نشریه رخساره های رسوبی
سال دهم شماره 1 (پیاپی 18، بهار و تابستان 1396)

The study area is located between Lut and Helmand blocks. This area is named Eastern Iran Flysch Basin. This basin is surrounded between Nehbandan fault in the west and Harirrud fault in the east (Stöcklin, 1968). Post Cretaceous deposits of Birjand area are composed of different facies with variations thickness. Paleogene deposits in Birjand area formed after Laramid orogeny phase in Paleocene and ended in late Middle Eocene (Eftekharnezhad, 1986).
The studied section is located about 60 kilometers west of Birjand. Access to the outcrop is along Birjand-Kerman road. After passing through Khusf city and Dastgerd village, a gravel road separated from Birjand-Kerman road. The measured section is near Gorong village. The geographical position of the section is 32o 52′ north latitude and 58o 52′ east longitude. This section is about 26 kilometers North West of Khusf City.
Paleocene deposits in the study area include sandstone and conglomerate at the base, then changes to sandy limestone, marly limestone, thick bedded to massive limestone in middle and upper parts, and marly limestone and conglomerate in uppermost part.
In order to study algae in carbonate beds, samples collected from different intervals. Sampling interval is between 1/5 meters and 3 meters, which in clastic beds the intervals are greater than carbonate beds. Ninety samples have been collected in the field and thin sections prepared from all samples.. The photomicrograph of fossils prepared and based on references, genera and species of algae, identified, described and introduced. The thickness of measured stratigraphical section is 342/5 meters and could be divided into four units. There are conglomerate beds above the boundary (unit A and B). In uppermost part of unit D also there are conglomerate beds. It seems the lower and upper boundaries are disconformable. The lithology of units are as follows:Unit A- The lower part of this unit is covered, then 53 meters of marl and with thin intercalated limestone beds are present.
Unit B- This unit include 111 meters of conglomerate at the base, then changes to sandstone and massive limestone.
Unit C- This unit is composed of 144.5 meters of thick bedded limestone with marly limestone.
Unit D- This unit is composed of 34 meters marly limestone in lower part and conglomerate and sandstone in upper part.
After studing thin sections of units B and C, the following algae are identified; Clypeina occidentalis, Clypeina aff. dragastani, Clypeina cf. haglani, Clypeina elliotti, Clypeina cf. elliotti Clypeina cf. lucana, Cymopolia cf. frugifera, Cymopolia edwarsi, Cymopolia cf. mayaensis, Cymopolia drobneae, Cymopolia satyavanti, Dissocladella aff. longijangensis, ?Broeckella sp., Orioporella villattai, and Ovulites cf. arabica. In all identified genera and species, all parameters such as outer and inner diameters, branch diameter in proximal and distal, number of branches in every verticil were measured. Although the Paleocene deposits in western Birjand consist of clastic and carbonate sequences, the carbonate deposits contain a good variety of algae especially green algae. The most important identified genera and species are Clypeina occidentalis, Clypeina aff. dragastani, Clypeina cf. haglani, Clypeina elliotti, Clypeina cf. elliotti Clypeina cf. lucana, Cymopolia cf. frugifera, Cymopolia edwarsi, Cymopolia cf. mayaensis, Cymopolia drobneae, Cymopolia satyavanti, Dissocladella aff. longijangensis, ?Broeckella sp., Orioporella villattai, Ovulites cf. arabica. The assemblage algae confirm Paleocene age and foraminifera such as Kathina sp., Mississippiana binkhorsti, Mississippiana sp., Rotorbinella detrecta, Rotalia sp. also support this age.

In this research, Calcareous Nannofossils of the Kharchang section have been studied. The area under study is located in the eastern Paratethys and the section with 260 meters thickness is located 10 kilometers far in south of Sari city and in the north of the Kharchang village. The lithology of the deposits consists of soft, yellow fine grained sandstones, gray, blue and yellow sandstone, and yellow and brown sandy claystone. In this study, 35 samples from the Kharchang section have been studied. Samples were prepared as smear slide method. In order to study of the thin sections and the prepared slides, Olympus Optical Microscope (BH2) with an object lens with a magnification of 100 was used and the gypsum plate was used for distinguishing certain species. In general, 23 genera and 43 species of the calcareous nannofossils have been recognized in this section. Nannofossils are suitable for biostratigraphical studies since they are abundant, planktonic, rapidly evolving and largely cosmopolitan. These fossils are found abundantly in the section and they are well preserved, especially Discoasters, which are protected from excess growth and dissolution and have a fairly large variety of species. The coccoliths in this section have relatively high diversity and good preservation. The biostratigraphic studies are done based on Martini (1971) zoning. In this zonation, the NN abbreviation represents Neogene nanoplanktons (Nannoplankton Neogene).
