Characterization of Hydrocarbon Bearing Jardepahar Porcellanite Formation, Vindhyan Basin

Characterization of Hydrocarbon Bearing Jardepahar Porcellanite Formation, Vindhyan Basin | Research Square window.SnipcartSettings = { analytics: { enabled: false } }; (function() { var accessVector = localStorage.getItem('access_vector') || ''; window.dataLayer = window.dataLayer || []; if (accessVector) { window.dataLayer.push({ user: { profile: { profileInfo: { snid: accessVector } } } }); } })(); (function(w,d,s,l,i){w[l]=w[l]||[];w[l].push({'gtm.start':new Date().getTime(),event:'gtm.js'});var f=d.getElementsByTagName(s)[0],j=d.createElement(s),dl=l!='dataLayer'?'&l='+l:'';j.async=true;j.src='https://www.googletagmanager.com/gtm.js?id='+i+dl;f.parentNode.insertBefore(j,f);})(window,document,'script','dataLayer','GTM-K279D39R'); Browse Preprints In Review Journals COVID-19 Preprints AJE Video Bytes Research Tools Research Promotion AJE Professional Editing AJE Rubriq About Preprint Platform In Review Editorial Policies Our Team Advisory Board Help Center Sign In Submit a Preprint Cite Share Download PDF Research Article Characterization of Hydrocarbon Bearing Jardepahar Porcellanite Formation, Vindhyan Basin Rajesh Pandey, Sanjay Ojha This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-3957834/v1 This work is licensed under a CC BY 4.0 License Status: Posted Version 1 posted You are reading this latest preprint version Abstract The commercial gas discovery has been established form Paleo-proterozoic Jardepahar Formation of Son valley sector, Vindhayan Basin. The geochemical, sedimentological and source rock analysis of the cutting samples collected during the drilling of Hatta#D were carried out, to comprehend the nature of source rock, their petrological characteristic. The geochemical and electro-log signatures help us to divide the porcellanite of Jardepahar Formation in to three cherty dominated units and a dolomitic limestone unit. Similar observations have been registered from petrographic studies, the bottom units is massive chert layer, middle unit is banded chert (limestone bands) and the upper unit is again massive with the interbed of shale. The middle unit has drawn lead attention, due to hydrocarbon discovery, it consists of amorphous silica interbedded with limestone with along with carbonaceous matter and micro-nano scale fractures. Textural characteristics of clasts indicates very limited transportation. The middle unit shows, higher biological productivity and better hydrocarbon source facies as compared to the lower and upper units, which is gas bearing in Hatta field of Oil and Natural Gas Corporation (ONGC). The sediments were derived from high K felsic to intermediate volcanic source (s) from active continental margin, deposited in anoxic environment. The trace elements postulate absence of biogenic fractions and negligible amounts of chemical alteration. The middle unit has the source potential and also act as reservoir with the dolomitic limestone as top seal. Vindhyan Basin Hydrocarbon Geochemical Source Rock Figures Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 Figure 8 Figure 9 Figure 10 Figure 11 Introduction Vindhyan Basin, by virtue of its age poses a number of challenges and uncertainties in exploration. The hydrocarbon exploration of Son Valley started in late eighties in the major structural highs (Damoh, Jabera, Kharkhari) targeting the deeper stratigraphic units (Kajrahat and Jardepahar formations). However, there was no significant success in this initial phase except in Jardepahar Formation in well Jabera#A. Well Jabera-A, a rank wildcat well, was drilled on Jabera dome, which flowed hydrocarbon gas from three zones tested within Jardepahar Formation and made a discovery of gas for the first time in the Vindhyan Basin. The gas was analyzed to be wet and thermogenic in nature and declared non-commercial due to lower flow rate. Encouraged by this lead, Wells Damoh-A and Kharkhari-A were drilled on structural plays and were found to be dry. Subsequently, the drilled well Jabera-B established the extension of gas bearing layers of Jabera-A within Jardepahar Formation besides another likely gas bearing layer within Kajrahat Limestone section. The well provided vital exploratory leads for evaluation of deeper petroleum systems in the basin. Efforts to capitalize initial successes could bear fruits through the recent significant discovery of gaseous hydrocarbons within the Proterozoic Jardepahar reservoir in the Hatta area (NELP Block VN-ONN-2009/3) of Son Valley, Vindhyan Basin. Subsequent activities to capitalize the Hatta lead have proved the viability and have given a major fillip to exploration program in the Indian Proterozoic Basins, particularly in the Vindhyan Basin. Vindhyan Basin has been studied thoroughly in terms of its geophysical, sedimentological, and palaeontological evolution (c.f., Adnan et al., 2015 ; Banerjee and Banerjee, 2010 ; Banerjee et al., 2015; Bengtson et al., 2009 ; Bose et al., 2015 ; Chakraborty, 2011 ; Kumar, 2016 ; Mishra, 2015 ; Prasad and Asher, 2016 ; Prasad and Rao, 2006 ; Sarkar et al., 2004 ; Samanta et al., 2016 ; Sur et al., 2006 ; Verma and Shukla, 2015 ) while geochemical and isotopic studies are limited that have tried to address sediment provenance, tectonic evolution and sub-basin connectivity (Shukla et al., 2019 ). The Porcellanite is a vital constituent of Lower Vindhyan rocks, due to the recent discovery of hydrocarbon gases, it is pertinent to evaluate the nature of rocks and their physiognomies. It is the oldest porcellanite deposit in India (Mondal and Singh, 2017 ). The term porcellanite is not very well defined; it is an argillaceous or calcareous chert with fine-grained acidic vitric tuff compacted with secondary silica (Mehrotra and Banerjee, 1982). Based on surface sample analysis it has been interpreted as the vitric tuffs are derived from felsic volcanic rocks with a high content of silica release in oceanic basins, which has facilitated chert precipitation; these cherts are also associated with tephra, tuff, or ignimbrite (Mondal and Singh, 2017 ). Mondal and Singh ( 2017 ) have established the presence of four types of porcellanite, based on its colour, i.e., yellow porcellanite, black porcellanite, white porcellanite, and green porcellanite, while the old workers have classified the Vindhyan porcellanite in to three units based on textural characters: banded, spotted and massive (Mehrotra and Banerjee, 1982). The sub-surface data from the drilled well ahs also suggested three units with a dolomitic limestone unit. The presence of slump folding and convolute lamination observed during field study also supports the theory of sub-aqueous eruption and active tectonics during transportation and deposition of the sediments (Mondal and Singh, 2017 ). The geochemistry of porcellanite, including trace elements, represents the average composition of parental volcano-clastic materials responsible for the deposition of fine grained, massive to banded, light grey to olive green, hard, waxy lusture and glassy nature porcellanite. Hard rock geochemistry is also considered an excellent proxy for provenance, tectonics, or palaeoclimate interpretation (Nesbitt and Young, 1982 ; Roser and Korsch, 1988 ; Li et al., 2012 ). As the rocks are Proterozoic, rapid alteration of feldspar and leaching of accessory minerals within interbedded limestones may result in an erroneous interpretation of provenance (Blatt, 1985 ), but the impermeable character of fine grained vitric tuff can easily retain and preserve the original signatures of tuffaceous material, which were erupted, transported, and deposited in an aqueous condition (Srivastav, 1997). The high biological productivity (organic carbon), during Palaeoproterozoic-Mesoproterozoic (2.0-1.6 Ga) may lead the generation of adequate source rocks (Condie et al., 2001 ). The giant oil discoveries of Canada, Oman and Russia (Craig et al., 2013 ) have intensified interest in the Mesoproterozoic Vindhyan Basin. This article provides an understanding to the origin and evolution of the Jardepahar Porcellanite Formation of Vindhyan Basin, primarily from a geochemical, petrographic and source rock perspective. General Geology The Vindhyan basin is the second largest Proterozoic intracontinental basin that developed in the central part of the Indian shield, surrounded by the Aravalli-Delhi fold belt in the west and north west, the Satpura orogeny in the south and east, and Bundelkhand granite in the north (Chakraborty et al., 2012 ; Singh and Chakraborty, 2021 ). The Indogangetic plain in the northern part and the Deccan volcanic in the south-western part conceal a major part of the basin (Krishnan, 1968 ; Gopalan et al., 2013 ); hence, the exact limit of the basin is uncertain. The exposed area of the basin is around 178,000 km 2 , with a more than 4500 m thick siliciclastic-carbonate package of mildly deformed and unmetamorphosed sediments (Tandon et al., 1991 ). The Vindhyan basin has been lithostratigraphically subdivided into four groups, in stratigraphic order these are: the Semri Group, the Kaimur Group, the Rewa Group, and the Bhander Group (Fig. 1 ). The