The document summarizes key information about the Cuddapah Supergroup, a large Proterozoic sedimentary basin in India. It describes the stratigraphy, tectonic setting, structure, sedimentation, and stratigraphic relationships of the basin. The Cuddapah Supergroup consists of a 12 km thick succession of sedimentary and volcanic rocks deposited in the basin. Younger groups in the west are less deformed compared to the tightly folded Nallamalai Group in the east. Widespread magmatism occurred during deposition, including basalt flows, sills, and felsic volcanism dated between 1862-1583 million years ago.

1. Jai Narain Vyas University Jodhapur
Department of Geology
Cuddapah Supergroup
-
Submitted by:- Submitted to:-
Vasudev Choudhary Prof.K.L.Shrivastva

2. INDEX
1.INTRODUCTION
2.STATIGRAPHY
3.TECTONIC SETTING
4.STRUCTURE
5.SEDIMENTATION
6.STATIGRAPHY RELATION
7.AGE
8.ECONOMIC IMPORTANCE

3. CUDDAPHA SUPERGROUP
INTRODUCTION
There are fourteen major types of basins in India;
among these basins Cuddapah Basin is the one of the biggest and
most important for Economic geology.
The present study areas (Chitrial and Amrabad outliers) at Srisailam
sub – basin located in the Cuddapah Basin is situated in the eastern
part of the Dharwar Craton and is one of the largest Proterozoic,
intra-cratonic, sedimentary basins in India. Cuddapah Basin is
crescent shaped and covers an area of around 44 500 km2
with a
maximum length and breadth of 440 km and 145 km, respectively
(Chalapathi Rao, 1997), (Chatterjee et al., 1998). The basin is in
filled by a >10 km thick succession of igneous and sedimentary
rocks of the Cuddapah and Kurnool Groups (McKenzie et al., 1980).
This basin comprises five sub-basins VIZ. Chitravathi, Nallamalai,
Srisailam, Kurnool and Palnad.
The Cuddapah Basin is situated in the eastern part of the Dharwar
Craton and is one of the largest Proterozoic, intra-cratonic,
sedimentary basins in India. It is crescent shaped and covers an
area of around 44 500 km2
with a maximum length and breadth of
440 km and 145 km, respectively

4. In India we have 12 Proterozoic basins. They are as follows:
Proterozoic Basins of India
NAME OF BASIN AREA OF THE BASIN IN SQ.KM.
1. Vindhyachal 60,000
2. CUDDAPAH 45,000
3. CHATTISGARH 35,000
4. PAKHAL 10,000
5. INDRVATI 9,000
6. KALADGI 8,000
7. BHIMA 5,000
8. ABUJHMER 3,000
9. SUKMA 700
10. KHARIAR 250
11. AMPANI 220
12. KESAL 150

5. Location map of study area:
Andhra Pradesh
Andhra Pradesh
Nalgonda
Chitrial
Amrabad
Mahaboob nagar
Location map of Chitrial & Amrabad.

6. 2. Stratigraphy
Table 1. Geological succession of the area (after Saha and Ttripathy, GSI, 2012)
Nandyal Shale
Koilkunta
Limestone
Paniam Group
KURNOOL GROUP Owk Shale
Narji Limestone
Banganapalli
quartzite
----------Unconformity--------
SrisailamFormation
Nallamalai Group ---------Tectonic Contact--------
Cumbum Slate
Bairenkonda Quartzite
(=Nagari Quartzite)
CUDDAPAH SUPER GROUP
----------- Tectonic Contact---------
Gandikota
Quartzite
ChitravathiGroup Tadpatri Shale
Pulivendla
Quartzite
Papaghni Group Vempalle Slate
Gulcheru Quartzite
------- Unconformity-----------
-------
Archean Granite & gneisses
Lithology: 12 km thick volcano-sedimentary pile consisting of
Arenaceous, Argillaceous, Carbonates, and Volcanic
(basic and acidic)

