð1Þ
4.1.2 | Peak assemblage (M
1
)
Garnet grains are associated with a matrix that contains biotite,
sillimanite, plagioclase, and quartz (Figure 4e), and are inferred to
have equilibrated during the peak granulite-facies metamorphic
stage. At this stage, the garnet grew continuously with the
consumption of biotite, sillimanite, and plagioclase according to the
following biotite-melting dehydration reaction (Vielzeuf &
Montel, 1994):
Biotite þsillimanite þplagioclase þquartz
!garnet þKfeldspar þmelt ð2Þ
Biotite þsillimanite þquartz !garnet þKfeldspar þmelt ð3Þ
Instead, the peak metamorphism is also characterized by the dele-
tion of solely biotite and quartz, with the appearance of garnet associ-
ated with a minor amount of sillimanite and plagioclase. This reaction
texture is represented by incorporating biotite and quartz in the
garnet grains where small sillimanite laths are present adjacent to the
garnet porphyroblast (Figure 4e,f).
Biotite þquartz !garnet þsillimanite þplagioclase þmelt ð4Þ
4.1.3 | Post-peak assemblage (M
2
)
The appearance of the cordierite phase is a consequence of iso-
thermal decompression (ITD), which is represented as the post-
peak assemblage (M
2
) of pelitic granulites. The possible assem-
blages at this stage of pelitic granulites have been observed as gar-
net, biotite, cordierite, plagioclase, K-feldspar, quartz, ilmenite, and
magnetite. The probable reaction texture has been identified, as
cordierite grains are present in the vicinity of garnet grains
(Figure 4g) (Currie, 1971).
Garnet þsillimanite þquartz !cordierite ð5Þ
Garnet þsillimanite þKfeldspar þquartz
!cordierite þbiotite þmelt ð6Þ
In part, matrix cordierite is formed in association with matrix biotite,
quartz, and plagioclase (Figure 4h), indicating the following reaction:
Biotite þplagioclase þquartz !cordierite þmelt ð7Þ
KUMAR ET AL.7
4.2 |Mafic granulites
Petrographical observation reveals that the studied mafic granu-
lites are overall similar and dominated by orthopyroxene, cli-
nopyroxene, amphibole, plagioclase, biotite, and quartz, with
iron oxides (ilmenite and magnetite) constituting the rest of the
phases.
Orthopyroxene occurs as sub-idioblastic to xenoblastic grains
and in a few specimens as idioblastic crystals (Figure 5a).
Orthopyroxene contains corroded amphibole, biotite, and quartz
(Figure 5a), and it is commonly rimmed by amphibole along with
clinopyroxene (Figure 5b). In mafic granulites, photomicrographs
show that the reaction of amphibole and quartz leads to the forma-
tion of orthopyroxene and clinopyroxene minerals, and this
records the peak metamorphic stage as the orthopyroxene, cli-
nopyroxene, and plagioclase assemblages (Figure 5c). Furthermore,
it follows the retrograde metamorphism in which orthopyroxene
and clinopyroxene react to form amphibole. The textural relations
described earlier provide the evidence of the following prograde
and retrograde reactions:
FIGURE 4 Photomicrographs and
back-scattered electron (BSE) images of
the pelitic granulite (D-3).
(a) Photomicrograph showing subrounded
to subhedral garnet grains associated
within a matrix-forming cordierite, biotite,
plagioclase, K-feldspar, sillimanite, and
quartz (in ppl: plane-polarized light).
(b) Matrix-forming cordierite closely
associated with the biotite and medium-
sized biotite flake grains are wrapped
around the garnet crystals (in ppl).
(c) Minute-sized biotite, sillimanite,
cordierite, and plagioclase incorporated
into the garnet porphyroblasts (ppl).
(d) BSE image showing cordierite, biotite,
and quartz present as an inclusion within
the porphyroblastic garnet. (e) Flakes of
sillimanites associated with the garnet,
whereas biotite and quartz present as an
inclusion of the garnet (in ppl). (f ) BSE
image showing an uncorroded
porphyroblastic garnet contains biotite.
(g) BSE image showing corroded garnet
and sillimanite flakes in which surrounded
by cordierite ground mass. (h) Small size
of biotite, plagioclase, and quartz
associated with the cordierite grains
(in ppl). The mineral abbreviations are
from Whitney and Evans (2010)
8KUMAR ET AL.
FIGURE 5 Representative
photomicrographs of the mafic granulites
(RP-1) (a–e) and granitic gneiss (D-10)
(f–h). (a) Idioblastic to sub-idioblastic
grains of orthopyroxene with the
inclusion of amphibole and biotite (in ppl).
(b) Orthopyroxene, clinopyroxene, and
biotite surrounded by the mass of
amphibole porphyroblast (in ppl).
(c) Occurrences of orthopyroxene,
clinopyroxene, and plagioclase
porphyroblast minerals (in ppl).
(d) Idioblastic grain of clinopyroxene
occurring with numerous fine sizes of the
amphibole and biotite (in ppl).
(e) Clinopyroxene and plagioclase
occurred as an inclusion in amphibole
porphyroblast (in ppl). (f) Plagioclase
porphyritic grains associated with finer
grains of quartz and biotite in granitic
gneisses (under crossed-polarized light).
(g) Perthitic K-feldspar with plagioclase
and biotite flakes present in granitic
gneisses (under crossed-polarized light).
(h) Foliation due to parallel orientation of
biotite flakes and amphibole alternating
with a granular mosaic of K-feldspar and
plagioclase (in ppl). The mineral
abbreviations are from Whitney and
Evans (2010)
Prograde
Amphibole þbiotite þquartz !orthopyroxene þplagioclaseþK
feldspar þH2Oð8Þ
Peak
Amphibole þquartz !orthopyroxene þclinopyroxene
þplagioclase þH2Oð9Þ
Retrograde
Orthopyroxene þclinopyroxene þplagioclase þH2O
!amphibole þquartz ð10Þ
Clinopyroxene is colourless to light green, medium-grained
prismatic crystals, sub-idioblastic to idioblastic (Figure 5d).
Coarse clinopyroxene is poikiloblastic containing inclusions of
amphibole, biotite, quartz, and ilmenite (Figure 5d). Corroded cli-
nopyroxene occurs within amphibole (Figure 5e), which suggests
retrograde metamorphism. Amphibole shows two distinct genera-
tions of crystallization. The pyroxenes rim commonly consists of
fine-grained aggregates of amphibole with the development of
occasional quartz (Figure 5d). This textural feature gives evidence
of reaction (8); this may represent amphibole of earlier genera-
tion which has reacted to form pyroxene through the reaction
(9). Amphibole also includes ilmenite, biotite, clinopyroxene,
KUMAR ET AL.9
orthopyroxene, and plagioclase (Figure 5b,e), suggesting the ret-
rograde metamorphism.
4.3 |Granitic gneisses
Granitic gneisses are present as major basement rock types of the
Daltonganj region. It is a medium- to coarse-grained mesocratic rock
with a well-developed gneissose structure and deformation
(Figure 3a). Plagioclase crystals vary in grain size greatly. They are
coarse-grained subidioblastic to idioblastic (Figure 5f). Plagioclase is
the most dominant mineral in the granitic gneisses and partly shows
an albitic rim and contact with microcline (Figure 5g). The fabric is typ-
ically gneissose with a well-defined foliation due to parallel orientation
of biotite flakes and amphibole alternating with a granular mosaic of
K-feldspar and plagioclase (Figure 5h).
5|MINERAL CHEMISTRY
We have analysed garnet, cordierite, sillimanite, biotite, and plagio-
clase minerals of the pelitic granulites from the Daltonganj area, and
representative data are given in Tables S2–S5.
