Maastrichtian to early Tertiary stratigraphy and palaeogeography of the Central and Northern Oman Mountains

Abstract

Maastrichtian to Tertiary sedimentary rocks outcrop extensively around the periphery of the Oman Mountains. They form part of a geologically distinct suite of strata deposited after obduction of the Semail ophiolite and thrusting of the Hawasina and Sumeini imbricates onto the eastern edge of the Arabian plate. The lithostratigraphy of Maastrichtian and early Tertiary rocks of the central and northern Oman Mountains is revised and a number of new formations are erected. The proto-Oman Mountains were emergent in the early Maastrichtian and were subject to subaerial erosion and weathering. NW and W of the mountains, gradual subsidence followed during the Maastrichtian, allowing for formation of a transgressive, onlapping sequence represented by the Qahlah (fluviatile to shallow marine terrigenous clastics) and Simsima (shallow shelf carbonate) Formations. More rapid subsidence NE of the mountains produced fan delta and submarine debris flow/turbidite apron sequences comprising the Al Khawd and Thaqab Formations respectively. A low-angle unconformity separates Tertiary strata from older units. During the Palaeogene, basinal and slope facies with debris flows and turbidite sequences were deposited directly upon the unconformity surface in rapidly subsiding basins NW (Muthaymimah Formation) and NNE (Ruwaydah Formation) of the Oman Mountains. Elsewhere, shallow carbonate shelf facies were extensively developed in less rapidly subsiding areas during the Palaeogene. The Palaeocene and early Eocene is represented by the Jafnayn Limestone Formation. This is succeeded and overlapped by a variety of later Eocene units. ENE and E of the mountains early Eocene regression is marked by restricted facies of the Rusayl Formation. Overlying the Rusayl Formation are shallow, open shelf limestones of the Seeb Formation which is rich in alveolinid and nummulitic foraminifera. On the Arabian side of the mountains the Rusayl Formation is not developed and the Jafnayn Formation is succeeded either by the Seeb Formation or fine-grained, faunally restricted limestones and marls of the Fahud Beds, which represent intra-shelf facies.

Late Campanian–Maastrichtian foraminifera from the Simsima Formation on the western side of the Northern Oman Mountains

“…Owing to the inaccessibility of the subsurface type sections, Nolan et al (1990) designated the Jabal Al Faiyah section, on the western side of the Northern Oman Mountains (19 km northwest of Jabal El Rawdah) as an alternative surface type section for this formation. It unconformably underlies the Muthaymimah Formation, which appears to be of Paleocene to (Middle?)…”

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

“…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.…”

“…and three younger formations which collectively comprise the Tertiary Ridge [1] (Figure 5). These three formations are the Jafnayn, Rusayl and Seeb fms.…”

“…are represented by competent limestone beds, the intervening Rusayl Fm. consists of various lithologies, T including large quantities of marl, making this formation significantly less competent than the underlying and overlying formations (e.g., [1][2][3]). Simplified geological map of the greater study area.…”

“…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).…”