محمد داستانپور

With the advancement of science and technology in third world and developing countries, more and more   harmful factors in the working environment endanger the employees’ lives. One of these detrimental factors is the incompatibility of work with people’s characteristics, which causes musculoskeletal disorders. In developing countries this happens at the cost of musculoskeletal disorders. Therefore, this study aimed to investigate the effect of ergonomic interventions on reducing the prevalence of musculoskeletal disorders, and finally, use the results obtained to prevent musculoskeletal disorders and improve the working environment among the staff of Qeshm Zinc Smelting company, in 1399.

In this study, staff were randomly evaluated as a case control by the Nordic questionnaire, using QEC method and body map. Ergonomic interventions were then performed on the case group. After one month and four months, re-evaluation was performed by QEC and body map methods.

Findings indicated that 84.21% of the participants had musculoskeletal disorders in the past year before the study. Ergonomic interventions for musculoskeletal disorders in the lower back, shoulders, neck, knees and hands were significantly reduced.ftAer ergonomic interventions, the  risk factor of these disorders was significantly reduced. 

Therefore, by doing ergonomic interventions, including  teaching ergonomic principles, using automatic equipment, etc., musculoskeletal disorders in the back, shoulders, neck and knees were created and musculoskeletal disorders were reduced to 13.58%.

One of the effective factors in the occurrence of musculoskeletal disorders is the mismatch between the mental workload on the person and his abilities and limitations. Therefore, this study aimed to investigate the effect of mental workload on the prevalence of musculoskeletal disorders in Bandar Abbas Production Company.

This cross-sectional descriptive-analytical study was conducted in 2019. The data collection tools included demographic information questionnaires, Nordic musculoskeletal disorders, and NASA- TLX mental workload. The participants were 172 people who were identified using Cochran's formula and simple random sampling. The collected data were analyzed by SPSS 25 software.

The results indicated that 76.74% of the subjects had musculoskeletal disorders. Most of disorders were reported in the low back (51.16%), knees (38.95%), and neck (23.84%). The mean score of mental workloads in Bandar Abbas Production Company in this study was high (66.67). Among the mental workload subscales, the effort subscale had the highest score (85.32) and the performance subscale had the lowest score (20.00). Statistical tests showed that there was a significant relationship between mental workload and the prevalence of musculoskeletal disorders.

According to the findings of the study, there was a direct relationship between mental workload and the prevalence of musculoskeletal disorders. Therefore, measures should be taken to reduce the perceived mental and psychological load, such as reducing working hours, interrupting and resting between working, increasing the variety of working postures, and thus preventing the occurrence of musculoskeletal disorders.

In order to study the biostratigraphy, paleoecology and paleogeography of Qom formation ostracods, the Gonjan stratigraphical section was sampled and studied. 36 species and 23 genera of ostracods from Gonjan stratigraphical section have been studied and identified, which belong to two podocopid and platycopid orders. Based on the diversity of the identified foraminifera in this section and abundance of lepidocyclinids, the suggested age of  Qom Formation deposits in Gonjan section are Rupelian?-Chattian. The presence and abundance of ostracoda with larger benthic foraminifera, Coralline red algae and Corals indicates the oligotrophic to mesotrophic conditions in the tropical to subtropical environments, with normal salinity and oxygen richness during the deposition of the Qom Formation.The Qom Formation consisting of limestones, marine marls, gypsum and siliciclastics was deposited at the last sea transgression in the Oligo-miocene age, with northwest-southeast trending in three basins of Sanandaj-Sirjan fore arc, Urumieh-Dokhtar intra arc and Central Iran back arc.

In order to conduct this research, based on lithology of layers, 45 marly and calcareous samples were collected.

Qom Formation in the study area consists of five limestone and marl informal members. These informal members are lower limestone, lower marl, middle limestone, upper marl, and upper limestone. 36 species and 23 genera of ostracoda from Gonjan stratigraphical section have been studied and identified:Cytherella sp., Cytherella dissimilis, Cytherella strangulat, Cytherelloidea sp., Paracypris sp.A, Paracypris sp.B, Krithe sp.A, Krithe sp.B,  Trachyleberis sp., Ambostracon sp., Xestoleberis sp., Dentokrithe comma, Krithe trinidadensis, Loxocorniculum sp., Acanthocythereis sp., Buntonia sp., Loxoconcha ? sp., Cyprideis sp.A, Cyprideis sp.B, Actinocythereis sp., Actinocythereis iragensis, Legitimocythere sp., Parakrithe sp.A,  Parakrithe sp.B, Cytheridea josephina, Cytheridea eggenburgensis, Ruggieria sp., Bairdia sp.A, Bairdia sp.B, Bairdia rafidainensis, Loxoconcha psedohamrinensis, Loxoconcha hamrinensis, Aurila sp., Costa tricostata, Mutilus sp., Ambocytherea sp.