Based on the identified nannofossils, age of the lower part of this section is Early Pliocene (Zanclean) corresponding to NN14 (Martini, 1971).
In the known fossil assemblage, a number of reworked Mesozoic fossils are seen such as Braarudosphaera bigelowii, Calculites obscurus, Calculites ovalis, Eiffellithus gorkae, Eiffellithus turriseiffelii, Micula concava, Watznaueria barnesae and Watznaueria biporta and some Palaeogene species such as Chiasmolithus bidens, Chiasmolithus nitidus, Coccolithus pelagicus, Cribrocenrum martini, Cruciplacolithus tenuis, Discoaster deflandrei, Discoaster kuepperi, Discoaster kugleri, Ellipsolithus lajollaensis, Ericsonia staerkeri, Fasciculithus tympaniformis, Helicosphaera reticulata, Helicosphaera seminulum, Neochiastozygus concinnus, Neochistozygus imbriei, Prinsius martini, Sphenolithus ciperoensis, Sphenolithus radians and Triquetrorhabdulus carinatus present and species commonly associated with the Neogene are Catinaster coalitus, Helicosphaera ampliaperta, Helicosphaera sellii, Pseudoemiliania lacunosa, Reticulofenestra pseudoumbilica, Sphenolithus belemnos and Sphenolithus heteromorphus.
The age that have been suggested for the studied section are introduced as follows:DISCOASTER ASYMMETRICUS ZONE (NN14)
Definition: From the first occurrence of Discoaster asymmetricus to the last occurrence of Amaurolithus tricorniculatus
Author: Gartner (1969)
Age range: Early Pliocene (Zanclean)
The mentioned zone is 28 meters thick in the Kharchang section and the biozone was identified in the base of the section.
Considerations: Because the species belonging to the mentioned genera are present in almost all specimens, their attribution to Neogene is ascertained. For example, the species Sphenolithus belemnos, Sphenolithus heteromorphus, Amaurolithus tricorniculatus , Ceratolithus acutus, Discoaster brouweri, Discoaster calcaris, Discoaster druggii, Discoaster exilis, Discoaster kugleri, Discoaster pentaradiatus, Discoaster surculus and Discoaster asymmetricus were observed. It should be noted that due to the presence of the Amaurolithus and Ceratolithus genera in the Late Miocene and the presence of the Amaurolithus tricorniculatus species in the first specimen, which is present at the basis of the studied deposits, it is indicative of the absence of deposits older than Late Miocene, but the Discoaster asymmetricus species appearing in the Lower Pliocene and at the base of the studied thickness indicates the age of Pliocene is the beginning of this sedimentary sequence. Since the species has been present throughout the studied section, the age of these deposits can be attributed to the Early Pliocene, which is compatible with the NN14 zone of the Standard Zoning of Martini (1971). Regarding the fact that the NN15 biozone begins with the last occurrence of Amaurolithus tricorniculatus, and the species is found in the last sample, unfortunately we cannot currently determine the age of the top of these deposits. In this research, Calcareous Nannofossils of the Kharchang section have been studied. The section with 260 meters thickness consists of soft, yellow fine grained sandstones, gray, blue and yellow sandstone, and yellow and brown sandy claystone. Based on the current studies, 23 genera and 43 species have been identified in the 35 studied samples and the age of these deposits is the Early Pliocene, which corresponds with the NN14 zone of the standard zoning of Martini (1971)..