5.1 |Garnet
The microprobe analyses and the structural formulae of garnet from
pelitic granulites are presented in Table S2. Garnet consists of 74.0–
80.1 almandine, 16.8–22.6 pyrope, 1.6–3.0 grossularite, and 1.1–1.4
spessartine (in mole %) as the end-members. The X
Mg
[Mg/(Mg
+Fe
2+
)] values fall in the range of 0.17–0.26 and are affected by the
minerals in contact with the garnets. Garnet rims mantled by cordier-
ite and biotites show lower contents of MgO (4.29–4.47 wt%) and
higher contents of FeO
T
(36.33–36.42 wt%) in comparison with the
MgO (6.30–6.39 wt%) and FeO
T
(33.29–34.29 wt%) contents of the
cores, whereas the X
Mg
values for the rim and core of the garnet
porphyroblast are 0.17–0.18 and 0.25–0.26, respectively. In contrast,
garnets in the matrix phase show a different chemical composition of
MgO (5.09–5.28 wt%) and FeO
T
(34.78–35.29 wt%) than those in
previous compositions. Garnet porphyroblasts are zoned with rim-
wards increases in X
Alm
and decreases in X
Prp
. The analysed garnets
are plotted in a Fe
2+
–Mg–(Ca +Mn) diagram, where the X
Mg
values
show the three domains of garnet (Figure 6a).
5.2 |Cordierite
Cordierites are present around the garnet porphyroblast formed by
ITD metamorphism. The mineral chemistry data of cordierite are pres-
ented in Table S3. Two types of cordierite are present in the studied
pelitic granulites. Several tiny crystals of cordierite occur as inclusion
within garnet porphyroblast with high X
Mg
values (0.73–0.78),
whereas large crystals of cordierite are present in the matrix, as the
surrounding area of garnet with comparatively low X
Mg
values ranged
from 0.65 to 0.67.
5.3 |Biotite
The mineral chemistry data of biotite are shown in Table S4. All the
data are straddled with the siderophyllite class (Figure 6b). Biotites of
pelitic granulites contain X
Mg
(0.58–0.72). The wide compositional
range of biotite represents the various modes of generations formed
at different metamorphic stages. The included biotite is more magne-
sian (X
Mg
ranges between 0.72 and 0.69) with slightly higher
F-content (2.2–1.7 wt%) than the matrix biotite with XMg ranging
between 0.58 and 0.6 with F-content of 1.5 to 1.3 wt%.
5.4 |Plagioclase
The representative microprobe analyses of plagioclase are given in
Table S5. The compositional variation of plagioclase is represented as
Or
0.32–0.94
Ab
60.78–61.23
An
37.84–38.67
, showing an andesine
composition.
5.5 |Sillimanite
The composition is relatively pure Al
2
O
3
. Sillimanite contained minor
amounts of Fe (0.023 p.f.u.). Representative mineral chemistry is
shown in Tables S5.
6|GEOCHEMISTRY
6.1 |Whole-rock geochemistry
Geochemical compositions of pelitic granulites provide relevant evi-
dence regarding the protoliths and their geodynamic settings. The
major, trace, and REE data of analysed pelitic granulites are depicted
in Table S5, where all samples with loss of ignition ranged from 0.66
to 2.57. SiO
2
composition shows a wide variation (58.81–63.64 wt%);
the total alkali-silica (TAS: Middlemost, 1994) diagrams (Figure 7a) of
pelitic granulites display different characteristics as diorite and
quartz–monzonite fields, implying that the protolith of pelitic granu-
lites was obtained from different sedimentary provenances. The
studied pelitic granulites have been compared to augen gneiss of
Dumka from CGGC (Mukherjee, Dey, Sanyal, Ibanez-Mejia, &
Sengupta, 2019), charno-enderbite of Eastern Ghats Mobile Belt
(Sarkar et al., 2015), Bathani porphyritic granite from CGGC (Saikia
et al., 2017), and Jhirgadandi Granite from MSB (Bora et al., 2013), to
know any possible similarities. Most of the samples are ferroan, with
two pelitic granulites showing magnesian character (Figure 7b),
although five samples are peraluminous, with two samples being
10 KUMAR ET AL.
FIGURE 6 (a) Plot showing the variation in spessartine–grossularite–almandine–pyrope end-member composition in the garnet. (b) Al-Mg-
Fe
2+
mica classification diagram showing Al and Fe
2+
rich nature of biotites from the pelitic granulite. An, annite; Es, eastonite; Ph, phlogopite;
Sd, siderophyllite
FIGURE 7 Chemical classification
diagrams using major element composition
of the studied rocks. (a) Total alkali versus
silica (TAS) diagram for plutonic rocks after
Middlemost (1994) (MD, monzodiorite; MG,
monzogabbro). (b) Granitoid classification
scheme by Frost et al. (2001) revealing
magnesian to ferroan. (c) A/CNK versus
A/NK diagram. (d) Calcic to alkali-calcic via
calc-alkaline nature of pelitic granulites. The
field of the Cordilleran granites is plotted
after Frost et al. (2001). The data are also
compared with Bathani porphyritic granite
(Saikia et al., 2017), Charno-enderbite of
Eastern Ghats Mobile Belt (Sarkar,
Schenk, & Berndt, 2015), Jhirgadandi
Granite (Bora, Kumar, Yi, Kim, & Lee, 2013),
and Augen gneiss of Dumka from
Chhotanagpur Granite Gneiss Complex
(Mukherjee, Dey, Sanyal, Ibanez-Mejia, &
Sengupta, 2019). (e) Na
2
O versus K
2
O
diagram (after Turner et al., 1996); (f) K
2
O
versus SiO
2
plot after Peccerillo and
Taylor (1976)
KUMAR ET AL.11
metaluminous (A/CNK =0.91–1.45) (Figure 7c). Moreover, (SiO
2
) ver-
sus (Na
2
O+K
2
OCaO) plot shows calcic to alkali-calcic nature via
calc-alkalic composition (Figure 7d). The Na
2
O versus K
2
O diagram
(Figure 7e) represents shoshonitic and ultra-potassic composition, but
the SiO
2
versus K
2
O diagram (Figure 7f) has also illustrated that the
shoshonitic nature and high–K calc-alkaline series are dominated by
the pelitic granulites.
6.2 |Trace and REE patterns
Trace elements are dominated by incompatible elements (Rb, Sr,
Ba, Y, Zr, and Th), and the availability of compatible elements is low
(Cr, Ni, Cu, and Co). The range of LFSE elements is extensive, which
may be due to the degrees of mobility of the elements during the
transformation of the protolith and varying conditions of metamor-
phism. The primitive-mantle-normalized trace-element spider diagram
deciphers positive anomaly for Ba, K, Ta, Pb, Nd, Sm, Gd, and Y,
whereas distinctive negative anomaly is detected for large-ion
lithophile element (LILEs) such as Rb, Sr, and high field strength element
(HFSEs) (Nb and Ti) (Figure 8a). The Th/U ratio is between 2.09 and
20.68; these values reflect the oxidation conditions during the deposi-
tional process of the argillaceous rocks (McLennan & Taylor, 1980).
On the chondrite-normalized REE patterns, three samples show
positive Eu anomalies (Figure 8b). Samples D-3 and D-7 exhibit high
fractionated light REE patterns with a low and unfractionated heavy
REE (HREE) pattern; it seems to be like a flat pattern, and Eu (Eu
N
/Eu* =0.60) shows negative anomalies. The variation of abundances
of these elements falls within a very narrow range, except La, Ce, and
Nd. These samples show a relatively high degree of fractionation,
where the (La/Lu)
N
ratios vary from 6.2 to 91.2. The trace-element data
plot various tectonic discrimination diagrams to emphasize the charac-
ter of the magmatic source and the type of tectonism (Figure 9a,b).