The presence and abundance of ostracoda with larger benthic foraminifera, Coralline red algae and Corals indicates the oligotrophic to mesotrophic conditions in the tropical to subtropical environments with normal salinity and oxygen richness during the deposition of the Qom Formation. Studies on the Qom Formation ostracoda in Gonjan section, indicate the similarity of these samples with other areas of Iran, India, north and north-east of Iraq, Turkey, eastern Mediterranean and North Africa. Thus it represents a seaway connection between these areas during Oligo-Miocene, which is considered as the Tethyan Seaway. The Qom Formation had a communicative role between Eastern Tethys and the Western Tethys region in the Iranian Plate.

The Zagros mountain belt extends over 1800 km from Kurdistan in N Iraq to the Strait of Hormuz in Iran (Lacombe and Mouthereau 2006). Zagros Mountain belt is one of the richest oil provinces in the world (Emmami 2008) and is important to paleontological, sedimentological, structural and geological studies. The Cretaceous sediments in the Zagros Mountain Belt (SW Iran), is characterized by a large diversity of rocks and facies. The Gurpi Formation is one of the source rock for petroleum in Zagros basin and outcrops extensively to southwest Iran (James and Wynd 1965). The type section of this Formation (49° 13´ 47″ E, 32° 26´ 50″ N) is measured at Tang-e Pabdeh, north of the Lali oilfield in Khuzestan (James and Wynd 1965). This section is composed of 320 meters of dark bluish gray, thin-bedded marl and shale beds and occasionally thin beds of marly limestone (Motiei, 1995). The following publications have appeared for this formation (e. g. Kalantari, 1976; Vaziri Moghaddam, 2002; Ghasemi-Nejad et al. 2006; Darvishzad et al. 2007; Bahrami 2009; Rabbani et al. 2009; Bahrami and Parvaneh-Nejad Shirazi 2010; Bieranvand and Ghasemi-Nejad 2013; Parvaneh-Nejad Shirazi et al. 2013; Beiranvand et al. 2013, 2014 and Fereydoonpour et al. 2014). Late Cretaceous calcareous nannofossils study is still scarce in Zagros basin and is a strong motivation for investigating calcareous nannofossils in southwest Iran. Late Cretaceous calcareous nannofossils in Gurpi Formation were studied by (Senemari and Azizi 2012; Badri and Kani 2014; Razmjooei et al. 2014; Najafpour et al. 2015; Senemari 2015 and Hadavi et al. 2016).
The aim of the present study was to establish the biostratigraphic zonation for the Gurpi Formation and determine age range of this formation in Izeh sub- zone by means of calcareous nannofossils. A 215-m-thick, well-exposed section was chosen for this purpose. The Kuh-e Siah section is located about 15 Km to the north of Deh-Dasht area. This section was measured in detail at 30°54'31. 86 N and 50°36 38. 80 E. Lithologically, it consists of shale, shaly limestone, and shales with thin bedded limestone. It conformably overlies the Ilam Formation and is overlain unconformably by the pabdeh Formation. Material and Methods: In this study a 215-m thick of Cretaceous sediments including the upper part of Illam Formation, Gurpi Formation and the lower part of Pbdeh Formation were recognized. A total of 122 samples with ~ 1 ‒ 2 m sampling interval were collected. Calcareous nannofossils were processed by smear slides technique described by Bown and Young (1998). The slides were studied with a polarized microscope Olympous (BH2) with 1000×magnification. The zonal scheme proposed in this study is based on the ranges of the most important stratigraphically nannofossil taxa. Calcareous nannofossil taxonomy follows Perch-Neilsen (1985) and Bown, (1998). In this study the stratigraphic zonation developed by Sissingh, (1977) modified by Perch-Nielsen (1985) was applied and is compared with, Burnett, (1998) biozones. Discussion of Result and Conclusion: According to the first and last occurrences of the index species of calcareous nannofossils, Late Coniacian to Early Maastrichtian age were recognized for the sediments of Gurpi formation in this area. The standard zones identified are listed below from the oldest to the youngest:Reinhardtites anthophorus biozone (CC15) (Equivalent of Subzone UC11a and UC11b), late Coniacian.
Lucianorhabdus cayeuxii biozone (CC16) (Equivalent of Subzone UC11c and UC12), late Coniacian- middle Santonian.
Calculites obscurus biozone (CC17) (Equivalent of Subzone UC12 and UC13), middle Santonian- Santonian Campanian boundary.
Aspidolithus parcus biozone (CC18) (Equivalent of Subzone UC14 a, b, cTP), early Campanian.
Calculites ovalis biozone (CC19) (Equivalent of Subzone UC14dTP and UC15aTP), late early Campanian.
Ceratolithoides aculeus biozone (CC20) (Equivalent of Subzone UC15bTP), late early Campanian.
Quadrum sissinghii biozone (CC21) (Equivalent of Subzone UC15cTP), early late Campanian.
Quadrum trifidum biozone (CC22) (Equivalent of Subzone UC15dTP andUC15eTP), middle late Campanian.
Tranolithus phacelosus biozone (CC23) (Equivalent of Subzone UC16 and UC17), middle late Campanian- early Maastrichtian.
Reinhardtites levis biozone (CC24) (Equivalent of Subzone UC18), middle early Maastrichtian.