The main Paleozoic sequences of Isfahan Province cropped out in the northern part of Isfahan e. g: Soh and Natanz (Najhaf, Neqeleh, Varcamar, North Tar and west Kesheh section) (Zahedi, 1973; Adhamian, 2003, Ghobadipour et al. , 2013; Bahrami et al. , 2015); Zefreh, Chahriseh and Dizlu areas (Brice et al. , 2006; Gholamalian, 2003; Habibi et al. , 2013). Kuh-e-Kaftar section (Chahriseh area) is one of the most complete sequence of Upper Devonian deposits in north Isfahan (central Iran), which have been devoted many papers by different researchers on the fossils content of these deposits (Ghavidel-syooki, 2001; Hamedani, 1996; Brice and Kebriae, 2000; Djafarian, 2000; Mistian and Gholamalian, 2000; Mistian et al. , 2000; Yazdi et al. , 2000; Turner et al. , 2002؛ Safari and kangazian, 2003; Gholamalian, 2003, 2007; Webster et al. , 2007 and Hairapetian et al. , 2000). This paper focused on the Famennian deposits of Kuh-e-Kaaftar section to establish precise age of the lower and upper boundary of sequence, as well as the lithostratigraphic characteristics. Forty-four samples (3-4 kg each) were collected from Kuh-e-Kaftar section, the samples were processed with conventional acetic/formic acid technique. All collected samples were prolific and yielded more than 1613 conodont elements which helped in erecting the stratigraphic framework of biozonation of the Shishtu I subformation. Although the abundance of conodont elements is scarce, but the acceptable diversity and presence of Zonal index taxa let to establish the age framework of the studied interval. The state of preservation of the conodonts is generally excellent, where many specimens are complete without contamination. The color of conodonts is dark black (C. A. I. 4. 5- 5) in total elements of sampled section. All the studied conodont specimens are coded under acronym of EUIC and redeposit in the Department of Geology, University of Isfahan, I. R. Iran The studied deposits of Kuh-e-Kaftar section, which is located in southwest of Chah-riseh village 55 km northeast of Isfahan, comprises Famennian deposits equivalent to the Shishtu Formation (Shishtu I subfromation). The thickness of the studied and measured profile is about 110 meters, including 4 lithostratigraphic units (limestone, sandy limestone, marly limestone, shale and sandstone levels) including: bivalve, bryozoan, crinoids stems, brachiopod, trilobite, goniatite, conodonts and vertebrate micro-fauna. Alternation of medium bedded limestone and shale can be seen at the basal levels of the section. Basal level overlies on Frasnian stage sediments and underlines with an eroded surface (red clays) can be dated to Permian system. In order to establish the biostratigraphical framework for the Shishtu I subfromation, 44 samples were collected systematically and the examined samples contain 1613 conodont elements. Twenty conodont species and subspecies belong to eight genera have been identified as follows: Bispathodus aculeatus aculeatus, Bispathodus aculeatus plumulus, Bispathodus costatus, Bispathodus stabilis, Branmehla bohlenana, Icriodus cornutus, Icriodus sp. , Mehlina strigosa, Pandorinellina insita, Pelekysgnathus inclinatus, Polygnathus delicatulus, Polygnathus deplanatus, Polygnathus nodocostatus, Polygnathus brevilaminus, Polygnathus semicostatus, Polygnathus sp. , Neopolygnathus communis group, and Scaphignatus velifer velifer. The abundance and distribution of conodont elements as well as the sedimentary record suggest marine conditions of an inner shelf environment. The conodonts are related to the following conodont biozones as: Upper marginifera, Uppermost marginifera to Upper trachytera, Middle expansa, and Upper expansa zones. In terms of biofacies, the conodonts can be assigned to the icriodid–polygnatid, polygnatid– bispathodid and bispatodid–polygnatid biofacies. This study undertaken at the Department of Geology, Faculty of Science, University of Isfahan. The financial supports by the Vice Chancellor for Research and Technology, University of Isfahan highly appreciated.

Talkhab watershed is located in the southwestern parts of Iran, longitude 45 50 '00' 'and 46 00', and latitude 33 40 'and 33 48', and has two branches in the northwest (Chaman) and northeast (Srachamlu) that are joined together and form the main Talkhab river. The basin area is covered an area of 161 square kilometers and is elongated in shape. According to The geological division of the Zagros structural zone which is location in the Lurestan in SW Iran, this basin contains a relatively thick sequence of sedimentary rocks including Ilam, Gurpi, Pandeh, Asmari and Gachsaran formations. In this study, the Arc GIS software used to evaluate the geomorphology and physiography studies on order to evaluate the distribution of different geological units in this area. Therefore, the map shows that most geologic units are carbonate (Gurpi and Pabdeh) and evaporate rocks (Kalhor and Gachsaran) that are most abundant rocks in this region and they are very sensitive to erosion. The purpose of this study is to identify different lithofacies that form in this watershed and evaluate the sedimentary link toward downstream.
