Early Eocene carbonaceous shales of Tadkeshwar Formation, Cambay basin, Gujarat, India: Geochemical implications, petrogenesis and tectonics

Pundaree, Nandigama; Krishna, A. Keshav; Subramanyam, K.S.V.; Sawant, S. S.; Kavitha, S.; Kalpana, M.S.; Patil, D. J.; Dayal, A. M.

doi:10.1016/j.marpetgeo.2015.08.028

Cited by 10 publications

(12 citation statements)

References 28 publications

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“…transported away (Fedo, Nesbitt, & Young, ). Therefore, such elemental enrichment and depletion can be used as a guide for estimating the intensity of chemical weathering for the siliciclastic source materials (Ghosh & Sarkar, ; Lee, ; Moradi et al, ; Pundaree et al, ). The concentrations of those chemical elements are generally controlled by weathering duration, diagenetic processes, original composition of the parent material, average tectonic uplift of the source region, and climatic variations (Akarish & El‐Gohary, ; Buggle, Glaser, Hambach, Gerasimenko, & Markovic, ; Ghosh & Sarkar, ; Hofmann, Li, Chen, MacKenzie, & Hinman, ; Moosavirad, Janardhana, Sethumadhav, Moghadam, & Shankara, ; Nagarajan et al, ).…”

Section: Discussionmentioning

confidence: 99%

Geochemical fingerprinting of Maastrichtian oil shales from the Central Eastern Desert, Egypt: Implications for provenance, tectonic setting, and source area weathering

et al. 2017

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Upper Cretaceous oil shales accumulated in intracratonic sedimentary basins along the Central Eastern Desert. Comprehensive geochemical analyses have been applied on 3 Maastrichtian oil shale horizons from the Duwi and Dakhla formations (El‐Beida and El‐Nakheil mines). We provide significant clues for chemical weathering, sediment recycling, petrogenesis, and tectonic setting of oil shales' source material. The mineralogical composition of the studied oil shales is generally characterized by carbonates, phyllosilicates, quartz, fluorapatite, and sulphides. The geochemistry is characterized by high Ca, P, Ni, U, and Cr values compared to standard post‐Archean Australian shales (PAAS). Their chondrite‐normalized patterns are distinguished by LREE enrichment, HREE depletion, negative Eu anomaly, and typical shale‐like PAAS‐normalized REE patterns. Furthermore, the total REE content is positively correlated with Si, K, Na, Fe, Al, Ti, and Mn, indicating that the REE of the investigated oil shales originated from terrigenous sources. Diverse proxies (e.g., CIA, CPA, and PIA) and the A–CN–K ternary diagram suppose that the source rock succession of the oil shales experienced moderate to intensive chemical weathering. Various geochemical parameters suggest that the oil shales were predominately derived from intermediate, with a minor contribution from felsic, igneous source rocks without any remarkable recycling signals. The average values of (Gd/Yb)N (1.39), Eu/Eu* (0.76), Th/U (0.29), and discrimination diagrams reveal that the oil shales were derived from Neoproterozoic island arc parent rocks. The geochemical results for oil shale provenance are in accordance with the composition and the palaeotectonic history of the igneous rocks in the Central Eastern Desert of Egypt.

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Section: Discussionmentioning

confidence: 99%

Geochemical fingerprinting of Maastrichtian oil shales from the Central Eastern Desert, Egypt: Implications for provenance, tectonic setting, and source area weathering