current well taken for this study is located in the son valley sector, with a primary focus on the Jardepahar Formation belonging to the Semri Group of Lower Vindhyan (Fig. 2 ). The Vindhyan Basin is mostly unmetamorphosed siliciclastic and carbonate rocks with minor deformation (Turner et al., 2013). Pb-Pb age are used to establish the ages of the Lower and Upper Vindhyan rocks, the carbonate sedimentation of the Kajrahat Formation initiated around 1729 ± 110 Ma ago in this basin (Sarangi et al., 2004 ) while Bhander Formation carbonates were deposited around 900 Ma ago based on Pb-Pb ages suggest closure of the basin (Gopalan et al., 2013 ). The Bundelkhand Granite Massif located at the central part of the basin divides the basin into the son valley sector in the east and the chambal valley sector in the west (Rajasthan). Metavolcanic and metasedimentary supracrustal sequence of the Mahakoshal and Bijawar Group occurs as a linear belt (Das et al., 1990 ) and are located towards southeastern edge of the basin. In the Rajasthan sector (chambal valley), most of the Vindhyan rocks are undeformed, except near to the Great Boundary Fault, where vertically dipping beds and large scale folded strata are observed (Gilleaudeau et al., 2018 ). Semri Group comprises a repetitive section of clastic and carbonate sequences with the presence of volcaniclastic unit (Jardepahar Formation), deposited within shallow marine (Banerjee, 1974 ) to deep marine (Chakraborty et al., 1996b). The oldest carbonate unit in the eastern sector is Kajrahat Limestone which shows development of stromatolites (Kumar et al., 2002 ) with large fan-fabrics in the upper part (Sharma and Kumar, 2012 ). The carbonate unit is deposited under subtidal to supratidal conditions (Banerjee, 1974 ). The intraformational conglomerates indicates repetitive transgression and regression (Kumar et al., 2002 ). Presence of Gypsum layers indicates an evaporative condition (Aktar, 1996 ). The stratigraphic equivalent of Kajrahat Limestone is Bhagwanpura Limestone in the Rajasthan sector (Prasad, 1984 ; Banerjee and Chopra, 1986 ). Bhagwanpura Limestone is extensively dolomitic in nature with localized microbialites (Ray et al., 2003 ). The final phase of Lower Vindhyan is represented by the carbonate sedimentation of the Rohtas and Nimbahera Limestone from the Son Valley and Rajasthan sector, respectively. In the Son valley, the Rohtas Limestone represents rhythmite-like intercalations between thin bedded limestone and shale with poorly developed columnar stromatolites (Kumar, 1977 ), deposited under subtidal to intertidal settings (Aktar, 1996 ). The Nimbahera Limestone from the Rajasthan sector is massive in nature and devoid of stromatolites and is deposited as a transgressional sequence (Prasad, 1981 ). A thick silicified tuff unit, occurs in the Semri Group of Son Valley sector i.e. Porcellanite Formation, suggests active volcanism in the near vicinity of the basin. The Palri Shale of the Chambal Valley sector also indicate the presence of porcellanite beds has been considered an equivalent of Jardepahar Porcellanite (Raza et al., 2002 ). Methodology The cutting samples collected during drilling of well Hatta#D were taken for the current study. Around 50g of samples from each 5m interval were washed and dried. Out of them, few representative samples were taken for thin section preparation and petrographic analysis. Remaining samples were introduced into the Rockwash machine at the first washing station, where they received a fixed dose of Quckwash detergent and were gently agitated for 90 seconds under running water. No solvents are used in the Rockwash sample washing process. The samples are then conveyed to the second washing station and rinsed in running water for a further 90 seconds to remove any remaining material from the surface of the cutting sample grains. Samples were then automatically conveyed to the drying modules, where they received 90 seconds of drying at each of the six drying stations. Later on, samples were dried at a temperature of less than 40°C. A washed and dried cutting sample was analysed using a Niton XL3T GOLDD + handheld XRF analyzer. Samples of a standard reference material (SdAR-M2 metal-rich sediment) were analysed during each sequence of analyses ( Appendix-1 ). Rock eval analysis is used to evaluate their free hydrocarbon content as well as petroleum potential to identify various potential or effective petroleum source rocks as well as potential accumulation intervals or zones in the area under study. Two state-of-the-art Rock-Eval-6 (Turbo model) instruments are available in the geochemistry lab of KDMIPE, ONGC. The results of the Rock Eval analysis provide data that are used to assess petroleum potential, organic matter type, extent of maturity of source rocks, and gravity of oil generated from sediments ( Appendix-2 ). Result and Discussion Geochemical Analysis: The major and trace element geochemistry helps us to establish the basinal characteristic during the deposition of the formation. The distribution of major element concentration in the entire formation divide the entire formation into three units. The middle unit is characterised by relatively lower MgO, Al 2 O 3 , SiO 2 , CaO, Fe 2 O 3 and higher K 2 O as compared to the top and bottom units (Fig. 3 ). Relatively higher concentrations of U, Th and Rb in the middle unit indicate the presence of organic substances, which may be precipitated with phosphates, glauconite and clay to form sedimentary rock. The higher concentration of Zn in the middle unit indicates high organic matter flux and reducing conditions (Tribovillard et al., 2006 ). A higher Si/Al ratio in the middle unit reflects the clastic influx with high to moderate energy condition (Riquier et al., 2007 ). It also supports the concept of high biological productivity in the middle unit as compared to the upper and lower units. The Zr/Rb ratio indicates the upper unit has coarser material followed by the middle and lower units, which also supports the textural interpretation (banded, spotted and massive) of three units in the Jardepahar Formation. Significant fluctuations are recorded in the abundance of major element concentrations. SiO 2 concentration varies from 40.22 to 61.42 wt % with an average of 51.77 wt %. Similarly, wide variations can also be observed in Al 2 O 3 (12.20 -25.28 wt %) and K 2 O content (0.94–7.51 wt %) with their averages being 18.10 wt% and 4.32 wt% respectively (Fig. 4 ). Harker diagrams shows increasing or constant trends in Fe 2 O 3 , MgO, Al 2 O 3 , CaO, K 2 O and TiO 2 with increasing silica indicates there was minor fractionation during or after deposition of the volcaniclastic sediments. The enrichment of potash (K) advocates andesite genesis/andesitic volcanic sources (Price et al. 1999 ; Winter, 2001 ; Zernack et al. 2012 ). The rocks exhibit higher TiO 2 content (0.08–1.36 wt%), and the ratios of Al 2 O 3 /TiO 2 indicates that the porcellanite ashes are derived from felsic to intermediate igneous source rocks. Provenance indicator diagrams (TiO 2 (wt%) versus Zr (ppm) also suggest the source rock for the porcellanite is acidic to intermediate volcanic rock (Hayashi et al., 1997 ) (Fig. 5 ). In addition, U/Th vs. V/Cr indicates, the most oxygenated conditions met during the porcellanite deposition, corroborated with the GOE (great oxygenation event) from 2000Ma-1700Ma (Large et al., 2022 ). The positive correlation of Fe and Ti indicates the presence of iron oxides i.e. magnetite and ilmenite, which are present in the interstitial spaces of plagioclase minerals (Fig. 6 ). Geochemical and Nd isotope signatures of Jardepahar/Deonar Porcellanites suggest that the volcanic tuff and pyroclast are derived from an Andean-type arc originated, due to collision between Bundelkhand Craton and Bhandara/Bastar Craton (Chakrabarti et al., 2007). The Geochemical signature Deonar and Chopan Porcellanite Formation suggests the sediments are derived from the mixing between mantle-derived rocks and average continental crust, under a continental rift environment (Mishra et al., 2017a , b ). This chemical characteristics indicates that the Jardepaher has mixed volaconogenic precursors. The concentrations of terrigenous proxy elements (Ti, Cr & Zr) in Vindhyan porcellanite are compared with Al 2 O 3 , which shows moderate to low correlation coefficients, i.e. 0.50, 0.126 and 0.143 respectively. It indicates that elements were fixed without magmatic differentiation along with the deposition of volcano-clastics with later stage minor alteration. The trace element concentration in the rocks are a good indicator of depositional dynamics along with provenance. Enrichment of Mo and U in the middle and lower parts of the formation indicates that the sediments were likely enriched in O 2 at the time of deposition of the porcellanite (Lyons et al., 2003; Algeo and Maynard, 2004; Tribovillard et al., 2005 ). Negative correlation coefficients of Ba (-0.093), Ni (-0.019) and Cr (-0.019) with respect to Al2O3 indicate the absence of biogenic fractions and sediments have suffered negligible amounts of chemical alteration in worm and humid environments ((Brumsack, 1989 ; Werne et al., 2002 ; Sageman et al., 2003 ; Algeo and Maynard, 2004; Tribovillard et al., 2005 ; Hu et al., 2020 ; Singh and chakraborty, 2021 ). Sedimentological Study: Jardepahar Porcellanite mainly consists of banded and massive chert with shale, limestone and ash beds. Shale is dark grey, hard, compact and feebly calcareous. Chert is fine grained, massive, banded, light grey to olive green, hard, waxy lustre, non-calcareous and glassy in nature. It belongs to vitric tuff to vitric crystal tuff class of Pettijohn (1957) and O’Brien (1963). Limestone is grey to off-white, hard and compact. Petrographic analysis shows vertical and horizontal fractures. These fractures are filled with argillaceous matter along with few silt size quartz grains and sparite (Fig. 7 A-D). Megascopic analysis shows alternation of chert, limestone and ash beds. Ash bed is white and black, crenulated and soft. Petrographically, Porcellanite consists of amorphous silica with presence of dark black coloured carbonaceous matter along with small-scale fractures. Volcaniclast shows angular to sub-angular volcanic Quartz and Feldspar grains along with chert and glass shards. Angularity of grains indicates short distance transportation (Fig. 8 ). Extensive dissolution of Feldspar along cleavage planes into sericite and at places kaolinite is noted (Fig. 9 A). Limestone reveals dolomite and recrystallized limestone. Dolomite microfacies consist of carbonaceous matter along with few feldspar grains. It also shows stylolamination filled with carbonaceous matter and spar filled vein. Profuse fractures and iron cement is also observed in the Dolomite facies. Glassy texture and patchy calcite cement has been observed in porcellanite (Fig. 9 B). The micro-scale fractures present in the Jardepahar Formation irrespective of lithology act as reservoir for the entrapment of hydrocarbons. Electrolog study: Electrologs helps to discriminate the porcellanite into three cherty lithounits and one dolomitic-limestone unit. The bottom most lithounit-I represents blocky log signature and is dominated by massive and flaky chert with very few intervals of ash bed and carbonaceous shale. The lithounit-II is characterised by fining upward log motif followed by coarsening upward trend on electro-log and this unit is characterised by banded porcellanite and limestone, the limestone thickness increases towards the top within this unit. Lithounit- III is separated by thick recrystallized dolomitic limestone from unit-I and unit-II and is dominated by ash beds, massive porcellanite and carbonaceous Shale (Fig. 10 ). Source Rock Analysis: The rock samples from the Jardepahar Formation were dried, crushed to powder and screened through BSS 60 mesh sieve. The crushed samples were analysed on Rock-Eval 6 for evaluation of source rock potential, quality and maturity. In the Jardepahar Porcellanite Formation, 13m source sequences are found in the depth intervals of 2171-2174m and 2180-2190m with fair to very good remaining hydrocarbon generation potential (Avg S2: 4.9 mg HC/g rock; ranges from 2.2–8.82 mg HC/g rock) and good to excellent organic richness (Avg TOC: 2.72%; ranges from 1.41–4.1%). In the identified source sequences hydrogen index values range from 154-207mg HC/g TOC (Fig. 10 ). Thermal maturity, Tmax: 434–436°C has been observed in these depth intervals. The rest of the samples indicate poor remaining hydrocarbon generation potential. The presence of a very high oxygen index is probably due to the great oxygenation event that occurred during Proterozoic time (Large et al., 2022 ), which brought the O/C ratio into the Type-III kerogen category on the Van Krevelon diagram (Peters, 1986 ; Nandy et al., 2015; Pandey et al., 2019 ). Conclusions The elctrolog characters, sedimentary nature and geochemical tracer elements suggest that the Jardepahar porcellanite Formation can be divided into the three units (upper, middle and lower). The middle unit has lithological heterogeneity and contains complete elements of insitu petroleum system. The petrological attributes and whole rock geochemistry of Jardepahar porcellanite demonstrate that the precursor for cherty bands/vitric tuff are andesitic to felsic nature, high K indicates andesitic volcanism resulted due to active continental margins. The top unit has coarser grain clasts represents higher energy condition that decreases towards the bottom unit (unit-I). The Harker diagram suggests very limited magmatic differentiation and fractionation within the source rock. The paleoclimatic condition at the time of deposition was oxic (lower to middle unit) to dysoxic (upper unit), with a moderate degree of chemical weathering. The middle and upper unit shows presence of organic matter along with micro and nano fractures. The organic matter indicates its humic character and Type III variety of kerogen, due to poor hydrogen content, extremely low H/C ratio and higher oxygen index. The presence of source and reservoir facies within the middle and upper unit designate it as an insitu tight gas petroleum system. Declarations Conflict of interest statement The interpretation provided in this research paper are the view of authors only, it does not have any relation with the organization they belong. The authors do no have any financial support or funding from any government / private agencies. Author Contribution Dr. Rajesh Pandey: Data analysis, figure prepration and writing ManuscriptDr. Sanjay Ojha: Data analysis, concept buildup and formatting of Manuscript Acknowledgment: Authors are grateful to the management of ONGC for giving permission to publish this work. Authors also acknowledge GGM-Basin Manager, Frontier Basin, ONGC, Dehradun, for providing an opportunity and all necessary facilities to prepare this paper. Authors wish to acknowledge the support given by all colleagues in the group. The views expressed in the paper are of the authors not the belonging organization. References Adnan A., Shukla U. K., Verma A., and Shukta T., 2015, Lithofacies of transgressive-regressive sequence on a carbonate ram in Vindhyan basin (Proterozoic): a case of tidal-flat origin from central India. Arab J Geosci, 8, 6985–7001. Aktar K., 1996, Facies, sedimentation processes and environments in the Proterozoic Vindhyan Basin, India In: Bhattacharya, A. 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Mondal, K., Singh, B.P., 2017, Felsic Xenocryst in the Bedded Porcellanite (Mesoproterozoic) of the Central India: An Evidence Suggesting the Rhyolitic Source of Silica. Global Journal of Earth Science and Engineering, 2017, 4, 18–26. Nady, M.M.E., Ramadan F.S., Hammad M.M., Lotfy N.M., 2015, Evaluation of organic matters, hydrocarbon potential and thermal maturity of source rocks based on geochemical and statistical methods: Case study of source rocks in Ras Gharib oilfield, central Gulf of Suez, Egypt. Egyptian Journal of Petroleum, 24, 203–211. Nesbitt, H.W., and Young, G.M., 1982, Early Proterozoic Climates and Plate Motions Inferred from Major Element Chemistry of Lutites. Nature, 299, 715–717. http://dx.doi.org/10.1038/299715a0 . Pandey, R., Kumar, D., Maurya, A.S., Pandey, P., 2019, Hydrocarbon generation potential of source rocks in Jaisalmer Basin, Rajasthan, India. Current Science, 116 (5), 822–827. Peters, K.E., 1986, Guidelines for evaluating petroleum source rocks using programmed pyrolysis. American Association Petroleum Geologists Bulletin, 70, 318–329. Prasad, B., 1981, A review of the Vindhyan Supergroup in southeastern Rajsthan. Misc Pub Geol Soc India, 50, 31–40. Prasad, B., 1984, Geology, sedimentation and paleogeography of the Vindhyan Supergroup, S.E Rajasthan. Memoir Geological Survey of India, 116, 148. Prasad, B.R., and Rao, V.V., 2006, Deep seismic reflection study over the Vindhyans of Rajasthan: Implications for geophysical setting of the basin. Journal of Earth System Science, 115, 135–147. Prasad, B., and Asher, R., 2016, Record of Ediacaran complex Acanthomorphic Acritarchs from the Lower Vindhyan succession of the Chambal Valley (East Rajasthan), India and their biostratigraphic significance. Journal of the Palaeontological Society of India, 61, 29–60. Price, R.C., Stewart, R.B., Woodhead, J.D., Smith, I.E.M., 1999, Petrogenesis of high-K arc magmas: evidence from Egmont Volcano, North Island, New Zealand. J. Petrol., 40, 167–197. Ray, J.S., Veizer, J., and Davis, W.J., 2003, C, O, Sr and Pb isotope systematics of carbonate sequences of the Vindhyan Supergroup, India: age, diagenesis, correlations and implications for global events. Precambrian Research, 121, 103–140. Raza, M., Casshyap, S.M., and Khan, A., 2002, Geochemistry of Mesoproterozoic Lower Vindhyan shales from Chittaurgarh, southeastern Rajasthan and its bearing on source rock composition, paleoweathering conditions and tectono-sedimentary environments. Journal of Geological Society of India, 60, 505–518. Riquier, P., Averbuch, O., Tribovillard, P., Albani A., 2007, Environmental changes at the Frasnian-Famennian boundary in Central Morocco (Northern Gondwana): Integrated rock-magnetic and geochemical studies. Geol. Soc. Of Lon. 278, 197–217. Roser, B.P., and Korsch, R.J., 1988, Provenance Signature of Sandstone-Mudstone