Arkhangelskiella cymbiformis biozone (CC25) (Equivalent of Subzone UC19), late early Maastrichtian.
Using of these results and their comparison to other global nanno events, which were reported on upper Cretaceous stage boundaries, can be used to better identify of these boundaries in this section. In this study the Coniacin- Santonian, Sntonian- Campanian and Campanian- Maastrichtian boundaries were identified as follows:Coniacin/ Santonian boundary: This boundary has been reported as the interval from the FO of M. staurophora to the FO of R. anthophorus by Perch-Nielsen (1985). Bralower et al. (1995) have been shown this boundary between the FO of the M. staurophora to the FO of L. cayeuxii. Burentt (1998), Melinte and Lamolda (2002) and Melinte and Lamolda (2007) have been considered the FOs of R. anthophorus, L. grillii, Micula concav, Lucianorhabdus inflatus and L. cayeuxii in the late Coniacin and the LO of L. septenarius in the Early Santonian. The Coniacin- Santonian boundary (CSB) has been placed between the FO of L. cayeuxii and the LO of L. septenarius, within the CC16 Zone of Sissingh (1977), and in the UC11c sub-zone of Burnett (1998). Also the presence of C. obscures after the FO of L. cayeuxii and higher abundance of M. concava, has been reported the CSB (Lamolda et al. 2014). The first sample of the Kuh-e Siah section contains R. anthophorus, L. grillii, Q. gartneri and M. staurophora. The FO of L. cayeuxii and the LO of L. septenarius has been recorded at 5m and 15 m, respectively. Based on these data, the lowermost part of the Kuh-e Siah section is late Coniacian and the CSB was considered in the Kuh-e Siah section in the UC11c/ CC16/ NC17 zones, between the FO of L. cayeuxii and the LO of L. septenarius.
Santonian/ Campanian boundary:At informal sections of GSSP (Hancock and Gale, 1996; Hampton et al. 2007). , this boundary is marked by the FO of A. parcus parcus. Two main suggested markers, i. e. the FO of A. parcus parcus and the LO of Dicarinella asymetrica occur closely to the base of Chron 33r which may be suggested as the main events for the base of the Campanian (Wagreich et al. 2015). The Santonian- Campanian boundary is described within the intetrval from the FO of A. cymbiformis (UC13a) to the FO of A. parcus parcus (UC14) (Gale et al. , 2008), while Melinte and Bojar, (2010) placed this boundary within the CC17/ UC13 and the LO of A. cymbiformis is located before the boundary. The Santonian- Campanian boundary is located at the base of CC18/UC14 zone, marked by the FO of Broinsonia parca parca, (Wagreich et al. , 2010; Cetean et al. , 2011; Russo, 2013; Dubicka et al. , 2017). In the Kuh-e Siah section, the Santonian- campanin boundary was marked by the FO of A. parcus parcus at the base of the CC18/ UC14/ NC18 at 45 m.
Campanian‒ Maastrichtian bondary: The Campanian ‒ Maastrichtian boundary (CMB) at GSSP is defined below the LO of Q. trifidum and Q. gothicus. The LO of B. parcus constricta is also recorded about 1. 8 Ma above the CMB (Gardin et al. 2001) and considered as an indicator of the CMB which is observed above the LO of Q. trifidum and Q. gothicus (Odin and Lamaurelle, 2001). At Gubbio area (Gardin et al. 2012), similar to Tercis-Les-Bains (Gardin et al. 2001), the LOs of Q. gothicus and Q. trifidum are followed by the LOs of A. parcus constrictus and Q. trifidum and differs with the proposed CC and UC zonations. It must be mentioned that the LOs of T. orionatus (Gardin et al. 2012) and A. parcus constrictus (Gardin et al. 2012; do Monte Guerra et al. 2016) are diachronous between different latitudes. Thibault also used the LO of Quadrum trifidum as marker for the CMB at low latitude site. In the Kuh-e Siah section, the Campanian- Maastrichtian boundary is identified by the LO of the Quadrum trifidum.
1- The presented data suggest that the age of sediments of Gurpi Formation in Kuh-e Siah section are late Coniacian to late early Maastrichtian. In kuhe Siah section
2- According to the continuous presence of L. grillii، M. concava و M. staurophora in samples of Illam and Gurpi Formations and the presence of Q. gartneri and R. anthophorus in the first sample of the Gurpi Formation, the Illam and Gurpi formations boundary is conformably.
3- The LO of B. hayi bio- evente has a reverse order in this study relative to biozones was described by Sissingh (1977). Although the LO of B. hayi was recorded in zone CC19 (Sissingh 1977), the LO of this species has been recorded up to the middle part of the CC20. In this section, the LO of Bukryaster hayi was recorded in the CC20. Razmjooei et al. , (2014) in the northeast of Kazeroon in Iran (Fars area) and Melinte and Bojar (2010) in southern Romania have also recorded the LO of B. hayi in zone CC20. Based on Melinte and Bojar, (2010), the LO of B. hayi in CC20 is attributed to diachronism or reworking.
4- Due to the presence of Biantholithus sparseus, Fasciculithus tympaniformis and Markalius inversus in the first sample of the Pabdeh Formation and the non-identification of the end zone of the CC25/ UC19 zones in this section, the Gurpi and Pabdeh Formations boundary is unconformably.