et al. 2017

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“…Общее число объектов в банке данных больше, чем обсуждается в данной работе), рифты, сформированные на ранних этапах распада суперконтинентов (объекты №№ 47, 74, 76, 79, 81, 83, 86 и 88), пулл-апарт бассейны (№ 75) и рифтовые структуры, так или иначе связанные с процессами субдукции (№ 77) и коллапсом орогенов (№ 82) на таких дискриминантных палеогеодинамических диаграммах, как K 2 O/Na 2 O-SiO 2 /Al 2 O 3 (Maynard et al, 1982), SiO 2 -K 2 O/Na 2 O (Roser, Korsch, 1986) и DF1-DF2 (Verma, Armstrong-Altrin, 2013). К рассматриваемым далее образованиям относятся глинистые породы: 1) неопротерозойской серии Юинта Маунтин, США (объект № 2) (Condie et al, 2001); 2) ордовикской (тремадок) формации Тину, Южная Мексика (№ 47) (Murphy et al, 2005); 3) серий Асу Ривер и Кросс Ривер Нижнего трога Бенуэ, Юго-Восточная Нигерия (№ 70) (Adeigbe, Jimoh, 2013); 4) формаций Бир Магхара и Сафа, байос-бат, Северный Синай, Египет (№ 74) (Ghandour et al, 2003); 5) осадочного выполнения бассейна Сатпура, пермь-триас, Центральная Индия (№ 75) (Ghosh, Sarkar, 2010); 6) бассейна Конго, нижний мел, Западная Африка (№ 76) (Harris, 2000); 7) основания разреза Японского моря, нижний миоцен, Юго-Западная Япония (№ 77) ; 8) бассейна Олите, альб, Северо-Восточная Испания (№ 78) (Lopez et al, 2005); 9) бассейна Кришна-Годавари, Бенгальский залив, Индия (№ 79) (Mazumdar et al, 2015); 10) нижнего виндия, палеопротерозой?-мезопротерозой, долина р. Сон, Центральная Индия (№ 80) (Paikaray et al, 2008); 11) верхнего триаса-нижней юры гор Пелоритани, Северо-Восточная Сицилия, Южная Италия (№ 81) (Perri et al, 2011); 12) Фракийского бассейна, эоцен-олигоцен, Северо-Восточная Греция (№ 82) (Perri et al, 2015); 13) среднего триаса-верхней юры Внутренних Доменов запада Центральносредиземноморского региона (№ 83) (Perri, Ohta, 2014); 14) нижнего виндия, палеопротерозой?-мезопротерозой, Юго-Восточный Раджастан, Индия (№ 84) (Raza et al, 2002); 15) неопротерозойской формации Джонни, Юго-Восточная Калифорния (№ 86) (Schoenborn, Fedo, 2011); 16) формации Тадкешвар, нижний эоцен, бассейн Камбей, Индия (№ 87) (Pundaree et al, 2015); 17) Рифского сектора Магрибской цепи, средний-верхний триас, Морокко (объект № 88) (Zaghloul et al, 2010). Средние, минимальные и максимальные содержания основных породообразующих оксидов в синрифтовых глинистых породах перечисленных объектов приведены в таблице.…”

Section: объекты исследованияunclassified

“…8). Точки 16-ти из 17 объектов локализованы на ней в области составов, характерных для обстановок пассивных континентальных окраин, и только средняя точка глинистых пород нижнего эоцена бассейна Камбей (№ 87) оказалась в области составов, отвечающих обстановкам активных континентальных окраин, хотя, по данным (Pundaree et al, 2015), указанный бассейн считается принадлежащим к категории интракратонных рифтов.…”

Section: объекты исследованияunclassified

Synrift clayey rocks: bulk chemical composition and position on discriminant paleogeodynamic diagrams

Maslov¹,

Подковыров²,

Kotova³

2019

Геохимия

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The paper analyzes the bulk chemical composition and distribution of the fields of syn-rift clayey rocks on a number of discriminant paleogeodynamic diagrams. It is shown that, in general, there are significant variations in the bulk chemical composition for syn-rift clayey rocks. Thus, for example, the average SiO2 content varies from 44.74 to 66.42 wt. %, the average content of Al2O3 varies from 16.62 to 29.92 wt. %, and the K2Oaver are in the range 0.24 ... 5.77 wt. %. Based on the distribution of the figurative points of the syn-rift clayey rocks of various objects/riftogenous structures in the F1–F2 diagram, it can be assumed that the sources of fine aluminosilicoclastic were magmatic and sedimentary rocks of a wide range of compositions. The substantial overlap of the fields of various objects in the classification diagrams [(Na2O + K2O)/Al2O3]–[(Fe2O3tot + MgO)/SiO2] and K/Al–Mg/Al indicates, in general, the similarity of the compositions of the syn-rift fine-grained clastic rocks of various types of riftogenic structures. The localization of the composition fields of the clayey rocks of different riftogenous structures on such discriminant paleogeodynamic diagrams as K2O/Na2O–SiO2/Al2O3 and SiO2–K2O/Na2O suggests that they do not allow correctly distinguishing between syn-rift clayey rocks and fine-grained rosks of other geodynamic environments. The position of the syn-rift clayey rocks fields presented in our database on the diagram DF1–DF2 has its own characteristics. In most cases, they occupy a particular position in the areas characterizing collision and rifting environments, and a number of fields are located in all three classification areas of this diagram. A significant part of the midpoints of the syn-rift clayey rocks is localized in the DF1–DF2 diagram in the collision field. It seems that all of the above indicates that the DF1–DF2 diagram also does not allow us to obtain a correct information about the geodynamic nature of terrigenous associations.