Suites Determined Using Discriminant Function Analysis of Major Element Data. Chemical Geology, 67, 119–139. http://dx.doi.org/10.1016/0009-2541(88)90010-1 . Sageman, B.B., Murphy, A.E., Werne, J.P., Ver Straeten, C.A., Hollander, D.J., Lyons, T.W., 2003, A tale of shales: the relative roles of production, decomposition, and dilution in the accumulation of organic-rich strata, Middle–Upper Devonian, Appalachian basin. Chem. Geol., 195, 229–273. Samanta, P., Mukhopadhyay, S., and Eriksson, P.G., 2016, Forced regressive wedge in the Mesoproterozoic Koldaha Shale, Vindhyan basin, Son valley, central India. Marine and Petroleum Geology, 71, 329–343. Sarangi, S., Gopalan, and Kumar, S., 2004, Pb–Pb age of earliest megascopic, eukaryotic alga bearing Rohtas Formation, Vindhyan Supergroup, India: implications for Precambrian atmospheric oxygen evolution. Precambrian Research, 132, 107–121. Sarkar, S., Eriksson, P.G, and Chakraborty, S., 2004, Epeiric Sea Formation on Neoproterozoic Supercontinent Break-up: A Distinctive Signature in Coastal Storm Bed Amalgamation. Gondwana Research, 73, 13–322. Sharma, M., and Kumar, S., 2012, Vindhyan basin, Son Valley area, Central India. The Palaeontological Society of India (PSI field guide) Shukla, A.D., George, B.G., and Ray, J.S., 2019, Evolution of the Proterozoic Vindhyan Basin, Rajasthan, India: insights from geochemical provenance of siliciclastic sediments. International Geology Review, 62, 153–167. https://doi.org/10.1080/00206814.2019.1594412 . Singh, A.K., Chakraborty, P.P., 2021, Geochemistry and hydrocarbon source rock potential of shales from the Palaeo-Mesoproterozoic Vindhyan Supergroup, central India. Energy Geoscience, 4(3), 1–20. https://doi.org/10.1016/j.engeos.2021.10.007 . Sur, S., Schieber, J., and Banerjee, S., 2006, Petrographic observations suggestive of microbial mats from Rampur Shale and Bijaigarh Shale, Vindhyan basin, India. Journal of Earth System Science, 115, 61–66. Tandon, S.K., Pant, C.C., and Casshyap, S.M., 1991, Sedimentary basins of India-Tectonic context Gyanodaya Prakashan, Nainital (proceedings of the Seminar Held at Department of Geology, Kumaun University, Nainital). Tribovillard, N., Algeo, T.J., Lyons, T., and Riboulleau, A., 2006, Trace metals as paleoredox and paleoproductivity proxies: An update. Chem. Geol., 232, 12–32. Tribovillard, N., Ramdani, A., Trentesaux, A., 2005, Controls on organic accumulation in Late Jurassic shales of Northwestern Europe as inferred from trace-metal geochemistry. In: Harris, N. (Ed.), Deposition of Hydrocarbon Source Rocks. SEPM Spec. Public., 82, 145–164. Tripathy, G.R., and Singh, S.K., 2015, Re–Os depositional age for black shales from the Kaimur Group, Upper Vindhyan, India. Chemical Geology, 413, 63–72. Verma, A., and Shukla, U.K., 2015, Deposition of the Upper Rewa Sandstone Formation of Proterozoic Rewa Group of the Vindhyan Basin, M.P., India: A reappraisal. Journal Geological Society of India, 86, 421–437. Werne, J.P., Sageman, B.B., Lyons, T.W., Hollander, D.J., 2002, An integrated assessment of a “type euxinic” deposit: evidence for multiple controls on black shales deposition in the Middle Devonian Oatka Creek Formation. Am. J. Sci. 303, 110–143. Winter, J.D., 2001, An Introduction to Igneous and Metamorphic Petrology. Prentice Hall Inc., Upper Saddle River, 697. Zernack, A.V., Price, R.C., Smith, I.E.M., Cronin, S.J., Stewart, R.B., 2012, Temporal evolution of a high-K andesitic magmatic system: Taranaki Volcano, New Zealand J. Petrol., 53 pp. 325–363. Additional Declarations No competing interests reported. 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Also discoverable on Platform About Our Team In Review Editorial Policies Advisory Board Help Center Resources Author Services Accessibility API Access RSS feed Manage Cookie Preferences © Research Square 2026 | ISSN 2693-5015 (online) Privacy Policy Terms of Service Do Not Sell My Personal Information {"props":{"pageProps":{"initialData":{"identity":"rs-3957834","acceptedTermsAndConditions":true,"allowDirectSubmit":true,"archivedVersions":[],"articleType":"Research Article","associatedPublications":[],"authors":[{"id":283226422,"identity":"377f0dfb-5b48-49c6-a4aa-75cf4c05df69","order_by":0,"name":"Rajesh Pandey","email":"data:image/png;base64,iVBORw0KGgoAAAANSUhEUgAAAZAAAAAyAQMAAABI0h/eAAAABlBMVEX///8AAABVwtN+AAAACXBIWXMAAA7EAAAOxAGVKw4bAAAA8UlEQVRIiWNgGAWjYHCCBAbGhgMJDOyNjQ+APB4+4rXwHD5sANLCRpQ9YC0SaWkSIA5BLebtBx4+/LnjTp7BgRyzyq85djJsDMwPH93Ao0XmTEKyMe+ZZ8UGB86Y3Zbdlgx0GJuxcQ4eLRIMCWnSjG2HEzcc7DG7LbmNGaiFh00arxb+B+k/f4K0HOYxK5bcVk+EFomENAZekJZjbGmMH7cdJkbLg2Rp3rZniTPPMB+WZtx2nIeNmZBf+HMSP/5su5PYd/9h48ef26rt+dmbHz7GpwUYdwlwJjMPmMSrHATYD8CZjD8Iqh4Fo2AUjIKRCADc7VAIsGnTiQAAAABJRU5ErkJggg==","orcid":"","institution":"Oil and Natural Gas Corporation","correspondingAuthor":true,"prefix":"","firstName":"Rajesh","middleName":"","lastName":"Pandey","suffix":""},{"id":283226424,"identity":"2785d7d1-0bba-44d7-84df-c4bb562f9809","order_by":1,"name":"Sanjay Ojha","email":"","orcid":"","institution":"Oil and Natural Gas Corporation","correspondingAuthor":false,"prefix":"","firstName":"Sanjay","middleName":"","lastName":"Ojha","suffix":""}],"badges":[],"createdAt":"2024-02-15 06:46:01","currentVersionCode":1,"declarations":"","doi":"10.21203/rs.3.rs-3957834/v1","doiUrl":"https://doi.org/10.21203/rs.3.rs-3957834/v1","draftVersion":[],"editorialEvents":[],"editorialNote":"","failedWorkflow":false,"files":[{"id":53400571,"identity":"eb0f988b-f7bd-4f5d-b517-8a229de0eea5","added_by":"auto","created_at":"2024-03-25 14:27:43","extension":"jpeg","order_by":1,"title":"Figure 1","display":"","copyAsset":false,"role":"figure","size":881529,"visible":true,"origin":"","legend":"\u003cp\u003eStratigraphic section of Son Valley sector with available radiometric ages (Tripathi and Singh, 2015)\u003c/p\u003e","description":"","filename":"image1.jpeg","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/5fbc8b8843263a35d9c6e082.jpeg"},{"id":53400576,"identity":"4c5be69f-97ce-4625-9d28-ae0c928e4456","added_by":"auto","created_at":"2024-03-25 14:27:44","extension":"png","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":1795616,"visible":true,"origin":"","legend":"\u003cp\u003eGeological map of Vindhyan Basin with Hatta area under study\u003c/p\u003e","description":"","filename":"image2.png","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/87c9bfabeef21eecea0023da.png"},{"id":53400574,"identity":"e8e7c33e-6f2a-4d0c-a297-95240cab7a5d","added_by":"auto","created_at":"2024-03-25 14:27:43","extension":"png","order_by":3,"title":"Figure 3","display":"","copyAsset":false,"role":"figure","size":417091,"visible":true,"origin":"","legend":"\u003cp\u003eDepth wise major and trace elements plot of Jardepahar Formation\u003c/p\u003e","description":"","filename":"image3.png","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/e8b96e042ece2deea0ab8a71.png"},{"id":53400577,"identity":"21dd9485-11ba-46f7-bdad-4499cacc291d","added_by":"auto","created_at":"2024-03-25 14:27:44","extension":"png","order_by":4,"title":"Figure 4","display":"","copyAsset":false,"role":"figure","size":139671,"visible":true,"origin":"","legend":"\u003cp\u003eHarker diagram of major elements in Jardepahar Formation\u003c/p\u003e","description":"","filename":"image4.png","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/754369c3fa4a90435125ae46.png"},{"id":53400581,"identity":"ab4bd5d7-d957-4069-ae6b-c866c0d4df38","added_by":"auto","created_at":"2024-03-25 14:27:44","extension":"png","order_by":5,"title":"Figure 5","display":"","copyAsset":false,"role":"figure","size":173471,"visible":true,"origin":"","legend":"\u003cp\u003eGeochemical discrimination diagrams of Jardepahar a) K2O vs SiO2, b) Al2O3 vs TiO2 and c) TiO2 vs\u003cstrong\u003e \u003c/strong\u003eZr\u003c/p\u003e","description":"","filename":"image5.png","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/f47f2fe638703d3da06098e4.png"},{"id":53400578,"identity":"a98ac5be-a593-4c86-8241-3e94450e38d8","added_by":"auto","created_at":"2024-03-25 14:27:44","extension":"png","order_by":6,"title":"Figure 6","display":"","copyAsset":false,"role":"figure","size":41908,"visible":true,"origin":"","legend":"\u003cp\u003eV/Cr vs U/Th and Ti vs Fe cross plot showing oxygen rich environment\u003c/p\u003e","description":"","filename":"image6.png","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/534b3ee451300cbf9c28fc14.png"},{"id":53400580,"identity":"d1ff6cac-569a-4afd-ac9d-d7362b2ba9e4","added_by":"auto","created_at":"2024-03-25 14:27:44","extension":"png","order_by":7,"title":"Figure 7","display":"","copyAsset":false,"role":"figure","size":1506028,"visible":true,"origin":"","legend":"\u003cp\u003eA \u0026amp; B. Limestone showing network of horizontal and vertical fractures filled with clay matter (PP and XN), C. Enlarged view exhibiting silt sized quartz grains in the fractures, D. Limestone showing clay filled fracture and spar.