7|METAMORPHIC P–TCONDITION
7.1 |Geothermobarometry
We have attempted to calculate the pressure and temperature condi-
tions of formation for the pelitic granulites, taking care to select the
most suitable mineral phases to obtain meaningful metamorphic P–T
conditions. The P–Tconditions constrained by using a variety of
geothermobarometers for pelitic granulite are listed in Table 1.
Garnet-biotite conventional geothermometer was applied to calculate
peak temperature from the compositions of garnet cores and biotite,
where biotite exists as inclusion within the garnet porphyroblast, it
shows 695 to 806C at 8 kbar. In contrast, comparatively low temper-
ature (695C) is shown by Ferry and Spear (1978), and high tempera-
ture (806C) is shown by Pigage and Greenwood (1982). Ti content in
biotite is considered as a function of temperature variation in meta-
morphic rocks (Kwak,1968), so we have estimated the metamorphic
temperature condition with a single-mineral as Ti-in-biotite geo-
thermometer (Henry, Guidotti, & Thomson, 2005) (Figure 10). It
FIGURE 8 (a) Primitive mantle
normalized multi-element spider
diagram of pelitic granulites.
Normalized values are after Sun and
McDonough (1989). (b) Chondrite-
normalized rare earth element plot.
Normalized values are after Sun and
McDonough (1989)
12 KUMAR ET AL.
reveals 611 ± 24ºC and 674 ± 34ºC temperature from matrix biotite
and biotite included in garnet respectively. This single-mineral
thermometry delivers low temperature compared to exchange ther-
mometry. However, garnet-biotite-plagioclase-quartz geobarometer
provides that the pressure of metamorphism is 7.86 kbar at 800C
(Wu, Zhang, & Ren, 2004). The studied sample shows a high X
Mg
(0.69–0.72) value of biotite from the included phase of biotite within
the garnet. Instead, compositions of the matrix garnet and garnet rim
may be affected by retrograde metamorphism, which provides com-
paratively lower X
Mg
values than the garnet core, that is, peak-
metamorphic compositions. Therefore, it reveals a low P–Tcondition
in which represents a post-peak metamorphism. The garnet-cordierite
geothermometer, using the garnet rim and matrix cordierite, gives
post-peak conditions with a temperature condition range of 671 to
727C at 6 kbar; here, Holdaway and Lee (1977) model shows low
temperature as 671C and Bhattacharya, Mazumdar, and Sen (1988)
FIGURE 9 (a) (Y/Nb)
N
versus
(Th/Nb)
N
diagram (to discriminate
tectonic regimes of pelitic granulites from
the Daltonganj of north-west
Chhotanagpur Granite Gneiss Complex
after Moreno et al. (2014)). (b) Zr versus
Nb/Zr plot to discriminate the tectonic
environment after Thieblemont and
Tegyey (1994)
TABLE 1 (a) Temperature estimates of pelitic granulite (D-3) from conventional geothermometry; (b) pressure estimates of pelitic granulites
(D-3) from conventional geobarometry
(a)
Grt-Bt geothermometer (at 8 kbar) Grt-Crd geothermometer (at 6 kbar)
Models D-3 Models D-3
1. Thompson (1976) 733C Thompson (1976) 688C
2. Ferry and Spear (1978) 695C Holdaway and Lee (1977) 671C
3. Pigage and Greenwood (1982) 806C Wells (1979) 718C
4. Hodges and Spear (1982) 772C Perchuk et al. (1985) 682C
5. Dasgupta, Sengupta, Guha, and Fukuoka (1991) 726C Bhattacharya et al. (1988) 727C
6. Aranovich, Lavrent'eva, and Kosyakova (1988) 767C Aranovich and Podlesskii (1989) 682C
7. Hoinkes (1986) 804C Dwivedi, Mohan, and Lal (1998) 688C
8. Average 758 ± 41C Average 693 ± 21C
(b)
Grt-Bt-Pl-Qz geobarometer (in kbar) (at 800C)
Model D-3
1. Wu, Zhang, & Ren (2004) 7.86
Grt-Crd-Sil-Qz geobarometer (kbar) (at 600C)
Models D-3
1. Thompson (1976) 6.02
2. Wells (1979) 6.24
3. Nichols, Berry, and Green (1992) 5.35
4. Newton (1978) 6.11
5. Aranovich and Podlesskii (1989) 5.89
6. Dwivedi, Mohan, and Lal (1997) 5.74
7. Average 5.89 ± 0.32
KUMAR ET AL.13
model shows a high temperature at 727C. The garnet-cordierite-silli-
manite-quartz geobarometer was used to estimate the pressure and it
ranged from 5.35 to 6.24 kbar. Corresponding garnet and biotite com-
positions with garnet and cordierite are showing ~2.0 kbar lower pres-
sure at temperatures lower by ~25–75C, suggesting post-peak near
ITD stage. This post-peak ISD stage is characterized by the presence
of cordierite in the pelitic granulite.
7.2 |Phase equilibrium modelling
The P–Tpseudosections are used for constraining the metamorphic
evolution of the granulitic rocks. Here, we have used Perple_X soft-
ware version 6.9.0 (Connolly, 2005, 2009) and thermodynamic data
from Holland and Powell (2011) (filename: hp62ver.dat), in
NCKFMASHTO (Na
2
O–CaO–K
2
O–FeO–MgO–Al
2
O
3
–SiO
2
–H
2
O–
TiO
2
–O
2
) model system for constraining the P–Tpseudosection for
pelitic granulites. The bulk composition of pelitic granulite (D-3) was
obtained by XRF analysis in weight percentage and converted into
mole percentage for calculating pseudosections. The sample D-3
composes: SiO
2
=67.83, TiO
2
=0.60, Al
2
O
3
=11.56, FeO =6.29,
MgO =3.62, CaO =1.69, Na
2
O=2.54, K
2
O=3.34, H
2
O=2.00,
and O
2
=0.52 (in mol%). There are different solution models used
for construction the pseudosection; garnet, biotite cordierite,
(White, Powell, Holland, Johnson, & Green, 2014), plagioclase
(Fuhrman & Lindsley, 1988), melt (Green et al., 2016), ilmenite
(White, Powell, Holland, & Worley, 2000); including some of the
pure end-member phases associated with it such as aluminosilicate
(sillimanite), quartz, and H
2
O. The low content of the MnO in the
pelitic granulite is not included as a component in pseudo-
section calculation. The O
2
has been estimated by integrating min-
eral compositions and modal abundance data of the phases
presented in the rock. The assumption of H
2
O has been determined
by the T-X
H2O
pseudosection, which indicates stable mineral phases
FIGURE 10 Ti-in-biotite geothermometer (Henry et al., 2005).
The dashed curves represent the intermediate 50C interval
isotherms. Symbols in the diagram show the Ti (a.p.f.u.) versus
Mg/(Mg +Fe) of biotites from different location points in the D-3
sample
FIGURE 11 T–X
H2O
pseudosection at
6.0 kbar, showing the effects of varying the
molar proportions of bulk-rock H
2
Oin
pelitic granulite (D-3). The yellow field
represents the peak metamorphic stage and
near-isothermal decompression stage with
the formation of the cordierite phase,
respectively. The black dashed line is the
modelled composition of H
2
O (2.00%)
14 KUMAR ET AL.
appeared with the appropriate amount of H
2
O. We have calculated
the T-X
H2O
pseudosection at 6.0 kbar pressure (Figure 11) for pelitic
granulite. The X
H2O
value of 2.00 mol% is an appropriate amount for
the stable mineral phases of pelitic granulite.