Barremian sediments of the Garau Formation have been investigated at the southwest of the Kabir-kuh anticline (Qaleh-Darreh section) with regard to calcareous nannofossils. According to the presence of index calcareous nannofossils, NC5 biozone and NC5c, NC5d and NC5e subzones of Roth (1978) and CC5-CC6 biozones of Sissingh (1977) have been identified. At the studied interval, warm water taxa like Cyclagelosphaera margerelii, Diazomatolithus lehmanii, Lithraphidites carniolensis, Micrantholithus spp., Nannoconus spp., Rhagodiscus asper and Watznaueria spp. have been recorded along with cool water taxa such as Biscutum constans, Helenea chiastia and Zeugrhabdotus embergeri. The abundance of warm water taxa is higher than cool water taxa and a reverse trend can be observed between them. Regarding cool and warm water taxa three warming phases and two cooling phases are identified which includes the warming event of early Early Barremian, cooling event of Early Barremian, warming event of Mid-Barremian, cooling event of late Barremian and warming event of Barremian-Aptian boundary. It must be mentioned that these data are in accord with other parts of the world in the Tethyan (e.g., Italy) and the Boreal realms (e.g., NW Germany and NE England).
Keywords: Barremian, Biostratigraphy, Paleoecology, Garau Formation, Calcareous nannofossils

Calcareous nannofossils have been investigated at the lower part of the Gurpi Formation at the southwest of Gurpi anticline. According to the index calcareous nannofossils CC22/UC15eTP to CC24/UC18 bio-zones have been identified and the age of Late Campanian ‒ Early Maastrichtian is considered for the studied interval. Statistical analysis of the assemblages indicate the presence of high and low nutrient taxa. The relative abundance of oligotrophic taxa (Watznaueria barnesae, Watznaueria fossacincta, Prediscosphaera spp., Eiffellithus spp., Lithraphidites carniolensis, Staurolithites spp., Micula staurophora, Cribrosphaerella ehrenbergii) is higher than eutrophic forms (Biscutum constans, Discorhabdus ignotus, Placozygus spiralis, Reinhardtites spp., Zeugrhabdotus spp., Tranolithus orionatus), and an increasing trend in the relative abundance of oligotrophic taxa along with a decreasing trend in the relative abundance of eutrophic forms can be observed towards the upper parts of the section (Campanian-Maastrichtian boundary and Early Maastrichtian).