\u003c/p\u003e","description":"","filename":"image7.png","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/042e547f578518efa227d5f1.png"},{"id":53400583,"identity":"285b5e8e-8a59-4ede-a6bd-8585606618f4","added_by":"auto","created_at":"2024-03-25 14:27:44","extension":"png","order_by":8,"title":"Figure 8","display":"","copyAsset":false,"role":"figure","size":767041,"visible":true,"origin":"","legend":"\u003cp\u003eTuffaceous Volcaniclastics showing volcanic quartz and feldspar grains\u003c/p\u003e","description":"","filename":"image8.png","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/79869b35aab41ccbfba73d11.png"},{"id":53400579,"identity":"810bd11b-40a0-41a2-86ba-68a8186634f1","added_by":"auto","created_at":"2024-03-25 14:27:44","extension":"png","order_by":9,"title":"Figure 9","display":"","copyAsset":false,"role":"figure","size":636980,"visible":true,"origin":"","legend":"\u003cp\u003eA. Enlarged view exhibiting alteration of Feldspar grain into Sericite along with kaolinite clay in the pore spaces, B. Enlarged view showing glass texture along with patchy calcite cement\u003c/p\u003e","description":"","filename":"image9.png","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/3c24f90e48a73660d545b960.png"},{"id":53400575,"identity":"234d3a01-1be2-461e-b72a-40457dd1f58b","added_by":"auto","created_at":"2024-03-25 14:27:43","extension":"png","order_by":10,"title":"Figure 10","display":"","copyAsset":false,"role":"figure","size":1903221,"visible":true,"origin":"","legend":"\u003cp\u003eElectrolog signature of different lithounits of Jardepahar porcellanite along with photomicrographs\u003c/p\u003e","description":"","filename":"image10.png","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/975c68f61c93422efec8daa2.png"},{"id":53400582,"identity":"3f590e60-4b5e-4bfb-a6bc-fc88ad4d1757","added_by":"auto","created_at":"2024-03-25 14:27:44","extension":"png","order_by":11,"title":"Figure 11","display":"","copyAsset":false,"role":"figure","size":169208,"visible":true,"origin":"","legend":"\u003cp\u003eFig. 10 Hydrocarbon generation potential vs TOC and HI vs OI plot of source rock data (Source: KDMIPE report)\u003c/p\u003e","description":"","filename":"image11.png","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/df912f69d41d2f64a1047704.png"},{"id":54351344,"identity":"b69ff9c3-579c-4ae1-b8de-a6429e82f5b4","added_by":"auto","created_at":"2024-04-09 08:37:21","extension":"pdf","order_by":0,"title":"","display":"","copyAsset":false,"role":"manuscript-pdf","size":7808564,"visible":true,"origin":"","legend":"","description":"","filename":"manuscript.pdf","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/92bec714-6ded-43c5-a575-8549b1f013b6.pdf"},{"id":53400572,"identity":"09d358a9-1cbb-43b0-8b05-c6340f68f69d","added_by":"auto","created_at":"2024-03-25 14:27:43","extension":"docx","order_by":1,"title":"","display":"","copyAsset":false,"role":"supplement","size":53952,"visible":true,"origin":"","legend":"","description":"","filename":"Appendix.docx","url":"https://assets-eu.researchsquare.com/files/rs-3957834/v1/42a65fa6eaf9b0eecafe50d3.docx"}],"financialInterests":"No competing interests reported.","formattedTitle":"\u003cp\u003eCharacterization of Hydrocarbon Bearing Jardepahar Porcellanite Formation, Vindhyan Basin\u003c/p\u003e","fulltext":[{"header":"Introduction","content":"\u003cp\u003eVindhyan Basin, by virtue of its age poses a number of challenges and uncertainties in exploration. The hydrocarbon exploration of Son Valley started in late eighties in the major structural highs (Damoh, Jabera, Kharkhari) targeting the deeper stratigraphic units (Kajrahat and Jardepahar formations). However, there was no significant success in this initial phase except in Jardepahar Formation in well Jabera#A. Well Jabera-A, a rank wildcat well, was drilled on Jabera dome, which flowed hydrocarbon gas from three zones tested within Jardepahar Formation and made a discovery of gas for the first time in the Vindhyan Basin. The gas was analyzed to be wet and thermogenic in nature and declared non-commercial due to lower flow rate. Encouraged by this lead, Wells Damoh-A and Kharkhari-A were drilled on structural plays and were found to be dry. Subsequently, the drilled well Jabera-B established the extension of gas bearing layers of Jabera-A within Jardepahar Formation besides another likely gas bearing layer within Kajrahat Limestone section. The well provided vital exploratory leads for evaluation of deeper petroleum systems in the basin.\u003c/p\u003e \u003cp\u003eEfforts to capitalize initial successes could bear fruits through the recent significant discovery of gaseous hydrocarbons within the Proterozoic Jardepahar reservoir in the Hatta area (NELP Block VN-ONN-2009/3) of Son Valley, Vindhyan Basin. Subsequent activities to capitalize the Hatta lead have proved the viability and have given a major fillip to exploration program in the Indian Proterozoic Basins, particularly in the Vindhyan Basin.\u003c/p\u003e \u003cp\u003eVindhyan Basin has been studied thoroughly in terms of its geophysical, sedimentological, and palaeontological evolution (c.f., Adnan et al., \u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Banerjee and Banerjee, \u003cspan citationid=\"CR4\" class=\"CitationRef\"\u003e2010\u003c/span\u003e; Banerjee et al., 2015; Bengtson et al., \u003cspan citationid=\"CR8\" class=\"CitationRef\"\u003e2009\u003c/span\u003e; Bose et al., \u003cspan citationid=\"CR9\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Chakraborty, \u003cspan citationid=\"CR16\" class=\"CitationRef\"\u003e2011\u003c/span\u003e; Kumar, \u003cspan citationid=\"CR27\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Mishra, \u003cspan citationid=\"CR32\" class=\"CitationRef\"\u003e2015\u003c/span\u003e; Prasad and Asher, \u003cspan citationid=\"CR45\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Prasad and Rao, \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e2006\u003c/span\u003e; Sarkar et al., \u003cspan citationid=\"CR56\" class=\"CitationRef\"\u003e2004\u003c/span\u003e; Samanta et al., \u003cspan citationid=\"CR54\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Sur et al., \u003cspan citationid=\"CR60\" class=\"CitationRef\"\u003e2006\u003c/span\u003e; Verma and Shukla, \u003cspan citationid=\"CR65\" class=\"CitationRef\"\u003e2015\u003c/span\u003e) while geochemical and isotopic studies are limited that have tried to address sediment provenance, tectonic evolution and sub-basin connectivity (Shukla et al., \u003cspan citationid=\"CR58\" class=\"CitationRef\"\u003e2019\u003c/span\u003e). The Porcellanite is a vital constituent of Lower Vindhyan rocks, due to the recent discovery of hydrocarbon gases, it is pertinent to evaluate the nature of rocks and their physiognomies. It is the oldest porcellanite deposit in India (Mondal and Singh, \u003cspan citationid=\"CR35\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). The term porcellanite is not very well defined; it is an argillaceous or calcareous chert with fine-grained acidic vitric tuff compacted with secondary silica (Mehrotra and Banerjee, 1982). Based on surface sample analysis it has been interpreted as the vitric tuffs are derived from felsic volcanic rocks with a high content of silica release in oceanic basins, which has facilitated chert precipitation; these cherts are also associated with tephra, tuff, or ignimbrite (Mondal and Singh, \u003cspan citationid=\"CR35\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). Mondal and Singh (\u003cspan citationid=\"CR35\" class=\"CitationRef\"\u003e2017\u003c/span\u003e) have established the presence of four types of porcellanite, based on its colour, i.e., yellow porcellanite, black porcellanite, white porcellanite, and green porcellanite, while the old workers have classified the Vindhyan porcellanite in to three units based on textural characters: banded, spotted and massive (Mehrotra and Banerjee, 1982). The sub-surface data from the drilled well ahs also suggested three units with a dolomitic limestone unit. The presence of slump folding and convolute lamination observed during field study also supports the theory of sub-aqueous eruption and active tectonics during transportation and deposition of the sediments (Mondal and Singh, \u003cspan citationid=\"CR35\" class=\"CitationRef\"\u003e2017\u003c/span\u003e). The geochemistry of porcellanite, including trace elements, represents the average composition of parental volcano-clastic materials responsible for the deposition of fine grained, massive to banded, light grey to olive green, hard, waxy lusture and glassy nature porcellanite. Hard rock geochemistry is also considered an excellent proxy for provenance, tectonics, or palaeoclimate interpretation (Nesbitt and Young, \u003cspan citationid=\"CR37\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Roser and Korsch, \u003cspan citationid=\"CR52\" class=\"CitationRef\"\u003e1988\u003c/span\u003e; Li et al., \u003cspan citationid=\"CR29\" class=\"CitationRef\"\u003e2012\u003c/span\u003e). As the rocks are Proterozoic, rapid alteration of feldspar and leaching of accessory minerals within interbedded limestones may result in an erroneous interpretation of provenance (Blatt, \u003cspan citationid=\"CR12\" class=\"CitationRef\"\u003e1985\u003c/span\u003e), but the impermeable character of fine grained vitric tuff can easily retain and preserve the original signatures of tuffaceous material, which were erupted, transported, and deposited in an aqueous condition (Srivastav, 1997). The high biological productivity (organic carbon), during Palaeoproterozoic-Mesoproterozoic (2.0-1.6 Ga) may lead the generation of adequate source rocks (Condie et al., \u003cspan citationid=\"CR17\" class=\"CitationRef\"\u003e2001\u003c/span\u003e). The giant oil discoveries of Canada, Oman and Russia (Craig et al., \u003cspan citationid=\"CR18\" class=\"CitationRef\"\u003e2013\u003c/span\u003e) have intensified interest in the Mesoproterozoic Vindhyan Basin. This article provides an understanding to the origin and evolution of the Jardepahar Porcellanite Formation of Vindhyan Basin, primarily from a geochemical, petrographic and source rock perspective.