The studied section is located in Central Iran, in 35km southeast of Shahreza in Ramsheh area. The Ramsheh area structurally belongs to the southwest Central Iran including the Shahreza- Abadeh- Hambast belt, which is separated by faults from the Gavkhoni- Abarquh depression to the northeast and from the Yazdekhast-Dehbid metamorphism belt to the southeast.The Carboniferous deposits with 620m thickness including Shishtu2 and sardar Formations, the former (Shishtu2 Fm), mainly consists of 315m dark to gray limestones with dolomites and alternation of thin to medium bedded platy shales. According to Conodont funa the following Conodozones are recognized: 1-? expansa-sulcata zone 2-duplicate zone 3-typicus zone 4-ancuralis-latus zone The upper part (Sradar Fm.) with 298m thickness consists of carbonate-terrigenous deposits including limestones, sandy limestones conglomerate and oolitic limestones with conodont funa. The following conodozones are recognized from this part: 1-muricatus zone 2-noduliferous zone 3-sinutus-minutus zone 4- sinusus-delicatus zone 5-?elongatus zone The section checked with regard to Conodont biostratigraphy and depositional environment. According to the above mentioned Conodozones, the Carboniferous deposits in Asadabad section dated from Tournasian to Moscovion in age.The topmost of the section with the Vajnan Formation have parallel disconformity and the lower boundary is covered. The upper located among rocks of late Carboniferous is probably related to global variation of sea level due to glacial epoch (Late Carboniferous) in vast area of Gondwanan Supercontinent.

The studied section is located in Central Iran, 135 km southeast of Isfahan in Ramsheh area (latitude N 31o 46' 65", longitude E 52o 8' 63") GPS-WGS84 coordinates. The Ramsheh area structurally belongs to the Southwest-Central Iran and is checked regarding to microfacial and paleoinvironmental points of view as well as to biostratigraphical evidences. Carboniferous depositions (including Shishtu II sub Formation and Sardar Formation) are formed from limestones, dolomylimestones, shales, sandylimestone, sandstones and oolitich limestones. Based on detailed petrographical investigations and field studies, 15 mircofacies have been identified: 13 of them belong to carbonate microfacies that form in four sub-sedimentary environments, including Open marine, Barrier, Lagoon and Tidal flat and the other 2 microfacies show clastic material presence. The facies sequences observed in the carbonate platform sedimentation are the result of changes in environment through time and by natural processes operating within the environment or by fluctuations in the external factors controlling sedimentation such as tectonic activities and change in a sea-level. A characteristic of carbonate platform is its continuation without any breakage into the deepwater sedimentation.

Rich assemblages of Carboniferous corals exist in the Zaladu stratigraphic section. After identification of corals, more than 200 thin sections of coral fossils and microfacies were selected and studied for environmental parameters. This association belonging to BASHKIRIAN age (the oldest stage of Late Carboniferous) and were found in two horizons. Based on the colonies geometry, the distance between them, the abundance and distribution of corals and microfacies study, the habitats of lower horizon is “ Coral meadows (subtype B1) “. The upper horizon made a“polyspecific Coral biostrome (subtype C2) “. These corals existed in a lagoon toward barrier and open marine toward barrier belonging to a shallow carbonate ramp environment. This association favored a shallow, warm, and clear marine environment with normal salinity and high oxygen, within the photic zone. The fasciculate rugoseFomichevella and Heintzella, have the most abundance, and these colonies form the main builders of the coral association. Colonial rugose coralsFomichevella and Minatoa have maximum diversity. Michelinia tabulate corals, has the least abundance and diversity.

The studied sections are located in southwestern of central Iran. Main lithology of these sections are including shale, sandstone and limestone. Four biozones had been recognized base on Conodont. That contain Idiognathodus delicates Zone, Streptognathodus oppletus Zone, Sweetognathus whitei Zone. And Neostreptognathodus pequopensis Zone. Based on recognized conodont, the age reveal for Sardar Formation is BASHKIRIAN-early Gzhelian and the Permian deposits are Artinskian (khan formation age equivalent). In this sections Carboniferous-Permian boundary has been seen paraconformity. Comparison this area with neighborhood showed after Kasimovian we have upward and erosion in these areas and with started melting due to glacial epoch in lower Permian so these areas covered with water although we have shallow basin comparable with another areas in Central Iran.

In this study, 60 samples have been studied from Carboniferous deposits of Khames stratigraphical section, 10 Km southeast of Khalkhal. The marine sequence of Khames stratigraphical section is about 163.5 m. thick and consists of gray to black Limestone and dolomitic limestone.The lower boundary of the under study section marked with yellowish limestones of Cretaceous and dark Sills with Faulted contact. The upper boundary of the Carboniferous strata is covered with Pliocene Polygenetic conglomerate disconformably. The Carboniferous unit studied here has not been named so far, so in this research, we have attempted to identify the stratigraphical position of the mentioned sequence. In this research 30 genera and 25 species of benthic foraminifera were identified similar to those reported from carboniferous strata of Qezelqaleh, Bagher Abad, Mobarak and Sardar formations suggesting a Late Visean to Early BASHKIRIAN age for the Khames Carboniferous marine sequence.

The Upper Palaeozoic strata widely crop out in the Marselan Valley, 28 km northeast of Loshan, north of Sangrud. The litho- and biostratigraphic study led to identification of 57 species (distributed among 37 genera) of foraminifera and 8 genera and species of algae. Three lithologic units (formations), seven lithozones and three assemblage zones are identified within the study interval. The rock units of the Permian system are in descending order as: a) Doroud Formation (Asselian- Sakmarian, thickness of 225 m), underlain disconformably by the middle Carboniferous (BASHKIRIAN- Moskovian) Khashachal Formation, consists of red conglomerate, sandstone, shale, siltstone and buff oncoid limestone that can be divided in to three lithozones. b) Ruteh Formation (Murghabian, thickness of 364 m) mainly composed of cliff forming limestone that can be divided into two lithozones, unconformably overlying the Doroud Formation. c) Nessen Formation (early Djulfian, thickness of 140 m) consists of marly limestone intercalated with shale (contains of two lithozones), unconformably underlain by the Ruteh Formation and overlain disconformably by Elika Formation of Early-Middle Triassic age. Thin beds of laterite-bauxite indicate an unconformity at the Permian-Triassic boundary. Also these beds reveal that the study area, with a humid warm temperature, was lying near lat. 30°S.