The pseudosection is characterized by large high-variance (F =3–
6) garnet-bearing fields. Cordierite, biotite and quartz are included
within garnet, defined as a pre-peak metamorphic condition, these
mineral phases coexisting under low pressure and temperature condi-
tions. The reaction textures suggest that pre-peak assemblage formed
through the reaction crd +bt !grt +kfs. The P–Tcondition of pre-
peak metamorphism is found at ~3.2 kbar and ~620C, and the P–T
condition of this stage is derived by the X
Mg
isopleth contour lines of
FIGURE 12 (a) NCKFMASHTO P–T
pseudosection for pelitic granulite (D-3)
showing calculated mineral equilibria for
the pre-peak condition, minerals
assemblage grt-pl-sil-kfs-bt-melt-ilm-qz for
peak condition, and retrograde
metamorphism are depicted in
pseudosection as grt +crd +bt +pl +kfs
+melt +ilm +qz +mag (mineral
abbreviations: Whitney & Evans, 2010).
(b) Isopleths for garnet, cordierite, and
biotite are contoured in the P–T
pseudosection
KUMAR ET AL.15
garnet and cordierite which are similar to the analysed microprobe
data. The P–Tstability field for the peak assemblage (grt +bt +pl
+sil +kfs +melt +ilm +qz) ranges from 7.40 to 9.10 kbar and from
815 to 835C. Reactions 2, 3, and 4 suggest that dehydration melt
was produced at peak stage, which is consistent with the observed
reaction textures preserved in this pelitic granulite. This peak meta-
morphic condition has been derived by the contouring of the X
Mg
iso-
pleths line of garnet and biotite (Figure 12). Tetravariant fields
dominate the pseudosection. The assemblage is tetravariant in
NCKFMASHTO and is bounded by pentavariant biotite-absent field at
high T and trivariant magnetite-bearing fields at low P and low T. The
cordierite-in and sillimanite-out boundaries define the assemblages
under lower pressure stability. The ITD retrograde reaction has been
observed from the petrographic investigation in which the consump-
tion of garnet results in the formation of cordierite under low-
pressure conditions with partial melting that suggests the following
reaction: Grt +sil +kfs +qz !crd +bt +melt. Garnet, biotite, and
sillimanite-bearing assemblages are stable at higher pressure, whereas
cordierite-bearing assemblages dominate at the low-pressure equilib-
ria field in the pseudosection. In the pre-peak metamorphic stage, cor-
dierite exists as inclusion within garnet porphyroblast with a higher
X
Mg
value of cordierite in the stable mineral assemblages. In contrast,
retrograde metamorphic stage is characterized by cordierite present
in the matrix with comparatively lower X
Mg
values. The textural inter-
pretation reveals that the retrograde metamorphic assemblage in P–T
pseudosection contains grt +crd +bt +pl +kfs +melt +ilm +qz
+mag, which is stable under the pressure and temperature of
~4.0 kbar and ~790C.
8|U–Pb ZIRCON GEOCHRONOLOGY
8.1 |Pelitic granulites
The pelitic granulite (D-3) sample was selected for LA-ICP-MS zircon
U–Pb dating. Zircon grains vary from 100 to 150 μm in size along the
FIGURE 13 (a) Scanning electron microscope-CL (cathodoluminescence) images of the representative zircon grains with different zoning
patterns of pelitic granulite from the Daltonganj area. (b) Analytical data from the pelitic granulite (D-3) plotted in Tera-Wasserburg Concordia
diagram. (c) Probability density plot and age histogram of
207
Pb/
206
Pb ages of the pelitic granulite sample with the two unmixed ages of 1,705
± 9 Ma and 1,629 ± 11 Ma. (d) Plots of zircon ages (
207
Pb/
206
Pb) versus Th/U ratios of analysed data
16 KUMAR ET AL.
longer dimension with rounded shapes. The SEM-CL imaging of the
internal texture of zircon grains has revealed that they contain distinct
core and rim structures. Core regions are mostly oscillatory zoned
with some lamellar zoned core regions as well with lighter CL
response. The thick to thin rim regions are mostly featureless with
dark CL response (Figure 13a). In some grains, thicker overgrowth on
core regions with slightly less dark CL response is also seen
(Figure 13a). Half of the studied grains are elongated in shape with a
high aspect ratio (nearly 4:1), and some of them have the aforemen-
tioned thick overgrowth rims.
TABLE 2 LA-ICP-MS zircon U–Pb data of pelitic granulite (D-3)
Spot label
238
U/
206
Pb
*
±2σ
207
Pb
*
/
206
Pb
*
±2σ
206
Pb
*
/
238
U age
±2σ(Ma)
207
Pb
*
/
235
U age
±2σ(Ma)
207
Pb
*
/
206
Pb
*
age
±2σ(Ma) Th/U Disc.
(1)
(%)
1 056D2-1c 3.447 0.107 0.104 0.0016 1,642.2 45.1 1,664.4 28.2 1,692.6 28.0 0.39 1.4%
2 057D2-1r 3.412 0.116 0.099 0.0012 1,656.9 49.9 1,637.0 29.7 1,611.7 22.6 0.05 1.2%
3 058D2-2c 3.241 0.075 0.105 0.0015 1,733.5 35.1 1,728.6 22.7 1,722.9 26.0 0.71 0.3%
4 059D2-2r 3.619 0.203 0.102 0.0011 1,572.6 78.6 1,611.8 47.1 1,663.3 20.5 0.07 2.5%
5 060D2-3 3.262 0.111 0.105 0.0012 1,723.7 51.6 1,717.9 30.3 1,710.9 20.4 0.12 0.3%
6 061D2-4r 3.386 0.132 0.103 0.0014 1,668.1 57.6 1,671.5 34.2 1,675.8 26.1 0.12 0.2%
7 062D2-4c 3.136 0.097 0.105 0.0017 1,784.4 48.5 1,750.4 29.6 1,710.1 29.7 0.41 1.9%
8 065D2-5 3.673 0.217 0.101 0.0013 1,552.1 81.9 1,590.2 49.4 1,641.1 24.3 0.01 2.5%
9 066D2-6 3.287 0.092 0.105 0.0018 1,712.3 42.2 1,709.7 27.7 1,706.5 31.6 0.43 0.2%
10 067D2-7 3.576 0.193 0.100 0.0013 1,589.7 76.5 1,607.7 46.2 1,631.6 24.4 0.02 1.1%
11 068D2-8r 3.378 0.115 0.105 0.0013 1,671.8 50.3 1,688.5 30.1 1,709.4 22.3 0.71 1.0%
12 069D2-8c 3.074 0.086 0.105 0.0016 1,815.7 44.5 1,770.3 27.2 1,717.3 27.8 0.26 2.5%
13 070D2-9r 3.207 0.083 0.099 0.0014 1,749.8 40.0 1,689.0 25.0 1,614.3 26.3 0.02 3.5%
14 071D2-9c 3.227 0.100 0.098 0.0015 1,739.9 47.4 1,671.6 28.3 1,587.0 28.3 0.10 3.9%
15 075D2-10 3.290 0.102 0.104 0.0017 1,710.7 46.7 1,700.4 29.3 1,687.8 29.8 0.21 0.6%
16 076D2-11 3.265 0.091 0.106 0.0016 1,722.2 42.5 1,727.6 26.9 1,734.2 27.8 0.51 0.3%
17 077D2-12 3.380 0.098 0.101 0.0016 1,670.9 42.8 1,656.7 27.3 1,638.8 30.1 0.02 0.8%
18 078D2-13 3.007 0.096 0.114 0.0018 1,850.9 51.7 1,860.6 31.2 1,871.5 29.1 0.29 0.5%