\u003c/p\u003e"},{"header":"General Geology","content":"\u003cp\u003eThe Vindhyan basin is the second largest Proterozoic intracontinental basin that developed in the central part of the Indian shield, surrounded by the Aravalli-Delhi fold belt in the west and north west, the Satpura orogeny in the south and east, and Bundelkhand granite in the north (Chakraborty et al., \u003cspan citationid=\"CR15\" class=\"CitationRef\"\u003e2012\u003c/span\u003e; Singh and Chakraborty, \u003cspan citationid=\"CR59\" class=\"CitationRef\"\u003e2021\u003c/span\u003e). The Indogangetic plain in the northern part and the Deccan volcanic in the south-western part conceal a major part of the basin (Krishnan, \u003cspan citationid=\"CR25\" class=\"CitationRef\"\u003e1968\u003c/span\u003e; Gopalan et al., \u003cspan citationid=\"CR21\" class=\"CitationRef\"\u003e2013\u003c/span\u003e); hence, the exact limit of the basin is uncertain. The exposed area of the basin is around 178,000 km\u003csup\u003e2\u003c/sup\u003e, with a more than 4500 m thick siliciclastic-carbonate package of mildly deformed and unmetamorphosed sediments (Tandon et al., \u003cspan citationid=\"CR61\" class=\"CitationRef\"\u003e1991\u003c/span\u003e). The Vindhyan basin has been lithostratigraphically subdivided into four groups, in stratigraphic order these are: the Semri Group, the Kaimur Group, the Rewa Group, and the Bhander Group (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e). The current well taken for this study is located in the son valley sector, with a primary focus on the Jardepahar Formation belonging to the Semri Group of Lower Vindhyan (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e2\u003c/span\u003e). The Vindhyan Basin is mostly unmetamorphosed siliciclastic and carbonate rocks with minor deformation (Turner et al., 2013). Pb-Pb age are used to establish the ages of the Lower and Upper Vindhyan rocks, the carbonate sedimentation of the Kajrahat Formation initiated around 1729\u0026thinsp;\u0026plusmn;\u0026thinsp;110 Ma ago in this basin (Sarangi et al., \u003cspan citationid=\"CR55\" class=\"CitationRef\"\u003e2004\u003c/span\u003e) while Bhander Formation carbonates were deposited around 900 Ma ago based on Pb-Pb ages suggest closure of the basin (Gopalan et al., \u003cspan citationid=\"CR21\" class=\"CitationRef\"\u003e2013\u003c/span\u003e). The Bundelkhand Granite Massif located at the central part of the basin divides the basin into the son valley sector in the east and the chambal valley sector in the west (Rajasthan). Metavolcanic and metasedimentary supracrustal sequence of the Mahakoshal and Bijawar Group occurs as a linear belt (Das et al., \u003cspan citationid=\"CR19\" class=\"CitationRef\"\u003e1990\u003c/span\u003e) and are located towards southeastern edge of the basin. In the Rajasthan sector (chambal valley), most of the Vindhyan rocks are undeformed, except near to the Great Boundary Fault, where vertically dipping beds and large scale folded strata are observed (Gilleaudeau et al., \u003cspan citationid=\"CR20\" class=\"CitationRef\"\u003e2018\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eSemri Group comprises a repetitive section of clastic and carbonate sequences with the presence of volcaniclastic unit (Jardepahar Formation), deposited within shallow marine (Banerjee, \u003cspan citationid=\"CR6\" class=\"CitationRef\"\u003e1974\u003c/span\u003e) to deep marine (Chakraborty et al., 1996b). The oldest carbonate unit in the eastern sector is Kajrahat Limestone which shows development of stromatolites (Kumar et al., \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e2002\u003c/span\u003e) with large fan-fabrics in the upper part (Sharma and Kumar, \u003cspan citationid=\"CR57\" class=\"CitationRef\"\u003e2012\u003c/span\u003e). The carbonate unit is deposited under subtidal to supratidal conditions (Banerjee, \u003cspan citationid=\"CR6\" class=\"CitationRef\"\u003e1974\u003c/span\u003e). The intraformational conglomerates indicates repetitive transgression and regression (Kumar et al., \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e2002\u003c/span\u003e). Presence of Gypsum layers indicates an evaporative condition (Aktar, \u003cspan citationid=\"CR2\" class=\"CitationRef\"\u003e1996\u003c/span\u003e). The stratigraphic equivalent of Kajrahat Limestone is Bhagwanpura Limestone in the Rajasthan sector (Prasad, \u003cspan citationid=\"CR41\" class=\"CitationRef\"\u003e1984\u003c/span\u003e; Banerjee and Chopra, \u003cspan citationid=\"CR5\" class=\"CitationRef\"\u003e1986\u003c/span\u003e). Bhagwanpura Limestone is extensively dolomitic in nature with localized microbialites (Ray et al., \u003cspan citationid=\"CR47\" class=\"CitationRef\"\u003e2003\u003c/span\u003e). The final phase of Lower Vindhyan is represented by the carbonate sedimentation of the Rohtas and Nimbahera Limestone from the Son Valley and Rajasthan sector, respectively. In the Son valley, the Rohtas Limestone represents rhythmite-like intercalations between thin bedded limestone and shale with poorly developed columnar stromatolites (Kumar, \u003cspan citationid=\"CR11\" class=\"CitationRef\"\u003e1977\u003c/span\u003e), deposited under subtidal to intertidal settings (Aktar, \u003cspan citationid=\"CR2\" class=\"CitationRef\"\u003e1996\u003c/span\u003e). The Nimbahera Limestone from the Rajasthan sector is massive in nature and devoid of stromatolites and is deposited as a transgressional sequence (Prasad, \u003cspan citationid=\"CR40\" class=\"CitationRef\"\u003e1981\u003c/span\u003e). A thick silicified tuff unit, occurs in the Semri Group of Son Valley sector i.e. Porcellanite Formation, suggests active volcanism in the near vicinity of the basin. The Palri Shale of the Chambal Valley sector also indicate the presence of porcellanite beds has been considered an equivalent of Jardepahar Porcellanite (Raza et al., \u003cspan citationid=\"CR48\" class=\"CitationRef\"\u003e2002\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e"},{"header":"Methodology","content":"\u003cp\u003eThe cutting samples collected during drilling of well Hatta#D were taken for the current study. Around 50g of samples from each 5m interval were washed and dried. Out of them, few representative samples were taken for thin section preparation and petrographic analysis. Remaining samples were introduced into the Rockwash machine at the first washing station, where they received a fixed dose of Quckwash detergent and were gently agitated for 90 seconds under running water. No solvents are used in the Rockwash sample washing process. The samples are then conveyed to the second washing station and rinsed in running water for a further 90 seconds to remove any remaining material from the surface of the cutting sample grains. Samples were then automatically conveyed to the drying modules, where they received 90 seconds of drying at each of the six drying stations. Later on, samples were dried at a temperature of less than 40\u0026deg;C. A washed and dried cutting sample was analysed using a Niton XL3T GOLDD\u0026thinsp;+\u0026thinsp;handheld XRF analyzer. Samples of a standard reference material (SdAR-M2 metal-rich sediment) were analysed during each sequence of analyses (\u003cspan refid=\"Sec10\" class=\"InternalRef\"\u003eAppendix-1\u003c/span\u003e). Rock eval analysis is used to evaluate their free hydrocarbon content as well as petroleum potential to identify various potential or effective petroleum source rocks as well as potential accumulation intervals or zones in the area under study. Two state-of-the-art Rock-Eval-6 (Turbo model) instruments are available in the geochemistry lab of KDMIPE, ONGC. The results of the Rock Eval analysis provide data that are used to assess petroleum potential, organic matter type, extent of maturity of source rocks, and gravity of oil generated from sediments (\u003cspan refid=\"Sec11\" class=\"InternalRef\"\u003eAppendix-2\u003c/span\u003e).