Method and Materials:In this study, 21 sediment samples from Srachamlu, 17 samples from Chaman and 32 samples from Talkhab Rivers have been collected for grain size analysis (coarser grains based on Lewis and McConchie, 1994; finer grains based on Coates and Hulse, 1985) in order to evaluate the finning to grain size toward downstream. Lithofacies were identified in the field based on Miall (2006). Textural parameters calculated based on Folk (1980).
Result and The results indicate that grain size decreases toward downstream is not exponential and has discontinuities and isolated sedimentary links in Talkhab river. Based on the sedimentary analysis, four discontinuities and five continuities in sediments of the Sarcham, five discontinuities and six continuities in sediments of the Chaman and three discontinuities and four continuities of sediment in the main river of Talkhab have been detected. Our results show that hydraulic sorting has more effective role in downstream fining of the particle size in each of sedimentary links. Particle size parameters indicate that the studied sediments consist mainly of poorly to very poorly sorting grain size, positive skewness and flattened and elongated kurtosis. This indicates that discontinuities resulted from laterally input of coarse grain sediments from banks and tributaries (Marren et al., 2006; Simon and Rinaldi,, 2013), increasing the bed slope, exposed bedrock, changes in lithologic units along the stream bed and structural activities such as joints and faults. The lithofaceis recognized along the studied rivers consist of three coarse-grain gravely lithofaceis (Gmm, Gcm, Gmg) and one medium sandy lithofaceis (Sh). These lithofaceis have formed two architectural elements including gravity flow deposits (SG), gravel bars and bed forms (GB). Based on identified facies associations and architectural elements, the sedimentary model of Talkhab watershed is proposed as gravelly-bed braided river with sediment-gravity flow deposits in upstream and toward downstream shallow gravel-bed braided river system. Finally, we believe that this study can help in a better understanding of erosion and sediment yield patterns in such a basin for better water and soil preservation and watershed management.

The silisiclastic-carbonate sediments of the Geirud formation (Upper Devonian) are deposited in the Central Alborz Basin, northern Iran. Generally, these sediments display four depositional systems as follow: fluvial (alternation of red-purple shale, sandstone and conglomerate), estuary (thick-bedded, white sandstone with bi- to multiple-directional planar cross bed and herringbone), shoreface (alternation of thin to thick-bedded sandstone with trough and planar cross bed and HCS and gray-black, fissile shale) and shallow shelf or offshore (fossiliferous limestone with HCS and tempestite and black, fissil shale) that indicate a deepening up-ward trend. A prevailed stressful and unsuitable condition with respect to salinity led to preservation of the ichnoassemblages with low diversity and small size of the trace fossils in the studied sediments (Gingras et al., 2008). The studied sediments indicate remarkable changes in sedimentation rate, water circulation and salinity level during the Late Devonian time. Ichnological analysis has become a valuable tool in basin analysis, especially for recognizing and interpreting genetically related sedimentary packages (e.g., Tovar
et al., 2007; Sharafi et al., 2012 & 2014). The primary controls on the distribution of different burrowing behaviors and lifestyle of the existing fauna and the trace markers in the marine realm are nutrient supply, hydrodynamic energy, salinity, sedimentation rate, oxygen level, water turbidity (Seilacher,1967; Bromley & Ekdale, 1984; Pemberton & Wightman, 1992; MacEachern & Burton, 2000; Gingrass et al., 2008, 2012; Sharafi et al., 2014). The Alborz Mountains with a E-W trend is one of the structural zones in the northern Iran (Stöcklin, 1968). This structural zone is sub-divided into the east, central, and west parts and the study area is located in the central part. The Geirud Formation crops out at the Dehmolla, and the Shahmirzad sections, geographical coordinates are 36º 21' 53'' N and 54º 45' 28'' E and 35º 46' 12'' N and 53º 19' 25'' E, respectively. In the studied areas, the Geirud Formation disconformably overlies the marine shale of the Milla Formation (Ordovician) and is conformably overlain by the black limestone-shale of the Mobarak Formation (Lower Carboniferous). Various paleontological studies on brachiopods (Bozorgnia, 1964), Palynomorphs (Ghavidel-Syooki, 1995) and Goniatites (Dashtban, 1995) indicate the age of the Geirud Formation is Late Devonian (Frasnian–Famennian).
