The Eocene Rusayl Formation, Oman, carbonaceous rocks in calcareous shelf sediments: Environment of deposition, alteration and hydrocarbon potential

Dill, Harald G.; Wehner, H.; J, Kuś; Botz, R.; Berner, Zsolt; Stüben, Doris; Al-Sayigh, Abdul Razak

doi:10.1016/j.coal.2006.12.012

Cited by 33 publications

(15 citation statements)

References 44 publications

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“…The calculated temperature, based on Land's equation (1985), from the heaviest 8 180 value (-1.1%0 PDB) of very fine to finely crystalline dolomite yield a temperature of~34' C. This temperature is close to the temperature of modem supratidal settings (~40' C), such as the Persian Gulfsabkha, in which dolomite is forming today (Dill et al 2007). For temperature c~lculation of dolomite type 1 (the earliest formed dolomite), the 8 w value of-l.2%o(SMOW) was used for the Upper Jurassic seawater (price and Sellwood 1994).…”

Section: Temperature Of Formationmentioning

confidence: 99%

Multistage dolomitization of upper jurassic mozduran formation, Kopet-Dagh Basin, n.e. Iran

Adabi

2009

Carbonates and Evaporites

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This paper is a study of the origin and diagenetic history of the Upper Jurassic dolomites of the Mozduran Formation, from north eastern Iran, in the Kopet-Dagh Basin. Petrographic and geochemical studies indicate that the Mozduran dolomites were subjected to a complex diagenetic history, resulting five different dolomite-rock textures.Dolomite type 1 consists ofvery fine to finely crystalline dolomite, forming penecontemporaneously or by early replacement ofcarbonate mud, soon after deposition, with Mg possibly derived from seawater. Dolomite type 1 has the most enriched 8180 values (-1.1%0 PDB), compared to other dolomite types. On the basis ofcrystal size, fabric, and absence offossils, dolomite type 1 is considered to have been formed in a supratidal to upper intertidal setting, under near surface, low temperature (~34'C) conditions. Dolomite type 2 consists mainly ofeuhedral rhombs floating in a limestone matrix. This dolomite type resulted from replacement ofprecursor calcium carbonate, mainly during early shallow burial, and Mg was probably derived from dissolution ofhigh-Mg calcite. Dolomite type 3 is considered to represent a diagenetic replacement ofpre-existing limestone and/or recrystallization of an early formed dolomite, possibly after some burial. Dolomite type 4has medium to coarse nonplanar crystals, often characterized by nomnimically replaced allochems, developed during deep burial (~3.5 to~4 km), in temperatures ranging from 84 to 113' C. The last dolomitizing events are represented by dolomite type 5, which consists of coarsely crystalline planar-C (cement) dolomite, lining voids, vugs and fractures. This dolomite type has been interpreted as having formed at the latest diagenetic stage, at elevated temperature, ranging from 94 to~lID'C. Dolomite types 4 and 5, with t~highest temperatures offormation, possibly formed during the period ofmaximum burial, between Paleocene and Eocene time.Compaction of shales and clay diagenesis, combined with basinal brines, could produce enough magnesium for shallow to deep burial dolomitization (dolomite types 3 and 4), and dolomite cementation (dolomite type 5). The presence ofhigher concentrations of organic carbon in dolomites than limestones (~2 to 5 times higher), may indicate that dolomitization occurr~d preferentially in limestones that originally had higher concentrations of organic matter.

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Section: Temperature Of Formationmentioning

confidence: 99%

Multistage dolomitization of upper jurassic mozduran formation, Kopet-Dagh Basin, n.e. Iran

Adabi

2009

Carbonates and Evaporites

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“…These three formations are the Jafnayn, Rusayl and Seeb fms. The thicknesses of these formations are 126 m, 144 m and 600 m, and their ages are of late Paleocene to Eocene, early Eocene, and middle to late Eocene, respectively [1][2][3]. The contacts between the three formations within the Tertiary Ridge are conformable, whereas the contact between the Al-Khod Fm.…”

Section: Lithologymentioning

confidence: 94%

“…Whereas the sedimentary rocks of the Tertiary Ridge are well described and understood (e.g., [1][2][3]), its deformation has remained a largely untackled issue, despite the high visibility of the superbly and invitingly well-exposed folds within the Rusayl and Jafnayn fms. as in the road outcrop, which cuts across the ridge along the road leading from the north into the village of Al-Khod (Figure 3a, b), or as in natural outcrops ~1 km farther ESE in the western part of the ridge (Figure 3c).…”

Section: Introductionmentioning

confidence: 99%

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Kinematics of Post-obduction Deformation of the Tertiary Ridge at Al-Khod Village (Muscat, Oman)