\u003c/p\u003e"},{"header":"Result and Discussion","content":"\u003cdiv id=\"Sec5\" class=\"Section2\"\u003e \u003ch2\u003eGeochemical Analysis:\u003c/h2\u003e \u003cp\u003eThe major and trace element geochemistry helps us to establish the basinal characteristic during the deposition of the formation. The distribution of major element concentration in the entire formation divide the entire formation into three units. The middle unit is characterised by relatively lower MgO, Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e, SiO\u003csub\u003e2\u003c/sub\u003e, CaO, Fe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e and higher K\u003csub\u003e2\u003c/sub\u003eO as compared to the top and bottom units (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e3\u003c/span\u003e). Relatively higher concentrations of U, Th and Rb in the middle unit indicate the presence of organic substances, which may be precipitated with phosphates, glauconite and clay to form sedimentary rock. The higher concentration of Zn in the middle unit indicates high organic matter flux and reducing conditions (Tribovillard et al., \u003cspan citationid=\"CR62\" class=\"CitationRef\"\u003e2006\u003c/span\u003e). A higher Si/Al ratio in the middle unit reflects the clastic influx with high to moderate energy condition (Riquier et al., \u003cspan citationid=\"CR51\" class=\"CitationRef\"\u003e2007\u003c/span\u003e). It also supports the concept of high biological productivity in the middle unit as compared to the upper and lower units. The Zr/Rb ratio indicates the upper unit has coarser material followed by the middle and lower units, which also supports the textural interpretation (banded, spotted and massive) of three units in the Jardepahar Formation.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eSignificant fluctuations are recorded in the abundance of major element concentrations. SiO\u003csub\u003e2\u003c/sub\u003e concentration varies from 40.22 to 61.42 wt % with an average of 51.77 wt %. Similarly, wide variations can also be observed in Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e (12.20 -25.28 wt %) and K\u003csub\u003e2\u003c/sub\u003eO content (0.94\u0026ndash;7.51 wt %) with their averages being 18.10 wt% and 4.32 wt% respectively (Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e4\u003c/span\u003e). Harker diagrams shows increasing or constant trends in Fe\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e, MgO, Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e, CaO, K\u003csub\u003e2\u003c/sub\u003eO and TiO\u003csub\u003e2\u003c/sub\u003e with increasing silica indicates there was minor fractionation during or after deposition of the volcaniclastic sediments. The enrichment of potash (K) advocates andesite genesis/andesitic volcanic sources (Price et al. \u003cspan citationid=\"CR46\" class=\"CitationRef\"\u003e1999\u003c/span\u003e; Winter, \u003cspan citationid=\"CR67\" class=\"CitationRef\"\u003e2001\u003c/span\u003e; Zernack et al. \u003cspan citationid=\"CR68\" class=\"CitationRef\"\u003e2012\u003c/span\u003e). The rocks exhibit higher TiO\u003csub\u003e2\u003c/sub\u003e content (0.08\u0026ndash;1.36 wt%), and the ratios of Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e/TiO\u003csub\u003e2\u003c/sub\u003e indicates that the porcellanite ashes are derived from felsic to intermediate igneous source rocks. Provenance indicator diagrams (TiO\u003csub\u003e2\u003c/sub\u003e (wt%) versus Zr (ppm) also suggest the source rock for the porcellanite is acidic to intermediate volcanic rock (Hayashi et al., \u003cspan citationid=\"CR22\" class=\"CitationRef\"\u003e1997\u003c/span\u003e) (Fig.\u0026nbsp;\u003cspan refid=\"Fig5\" class=\"InternalRef\"\u003e5\u003c/span\u003e). In addition, U/Th vs. V/Cr indicates, the most oxygenated conditions met during the porcellanite deposition, corroborated with the GOE (great oxygenation event) from 2000Ma-1700Ma (Large et al., \u003cspan citationid=\"CR28\" class=\"CitationRef\"\u003e2022\u003c/span\u003e). The positive correlation of Fe and Ti indicates the presence of iron oxides i.e. magnetite and ilmenite, which are present in the interstitial spaces of plagioclase minerals (Fig.\u0026nbsp;\u003cspan refid=\"Fig6\" class=\"InternalRef\"\u003e6\u003c/span\u003e). Geochemical and Nd isotope signatures of Jardepahar/Deonar Porcellanites suggest that the volcanic tuff and pyroclast are derived from an Andean-type arc originated, due to collision between Bundelkhand Craton and Bhandara/Bastar Craton (Chakrabarti et al., 2007). The Geochemical signature Deonar and Chopan Porcellanite Formation suggests the sediments are derived from the mixing between mantle-derived rocks and average continental crust, under a continental rift environment (Mishra et al., \u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e2017a\u003c/span\u003e, \u003cspan citationid=\"CR34\" class=\"CitationRef\"\u003eb\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003eThis chemical characteristics indicates that the Jardepaher has mixed volaconogenic precursors. The concentrations of terrigenous proxy elements (Ti, Cr \u0026amp; Zr) in Vindhyan porcellanite are compared with Al\u003csub\u003e2\u003c/sub\u003eO\u003csub\u003e3\u003c/sub\u003e, which shows moderate to low correlation coefficients, i.e. 0.50, 0.126 and 0.143 respectively. It indicates that elements were fixed without magmatic differentiation along with the deposition of volcano-clastics with later stage minor alteration. The trace element concentration in the rocks are a good indicator of depositional dynamics along with provenance. Enrichment of Mo and U in the middle and lower parts of the formation indicates that the sediments were likely enriched in O\u003csub\u003e2\u003c/sub\u003e at the time of deposition of the porcellanite (Lyons et al., 2003; Algeo and Maynard, 2004; Tribovillard et al., \u003cspan citationid=\"CR63\" class=\"CitationRef\"\u003e2005\u003c/span\u003e). Negative correlation coefficients of Ba (-0.093), Ni (-0.019) and Cr (-0.019) with respect to Al2O3 indicate the absence of biogenic fractions and sediments have suffered negligible amounts of chemical alteration in worm and humid environments ((Brumsack, \u003cspan citationid=\"CR13\" class=\"CitationRef\"\u003e1989\u003c/span\u003e; Werne et al., \u003cspan citationid=\"CR66\" class=\"CitationRef\"\u003e2002\u003c/span\u003e; Sageman et al., \u003cspan citationid=\"CR53\" class=\"CitationRef\"\u003e2003\u003c/span\u003e; Algeo and Maynard, 2004; Tribovillard et al., \u003cspan citationid=\"CR63\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Hu et al., \u003cspan citationid=\"CR24\" class=\"CitationRef\"\u003e2020\u003c/span\u003e; Singh and chakraborty, \u003cspan citationid=\"CR59\" class=\"CitationRef\"\u003e2021\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec6\" class=\"Section2\"\u003e \u003ch2\u003eSedimentological Study:\u003c/h2\u003e \u003cp\u003eJardepahar Porcellanite mainly consists of banded and massive chert with shale, limestone and ash beds. Shale is dark grey, hard, compact and feebly calcareous. Chert is fine grained, massive, banded, light grey to olive green, hard, waxy lustre, non-calcareous and glassy in nature. It belongs to vitric tuff to vitric crystal tuff class of Pettijohn (1957) and O\u0026rsquo;Brien (1963). Limestone is grey to off-white, hard and compact. Petrographic analysis shows vertical and horizontal fractures. These fractures are filled with argillaceous matter along with few silt size quartz grains and sparite (Fig.\u0026nbsp;\u003cspan refid=\"Fig7\" class=\"InternalRef\"\u003e7\u003c/span\u003eA-D). Megascopic analysis shows alternation of chert, limestone and ash beds. Ash bed is white and black, crenulated and soft. Petrographically, Porcellanite consists of amorphous silica with presence of dark black coloured carbonaceous matter along with small-scale fractures. Volcaniclast shows angular to sub-angular volcanic Quartz and Feldspar grains along with chert and glass shards. Angularity of grains indicates short distance transportation (Fig.\u0026nbsp;\u003cspan refid=\"Fig8\" class=\"InternalRef\"\u003e8\u003c/span\u003e). Extensive dissolution of Feldspar along cleavage planes into sericite and at places kaolinite is noted (Fig.\u0026nbsp;\u003cspan refid=\"Fig9\" class=\"InternalRef\"\u003e9\u003c/span\u003eA). Limestone reveals dolomite and recrystallized limestone. Dolomite microfacies consist of carbonaceous matter along with few feldspar grains. It also shows stylolamination filled with carbonaceous matter and spar filled vein. Profuse fractures and iron cement is also observed in the Dolomite facies. Glassy texture and patchy calcite cement has been observed in porcellanite (Fig.\u0026nbsp;\u003cspan refid=\"Fig9\" class=\"InternalRef\"\u003e9\u003c/span\u003eB). The micro-scale fractures present in the Jardepahar Formation irrespective of lithology act as reservoir for the entrapment of hydrocarbons.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec7\" class=\"Section2\"\u003e \u003ch2\u003eElectrolog study:\u003c/h2\u003e \u003cp\u003eElectrologs helps to discriminate the porcellanite into three cherty lithounits and one dolomitic-limestone unit. The bottom most lithounit-I represents blocky log signature and is dominated by massive and flaky chert with very few intervals of ash bed and carbonaceous shale. The lithounit-II is characterised by fining upward log motif followed by coarsening upward trend on electro-log and this unit is characterised by banded porcellanite and limestone, the limestone thickness increases towards the top within this unit. Lithounit- III is separated by thick recrystallized dolomitic limestone from unit-I and unit-II and is dominated by ash beds, massive porcellanite and carbonaceous Shale (Fig.