The Asmari Formation is composed of limestones, marly limestones, and marls, whose subsurface thickness in this region is about 148 m. Two assemblage zones have been recognized through the distribution of large foraminifera in the study area, indicating a Late Oligocene (Chattian)-Early Miocene (Aquitanian) age. The gradual facies changes and the lacking of turbiditic deposits show that the Asmari Formation was deposited in a carbonate ramp environment. Based on the depositional textures and petrographical studies, characterizing gradual shallowing upward trends of an open marine carbonate ramp, three distinct depositional settings have been recognized: lagoon, barrier, and open marine. MF1 was characterized by the occurrence of hyaline benthic and planktonic foraminifera representing distal middle ramp and below the storm wave base of other ramp. Paleolatitudinal reconstructions based on skeletal grains suggest that carbonate sedimentation of the Asmari Formation took place in tropical waters within the photic zone.
- Asmari Formation
- benthic foraminifera
- Qeshm Island
This chapter deals with the Asmari Formation (one of the best known carbonate reservoirs in the world) , an Oligocene-Miocene carbonates succession cropping out in the south-eastern Zagros basin, southern Iran (Figure 1). At the type section outcropping in Tang-e Gel-e Tursh (Valley of Sour Earth), which is located on the south-western flank of the Kuh-e Asmari anticline, the Asmari Formation mainly consists of limestones, dolomitic limestones, and argillaceous limestones [3, 4], having an average thickness of 314 m. In the Qeshm Island, the Asmari shallow marine limestone is located in the subsurface and was deposited over the Pabdeh Formation with a gradational stratigraphic contact. The contact with the overlying Gachsaran Formation (i.e., evaporitic rocks) is conformable and gradual (Figure 2). This formation is present in the most part of the Zagros basin, and its lithology is characterized by limestones, dolomitic limestones, dolomites, and marly limestones. Some anhydrite (Kalhur Member) and lithic and limy sandstones (Ahwaz Member) also occur within the Asmari Formation [3, 4]. Previous studies have focused on biostratigraphy and lithostratigraphy of the Asmari Formation and were originally defined in primary works [5, 6, 7, 8]. Later, other researchers have introduced the microfaunal characteristics and the assemblage zones for the Asmari Formation [2, 9, 10]. More recent studies of the Asmari Formation have been conducted on facies and sedimentary environment [8, 11, 12, 13, 14, 15, 16, 17]. Referring to the biostratigraphy of the Asmari Formation, it was earlier outlined in the 1960s based on unpublished reports . The application of the isotopic stratigraphy has later proved that the sediments ascribed to the Miocene “Aquitanian” are in fact Late Oligocene, Chattian in age. This was proved by the application of Sr-isotope stratigraphy to cored sections from 10 Iranian oil fields and 14 outcrop sections, within the framework of a high-resolution sequence stratigraphic study down to fourth order cycles. The Chattian/Aquitanian boundary is marked by a major faunal turnover, with the general extinction of
2. Geological setting
The Zagros Basin is the second largest basin in the Middle East and is defined by a 7–14-km thick succession of coverage sediments deposited over a region located along the north-northeast edge of the Arabian plate. This basin was part of the stable Gondwana supercontinent in the Paleozoic era and of a passive margin in the Mesozoic era, and it became a site of plate convergence and formation of thrust belts in the Cenozoic era . The Zagros Fold-and-Thrust Belt of Iran is a result of the Alpine orogenic events [21, 22] in the Alpine-Himalayan mountain range. It extends in a NW-SE direction from eastern Turkey to the strait of Hormoz in southern Iran. The tectonic activity of this area was entirely due to the convergence of the Arabian and Eurasian continents. After the closure of the Neo-Tethys basin, during late Oligocene-early Miocene times, the Zagros basin was gradually narrowed and the Asmari Formation was deposited with a lithology including lithic sandstone (Ahwaz Member) and evaporites (Kalhur Member) [1, 23]. The maximum thickness of the Asmari Formation is found in the north-eastern corner of the Dezful Embayment. On the basis of the lateral facies variations, the Iranian Zagros fold-thrust belt is divided into different tectono-stratigraphic domains, which are from SE to NW: the Fars Province or eastern Zagros, the Khuzestan province or Central Zagros, and finally the Lurestan Province or Western Zagros [3, 4] (Figure 3b). Also, from south-west to north-east of the Zagros basin, there are the Zagros folded belt, folded and thrusted belt, and High Zagros and crush zone [25, 26, 27, 28]. The Hormozgan Province is located in southern Iran and is part of Zagros Folded belt. This region is accompanied by NW-SE, W-E, and N-S trending simple anticlines and synclines with very great thickness of Fars Group deposits (Gachsaran, Mishan, Aghajari, and Bakhtiari Formations) and presence of 118 salt plugs. So, for these specific features, Motiei [3, 4] called this area as the “Bandar Abbas Hinterland” (Figure 3).