Tow stratigraphic sections measured in the Alborz mountain north of Iran for the purpose of this research. Tow hundreds and Eighty thin sections were examined to identify fine-scale sedimentological and textural characteristics such as grain size and sedimentary structures that are recorded in the studied successions. Both sedimentological and trace fossils features were examined on fresh and weathered surfaces in the field. Degree of bioturbation is assessed according to Taylor and Goldring (1993) and is done with using of comparative charts. The bioturbation index (BI) aims to relate the degree of bioturbation to the preservation of primary bedding features (Taylor & Gawthorpe, 1993). In this scheme, a BI is defined, ranging from 0 (no bioturbation) to 6 (complete bioturbation, total biogenic homogenization of sediments). Results and Conclusion: Nine ichnoassemblages are identified in the studied successions that indicate considerable environmental changes (e.g. salinity, nutrient supply, hydrodynamic energy, sedimentation rate, oxygen level) within a generally deepening up-ward sequence from fluvial-estuary depositional setting to open marine environment (shoreface, shallow shelf). Alternation of the red-purple, thick-bedded sandstone-conglomerate and red shale of the fluvial system in the lower part of the formation with low diversity of vertical trace fossils and low bioturbation index (B.I.= 0-1) (Skolithos-Arenicolites ichnoassemblage) indicate high sedimentation rate of the silisiclastic sediments in a high energy and agitated setting with unstable and mobile substrate. White, medium-thick bedded sandstone in the lower part of the successions with a few shell fragments and Skolithos-Arenicolites and Thalassinoides-Rhiocorallium ichnoassemblages displayed by mainly vertical burrow elements and low B.I. (1-4) indicate high energy, unstable substrate and periodically water circulation in a beach setting with high sedimentation rate. In the middle part of the studied successions thin-medium bedded fossiliferous sandstone with planar and trough cross beds and HCS and Thalassinoides-Rhizocorallium-Palaeophycus, Arenicolites-Thalassinoides and Arenicolites ichnoassemblages with medium B.I. (3-4) and a mixed vertical (suspension feeders) and horizontal (deposit feeders) burrow elements, display the various life style of the trace markers from suspension feeding during high energy phase with high sedimentation rate and deposit feeding during low energy periods with low sedimentation rate and more stable substrate, in a shoreface setting. Diversity and abundance of the trace fossils and shells in these sediments indicate a suitable marine condition with respect to salinity, light and water circulation. The High diversity and abundance of the trace fossils and the skeletal elements of the Arenicolites-Diplocraterion, Thalassinoides-Rhizocorallium-Palaeophycus, Arenicolites-Protovirgularia and Protovirgularia ichnoassemblages within the black, thin bedded fossiliferous limestone in the upper part of the formation display establishment a fully marine condition (e.g., light, water circulation, and salinity) along with a decrease in hydrodynamic level and turbulence in a shelf setting

In this research, we tried to study the Ilam Formation using petrography (thin sections) and geochemical analysis (major and trace elements). Petrophysical studies have also been used to identify the characteristics and diagenetic environment, and to determine the sedimentary environment and evaluation of reservoir quality. 500 thin sections prepared from cutting samples in X and Y wells and 80 thin sections from Asaluyeh section have been studied to identify, evaluate facies and type of sedimentary environment beside diagenetic processes of The Dalan Formation. For classification and texture descriptions, the classification schemes of Dunham (1962) used. The method of Dickson (1965) used to differentiate calcite from dolomite, with Alizarin (Red-S) and potassium Ferosianid. Types of dolomites were identifies (Adabi, 2009). For description of the microfacies and interpretation of depositional environment model, Flügel (2010) scheme was used. Study of Petrophysical Properties of Ilam Formation in the South Pars Gasfield have been done based on petrophysical logs (gamma, sonics and acoustic), geological reports and reservoir data. Major and trace elements analysis and especially their diagenesis are the important part of carbonates studies. According to the major and trace elements studies and the ratio of these elements in the limestone samples of Ilam Formation, the original aragonite mineralogy in shallow parts and original calcite mineralogy in deeper parts of these deposits were interpreted. Comparison of the Ilam limestone samples with ranges that presented to aragonitic limestone of other fields and plotting the samples in this area confirmed the mixed aragonite-calcite mineralogy. High contents of Sr and Na, low Mn content and high Sr/Na ratio for aragonitic samples and low Sr/Na ratio for calcite samples show that the limestone samples have been stabilized by fluids in a closed to open diagenetic system. The shale zones are almost similar in both wells, and the shale volume has peaked at the lower boundary of both wells due to the high percentage of shale in the Lafan Formation. The sharp changes in the upper and lower limits of the Ilam Formation represents a change in the boundary of this formation with upper and lower formations.