Introduction: Garau Formation has a good distribution and outcrops at the Zagros sedimentary basin in Iran. This formation has been studied from different aspects of sedimentology and paleontology (e.g., Vincent et al. 2010; Jamalian et al., 2011; Ezampanah et al., 2012). In the present study, 510 m from the upper part of the Garau Formation at the south west of the Kabir-Kuh anticline has been investigated. The Kabir-Kuh anticline is located at the south east of Ilam and north east of Qaleh-Darreh village. The studied interval consists mainly of green to gray marls, marly limestone, limestone, shale and marly shale. This formation overlies the Gotnia Formation and is overlain by Sarvak Formation disconformably at the studied interval. The studied interval is investigated with regard to the calcareous nannofossils for determining the exact age the studied interval.

Materials and Methods: A total of 226 samples with a sampling resolution of 1 to 4 m were collected from the upper part of the Garau Formation and were processed using the simple smear slide technique described in Perch-Nielsen (1985). The prepared slides were examined using an Olympus BH2 transmitting light microscope at x1000 magnification.

Discussion: In the present study, the standard calcareous nannofossil zonation in low-latitude sections of Sissingh (1977) emended by Perch-Nielsen (1979, 1985) and Applegate and Bergen (1988) and Roth (1978) emended by Bralower (1987) and Bralower et al. (1993, 1995) were applied. The studied interval spans from CC5 to CC7 biozone of Sissingh (1977) and from NC5C to NC7B biozone of Roth (1978). Regarding to calcareous nannofossils, ninety species from 43 genus and 15 families have been recognized at the studied interval. Six important calcareous nannofossil bioevents were identified within the studied interval. Calcicalathina oblongata is recorded from the first part of the studied interval and its last occurrence (LO) is the lowermost nannofossil datum observed at 28 m of the studied interval, which defines the top of CC5 and NC5C. The first occurrence (FO) of H. irregularis (75 m) is recorded after the FO of Braarudosphaera africana (48 m) and Flabellites oblongus (64 m) at the studied interval and marks the top of CC6 zone of Sissingh (1977) and NC5 zone of Roth (1978) emended by Bralower et al. (1993, 1995). At low latitudes, the FO of R. irregularis and H. irregularis are the most reliable bio-events for defining the Barremian/Aptian boundary (e.g., Applegate and Bergen, 1988). The next important bio-event at the studied interval is the FO of E. floralis (122 m), defining the top of NC6 and CC7a (Early Aptian). The other important bio-event at the studied interval is the last occurrence of Micrantholithus hoschulzii (370 m) defines the top of NC7A biozone of Roth (1978) emended by Bralower et al. (1993, 1995)

Late Devonian-Early Carboniferous strata in the Kerman area fourteen chondrichthyan taxa were identified. The abundance of chondrichthyan teeth in Famennian strata is considerable. The high abundance of protacrodonts and larger proportion of shallower shelves of pheobodonts appeared to dominate in a shallow environment at the Famennian. The chondricthyan assemblage the Famennian of the Hutk section resembles the Chahriseh fauna in Esfahan district that reveals similar palaeoenvironmental conditions in Central Iran basin. The occurrence of Deihimmansureae in duplicate Zone marks the youngest record for the species up to Early Tournaisian.

