Geochemical characterization of the Krishna–Godavari and Mahanadi offshore basin (Bay of Bengal) sediments: A comparative study of provenance

Mazumdar, Aninda; Kocherla, M.; Carvalho, M. A.; Peketi, A.; Joshi, R.; Mahalaxmi, P.; Joao, H.M.; Jisha, R.

doi:10.1016/j.marpetgeo.2014.09.005

Cited by 57 publications

(31 citation statements)

References 69 publications

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“…Increase in contribution from basalt to the sediment load is further supported by an upcore decrease in La/Yb ratios (Figure 9b) [Dezileau et al, 2004]. The average La/Yb ratio of Deccan basalt is 5.9 6 1.7 and it varies from 2.6 to 9.4 [Chandrasekharam et al, 1999;Sano et al, 2001;Melluso et al, 2004;Sheth et al, 2004;Bondre et al, 2006] and that of APGC is 47.6 6 27.3 (7.3-109.7) [Moyen et al, 2003]. Based on magnetic studies of Godavari river sediments, Sangode et al [2007] suggested Deccan provenance as the most significant source of ferrimagnetic iron minerals.…”

Section: Possible Iron Sourcesmentioning

confidence: 79%

“…The sediments of the K‐G basin are derived from the Archean‐Proterozoic peninsular gneissic complexes (APGC) and Deccan basalts [ Mazumdar et al ., ]. Ferruginous soil covers [ Rengasamy et al ., ; Bhattacharyya et al ., ; Goulart et al ., ; Kisakurek et al ., ; Ollier and Sheth , ; Bhattacharyya et al ., ] developed over these provenances are the sources of reactive iron (Fe HR ) to the depositional basin.…”

Section: Discussionmentioning

confidence: 99%

“…Tropical semiarid climatic conditions prevail in most parts of the catchment area. The catchment area is occupied by Archaean‐Proterozoic granitic complex, Tertiary Deccan traps (basaltic) and recent sediments [ Ramesh and Subramanian , ; Biksham and Subramanian , ; Mazumdar et al ., ].…”

Section: Geologymentioning

confidence: 99%

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Coupled C–S–Fe geochemistry in a rapidly accumulating marine sedimentary system: Diagenetic and depositional implications

Peketi

Mazumdar

Joao

et al. 2015

Geochem Geophys Geosyst

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In the present study, we have investigated the C–S–Fe systematics in a sediment core (MD161‐13) from the Krishna‐Godavari (K‐G) basin, Bay of Bengal. The core covers the late Holocene period with high overall sedimentation rate of ∼573 cm kyr−1. Pore fluid chemical analyses indicate that the depth of the present sulfate methane transition zone (SMTZ) is at ∼6 mbsf. The (ΔTA + ΔCa + ΔMg)/ ΔSO42− ratios suggest that both organoclastic degradation and anaerobic oxidation of methane (AOM) drive sulfate reduction at the study site. The positive correlation between total organic carbon content (TOC) and chromium reducible sulfur (CRS) content indicates marked influence of organoclastic sulfate reduction on sulfidization. Coupled occurrence of 34S‐enriched iron sulfide (pyrite) with 12C‐enriched authigenic carbonate zones is the possible records of paleo‐sulfate methane transition zones where AOM‐driven‐focused sulfate reduction was likely fueled by sustained high methane flux from underlying gas‐rich zone. Aluminum normalized poorly reactive iron (FePR/Al) and La/Yb ratios suggest increasing contribution from Deccan basalts relative to that of Archean‐Proterozoic granitic complex in sediment flux of Krishna‐Godavari basin during the last 4 kyr.

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Section: Possible Iron Sourcesmentioning

confidence: 79%

Section: Discussionmentioning

confidence: 99%

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Coupled C–S–Fe geochemistry in a rapidly accumulating marine sedimentary system: Diagenetic and depositional implications

Peketi

Mazumdar

Joao

et al. 2015

Geochem Geophys Geosyst

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“…Deccan basalts and Precambrian metamorphic rocks in the hinterlands surrounding the K‐G basin are potential sources of detrital pyrrhotite in the studied samples (Ramesh & Subramanian, ). Clay mineralogical studies have demonstrated that the peninsular rivers are the major supplier of sediments to the K‐G basin (Mazumdar et al, ; Rao et al, ; Rao, ). Hence, the monoclinic pyrrhotite identified in the much wider gas hydrate bearing sediment magneto zone (Z‐III) of Hole‐NGHP‐01‐05C (Figures i–j) is interpreted to have a detrital origin.…”

Section: Discussionmentioning

confidence: 99%

Magnetic Mineralogical Approach for the Exploration of Gas Hydrates in the Bay of Bengal

et al. 2019

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We evaluate the environmental magnetic, geochemical, and sedimentological records from three sediment cores from potential methane-hydrate bearing sites to unravel linkages between sedimentation, shale tectonics, magnetite enrichment, diagenesis, and gas hydrate formation in the Krishna-Godavari basin. Based on downcore rock magnetic variations, four sedimentary magnetic property zones (I-IV) are demarcated. A uniform band of enhanced magnetic susceptibility (zone III) appears to reflect a period of high-sedimentation events in the Krishna-Godavari basin. Highly pressurized sedimentary strata developed as a result of increased sedimentation that triggered the development of a fault system that provided conduits for upward methane migration to enter the gas hydrate stability zone, leading to the formation of gas hydrate deposits that potentially seal the fault system. Magnetic susceptibility fluctuations and the presence of iron sulfides in a magnetically enhanced zone suggest that fault system growth facilitated episodic methane venting from deeper sources that led to multiple methane seepage events. Pyrite formation along sediment fractures resulted in diagenetic depletion of magnetic signals and potentially indicates paleo sulfate-methane transition zone positions. We demonstrate that a close correlation between magnetic susceptibility and chromium reducible sulfur concentration can be used as a proxy to constrain paleomethane seepage events. Our findings suggest that the interplay between higher sedimentation events and shale tectonism facilitated fluid/gas migration and trapping and the development of the gas hydrate system in the Krishna-Godavari basin. The proposed magnetic mineralogical approach has wider scope to constrain the understanding of gas hydrate systems in marine sediments.

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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

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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Geochemical characterization of the Krishna–Godavari and Mahanadi offshore basin (Bay of Bengal) sediments: A comparative study of provenance

Cited by 57 publications

References 69 publications

Coupled C–S–Fe geochemistry in a rapidly accumulating marine sedimentary system: Diagenetic and depositional implications

Coupled C–S–Fe geochemistry in a rapidly accumulating marine sedimentary system: Diagenetic and depositional implications

Magnetic Mineralogical Approach for the Exploration of Gas Hydrates in the Bay of Bengal

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

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