The Kopet-Dagh Basin formed on the southern margin of the Eurasian Plate since the Jurassic up to the Tertiary. The Kopet-Dagh Basin marks the northern boundary of the Alpine-Himalayan Orogeny in northeastern Iran and also corresponds to the morphological boundary between Turkmenistan and Iran. The Kopet-Dagh Basin is an intracontinental basin and its topography dies out toward southeast in the Afghanistan, indicating a tectonically stable part of the basin. Kalat Formation (Late Cretaceous) is one of carbonate unit in the Kopet-Dagh sedimentary basin (Afshar-Harb, 1994). So far, various studies have been done on this formation, but for the first time, the microfacies and palynofacies of the Kalat Formation have been carried out simultaneously.
In order to study Kalat Formation, one section is measured in the Chehel-Kaman valley. Kalat Formation in this section is located about 163 km from Mashhad with a geographic coordinates of 36° 28ʹ 8ʺ North and 60° 23ʹ 42.4ʺ East and is 310 meters thick and consists of shale and limestone alternation. In order to study palynofacies and microfacies in Chehel-Kaman section (310 m shale and limestone), 36 samples of limestone and 22 samples of shale have been studied. The description of the limestone textures follows the Dunham (1962) classification and shales Tyson charts (1993). Study of limestone thin sections led to identification of three sedimentary facies, A, B, C, including barrier, restricted lagoon and tidal flat that are composed of 12 subfacies. These facies can be classified in two group, carbonates and hybrid. Studying of shale led to identify two facies, A and B. Facies A is equivalent to type I Palynofacies and facies B is equivalent to type II Palynofacies. Shale facies A shows semi restricted lagoon into tidal flat and shale facies B shows deeper semi restricted lagoon to shoal and open marine environment. In the basis of microfacies and palynofacies studies, we can say that Kalat Formation has been deposited in a homoclinal carbonate ramp (Flugle, 2010).
Because the palynofacies and paleo-sedimentary environments of the shale parts of Kalat Formation were based on palynomorphs (dinoflagellates), 52 species of 36 genera of dinoflagellates were identified. In addition to dinoflagellates, spores and bisaccate pollen grains, fungal spores and foraminiferal test linings are also observed.
The palynological parameters of the shale facies of this formation indicate that the lability factor in this section is less than one. Decreasing this factor indicates an increasing the amount of oxygen in the sedimentary environment. Therefore, it is possible that semi-oxygenated conditions dominate during the time of the deposition of these facies. However, according to the numbers obtained, the oxygen content in type palynofacies (A) is more than type (B). On the other hand, the ratio of AOM trans to dark AOM indicates that despite the presence of oxygen, the amount of this element is not high (the number obtained is greater than one), which indicates low oxygen conditions in the parts of shale at the time of sedimentation. However, the amount of oxygen in type palynofacies (A) is more than type (B) (Boulter & Riddick, 1986).
To determine more precisely the amount of oxygen and sedimentation rate from a complementary factor (transparent and dark AOM ratio to marine palynomorphs), the best conservation degree of marine palynomorphs (especially dinoflagellates) is in high oxygen saturation and sedimentation rhythms.
If the low sedimentation rate and the low oxygen content transmitted are of the palynomorphs to the transparent AOM, and in the opposite case, palynomorphs into a dark AOM. According to the measurement of the percentage of transparent AOM percent to marine palynomorph along the stratigraphic column, this is high which indicates low oxygen conditions, and the ratio of the percentage of dark AOM to marine marine palynomorph is low, which indicates low oxygen conditions and high sedimentation rate for palynofacies of the Kalat Formation. Of course, the numbers indicate higher oxygen content and higher precipitation rates for type palynofacies (A) than type (B) (Bombardier & Gorin, 2000).