Introdaction
Upper Devonian-Lower Carboniferous rocks are widely exposed throughout Kerman Province (Central-East Iran Microplate). They are mainly represented by limestones, sandstones and interbedded shales, of the Bahram and Hutk Formations. The regional geology and stratigraphy of the Kerman area have been described by Huckriede et al. (1962) and Wendt et al. (2002). The Hutk section is located about 35 km north of Kerman in the Khajeh Mountain, where the Precambrian to Jurassic rocks are exposed. The study area is located in the southwestern part of the geological map of Zarand (Vahdati Daneshmand et al., 1995), and structurally belongs to the southwestern part of the Central-East Iran Microplate. This paper is the first study on stratigraphy and biostratigraphy of the Hutk Formation in the Hutk section, providing evidence of a Tournaisian age of the Formation. Nineteen samples (3-4 kg each) were collected from the Hutk Formation in Hutk section, and processed for conodonts. Of these, twelve samples yielded more than 101 conodont elements. In general, the preservation of the conodont elements is good, although a few specimens being broken or incomplete. The identified conodont fauna consists of thirteen species and subspecies of seven genera including: Gnathodus, Protognathodus, Polygnathus, Mehlina, Bispathodus, Clydagnathus, Siphonodella. In the present paper, we follow the standard conodont zonations of the Early Carboniferous, established by Sandberg et al. (1978). The conodont associations found in the 12 productive conodont samples from the Hutk section allows us to subdivide the deposits into three conodont biozones: the duplicata Zone, Upper part of Upper duplicata-Lower crenulata zones and anchoralis-latus Zone
duplicata Zone: Neopolygnathus communis, Polygnathus inornatus, Polygnathus sp. B, Polygnathus longiposticus, Mehlina sp., Clydagnathus cavusformis occur in this interval associated with the Bispathodus aculeatus aculeatus and Bispathodus stabilis. According to Molloy et al., (1997) Polygnathus longiposticus ranges from within the Lower duplicata Zone in to the Lower Crenulata Zone. Co-occurrence of this species with Clydagnathus cavusformis, which ranges from Middle expansa-Upper duplicata zones, defines the interval.
Upper part of Upper duplicata-Lower crenulata zones: An undifferentiated Upper part of Upper duplicata-Lower crenulata zones interval is discriminated from samples A12 to A16 by co-occurences of Neopolygnathus dentatus and Siphonodella obsoleta. Its lower limit is recognized by the first occurrence Siphonodella obsoleta, which ranges from the Upper part of Upper duplicata to the isostica-U. crenulata zones (Sandberg et al., 1978). The upper limit is identified by the last occurrence of Neopolygnathus dentatus, which ranges from the Latest marginifera to the Lower crenulata zones (Barskov et al., 1991; Ji & Ziegler, 1993).
Barren interval: There is a five-meter barren zone intervenes between the lowest sample attributable to anchoralis-latus Zone and the uppermost bed attributable to Upper part of Upper duplicata-Lower crenulata zones which do not yield any conodont specimen, so the age of this bed has been recognized on the basis of stratigraphic position as Upper crenulata-typicus zones.
anchoralis-latus Zone: The assosiation of Gnathodus pseudosemiglaber and Neopolygnathus communis can be seen here. Its lower boundary is defined by FAD of Gnathodus pseudosemiglaber that ranges from anchoralis–latus Zone to texana Zone (Lane et al., 1980). Co-occurences of this species with Neopolygnathus communis which extinct at anchoralis-latus Zone defines the interval.
Biofacies and Paleoecology: During the Early Carboniferous, the lateral distribution of conodonts across the shallow carbonate shelf to the open sea and basinal environments follows a similar pattern as during the Late Devonian time (Schonlaub & Kreutzer, 1993). The basic concept of conodont biofacies introduced by Sandberg (1976) and later completed by others (e.g. Sandberg & Ziegler 1979; Sandberg et al., 1988; Sandberg & Dreesen, 1984, 1987; Pohler and Barnes, 1990 and Savoy & Haris, 1993). The Paleoenvironment and paleoecology were interpreted from field observation and conodont assemblages. Shallow water conodont biofacies (icriodid-polygnathid) in Lower Famennian deposits of the studied section indicates an inner shelf to foreshore depositional environment for this part of section (Ahmadi et al., 2012). This is similar to most Iranian sequences of Central Iran such as Hojedk (Gholamalian & Kebriaei, 2008), Dalmeh (Hairapetian & Yazdi, 2003) and Chahriseh (Gholamalian, 2007). The middle-late Famennian deposits are characterized by clastic sediments which indicates a considerable sea level fall and marine regression at the Latest Devonian time. This situation is different from other sequences of Central Iran. Middle and late Famennian in some sections (eg. Ghale-Kalaghu and Howz-e-Dorah 1, 2) shows predominance an inner shelf environment (Bahrami et al., 2011) whereas in Kale-e-Sardar section (Eastern Tabas) deep marine sediment were deposited (Gholamalian et al., 2009). The duplicata Zone is characterized by 8 conodont taxa. Species of Polygnathus is most abundant followed by those of Clydagnathus and a low number of Bispathodus+Mehlina. The polygnathid biofacies and occurrences of Clydagnathus represent an inner shelf to mid-continental shelf environment. The upper beds (Upper part of Upper duplicata-Lower crenulata zones, anchoralis latus Zone) is characterized by the appearances of Gnathodus and Siphonodella. These genera have low abundance so the statical analysis is impossible but the presence of these genera represents a sea level rise and establishment of deeper environment during the late Tournaisian. From the Early Carboniferous sequences of Hutk section, north of Kerman, thirteen species and subspecies of conodonts were identified. The age of Hutk Formation has been determined as Tournaisian based on its fauna. Three biozones were recognized on the basis of vertical distribution of these taxa along the stratigraphic column. These strata lie unconformably over the Middle-Upper Famennian terrigenous sediments and covered disconformably by dolostones of Jamal Formation.