19 079D2-14 3.257 0.088 0.104 0.0015 1,726.2 41.0 1,710.5 25.1 1,691.4 26.0 0.37 0.9%
20 080D2-15 5.055 0.126 0.105 0.0015 1,163.6 26.7 1,375.3 22.1 1,721.3 26.0 0.03 18.2%
21 081D2-16 3.696 0.200 0.104 0.0017 1,543.7 74.6 1,611.4 46.3 1,701.1 29.8 1.54 4.4%
22 084D2-17 3.375 0.111 0.102 0.0014 1,672.9 48.8 1,666.3 29.9 1,658.2 26.2 0.02 0.4%
23 085D2-18 3.386 0.105 0.101 0.0014 1,668.1 45.7 1,658.9 28.2 1,647.3 26.2 0.02 0.6%
24 086D2-19 3.206 0.096 0.105 0.0015 1,750.3 46.1 1,737.6 27.8 1,722.3 25.9 0.85 0.7%
25 087D2-20 3.328 0.096 0.101 0.0014 1,693.9 43.3 1,669.8 26.6 1,639.7 26.3 0.01 1.4%
26 088D2-21 3.628 0.112 0.098 0.0015 1,569.2 43.3 1,574.3 27.6 1,581.2 28.3 0.01 0.3%
27 089D2-22 3.272 0.095 0.105 0.0020 1,719.1 43.9 1,717.5 29.4 1,715.7 35.4 0.39 0.1%
28 090D2-23 3.324 0.123 0.099 0.0016 1,695.6 55.4 1,652.6 33.2 1,598.4 30.1 0.06 2.5%
29 091D2-24 3.393 0.105 0.101 0.0014 1,664.9 45.6 1,653.9 28.1 1,639.9 26.3 0.05 0.7%
30 092D2-25 3.509 0.190 0.101 0.0013 1,616.3 77.7 1,626.5 46.4 1,639.7 24.3 0.03 0.6%
31 095D2-27 3.181 0.089 0.103 0.0015 1,762.3 43.3 1,724.1 26.9 1,678.0 27.9 0.19 2.2%
32 096D2-28c 3.217 0.109 0.106 0.0018 1,744.8 52.2 1,737.0 32.1 1,727.7 31.5 0.44 0.4%
33 097D2-28r 3.358 0.138 0.101 0.0016 1,680.3 60.9 1,659.6 36.6 1,633.6 30.0 0.03 1.2%
34 098D2-29r1 4.264 0.350 0.100 0.0017 1,358.2 101.2 1,468.4 67.4 1,631.6 32.0 0.13 8.1%
35 099D2-29r2 3.549 0.231 0.105 0.0014 1,600.2 92.8 1,651.4 55.3 1,717.1 24.1 0.19 3.2%
36 100D2-30c 3.304 0.109 0.100 0.0015 1,704.5 49.6 1,669.4 29.9 1,625.5 28.2 0.07 2.1%
37 101D2-30r 3.719 0.234 0.101 0.0014 1,535.1 86.6 1,579.2 53.4 1,638.7 26.3 0.01 2.9%
38 102D2-31r 3.442 0.151 0.099 0.0015 1,644.2 64.2 1,628.4 38.0 1,608.2 28.2 0.01 1.0%
39 103D2-31c 3.161 0.088 0.103 0.0013 1,772.1 43.5 1,729.0 26.1 1,677.2 24.2 0.53 2.4%
40 104D2-32r 3.290 0.112 0.101 0.0017 1711.0 51.3 1,684.1 31.7 1,650.8 31.9 0.07 1.6%
Abbreviations: c, core; LA-ICP-MS, Laser Ablation Inductively Coupled Plasma Mass Spectrometry; r, rim.
KUMAR ET AL.17
A total of 40 spots have been analysed from 32 zircon
grains. Some grains are measured for both core and rim regions.
The U–Pb geochronological data are presented in Table 2, while
the Tera-Wasserburg Concordia diagram is shown in Figure 13b.
The probability density diagram and analysis spot-wise Th/U
ratio versus age are shown in Figure 13c,d (except for two spot
data, all others have discordance values of less than 5% and are
interpreted as concordant data). The grains where both the core
and rim regions are measured of which the core regions (mostly
oscillatory zoned, light CL) yield older spot ages than the
corresponding rim regions. The age of detrital (magmatic) zircon
demarcated that the age of protolith ranges from 1,734 Ma to
1,677 Ma, concentrated mainly in the core regions. In contrast,
the oldest age of the metamorphic zircon of the rim regions is
1,678 Ma and the youngest is 1,581 Ma, yielding a younger
weighted average
207
Pb/
206
Pb age of 1,638 ± 22 Ma (2σ,
MSWD =4.0). In the two grains, the pattern is somewhat dif-
ferent; in grain 9, core reveals younger age; and in grain 30, the
age values between core and rim are nearly the same within
their error values. The Th/U ratio of the older core range
between 0.12 and 0.71, while that of the rim regions range
between 0.01 and 0.2 (except data all below 0.07). Thirty-eight
concordant data (discordance <5%) are plotted on the probabil-
ity density diagram using their
207
Pb/
206
Pb age values. There
are two major clusters of which 1,705 ± 9 and 1,629 ± 11 Ma
(errors are in 2σ) with single older spot age of 1,872 ± 29 Ma
(Figure 13c).
8.2 |Mafic granulites
The mafic granulite (RP-1) was selected for LA-ICP-MS zircon U–Pb
dating. The zircon grains are subhedral to anhedral in shape, and their
colour is light pink to pinkish-white under the binocular microscope.
The size ranges from 150 to 300 μm along the longer dimension and
1:1–3:1 in aspect ratios. The CL images show that most recrystalliza-
tion zircon grains show chaotic textures, while others are homoge-
neous with light luminescence (Figures 14a).
A total of 35 spots have been analysed on 34 zircon grains. One
large grain is measured both at the core and rim regions. The
FIGURE 14 (a) CL images of the representative zircon grains with different zoning patterns of zircons from mafic granulite. (b) Analytical data
from the mafic granulite (RP-1) plotted in Tera-Wasserburg Concordia diagram (inset: plots of zircon ages [
207
Pb/
206
Pb] vs. Th/U ratios).
(c) Weighted average
207
Pb/
206
Pb ages of the mafic granulite sample. Two data labelled with the blue colour indicate the rejected data from the
weighted average calculation
18 KUMAR ET AL.
measured data are presented in Table 3, whereas the Concordia plot
and weighted average age diagram are shown in Figure 14b,c. The
Th/U ratio varies between 0.39 and 1.44 (inset in Figure 14b), except
for one data rest all of the data mark a clustered of ~1. All the
analysed data show a low discordance value of less than 4% (Table 3).
All the age data mark a single age cluster on the Concordia diagram at
~1,600 Ma (Figure 14b). Weighted average
207
Pb/
206
Pb age shows
1,629.0 ± 6.0 Ma (2σ, MSWD =1.4, probability =0.068) with the sta-
tistical rejection of two points (Figure 14c).
9|DISCUSSION
9.1 |P–T–tpaths and metamorphic evolution
The igneous domains from the pelitic granulite represent the detrital
zircon. Approximated maximum depositional timing is estimated as
~1,677 Ma from the age of the youngest detrital zircon, and the
weighted mean age of the metamorphic zircons represents the meta-
morphic event of 1,638 ± 22 Ma. Instead, mafic granulite has shown
TABLE 3 LA-ICP-MS zircon U–Pb data of mafic granulite (RP-1)
Spot label
238
U/
206
Pb
*
±2σ
207
Pb
*
/
206
Pb
*
±2σ
206
Pb
*
/
238
U age
±2σ(Ma)
207
Pb
*
/
235
U age
±2σ(Ma)
207
Pb
*
/
206
Pb
*
age
±2σ(Ma) Th/U Disc.