The ratio of the equal dark palynomaceral to the blade - shaped dark, along with the labilatory factor, expresses the amount of energy governing the environment. Blade - shaped dark palynomaceral can travel a long distance due to high flotation, and are abundant in remote areas. According to the results obtained from the study of palynological slides, the equal dark palynomaceral is also greater than the blade, indicating the close proximity to the coast of the shale parts of the Kalat Formation and the resulting numbers indicate the shallowness of the type Palynofacies (A) than type (B), Kleithriasphaeridium truncatum. The presence of species Cannosphaeropsis utinensis Oligosphaeridium buciniferum and Spiniferites ramosus is an open sea. The abundance of the above examples in Palynofacies type (B) is likely to be related to open sea environment for this facies (Chiaghanam et al., 2013).
On the other hand, species like Alterbidinium varium, Andalusiella dubia, Andalusiella gabonensis, Andalusiella polymorpha, Circulodinium distinctum, Cerodinium diebelii, Godavariella venkatachalae, Palaeocystodinium bulliforme, Phelodinium kozlowskii and Palaeocystodinium lidiae show shallow conditions. The palynological factors and the presence of the above species, as well as the presence of spores and bisaccate pollen in Palynofacies type (A), are indicative of the shallow conditions of these deposits.

During the Late Paleozoic, as a result of the north Gondwana continental collision of the Europe, Hercynian Mountains have created (Berberian & King, 1981; Haq & Al-Qahtani, 2005). Most geologists and researchers e.g.: Stöcklin (1974), Nabavi (1976), Berberian (1976) and Stampfli (1978), believed Hercynian phase has influenced the Iranian platform on the type of epeirogenesis, but new studies has proved evidence of Hercynian orogenic movements in Iran. Furon (1941), Gansser (1955), and Gansser et al. (1965) for the first time studied the geology of the Shotori range in the frame of the general geology, sedimentology and the mapping geology.
Stöcklin et al. (1965) assigned the Ozbak -Koh Group deposits to the Late Paleozoic (Devonian and Carboniferous) in the Central Iran which includes the Bahram, Shishtu and Sardar formations to the pre-Permian and the Jamal Formation with Permian age. This study conducts the effects of the Hercynian movements and the related evidences in the north, west and central Iran on the base of sedimentology and geochemistry of the basal Permian siliceous sandstone and the fossils (fauna and flora).
Yazdi et al (1989) compared the “top quartzite of the Sardar Formation” with many other sections of Iran to identify the sources of sands with detailed geochemical study and its economic uses of this horizon which has been named ''transgressive basal Permian sandstone'' (Yazdi, 1999).
Yazdi et al. (2004), Parvaneh et al. (2004), Rabiey & Yazdi (2001), Yazdi & Archbold (2002) and Yazdi (2001) also studied the Paleo-events in Upper Carboniferous - Early Permian with emphasizing on the plants fossils at the topmost Carboniferous which were the markers to the epirogenetic movements and the sea level fall at the Carboniferous – Permian boundary. Several siliceous sandstone samples were collected from eight sections for this research include: Stabragh Sirjan destructive sand granitic, silica sand base of the Permian Zagros in sections Gahkom, Faraghon, Surmeh, Zardkuh and Dashtak (Zard kuh-e-Zagros), Chiruk-e- Tabas and DJam Semnan. Samples studied using semi industrial and industrial analysis for percentage, weight, volume, granulometry and melting point, based on the obtained results this siliceous sandstone has the same source and paleoenvironment condition. According to plant fossil remains, conglomerate unit, crinoidal beds and the siliceous sandstone at the transition zone of the C/P boundary, also lack of Carboniferous and different thickness and age of the pre-Permian deposits in Tabas, Zagros, Isfahan and Alborz areas reveal the act of Hercinan movements in Iranian platform. Presence of Permian marine deposits show the privilege of the deeper marine condition at beginning of Permian in comparison to the Late Carboniferous time interval (Bahrami et al., 2015a; Bahrami et al., 2015b; Yazdi, 1999; Webster et al., 2011; Rabiey & Yazdi, 2011; Yazdi & Archbold, 2002; Leven & Gorgij, 2004). This research undertaken at Department of Geology, Faculty of Sciences, University of Isfahan. Financially and logistically supported by the Vice chancellor for Research and Technology office at University of Isfahan which deeply appreciated.