The marine Qom Formation was deposited at the north-eastern coast of the Tethyan Seaway (Reuter et al., 2009). Its deposition took place in three NW-SE-trending basins: Sanandaj-Sirjan fore-arc basin, Urumieh-Dokhtar magmatic arc (Intra-arc basin) and Central Iran back-arc basin (Mohammadi et al., 2013, 2015). Transgression of the Qom Sea started from the southeast and continued northwestward gradually. Evaporate deposits of the Qom Formation were deposited merely in a rather small area of the Central Iran back-arc basin and deposited in the Early Miocene (Aquitanian-Burdigalian). Because of high facies changes of the Qom Formation and its situation in intermountain basins, defining a depositional model for the Qom Formation for the whole of the Central Iran is impossible. The aim of this research is to study of the biostratigraphy, microfacies and depositional model of the Qom Formation in Natanz area.

One stratigraphic section of the Qom Formation was measured and sampled in Natanz area with the aim to study its biostratigraphy, microfacies and depositional model. A total of 166 samples were collected systematically and based on facies and texture changes. All samples were studied in detail by microscope. Based on different studies the obtained foraminifera were identified and age of the study section was determinate. The classification of carbonate rocks followed the scheme of Dunham (1962) and Embry & Klovan (1971). Finally, depositional model of the study section was reconstructed. 

The study succession with 330 m thickness is one of the most cliff-forming outcrops of the Qom Formation and lithologicaly are composed of two parts: the lower part with 210 m thickness consists mainly of medium to thick bedded and massive limestone, reefal limestone and shale; while, the upper part with 120 m thickness is composed of medium to thick bedded limestone and marl. On the basis of recognized foraminifera and their vertical distribution, the Qom Formation is Rupelian?-Chattian-Aquitanian in age in the study area. Field and laboratory studies caused to identification of 9 microfacies, they are: A) Shale; B) Bioclastic imperforate foraminifera packstone; C) Sandy bioclastic miliolida wackestone; D) Coral boundstone; E) Bioclastic perforate and imperforate foraminifera packstone; F) Marl; G) Bioclastic perforate foraminifera packstone; H) Bioclast wackestone; I) Bioclastic bryozoan packstone. The investigation results indicate that the lower part of the study section deposited mainly in lagoonal settings; while its upper part deposited entirely in the open marine setting. At the end of the deposition of the lower part, increasing of the colloidal grain inputs (which characterized by the abundance presence of the marly facies) and depth (which characterized by the presence of typical fauna of the deeper settings) prevented the growth of the reef-forming corals. According to recognized microfacies and field investigations, deposition of the Qom Formation in northeastern Natanz took place on a carbonate ramp. The proposed carbonate ramp can be divided into inner ramp and middle ramp. Inner ramp is characterized by high abundance of imperforated foraminifera and mainly includes the lower part of the study section. Inner ramp is dominated mainly by A to E microfacies. Middle ramp is characterized by high abundance of larger benthic foraminifera with hyaline wall and mainly includes the upper part of the study section. Middle ramp is dominated mainly by F to I microfacies. Deposits of the outer ramp, which is characterized by absence of larger benthic foraminifera together with the presence of planktonic foraminifera and light-independent organisms, are not recognized in the study section.