Scharf

Mattern

Al-Sadi

2016

SQU Journal for Science

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Structural investigations in post-obductional Paleocene to Eocene limestones of the Tertiary Ridge reveal a ~1 km long WNW-ESE striking strike-slip fault system within the ridge, consisting of two main sub-parallel, strike-slip faults. Considering the geometry of the Harding Strain Ellipse, the orientation of structures between the two strike-slip faults (e.g., Riedel shears, folds, reverse faults) point to left-lateral motion. The abundance of large-scale folds (up to 100 m in wave length and amplitude) between the two strike-slip faults led us to the interpretation of transpressive conditions in a first approximation. Moreover, the Tertiary Ridge of the study area consists of three distinct structural domains. The faults of Domain A and C are oriented WNW-ESE, but the trend of the faults in the central Domain B differs by ~10°. The left-lateral strike-slip fault system exists only in Domain B. We propose that the direction of greatest stress during Miocene plate convergence (sigma 1) was oriented 032°/212°. Considering the trend of the strike-slip zone and the orientation of sigma 1, the left-lateral motion must have been transpressive. Sigma 1 is perpendicularly oriented to the domains A and C.Prior to the Miocene D2 compressional event the study area was affected by a D1 extensional event, related to the opening of the Red Sea and the Gulf of Aden or to gravity-driven normal faulting. The D2 compressional/transpressional structures of the Miocene are reactivating the D1 structures of the Oligocene.

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“…The paleoenvironmental models of Eocene assemblages described inter alia by Eichenseer and Luterbacher (1992), Loucks et al (1998), andRacey (2001) refer to a ''bank'' of larger foraminifera made up of Nummulites and Alveolina. A subtidal (to intertidal) depositional environment down to a depth of 40 m on the middle ramp with sea grass meadows was described for the calcareous lower Eocene Seeb Formation in Oman and may be a facies description also to be adopted for the lithofacies of section I (Dill et al 2007). Dolomite in places ferroan and little siderite in section II are indicative of an early diagenetic alteration stage under rather moderate temperatures of formation and, locally, anoxic conditions.…”

Section: Middle Me´tlaoui Formationmentioning

confidence: 99%

Paleontological, mineralogical and chemical studies of syngenetic and epigenetic Pb–Zn–Ba–P mineralizations at the stratotype of the K/P boundary (El Kef area, Tunisia)

Dill

Weiss

Botz

et al. 2010

Int J Earth Sci (Geol Rundsch)

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The El Kef area, Tunisia, is host of the official stratotype of the K/P boundary and of a complex metallic and non-metallic mineralization at Djebel Sekarna, encompassing syn(dia)genetic shale-and carbonate-hosted Zn-P and epigenetic Pb-Zn-Ba ore mineralizations. Micropaleontological, geological, mineralogical, and chemical studies (major and minor elements, C-and O-isotopes) of Upper Santonian to Lower Eocene calcareoussiliciclastic sediments resulted in a subdivision of this mineralization into eight mineralizing stages. Stages 1 and 2 (late Cretaceous-early Paleogene) are representative of syn(diagenetic) shale-and carbonate-hosted sulfidic and siliceous (Fe)-Zn-P mineralization deposited in shallow marine to slightly brackish sediments. Stages 3-5 (early Eocene respectively-pre-and post-Nummulites involutusexilis zones) are representatives of epigenetic sulfidic and sulfatic (Fe)-Zn-Pb-Ba mineralizations at temperatures as high as 170/200°C and stages 6 and 7 (early Eocene respectively-post-Alveolina oblonga zone) cover the nonsulfidic Zn-(Pb) mineralization at temperatures as high as 60°C which is transitional from hypogene into supergene mineralization (''epithermal calamine deposits''). Stage 8 represents alteration of the pre-existing mineral assemblages in course of the Holocene weathering. The Cretaceous through Paleogene aquatic system is characterized by a poisoning of the sea with base metals, mainly Zn, and the atmosphere was chocked with clouds of fine-grained volcanic ejecta. Both processes contributed to the build-up of Zn-(Pb) deposits and vast, but uneconomic bentonitic clay deposits around the K/P boundary. Ore mineralization in the El Kef area is a multiple-phase process which reached its climax during the early Eocene as indicated by the large foram zones. These inorganic concentration processes resulting in the formation of mineral deposits had obviously also a negative effect on the long-term course of regional Earth's biological history during the late Cretaceous-early Eocene period with lethal consequences for some species. The joint studies of inorganic and organic data reveal that such extraordinary metallogenetic processes close to the K/P boundary in its stratotype area in Tunisia were ''strictly terrestrial''.

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The Eocene Rusayl Formation, Oman, carbonaceous rocks in calcareous shelf sediments: Environment of deposition, alteration and hydrocarbon potential

Cited by 33 publications

References 44 publications

Multistage dolomitization of upper jurassic mozduran formation, Kopet-Dagh Basin, n.e. Iran

Multistage dolomitization of upper jurassic mozduran formation, Kopet-Dagh Basin, n.e. Iran

Kinematics of Post-obduction Deformation of the Tertiary Ridge at Al-Khod Village (Muscat, Oman)

Paleontological, mineralogical and chemical studies of syngenetic and epigenetic Pb–Zn–Ba–P mineralizations at the stratotype of the K/P boundary (El Kef area, Tunisia)

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