(1)
(%)
1 007B3-1r 3.441 0.100 0.100 0.0016 1,644.8 42.2 1,636.2 27.2 1,625.3 30.0 1.01 0.5%
2 008B3-1c 3.527 0.095 0.100 0.0019 1,609.0 38.6 1,617.3 27.1 1,628.1 35.7 1.16 0.5%
3 009B3-2 3.448 0.093 0.100 0.0017 1,641.5 39.2 1,635.5 26.3 1,628.0 32.0 1.28 0.4%
4 010B3-3 3.505 0.105 0.100 0.0023 1,618.0 43.1 1,618.3 31.2 1,618.8 43.5 1.09 0.0%
5 011B3-4 3.613 0.112 0.100 0.0018 1,575.1 43.5 1,599.6 29.4 1,632.1 33.8 1.03 1.6%
6 012B3-5 3.538 0.099 0.100 0.0019 1,604.5 39.9 1,609.2 27.8 1,615.4 35.8 0.78 0.3%
7 013B3-6 3.432 0.096 0.101 0.0018 1,648.2 40.9 1,645.2 27.2 1,641.4 33.8 1.37 0.2%
8 014B3-7 3.530 0.099 0.099 0.0021 1,607.8 40.0 1,607.5 28.6 1,607.2 39.7 1.21 0.0%
9 018B3-8 3.592 0.090 0.100 0.0020 1,583.4 35.2 1,601.9 26.1 1,626.5 37.6 0.76 1.2%
10 019B3-9 3.713 0.130 0.097 0.0022 1,537.5 48.1 1,552.1 34.0 1,572.0 43.7 0.98 0.9%
11 020B3-10 3.470 0.097 0.101 0.0016 1,632.3 40.5 1,640.1 26.4 1,650.1 30.0 1.41 0.5%
12 021B3-11 3.471 0.104 0.102 0.0018 1,631.9 43.4 1,644.3 28.9 1,660.3 33.7 1.29 0.8%
13 022B3-12 3.525 0.120 0.101 0.0017 1,609.9 48.6 1,624.6 31.3 1,643.7 31.9 1.05 0.9%
14 023B3-13 3.521 0.113 0.100 0.0022 1,611.3 45.8 1,614.6 32.0 1,619.0 41.5 0.95 0.2%
15 024B3-14 3.474 0.115 0.099 0.0020 1,631.0 47.7 1,616.0 32.0 1,596.6 37.8 1.04 0.9%
16 027B3-15 3.554 0.100 0.098 0.0016 1,598.3 39.8 1,596.8 26.1 1,594.8 30.2 1.00 0.1%
17 028B3-16 3.500 0.105 0.100 0.0017 1,620.1 43.1 1,624.8 27.9 1,631.0 32.0 1.08 0.3%
18 029B3-17 3.632 0.123 0.102 0.0027 1,567.9 47.5 1,609.0 35.3 1,663.3 48.9 0.99 2.6%
19 030B3-18 3.565 0.103 0.098 0.0017 1,593.9 41.1 1,592.4 27.7 1,590.5 32.1 0.82 0.1%
20 031B3-19 3.618 0.116 0.099 0.0021 1,573.1 44.8 1,582.9 30.9 1,596.0 39.7 0.39 0.6%
21 032B3-20 3.619 0.134 0.101 0.0028 1,572.9 51.8 1,599.4 37.7 1,634.7 53.0 0.75 1.7%
22 033B3-21 3.623 0.087 0.099 0.0016 1,571.4 33.6 1,588.3 23.6 1,610.9 30.1 1.33 1.1%
23 037B3-22 3.717 0.100 0.101 0.0021 1,535.8 37.0 1,583.0 27.6 1,646.5 39.4 1.03 3.1%
24 038B3-23 3.552 0.099 0.100 0.0019 1,599.1 39.8 1,613.0 27.9 1,631.2 35.7 1.31 0.9%
25 038B3-24 3.579 0.111 0.100 0.0016 1,588.5 43.8 1,604.4 28.6 1,625.4 30.1 1.44 1.0%
26 040B3-25 3.634 0.105 0.104 0.0021 1,567.1 40.5 1,626.6 28.8 1,704.5 37.3 1.21 3.8%
27 041B3-26 3.524 0.116 0.099 0.0019 1,610.4 47.2 1,607.8 31.1 1,604.5 35.9 1.38 0.2%
28 042B3-27 3.528 0.109 0.102 0.0018 1,608.5 44.3 1,629.0 29.6 1,655.7 33.7 0.92 1.3%
29 043B3-28 3.633 0.102 0.101 0.0018 1,567.6 39.1 1,601.0 26.9 1,645.4 33.7 1.28 2.1%
30 047B3-29 3.400 0.092 0.101 0.0015 1,662.3 39.7 1,649.9 25.6 1,634.2 28.2 0.93 0.7%
31 048B3-30 3.479 0.090 0.102 0.0014 1,628.5 37.5 1,638.8 24.7 1,652.1 26.2 1.34 0.6%
32 049B3-31 3.608 0.112 0.099 0.0024 1,577.2 43.5 1,586.7 31.8 1,599.4 45.5 1.04 0.6%
33 050B3-32 3.541 0.103 0.101 0.0025 1,603.6 41.3 1,617.4 31.2 1,635.4 47.2 0.90 0.9%
34 051B3-33 3.458 0.104 0.102 0.0020 1,637.4 43.5 1,650.5 29.8 1,667.3 37.4 1.09 0.8%
35 052B3-34 3.480 0.090 0.100 0.0017 1,628.3 37.5 1,628.8 25.5 1,629.5 32.0 1.28 0.0%
Abbreviations: c, core; LA-ICP-MS, Laser Ablation Inductively Coupled Plasma Mass Spectrometry; r, rim.
KUMAR ET AL.19
the age of magmatic emplacement during ~1,629 Ma, which coincides
with the estimated metamorphic age of the pelitic granulite. The
pseudosection of pelitic granulite in the NCKFMASHTO system has
shown pre-peak metamorphism (M
0
), prior to the peak metamorphism
(M
1
), and underwent subsequent ITD path (M
2
). The pre-peak meta-
morphism represents ~3.2 kbar and ~620CP–Tcondition; here, tiny
crystals of cordierite, biotite, and quartz are embedded into garnet
porphyroblast, and this leads to the formation of garnet. The peak
metamorphic event (M
1
) is characterized by garnet, sillimanite, plagio-
clase, biotite, K-feldspar, ilmenite, melt, and quartz as a stable mineral
assemblage, with a narrow temperature and large pressure range;
however, it has required X
Mg
isopleths of various minerals to constrain
the appropriate P–Tcondition. The isopleths of Grt (X
Mg
)=Mg/(Mg
+Fe +Ca) and Bt(X
Mg
)=Mg/(Mg +Fe) have plotted to estimate the
peak metamorphic P–Tcondition which ranges from 7.40 to 9.10 kbar
and from 815 to 835C. Following these interpretations, we specu-
lated that a limited period for depositi on was observed for the
pelitic protolith after ~1,677 Ma, and then it buried into the
deeper crust and metamorphosed at the peak metamorphic event
(M
1
) during ~1,638 Ma. Cordierite in this pelitic granulite was
formed at the decreasing of pressure after the peak metamor-
phism. Sillimanite is present in pre-peak and peak metamorphic
assemblages, along with garnet and biotite assemblages in various
stable phases. The high availability of bulk alumina in pelitic granu-
lite is favourable for sillimanite formation. The cordierite appears
below 6.4 kbar pressure. The isopleth line of Crd (X
Mg
)=Mg/(Fe
+Mg) and Grt (X
Mg
)=Mg/(Mg +Fe +Ca) are contoured to rep-
resent the ITD stage, which lies under the pressure and tempera-
ture of ~4.0 kbar and ~790C. The retrograde metamorphic event
(M
2
) was recorded in pelitic granulites after the peak stage
~1,638 Ma, as well as the intrusion of felsic magmatic rock was
reported during ~1,470–1,400 Ma (Dey et al., 2019). The felsic
magmatism engulfed pre-existing pelitic granulites; after that, it
remained as an enclave. Various P–T–tpaths have been proposed
from different localities within the CGGC, most of which represent
the clockwise paths (Figure 15), with the steep decompression
stages.