7. Table 2. Paleoproterozoic magmatic events along with their geographical locations,
ages and nature of occurrence at variousstratigraphic horizons in the Cuddapah
Supergroup (by Sesha Sai et al., present work; modified after Nagaraja Rao et al., 1987).
SUPER STRATIGRAP
HIC MAGMATIC ROCKS IN LOCATION IN
GROUP / AGE AVAILABLE AGE DATA
SUCCESSION CUDDAPAH SUPERGROUP CUDDAPAH BASIN
GROUP
Kurnool Group (Kurnool and Palnad sub basins)
~~~~~~~~~~~~~~~~~~~~Unconformity~~~~~~~~~~~~~~~~~~~~
Srisailam
Quartzite
Conglomerate,
arenite, No Igneous rocks are reported within Srisailam Quartzite
siltstone sequence
Tuffaceous sequences /
Nallamlai
group
associated (lapilli rosette) baryte Mangampeta area in
Cumbum /
Pullampet (Karunakaran, 1976; Pullampet sub basin.
Formation Neelakantam, 1987; Deb and (Southern part of the NFB)
Bheemalingeswara, 2008) No age data available
Shale, dolomite and ultrapotassic rocks (Reddy, 1999) Rajampet areas in
arenite sequence Pullampet sub basin.
Mafic sills and felsic volcanics (Southern part of the NFB)
(Das and Chakraborty, (2017)
Bairenkonda / Nagari Quartzite Southern part of NFB No age data available
Conglomerate and arenite sequence Rajampet area
~~~~~~~~~~~~~~~~~~~~Unconformity~~~~~~~~~~~~~~~~~~~~
Cuddaoah
Suoergroup
Gandikota
Quartzite
Olivine gabbro (Babu and Satyanarayana, 2007 b) No age data available
Shale and arenite
Paleoprotoro
zoic
Chitravati
Group
Olivine Gabbro Velupucherla section No age data available
Felsic tuff - 1862 ± 9 Ma
Rhyolite / Felsic tuff / (Sheppard et al., 2017)
Tadpatri
Formation
Albite rich volcanic Mallela section
Ultramafic sill
Shale, dolomite,
chert,
1817±24 Ma Rb-Sr
jasper, shale and arenite
Bhasker Rao et al. (1995)
sequence
Ultramafic-mafic sills Peddakudala-Pulivendla- 1.9 Ga 40
Ar-39
Ar,
(contemporaneous with basin Velpula section in SW part (Anand et al., 2003)
evolution) of Cuddapah basin 1885.4±3.1 Ma U-Pb
(French et al., 2008)
Pulivendla
Quartzite
Conglomerate and No Igneous rocks reported in Pulivendla Quartzite
arenite sequence
~~~~~~~~~~~~~~~~~~~~Disconformity~~~~~~~~~~~~~~~~~~~~
Basic flows, felsic tuff, Mafic
Papaghni
Group
pyroclastics and mafic sills
1841±71 Ma K-Ar
Vempalle Formation Rai, et al., (2015) Pb-Pb age of Kuppalapalle-Vemula- (Murty et al., 1987)
Dolomite, chert and 1900-2000 Mafor dolomitisation Lingala-Lopatnutala 1583±143 Ma Rb-Sr
P
A
P
A
G
p
a
p
a
p
H
A
N
I
siltstone sequence and uranium mineralisation section in SW part of basin (Crawford and Compston,Gulcheru Q uartzite Initiation of sedimentation Westernmargin of
Zachariah et al., (1999) 1756 ± 1973)
29 Ma, uranium mineralisation
in Vempalle Formation
Conglomerate and ~ 2.1 Ga Gulcheru Red beds Cuddapah basin -
arenite sequence (Sesha Sai et al., 2016 a)
~~~~~~~~~~~~~~~~~~~~Nonconformity~~~~~~~~~~~~~~~~~~~~
Archaean granite-greenstone basement of eastern Dharwar craton

8. Table 3. Chronostratigraphic illustration of the Paleoproterozoic magmatic
rocks in various stratigraphic horizons in theCuddapah Supergroup. Litholog
not to scale, (modified after Nagaraja Rao at al., 1987).
Papaghni Group
King (1872) has observed that the basic flows, along
with some igneous rocks remarkably follow bedding plane (sills) in the
lower Cuddapah. Vesicular tholeiitic basalt flows and basic sills represent
prominent mafic magmatism associated with the Vempalle formation
within the Papaghni sub-basin. Crawford and Compston, (1973) provided
an Rb-Sr age of 1583 ± 147 Ma for the basic lavas from Vemula area in
south-west part of the Cuddapah basin. A Pb-Pb radiometric age of 1756
± 29 Ma has been interpreted as the timing of uranium mineralisation in
the Vempalle formation with predominantly carbonate sequence
(Zachariah et al., 1999). Pyroclastic volcanism in the Papaghni sub-basin
has been reported from the south-west part of the Cuddapah basin
(Sesha Sai, 2014). Geochemical studies (Chakraborty et al., 2016)
suggested that basic flows in the Vempalle formation resulted due to
low degree of partial melting of a mantle peridotite source.
Chitravati Group
Widespread Proterozoic magmatic events were
recorded in the Tadpatri formation of the Chitravathi Group (Nagaraja
Rao et al., 1987; Bhasker Rao et al., 1995; Anand et al., 2003; French et
al., 2008; Chakraborty et al., 2016; Sheppard et al., 2017). Disposed