In the Zagros structural zone of Iran, there is a broad range of emergent salt domes, a unique morphology in the world that is developed in tectonic environment. In the Zagros fold-thrust belt, emergent salt domes exhibit the linear patterns. Such trends indicate their relation to the linear structural features which are observable by Landsat imagery. Detection of fault lineaments and their spatial relationship with salt dome locations have been the matter of this study on statistically viewpoints. Based on the remote sensing analysis, horizontal displacements of parts of folded structures and distribution of Hormoz series salt domes, 33 fault lineaments were detected. A statistical method called the weight of evidence modeling is used for determination of the relationship between salt domes places and fault lineaments trends. For this purpose, the fault lineaments map and the center of salt domes map are converted to the raster one and buffers extracted around the fault lineaments; then, the spatial relationship between the salt domes and fault lineaments are quantified using weights of evidence method. The salt domes are associated spatially with the fault lineaments within distances of 1 km in horizon. Weights of evidence method show that the fault lineaments could be the most important foci for emplacement of salt domes in the study area.

The spatangoid genus Schizaster Agassiz is recorded, for the first time, from the Lutetian (Middle Eocene) deposits of Sargaz area, south of Kerman, Iran. The Lutetian sediments of Sargaz region contain a rich and divers echinoid fauna represented by Cidaridae, Conoclypeidae, Echinolampadidae, Toxopneustidae, Phymosomatidae and Schizasteridae. Schizasteroid echinoids are an important component of this fauna. Five Schizasteroid echinoids assigned to genus Schizaster are described and illustrated in the present paper. The Schizaster species are Schizaster ambulacrum, S. archiaci, S. globulus, S. lucidus and S. spado. The Schizaster specimens occur in association with a rich nummulitids and alveolinids fauna, and macro-invertebrates consisting of bivalves and gastropods, which suggest a Lutetian age for the sediment. Associated micro-macro fauna also indicate a warm and shallow water environment was prevailed during the deposition of the sediments.

In order to study of the systematic and paleoecology of Cretaceous (Aptian-Early cenomanian) Brachiopods, the Estakhrooyeh section in NW Baghin, west of Kerman City with 190 m in thickness was studied and sampled. The Middle part of this section contains diverse assemblages of macrofossils such as Brachiopods, Echinoderms, Gastropods, Bivalves and Corals. This biostratigraphic research resulted in to examine 5 genera and 10 species of brachiopoda of Sellithyrididae family for the first time from this section. The Brachiopods indicate Aptian-Early Cenomanian ages for these sediments. The Faunal assemblages suggest a shallow and suitable environment prevailed during the deposition of the strata.

The Guri limestone member of the Mishan formation in SE of Zagros Basin (N of Bandar-e Abbas) consists of the thick bedded limestone bearing oyster shells. Seven species of Ostreidae and Gryphaeidae belonging to four genera of Crassostrea, Cubitostrea, Ostrea and Hyotissa were identified as: Cubitostrea frondosa, Ostrea (cubitostrea) dubertreti, Cubitostrea digitalina, Crassostrea gryphoides, Hyotissa virleti, Ostrea vesitata and Ostrea plicatula. These fossils are reported from the Zagros Basin for the first time. These deposits assign to a Burdigalian age based on the presence of Borelis melo curdica. The reclining mode of life, adjacent right and left valves and rare erosion traces on shells indicate an in situ buried in hyper saline shallow and near shore water with moderate to low sedimentation rate. The early Miocene oyster assemblages similar to this studied assemblage have been reported from the other parts of Tethys showing a seaway connected to Tethys during the early Miocene. Therefore, the oysters can be used for the Paleogeographical correlation in the early Miocene deposits.

To study biostratigraphy and paleoecology of Lower Cretaceous sediments in north of Kerman (Ravar) three sections have been chosen and sampled. The thicknesses of sections are measured 235 meters in Kaleh Gav section, 162 meters in Ghadroon section and 229 meters in Markesh section. The sections have a divers assemblage of fossils such as macrofossils, ostracodes and foraminifera, among which the later is the most important one. The sediments are Barremian?- Aptian – Albian in age. In benthic foraminifera, both the epifaunal and infaunal are present and eight morphogroups are recognized. High diversity and abundance of foraminifera and also presence of platycopid and podocopid ostracods in Markesh section, confirm that an oxygenated environment has been prevailed during the deposition of the strata. Also the proportion of planktonic foraminifera and consequently low P/B ratio suggests a shallow marine environment for the strata. The presence of some larger foraminifera such as orbitolinids and calcareous algae indicates a warm shallow and photic environment as well. Trophic strategies of foraminifera show that sufficient food have been available in these environments.