The geochronological constraints and evolution of the mafic gran-
ulite in the CGGC have not been resolved. Dey et al. (2019) reported
the first stage of metamorphism (1,450 ± 37 Ma) in mafic granulite
from the Dumka region of CGGC, and the second stage of metamor-
phism has occurred at ~950 Ma. In this study, the magmatic emplace-
ment age of mafic granulites has been revealed as a weighted average
207
Pb/
206
Pb age of 1,629 ± 6 Ma from the northwestern region
of CGGC.
9.2 |Age of the protolith and tectonic implications
The sedimentation period and their provenance, along with the post-
depositional metamorphic stages, play an essential role in uncovering
the tectonic history of the Indian landmass. The isotopic nature of U–
Pb in zircon from metapelites rocks plays a vital role in constraining
the sedimentation age and tectonic history after deposition (Corfu,
Hanchar, Hoskin, & Kinny, 2003; Sengupta et al., 2015). Pelitic rocks
are formed by the accumulation and diagenesis of the weathering
product of the pre-existing rocks. The analysis of U–Pb zircon dating
is the best way to constrain the protolith's age and sedimentation.
The youngest detrital zircon age of ~1,677 Ma shows the approximate
timing of the sedimentation period, and ~1,638 Ma represents the
first metamorphic event of the CGGC. The older age group has a
higher Th/U ratio (>0.2) and typically exhibits oscillatory-zoning,
which indicates that zircons were formed by the magmatic origin
(Scherer, Whitehouse, & Münker, 2007). However, various zircon
grains from pelitic granulite have less defined zoning features (weak
CL), as well as most of the studied zircon grains have low Th/U ratio
FIGURE 15 Pressure–temperature–time (P–T–t) evolution
history of the Pelitic granulites from the Chhotanagpur Granite Gneiss
Complex (CGGC) constrained by this study. The P–T ranges of
individual events have been obtained from phase equilibria modelling.
The apparent geothermal gradients and their tectonic implications are
adapted from Brown (2007). Available P–T–tpaths for the early
Mesoproterozoic and Neoproterozoic events as recorded from
various localities of the CGGC by the following: a and b. Dey
et al. (2020); c. Mukherjee et al. (2017); d. Dey et al. (2019);
e. Karmakar et al. (2011); f. Chatterjee (2018). The P–T–tpath
obtained by this study is marked red line, and star signs represent the
stages of P–Tconditions
20 KUMAR ET AL.
(<0.2), indicating the metamorphic origin of zircon (Rubatto, 2002,
2017; Singh, 2019).
The igneous zircons of metapelites from the Dumka region of the
NE CGGC show ages from 2,700 to 1,678 Ma (Dey et al., 2017) and
1,764 to 1,650 Ma (Rekha et al., 2011), suggesting a period of sedi-
mentation. This study has also found ~1,734 Ma to ~1,677 Ma age of
detrital domains from the NW part of CGGC. These geochronological
data suggest that NW and NE portions of the CGGC were received
sediments from the exact provenance of the Palaeoproterozoic age.
The sediments of pelitic granulites were deposited between
~1,677 Ma (Youngest detrital zircon) and >1,638 Ma (weighted mean
age of metamorphic domain), whereas simultaneously another mafic
magmatic emplacement event occurred. The pelitic granulites from
the NE of CGGC preserve three metamorphic events during ~1,640,
~1,450, and ~950 Ma (Dey et al., 2017; Rekha et al., 2011); similarly,
we have found a major metamorphic domain of ~1,638 Ma.
The geodynamic evolution of the CGGC is generally controversial
(see Mukherjee, Dey, Sanyal, Ibanez-Mejia, & Sengupta, 2019 and ref-
erences therein); however, it establishes one of the broadest studied
regions of the Indian shield. The geochemical data have been used to
constrain the tectonic setting between the oceanic island, continental
crust, and convergent margin rocks after establishing a relationship
between (Y/Nb)
N
versus (Th/Nb)
N
discrimination diagram (Moreno
et al., 2014), and all the pelitic granulites are located in the convergent
margin rock field (Figure 9a). The Zr versus Nb/Zr diagram (Figure 9b)
indicates that the protolith of pelitic granulites was encountered a
subduction-related tectonic setting (Thieblemont & Tegyey, 1994).
Similar tectonic affinity has been demarcated for granites from the
Gaya region of the Mahakossal Supracrustal Belt (MSB) (Yadav
et al., 2020; Yadav, Wanjari, Ahmad, & Chaturvedi, 2016); it has pro-
vided consolidated evidence for the protolith of pelitic granulites
derived from the MSB. The positive anomaly of Pb and negative Nb
anomaly have supported the collisional tectonic setting. The enrich-
ment of K, Th, U, Pb, and ΣHREE and the depletion in Nb, Sr, and Ti
of studied pelitic granulites are significantly involved in a subduction-
related generation of their protolith (Rudnick & Fountain, 1995;
Rudnick & Gao, 2003); this same trend has also been found from the
MSB granite intruded during ~1,800 to ~1,700 Ma. However, a similar
older age has been achieved from the study area, which has consid-
ered the MSB, and other terrains act as the provenance region from
where the CGGC basin received the sediments.
The geotectonic model (Figure 16) suggests that the Archean cra-
tons such as Bundelkhand Craton in northern and SC along with the
Baster Craton in the southern part were rifted during the late
Archean-Palaeoproterozoic period, leading to the development of a
new sedimentary basin. The rifted portion serves as a sink horizon for
sedimentation, where sediments arrive from various cratons and
mobile belts. Phase equilibria diagram of pelitic granulite has revealed
peak metamorphism, after which it follows the post-peak nearly ITD
path. A nearly ITD P–Tpath has characterized the continental collision
or over-thrusting (Cai et al., 2017; and references therein). We
inferred that the pelitic granulite from the study area followed
tectono-metamorphic evolutionary processes, in which subduction-
related tectonic activity influenced the crustal thickening (M
1
) and it
further followed to the exhumation of the crustal lithosphere (M
2
).
The emplacement of mafic magma in the study area was recorded
during ~1,629 Ma, providing solidary evidence of subduction tecto-
nism. Instead of this, another magmatic eruption was reported in a
nearby region on the northern extent of CGGC (1,690 Ma:
Chatterjee & Ghose, 2011), and substantial magmatic emplacement
was recorded in the Mahakoshal Belt (~1,700 Ma: Deshmukh,
Prabhakar, Bhattacharya, & Madhavan, 2017; Yadav et al., 2020).
FIGURE 16 Cartoon diagram showing
the stages of (a) the protolith of pelitic
granulites and deposition of sediments,
(b) M
1
stage of metamorphism of pelitic
granulite, which is present as patches and
simultaneous mafic magma intruded as the
protolith of mafic granulite within the
granitic gneisses of CGGC. CGGC,
Chhotanagpur Granite Gneiss Complex;
DOB, Dalma Ophiolite Belt; MGB,
Makrohar Granulite Belt; SNNF, Son
Narmada North Fault; SNSF, Son Narmada
South Fault (modified after Mukherjee, Dey,
Sanyal, & Sengupta, 2018; Yadav
et al., 2020)
KUMAR ET AL.21
Before the age of ~1,638 Ma, the rift basin was formed, and the oce-
anic environment developed; moreover, a variety of sediments were
deposited in this oceanic basin and further HP/MT pelitic granulites
evolved during ~1,629 Ma; it was due to the subduction of the oce-
anic lithosphere. The age of ~1,638 Ma is considered the oldest meta-
morphic (M
1
) event in pelitic granulites of the CGGC, which coincide
with the magmatic emplacement age of mafic granulites (~1,629 Ma).