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“…Surprisingly, despite the availability of a large set of geochemical data on the shale litho-units of India spanning the Archean and post-Archean time, no attempt has been made to date to estimate an average composition of Indian shales. For example, major and trace element data are available on shale samples from different sedimentary basins of India such as the Vindhyan Basin, − Gwalior Basin, Cuddapah Basin, − Kaladgi-Badami Basin, , Satpura Basin, Cambay Basin, Marwar Basin, Chhattisgarh-Indravati Basin, Spiti Basin, Assam-Arakan Basin, Kutch Basin, etc. Several studies have also reported the composition of shales from cratonic environments such as the Aravalli Craton and Dharwar Craton. , …”

Section: Introductionmentioning

confidence: 99%

Major and Trace Element Characteristics of the Average Indian Post-Archean Shale: Implications for Provenance, Weathering, and Depositional Environment

Ray

Paul

2021

ACS Earth Space Chem.

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We estimate the average chemical composition of Indian post-Archean Shale (IPAS) and conclude that it is comparable to that of global shale standards: post-Archean Australian Shale (PAAS) and North American Shale Composite (NASC). These shales are widely considered as continent wide, average compositional representatives of the post-Archean upper continental crust (UCC). Our IPAS estimate includes compiled literature (n = 444) and newly obtained (23 samples from 16 shale litho-units) data. The average IPAS has a composition comparable to that of the average, finegrained matrix of glacial diamictites (tillite). Compared to a global model of UCC, notable differences in some elements are observed. Our estimated IPAS composition is more comparable to PAAS than NASC, with the latter being distinctly different likely due to having been recently glaciated and significantly resurfaced by the last glaciation, resulting in new shale production starting only about 12,000 years ago. Comparisons between the post-Archean and Archean Indian shales finds the latter with lower ΣREE; smaller negative Eu anomaly; lower Th/Sc, Th/Cr, and Th/U ratios; and higher Sc, V, Cr, Cu, and Zn contents. These findings suggest a greater contribution from mafic sources to Archean shales. A higher chemical index of alteration (CIA = 80 ± 2) for Indian Archean shales, relative to the post-Archean shales (72 ± 3) and UCC (59−65), suggests more intense weathering in the pCO 2 -rich Archean time. Indian shales were mostly deposited in plate interiors or intracratonic basins along a passive margin based on tectonic discrimination diagrams. Our IPAS estimate reflects the average composition of Indian sedimentary rocks and serves as the first step toward estimating the chemical composition of Indian UCC.

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Early Eocene carbonaceous shales of Tadkeshwar Formation, Cambay basin, Gujarat, India: Geochemical implications, petrogenesis and tectonics

Cited by 10 publications

References 28 publications

Geochemical fingerprinting of Maastrichtian oil shales from the Central Eastern Desert, Egypt: Implications for provenance, tectonic setting, and source area weathering

Geochemical fingerprinting of Maastrichtian oil shales from the Central Eastern Desert, Egypt: Implications for provenance, tectonic setting, and source area weathering

Synrift clayey rocks: bulk chemical composition and position on discriminant paleogeodynamic diagrams

Major and Trace Element Characteristics of the Average Indian Post-Archean Shale: Implications for Provenance, Weathering, and Depositional Environment

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