9. parallel to the basin configuration in its southwestern part, the NNW-SSE
to NW-SE trending ultramafic-mafic sills (Sesha Sai, 2011) and
interbedded felsic magmatic rocks are contemporaneous with the
sedimentation, and form part of the magmato-stratigraphy in the
Tadpatri Formation with dolomite-shale sequence. During the course of
cut-off trench excavation near Simhadripuram large sized spindle shaped
bodies resembling pyroclastic (5mm to 500mm diameter) were observed
in Tadpatri formation (Babu and Satyanarayana, 2007 a). The basalt
flows of Vempalle Formation (e.g., Srikantia, 1984; Murthy et al, 1987;
Chatterjee and Bhattacharji, 2001; Chakraborty,et al., 2016) represent
the early stage of volcanism in the Cuddapah basin. Incidentally, the
basic volcanic flows are not seen in the stratigraphic horizons above the
Papaghni group. However, felsic volcanics and fine-grained albite rich
are reported rocks in Tadpatri and Nallamalai groups (Sesha Sai et al.,
2016b; Das and Chakraborty, 2017. In a recent geochronologic study,
Sheppard et al., (2017), indicated an age of 1862 ± 9 Ma for the felsic
tuff in upper part of Tadpatri sequence in Chitravathi Group. A
concealed body of olivine gabbro has been intersected in borehole
during drilling at exit portal of Gandikota Tunnel, upstream of Gandikota
Dam.
Nallamalai Group
The southern part of the Nallamalai sub basin, is
characterized by the presence of extensive sequences of dolomite and
argillites with intercalated carbonaceous - variegated tuffaceous rocks
(see GSI, 1981; Nagaraja Rao et al., 1987). The Mangampeta baryte
deposit (Neelakantam, 1987), in Pullampet sub basin is perhaps the
world’s largest single bedded baryte deposit.
Karunakaran (1976) ascribed a volcanogenic origin for the bedded
baryte near Mangampeta. Deb and Bheemalingeswara (2008) suggested
the role of barium rich hydrothermal solution in submarine conditions
with prolific biologic activity for the origin of the bedded baryte.
Presence of fine dusty opaque material and two generations of pyrites
and detrital clastic components are noticed in the carbonaceous shale of
Pullampet Formation (Sesha Sai and Rajesham, 2010). Manikyamba et
al., (2008) studied the geochemical aspects of black shale in Cuddapah
basin. Ultra-potassic rocks, mafic sills and rhyolite have been recorded in
the Pullampet sub basin (Reddy, 1999; Das and Chakraborty 2017).

10. Tectonic Setting
The Cuddapah Basin is an epicontinental
platform cover overlying an Archaean basement. The basement
contains two major tectonic zones. To the west is a cratonic zone,
comprising the· Peninsula Gneisses and several greenstone belts
of the Dharwar Supergroup and older Sargur Schists . To the east
is a mobile belt, the "Eastern Ghats" part of the well-known
charnOCkite belt of India and Ceylon. This belt is a
polymetamorphic belt, subjected to successive episodes of
medium to high-grade (granulite) metamorphism between 3100-
450 m.y. ago. In the basement, we only saw representatives of the
Peninsula Gneisses, and younger intrusive granites. The most
impressive feature is the extreme compositional uniformity of the
gneisses over hundreds of kilometres it is difficult to imagine them
being metasedimentary. The other feature is very well-developed
and exposed dolerite dykes, several ages of which intruded the
craton before the Cuddapah Basin was developed. The Cuddapah
Basin itself contains two distinctive tectonic belt boundary
between them corresponding to that between the underlying
basement belts, just described The western block is mildly
deformed with flate lying Kurnool Group unconformably overlying
gently-dipping Chitravati and Papaghni Groups. The eastern belt
contains tightly overfolded and overthrust Nallamalai Group rocks.
There is almost no overlap between th~ depositional belts of these
sequences; they virtually represent quite separate basins, with the
younger thrust over the older.