\u0026nbsp;\u003cspan refid=\"Fig11\" class=\"InternalRef\"\u003e10\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec8\" class=\"Section2\"\u003e \u003ch2\u003eSource Rock Analysis:\u003c/h2\u003e \u003cp\u003eThe rock samples from the Jardepahar Formation were dried, crushed to powder and screened through BSS 60 mesh sieve. The crushed samples were analysed on Rock-Eval 6 for evaluation of source rock potential, quality and maturity. In the Jardepahar Porcellanite Formation, 13m source sequences are found in the depth intervals of 2171-2174m and 2180-2190m with fair to very good remaining hydrocarbon generation potential (Avg S2: 4.9 mg HC/g rock; ranges from 2.2\u0026ndash;8.82 mg HC/g rock) and good to excellent organic richness (Avg TOC: 2.72%; ranges from 1.41\u0026ndash;4.1%). In the identified source sequences hydrogen index values range from 154-207mg HC/g TOC (Fig.\u0026nbsp;\u003cspan refid=\"Fig11\" class=\"InternalRef\"\u003e10\u003c/span\u003e). Thermal maturity, Tmax: 434\u0026ndash;436\u0026deg;C has been observed in these depth intervals. The rest of the samples indicate poor remaining hydrocarbon generation potential. The presence of a very high oxygen index is probably due to the great oxygenation event that occurred during Proterozoic time (Large et al., \u003cspan citationid=\"CR28\" class=\"CitationRef\"\u003e2022\u003c/span\u003e), which brought the O/C ratio into the Type-III kerogen category on the Van Krevelon diagram (Peters, \u003cspan citationid=\"CR39\" class=\"CitationRef\"\u003e1986\u003c/span\u003e; Nandy et al., 2015; Pandey et al., \u003cspan citationid=\"CR38\" class=\"CitationRef\"\u003e2019\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e"},{"header":"Conclusions","content":"\u003cp\u003eThe elctrolog characters, sedimentary nature and geochemical tracer elements suggest that the Jardepahar porcellanite Formation can be divided into the three units (upper, middle and lower). The middle unit has lithological heterogeneity and contains complete elements of insitu petroleum system. The petrological attributes and whole rock geochemistry of Jardepahar porcellanite demonstrate that the precursor for cherty bands/vitric tuff are andesitic to felsic nature, high K indicates andesitic volcanism resulted due to active continental margins. The top unit has coarser grain clasts represents higher energy condition that decreases towards the bottom unit (unit-I). The Harker diagram suggests very limited magmatic differentiation and fractionation within the source rock. The paleoclimatic condition at the time of deposition was oxic (lower to middle unit) to dysoxic (upper unit), with a moderate degree of chemical weathering. The middle and upper unit shows presence of organic matter along with micro and nano fractures. The organic matter indicates its humic character and Type III variety of kerogen, due to poor hydrogen content, extremely low H/C ratio and higher oxygen index. The presence of source and reservoir facies within the middle and upper unit designate it as an insitu tight gas petroleum system.\u003c/p\u003e"},{"header":"Declarations","content":"\u003cp\u003e \u003ch2\u003eConflict of interest statement\u003c/h2\u003e \u003cp\u003eThe interpretation provided in this research paper are the view of authors only, it does not have any relation with the organization they belong. The authors do no have any financial support or funding from any government / private agencies.\u003c/p\u003e \u003c/p\u003e\u003ch2\u003eAuthor Contribution\u003c/h2\u003e\u003cp\u003eDr. Rajesh Pandey: Data analysis, figure prepration and writing ManuscriptDr. Sanjay Ojha: Data analysis, concept buildup and formatting of Manuscript\u003c/p\u003e\u003ch2\u003eAcknowledgment:\u003c/h2\u003e \u003cp\u003eAuthors are grateful to the management of ONGC for giving permission to publish this work. Authors also acknowledge GGM-Basin Manager, Frontier Basin, ONGC, Dehradun, for providing an opportunity and all necessary facilities to prepare this paper. Authors wish to acknowledge the support given by all colleagues in the group. The views expressed in the paper are of the authors not the belonging organization.\u003c/p\u003e"},{"header":"References","content":"\u003col\u003e\u003cli\u003e\u003cspan\u003eAdnan A., Shukla U. K., Verma A., and Shukta T., 2015, Lithofacies of transgressive-regressive sequence on a carbonate ram in Vindhyan basin (Proterozoic): a case of tidal-flat origin from central India. Arab J Geosci, 8, 6985\u0026ndash;7001.\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eAktar K., 1996, Facies, sedimentation processes and environments in the Proterozoic Vindhyan Basin, India In: Bhattacharya, A. (Ed.), Recent Advances in Vindhyan Geology. 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Petrol., 53 pp. 325\u0026ndash;363.\u003c/span\u003e\u003c/li\u003e\u003c/ol\u003e"}],"fulltextSource":"","fullText":"","funders":[],"hasAdminPriorityOnWorkflow":false,"hasManuscriptDocX":true,"hasOptedInToPreprint":true,"hasPassedJournalQc":"","hasAnyPriority":false,"hideJournal":true,"highlight":"","institution":"","isAcceptedByJournal":false,"isAuthorSuppliedPdf":false,"isDeskRejected":"","isHiddenFromSearch":false,"isInQc":false,"isInWorkflow":false,"isPdf":false,"isPdfUpToDate":true,"isWithdrawnOrRetracted":false,"journal":{"display":true,"email":"[email protected]","identity":"researchsquare","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":true,"externalIdentity":"","sideBox":"","snPcode":"","submissionUrl":"/submission","title":"Research Square","twitterHandle":"researchsquare","acdcEnabled":true,"dfaEnabled":false,"editorialSystem":"","reportingPortfolio":"","inReviewEnabled":false,"inReviewRevisionsEnabled":true},"keywords":"Vindhyan Basin, Hydrocarbon, Geochemical, Source Rock","lastPublishedDoi":"10.21203/rs.3.rs-3957834/v1","lastPublishedDoiUrl":"https://doi.org/10.21203/rs.3.rs-3957834/v1","license":{"name":"CC BY 4.0","url":"https://creativecommons.org/licenses/by/4.0/"},"manuscriptAbstract":"\u003cp\u003eThe commercial gas discovery has been established form Paleo-proterozoic Jardepahar Formation of Son valley sector, Vindhayan Basin. The geochemical, sedimentological and source rock analysis of the cutting samples collected during the drilling of Hatta#D were carried out, to comprehend the nature of source rock, their petrological characteristic. The geochemical and electro-log signatures help us to divide the porcellanite of Jardepahar Formation in to three cherty dominated units and a dolomitic limestone unit. Similar observations have been registered from petrographic studies, the bottom units is massive chert layer, middle unit is banded chert (limestone bands) and the upper unit is again massive with the interbed of shale. The middle unit has drawn lead attention, due to hydrocarbon discovery, it consists of amorphous silica interbedded with limestone with along with carbonaceous matter and micro-nano scale fractures. Textural characteristics of clasts indicates very limited transportation. The middle unit shows, higher biological productivity and better hydrocarbon source facies as compared to the lower and upper units, which is gas bearing in Hatta field of Oil and Natural Gas Corporation (ONGC). The sediments were derived from high K felsic to intermediate volcanic source (s) from active continental margin, deposited in anoxic environment. The trace elements postulate absence of biogenic fractions and negligible amounts of chemical alteration. The middle unit has the source potential and also act as reservoir with the dolomitic limestone as top seal.\u003c/p\u003e","manuscriptTitle":"Characterization of Hydrocarbon Bearing Jardepahar Porcellanite Formation, Vindhyan Basin","msid":"","msnumber":"","nonDraftVersions":[{"code":1,"date":"2024-03-25 14:27:38","doi":"10.21203/rs.3.rs-3957834/v1","editorialEvents":[{"type":"communityComments","content":0}],"status":"published","journal":{"display":true,"email":"[email protected]","identity":"researchsquare","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":true,"externalIdentity":"","sideBox":"","snPcode":"","submissionUrl":"/submission","title":"Research Square","twitterHandle":"researchsquare","acdcEnabled":true,"dfaEnabled":false,"editorialSystem":"","reportingPortfolio":"","inReviewEnabled":false,"inReviewRevisionsEnabled":true}}],"origin":"","ownerIdentity":"df4a5611-37a4-4758-a3d6-794e04c64cda","owner":[],"postedDate":"March 25th, 2024","published":true,"recentEditorialEvents":[],"rejectedJournal":[],"revision":"","amendment":"","status":"posted","subjectAreas":[],"tags":[],"updatedAt":"2024-04-09T08:29:13+00:00","versionOfRecord":[],"versionCreatedAt":"2024-03-25 14:27:38","video":"","vorDoi":"","vorDoiUrl":"","workflowStages":[]},"version":"v1","identity":"rs-3957834","journalConfig":"researchsquare"},"__N_SSP":true},"page":"/article/[identity]/[[...version]]","query":{"redirect":"/article/rs-3957834","identity":"rs-3957834","version":["v1"]},"buildId":"qtupq5eGEP_6zYnWcrvyt","isFallback":false,"isExperimentalCompile":false,"dynamicIds":[84888],"gssp":true,"scriptLoader":[]}