3. Methods and study area
This study involves one stratigraphic subsurface section from the Asmari Formation. The study area is located at Qeshm Island, southern Iran (Figure 3c). The lithologies and the microfacies types were classified and described according to Dunham . Some samples from the underlying Pabdeh and overlying Gachsaran Formations were also analyzed for boundaries distinction. A total of 60 thin sections of the cores and cuttings have been analyzed under the microscope for biostratigraphy and facies. Petrographic studies were carried out for facies analysis and paleoenvironmental reconstruction of the Asmari Formation. Facies have been determined for each paleoenvironment according to carbonate grain types, textures, and interpretation of functional morphology of small and larger foraminifers. Biostratigraphy has been determined based on the well-known benthic foraminifera biozones of Adams and Bourgeois .
Biostratigraphic criteria of the Asmari Formation were established by Wynd  and reviewed by Adams and Bourgeois  in unpublished reports only. Biozonation and age determinations in the study area are based on benthic foraminifera biozonation of Adams and Bourgeois . From the base to the top, two foraminiferal assemblages have been recognized and were discussed as it follows:
4.2 Microfacies analysis
The microfacies analysis of the Asmari Formation in the study area has resulted in the definition of seven types of facies, which characterize the platform development. Each microfacies exhibits typical skeletal and non-skeletal components and related sedimentary textures. These facies are related to the three depositional settings (lagoon, barrier, and open marine) of inner, middle, and outer portions of a carbonate platform (Figure 4). Since the Asmari Formation overlies the Pabdeh Formation and conformably underlies the Gachsaran Formation, some samples from the Pabdeh and Gachsaran Formations have also been studied. The general environmental interpretation of the microfacies is discussed in the following paragraphs.
4.2.1 MF1 marl facies
There are intercalations of marl across the section, but this facies mainly occurs in the lower part of the succession (Figure 5A–D). They are gray to green marl and contain benthic (miliolids,
The features of benthic faunas and the stratigraphic relationships with the other microfacies suggest that the marly facies was deposited in an open lagoon with a normal-salinity water, but the coexistence of planktonic and some benthic (Nummulitidae) foraminifera in the base of the Asmari marls and marly limestones has suggested that this facies was deposited in calm, low-energy hydrodynamic, and deep normal-salinity water, which indicates a deposition below the storm wave base [33, 34, 35, 36].
4.2.2 MF2 bioclastic wackestone-packstone with Lepidocyclinidae, Nummulitidae, and Neorotalia
This microfacies is composed of grain-supported texture with abundant large benthic foraminifera (Figure 5E–G). The foraminiferal assemblage is represented by numerous large benthic perforate foraminifera such as Lepidocyclinidae and Nummulitidae (
It consists of gray marly limestone beds. The combination of micritic matrix and abundance of typical open marine fauna including large Nummulitidae, Lepidocyclinidae and Neorotalia suggest a low-medium energy, open marine environment. Other bioclasts such as red algae and shell fragments are rare. This microfacies shows an environment between the storm wave base and fair-weather wave base (FWWB) [35, 36]. The presence of large
4.2.3 MF3 coral boundstone
This microfacies is interpreted to be formed by in situ organisms as an organic reef (Bioherm) in margin of platform and was located above the fair-weather wave base (FWWB) .
4.2.4 MF4 miliolids corallinacea bioclastic wackestone
Miliolids, coralline red algae and coral are dominating components in this microfacies (Figure 5J and K). Other bioclasts are rare but include
The MF5 represent low- to medium-energy open lagoon shallow subtidal environments, but there is different from MF4 by their texture and grain composition.
Depositional textures, fauna and stratigraphic position took place in warm, euphotic and shallow water, with low to moderate energy conditions, in a semirestricted lagoon. This area is located within inner carbonate platform setting . The presence of well-preserved coralline algae indicates a relatively quiet-water environment with a stable substrate and low sedimentation rates . The associations of miliolids within this facies support the additional interpretation of a relatively protected environment, probably the inner part of a platform .