11. STRUCTURE:
Structurally and tectonically the area is highly disturbed.
Western part is flat lying and Eastern part is folded, faulted and thrusted.
The undrformed western sub-basins give way to the highly deformed
nallamlai fold belt in the east. Low amplituted open folds in the west
become tight to isoclinals and doubly plunging fold in the east. The
drape around the basement inlier like iswarakuppam dome or intrusive
granite like vellature granite. The fold axial traces curve toward south in
the nagari quartzite , which are displaced to east alomg the karkambadi
foult. Nallamlai fold belt is affected by three phases of deformation. D1-
structure are tight to isoclinals fold;. D2-structure include NE trending
tight to open fold;. D3-folds trending E-W overprint to earlier structure
and are involve in the contractional deformation of nallamlai and palnad
sub basin.
The folding and thrust foulting are suggested to be post Kurnool because
of overriding relations of nallamlai fold belt into the flat lying sediment
in the western sub basin. It is likely, however, that the thrusting and
folding is multi-episodic, the time sequence being uncertain.
SEDIMENTATION
The Cuddapah Supergroup sediments deposited
non – conformably over peninsular gneisses and Dharwar comprises
conglomerate, quartzite, limestone, dolomite and shale.

12. Stratigraphic Relationships
The nallamlai group much more deformed
than the older Papaghni and Chitravati Groups, and has widespread
cleavage development. This is apparently anomalous to some people,
but can be explained by the fact that the Nallamalai Group overlies
the eastern mobile zone, while the older units overlie a creaton The
stratigraphic relationship is crucial, so we attempted to confirm it. a
straight stratigraphic contact apparently occurs only a short belt near
Cuddapah. There is clearly a marked angular discordance between the
units here, but the question arises whether it is an unconformity or flat-
dipping thrust. Attempts to reach the contact on the ground were
thwarted by ·time. Several efforts to interpret air photos of the contact
were foiled by government policy which restricts access to air
photographs, apparently a defence policy, and a considerable hindrance
to both our work and. the local geologists. One can only assume that the
relationship is correct. It is certainly the easiest interpretation of the
available 1:250 000 map, assuming that the mapping is correct. The
interpretation requires that the increase in deformation and
metamorphism takes place rapidly,' over a short distance.
AGE:-
Pri-cuddapah basement dykes are of two prominent ages at 2100 and
Ma. Rb-sr dating of dolerite and picritic sills of pulivendla formation
gives an age of 1800Ma. K-Ar ages of some dolerite dykes underlying the
cuddapah basin are also similar at 1800Ma indicating later thermal
impress. This date also correspond to the ages of U mineralisation in
lower cuddapah carbonate at 1800Ma. Velluture granite from eastern
margin of the basin gives Rb-Sr age of 1575Ma, and vinukonda granite in
the victinity at 1615 Ma, suggesting an intrusive event at 1600 Ma .
some dolerite dykes of 1650 Ma age belong to this event. The age of
galena mica cumbum shales 1350 to 1450 Ma, mengampeta felsic tuff
1470 Ma, chelima lamporite1350 Ma, suggest thermal event in the basin
around 1350-1450ma. Younger event recordet by mineral ages range
from 500 to 950 Ma, which may span the time of evolution of Kurnool

13. and palnad sub basin. Kimeberlite in the granitic basement near the
cuddapah basin generally age of 1050 Ma. Dimendiferous conglomerate
having kimberlite as its source for diamond , and Rb-Sr age of 980 ma for
dolerite dykes intruding Kurnool sub basin suggest neoprotorozoic age
of Kurnool group. The paleoprotorozoic age of papaghni sub basin the
early mesoprotorozoic age of the rest of the cuddapah succession,
neoprotorozoic age of Kurnool group are comparable with the
chronology of bijawar Gwalior and vindhyan successions surrounding the
bundelkhand craton.
ECONOMIC IMPORTANCE
Uranium- found in vempalli formation of papaghni group , host rock is
phosphatic dolostone, promising,mineallisation at Tumalapalle, rachak-
untapalli and gadankipalli
Barites- found in pullampet formation of nallamlai group at mangameta ,
form the single largest deposit of bedded barites in the world , has been
declared as a national geological monument
Diamond- Found as placer in banganapalle quartzite of Kurnool group
Limestone and dolomite
Chrysotile- asbestoes and steatile – vempalle formation of papaghni
group
Ornamentle stone like jasper , chert , etc.
Pb- zn deposit-hosted by dolomite , found in pullampet formation of
nallamalai group at agnikundala , varikunda.