A cartoonographic diagram has been constructed to show the various
evolutionary stages of the CGGC, in which the formation of oceanic
basin and sedimentation were reported at ~1,750 Ma and onward
(Figure 16a); furthermore, these sediments were consolidated to form
the pelitic rocks and underwent the first phase of metamorphism dur-
ing ~1,638 Ma, with the protoliths of mafic granulite being emplaced
over the same period (Figure 16b).
9.3 |Correlation of CGGC with the Columbia
Supercontinent
The Indian Peninsular shield has preserved a strong signature of the
Columbia Supercontinent assembly. It has been observed that the
evolutionary history of the Earth must have been a cycle of multiple
stages leading to the accretion and breakup of a Supercontinent
(Nance, Worsley, & Moody, 1988). The amalgamation of the Columbia
Supercontinent occurred between ~2,000 Ma and ~1,800 Ma, and
further breakdown processes began after ~1,500 Ma (Rogers & San-
tosh, 2002; Zhao, Cawood, Wilde, & Sun, 2002; Zhao, Sun, Wilde, &
Li, 2004). Several magmatic and metamorphic activities have been
reported in Late Palaeoproterozoic, and available palaeomagnetic data
suggest that the Indian shield has played a crucial role at the time of
Columbia Supercontinent construction. The position of the Indian
landmass in this supercontinent is highly debatable, and the timing of
CITZ is also regularly discussed (Acharyya, 2003; Roy & Prasad, 2003).
The E–W-trending CITZ belt preserves an orogenic crust of ~1,650–
1,600 Ma age. Geochronological data of magmatic pulses and meta-
morphic events have been used to correlate the CGGC and other
adjacent terrains. Metamorphism and magmatic activities coincided in
the CGGC around 1,600 Ma. They were also recorded in the Sausar
Mobile Belt (CITZ) (Bhowmik et al., 2014), Mahakoshal Belt (CITZ)
(Deshmukh & Prabhakar, 2020), CGGC (Sequeira, Bhattacharya, &
Bell, 2021), Aravalli Fold Belt (Bijusekhar, Yoshida, Santosh, &
Pandit, 2001), EGB (Bose, Dunkley, Dasgupta, Das, & Arima, 2011), as
well as in the SMGC (Chatterjee, Mazumder, Bhattacharya, &
Saikia, 2007). The SC and the North Singhbhum Fold Belt experienced
metamorphic activity between ~1,660 and 1,580 Ma (Pal &
Rhede, 2013; Rao, Aggarwal, & Rao, 1979); these pieces of evidence
suggest that they were tectonically active during the formation
of CITZ.
Late Palaeoproterozoic expansionary events have been recog-
nized worldwide, with similar ages being recorded from the Indian
Peninsular Shield, Western Australia (Bagas, 2004; Pirajno, Jones,
Hocking, & Halilovic, 2004; Sheppard et al., 2016), and the Napier
Complex of Antarctica (Kemp Land) (Halpin, Daczko, Clarke, &
Murray, 2013; Halpin, Gerakiteys, Clarke, Belousova, & Griffin, 2005;
Kelly, Clarke, & Fanning, 2002). In Western Australia, the Capricorn
orogeny represents the collisional boundary among the Pilbara and
Yilgarn cratons. This orogeny consists of medium- to high-grade
metamorphic basements as well as volcanic-sedimentary basins of
low-grade metamorphic rocks, for example, Yerrida, Bryah, and
Padbury basins (Cawood & Tyler, 2004 and references therein).
This evidence concludes that the tectonic episodes in the Capri-
corn orogeny between ~1,800 and ~1,600 Ma resemble those
recorded in the CITZ (Mohanty, 2010, 2012). However, these
observations conclude the fact that Greater India, Australia, and
Antarctica plates were amalgamated as the Columbia Superconti-
nent during the Palaeoproterozoic age.
10 |CONCLUSIONS
The significance of this communication provides many new pieces of
evidence regarding the tectono-metamorphic evolution of the
Daltonganj region of the northwestern CGGC:
1. The pelitic granulites from the northwestern part of the CGGC
preserve metamorphic events. Zircon U–Pb age dating of the
pelitic granulites showed that the approximated maximum deposi-
tional age of the protolith was ~1,677 Ma and the first phase of
metamorphism occurred during 1,638 ± 22 Ma.
2. The first metamorphism of the CGGC is only recorded in the pelitic
granulites. Phase equilibrium modelling has been used to calculate
the maximum P–Tcondition of M
1
metamorphism, which is
9.10 kbar/835C. Later metamorphic event (M
2
) has been success-
fully recorded at ~4.0 kbar/~790C with a clockwise isothermal
decompressive retrograde P–Tpath.
3. Zircon U–Pb age dating result of the mafic granulites shows the
weighted mean age of 1,629 ± 6 Ma as an age of magmatism of
the protolith, which coincides with the timing of M
1
metamor-
phism of the pelitic granulites (1,638 ± 22 Ma).
4. Investigations on the pelitic granulites indicate that their sedimen-
tary protolith was of a reworked nature, most likely from an origi-
nal diorite source. The sedimentation occurred along the
convergent margin under the subduction tectonic setting.
5. The zircon U–Pb studies decipher the late-Palaeoproterozoic geo-
tectonic events in the NE CGGC during ~1,638 Ma, leading to the
amalgamation of India, Australia, and Antarctica landmasses during
the creation of the Columbia Supercontinent.
ACKNOWLEDGEMENTS
We are thankful to the Director, Indian Institute of Technology (BHU),
for providing infrastructure and funds to complete this work. R. R.
Kumar is also grateful to the UGC-JRF scheme for providing financial
support for the present work. The authors express their gratitude to
Professor N. V. Chalapathi Rao and Dr. Dinesh Pandit from Mantle
Petrology Laboratory, Department of Geology (CAS), Institute of Sci-
ence, BHU, for providing the EPMA analyses facility. We are thankful
22 KUMAR ET AL.
to the Microscopy Laboratory (BHU) for providing the facility to cap-
ture the photomicrograph images. K. K. and K. D. are grateful to Profs.
T. Shibata and Y. Hayasaka for allowing them to use the LA-ICPMS
Facility at Hiroshima University. We are thankful to M. Santosh and
the anonymous reviewers for their constructive comments to improve
the manuscript.
CONFLICT OF INTEREST
The authors declare no conflicts of interest..
PEER REVIEW
The peer review history for this article is available at https://publons.
com/publon/10.1002/gj.4340.
DATA AVAILABILITY STATEMENT
Data will be available upon request.
ORCID
Ravi Ranjan Kumar https://orcid.org/0000-0003-2554-1375
Kenta Kawaguchi https://orcid.org/0000-0003-4495-7165
Shyam Bihari Dwivedi https://orcid.org/0000-0003-3159-6452
Kaushik Das https://orcid.org/0000-0002-2372-2095
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How to cite this article: Kumar, R. R., Kawaguchi, K., Dwivedi,
S. B., & Das, K. (2021). Metamorphic evolution of the pelitic
and mafic granulites from Daltonganj, Chhotanagpur Granite
Gneiss Complex, India: Constraints from zircon U–Pb age and
phase equilibria modelling. Geological Journal,1–27. https://
doi.org/10.1002/gj.4340
KUMAR ET AL.27