4.2.5 MF5 miliolids bioclastic wackestone
This facies is characterized by the dominant presence of small benthic foraminifera (miliolids) (Figure 5L and M). Other components such as
This facies is characterized by low diversity skeletal fauna and was deposited in a restricted low-energy lagoonal environment. There is a low biotic diversity of fauna, which shows a high-stressed habitat in very shallow restricted areas, where great fluctuations in salinity and temperature probably occurred .
4.2.6 MF6 imperforate foraminifera bioclast wackestone-packstone
The main elements of this microfacies are skeletal and non-skeletal components (Figure 5N and O). The skeletal components include a high diversity of imperforate foraminifera in grain-supported textures and several genera of benthic foraminifera (
The occurrence of large number of porcelain imperforate foraminiferal tests may point to the depositional environment being slightly hypersaline . These deposits include different textures ranging from wackestone to packstone. Some porcelain imperforate foraminifera (
4.2.7 MF7 evaporite
Anhydrite and gypsum facies have been observed in the upper part of the Asmari Formation, which represents the beginning of the Gachsaran Formation (Figure 5P). The first anhydrite has been deposited above the marly limestones with a sharp contact.
Considering the deposition of anhydrite implies that the depositional environment became isolated from the open marine at that time, which has allowed for the concentration and submarine precipitation of salt. The thickness of the evaporate deposits indicates that they are submarine deposits formed in an isolated saline basin. A eustatic sea level fall is one of the most likely causes. This event took place around the early Miocene (Aquitanian), and its stratigraphic expression was recorded at the boundary of the Asmari and Gachsaran Formations. Based on Ehrenberg et al. , this anhydrite is exposed at the top of the Asmari Formation and indicates the Oligocene-Miocene boundary. Ehrenberg et al.  noted that strontium dates got from anhydrite formed as an evaporate rather than as a later diagenetic product.
5.1 Sedimentary development of the Oligocene-Miocene Fars sub-basin
Planktonic and benthic foraminifera and non-foraminifera distribution of the Oligocene deposits can represent the type of sedimentary environment, adopted from joint project of French and Iran Oil Company  (Figure 6). During the Paleogene, Pabdeh (basinal marls and argillaceous limestones) Formation was deposited in the middle and on both sides of the Zagros basinal axis  (Figure 1). The shallow marine limestones of the Asmari Formation were deposited above the Pabdeh Formation in the section of this study (Figure 1). During the Rupelian and early Chattian, outer ramp facies (Pabdeh Formation) was predominant at the Qeshm section (well no. 3) (Figure 2). This is visible in the lower part of the Asmari Formation. So, the Chattian sediments of the Asmari Formation in this section gradationally overlie the Pabdeh Formation. Indeed, Chattian basin in this time restricted by shallow subtidal environments.
Large benthic foraminifera (such as Nummulitidae) produced great amount of carbonates during the Early and Middle Paleogene. In the Oligocene, euphotic conditions prevailed and carbonate production related to these foraminifers (especially
5.3 Depositional environments
Three depositional environments have been identified in the Oligocene-Miocene succession of the Qeshm Island, on the basis of the biostratigraphic content and of the facies relationships (Figure 6). These include lagoon, barrier and open marine (Figure 4). These three environments are represented by seven microfacies types (MF1: distal middle ramp and below the storm wave base of other ramp, MF2: deeper fair water wave base of a middle ramp setting and MF 3–6: shallow water setting of an inner ramp influenced by wave and tide processes). Carbonate ramp environments are characterized by (1) the inner ramp, between the upper shore face and fair weather wave base, (2) the middle ramp, between fair weather wave base and storm wave base and (3) the outer ramp, below normal storm wave base down to the basin plain . Inner ramp deposits represent marginal marine deposits indicative of open lagoon and protected lagoon. In the restricted lagoon environment, faunal diversity is low and normal marine faunae are lacking, except for imperforate benthic foraminifera such as miliolids and
The Oligo-Miocene Asmari Formation is a thick sequence of shallow water carbonates and is widespread in the Zagros basin. The subsurface section of the Asmari Formation in the south-eastern part of the Zagros and Qeshm Islands has allowed to recognize different depositional environments based on the sedimentological analysis, on the distribution of the foraminifera and on the microfacies studies. The occurrence of large foraminifera (
The studies were supported by National Iranian Oil Company (NIOC). The authors wish to thank the Exploration Directorate (NIOC) for financial support and permission to publish this research.