Biostratigraphy of Late Triassic deposits, based on foraminiferal fauna in the Central Iran Zone (Posht badam Block)

Biostratigraphy of Late Triassic deposits, based on foraminiferal fauna in the Central Iran Zone (Posht badam Block) | Research Square window.SnipcartSettings = { analytics: { enabled: false } }; (function() { var accessVector = localStorage.getItem('access_vector') || ''; window.dataLayer = window.dataLayer || []; if (accessVector) { window.dataLayer.push({ user: { profile: { profileInfo: { snid: accessVector } } } }); } })(); (function(w,d,s,l,i){w[l]=w[l]||[];w[l].push({'gtm.start':new Date().getTime(),event:'gtm.js'});var f=d.getElementsByTagName(s)[0],j=d.createElement(s),dl=l!='dataLayer'?'&l='+l:'';j.async=true;j.src='https://www.googletagmanager.com/gtm.js?id='+i+dl;f.parentNode.insertBefore(j,f);})(window,document,'script','dataLayer','GTM-K279D39R'); Browse Preprints In Review Journals COVID-19 Preprints AJE Video Bytes Research Tools Research Promotion AJE Professional Editing AJE Rubriq About Preprint Platform In Review Editorial Policies Our Team Advisory Board Help Center Sign In Submit a Preprint Cite Share Download PDF Research Article Biostratigraphy of Late Triassic deposits, based on foraminiferal fauna in the Central Iran Zone (Posht badam Block) Nooshin Hadadi, Massih Afghah This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-5840499/v1 This work is licensed under a CC BY 4.0 License Status: Posted Version 1 posted You are reading this latest preprint version Abstract In order to conformity of the sedimentary environment and biological fauna of Late Triassic deposits in each of blocks of the Central Iran, including Lut, Tabas, Posht badam and Yazd blocks, as well as to study the tectonics of the region, were selected sever sections in these blocks, including one section It was studied in the south of Posht badam block in Kerman region, this section is located in the northwest of Kerman city, and Between the Kohbanan and Posht badam faults. The studied section with a thickness of 112 meters is mostly composed of shale, sandstone and limestone. it has many fossils including Bivalves, Sponges, Corals, Bryozoa, Microgastropods and Cephalopods, especially Belemnite, which generally shows the presence of Late Triassic sediments (Norian-Rhaetian) in this area. According to the identified index foraminifera, 8 interval & Concurrence rang biozones Including 5 interval Zone Rectoglandulina tenuis, Triassina hantkeni , Ophtalmidum exigum , Angulodiscus communis, Planiinvoluta regularis and 3 Concurrence rang Zone Turrispirillina minima , Involutina liassica , Duostomina alta, were recognized in the Upper Triassic deposits. Based on the identified biozones, the age of the studied sequences, Late Norian - Early Rhaetian, Middle Rhaetian, Until the end of the Triassic, Late Rhaetian to the beginning of Lias is suggested that they are formation considered equivalent to the members of Howz Khan and Qhadir members from the Nayband Formation in central Iran. Late Triassic deposits Nayband formation Posht badam block Central Iran Kerman Figures Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 Figure 8 1. Introduction Central Iranian Microcontinent (CEIM) () includes Lut, Tabas and Yazd blocks (Takin, 1972; Davodzadeh and Schmidt, 1982). According to the geological evidence, the sheet of Iran, which covers the entire area of ​​central, northern and southern parts of Iran, was a part of the Cimmerian continent (Shengur, 1990). Central and northern Iran were separated from the northern edge of the Gondwana supercontinent and pushed northward during the Permian and Triassic periods due to the action of rifting, simultaneously with the subsidence andgradual closing of the Paleotethys oceanic basin and the collision of the Iranian plate with the southern edge of the Eurasian supercontinent or the Turan Plate at the beginning of the Late Triassic (Shtoklin, 1974), the orogeny event of the early Simmerian and the formation of the Simmerid Mountains were established (Fig. 1 ) . At the front of the rising mountains of Simmerid and along with the simultaneous dynamic tectonics of sedimentation, a thick series of siliceous-clastic rocks related to alluvial plains, marshes, coastal and sea environments has been deposited, which is called Shemshak Group (Aghanbati, 1998; Seyid Emami. et al., 2001). The Shemshak Group is actually a large structural-sedimentary cycle that is limited by the Early Cimmerian (Norian) and Middle Cimmerian (Middle Bajocian) events (Aghanbati, 1998). The homogeneity and adaptation of rock strata facies of Shemshak group (Norian to Lower Bajocian) in central and northern Iran shows that the Iranian plate has acted as a continuous and integrated area during this cycle. The Upper Triassic deposits of the Nayband Formation are distributed over a large area from different provinces such as Yazd, Khorasan, Isfahan, Arak and Kerman (Fig. 1 ), (Seyed-Emami, 2003; Aghanabati, 2004). In fact, the breaking of the Iranian plate into several structural and sedimentary units such as Lut, Tabas, Posht Badam and Yazd blocks has been done in relation to the Middle Cimmerian event at the end of the early Bajocian (Seied Emami and Alavi Naini, 1990). Among the three Simrid events, it has had the greatest impact on the tectonics of central and northern Iran. As a result, after the middle Cimmerian event in the early Bajocian, which caused the Iranian plate to break into several structural pieces or blocks, tectonic unrest has intensified in it. finally, during the following periods, in the Middle and Late Jurassic, numerous tectonic movements, in the form of block movements along with frequent global fluctuations of sea water, played a decisive role in the sedimentation pattern of the region and it has created various stratigraphic facies, whose time regulation and correspondence of stratigraphy with each other in the past has led to many inadequacies and ambiguities in the geological in perception and interpretation of the region (Shtoklin et al., 1965). After this event in the Late Bajocian, another structural-sedimentary cycle (Mago Group) begins, which ends with the Late Cimmerian event at the end of the Jurassic and the beginning of the Early Cretaceous. During this cycle, especially in the microcontinent of Central Iran, due to a combination of tractional, traversal and rotational movements and general block movements in connection with numerous tectonic movements (Seyed Emami et al., 2004), various series of different lithostratigraphy facies related to continental, evaporite, marsh, coastal, shallow to deep marine sedimentation environments have been formed. Determining the correlation of stratigraphy and their compatibility with each other requires very detailed geological and paleontology studies. 2. Geological settings The study area is a small part of the Central Iran Zone (Fig. 1 ). Extensive structural-sedimentary disparities have caused the Central Iran subcontinent to be divided into the Lut block, Tabas block, Kalmard block, Posht Badam block, and Yazd block (Aghanbati, 2004) (Fig. 1 ). The studied zone which limited from the north -northwest by the Daroneh fault (Great Desert fault), from the east by the Nehbandan, and from the southwest by Nain - Dehshir - Baft fault. The structural pattern of this subcontinent is the type of blocks separated by major faults, each of them has separated features, and the dynamics of the subcontinent are not the same. The studied Shams abad region in the NW Kerman, is located in the southern part of the Posht badam block, which is located between the Nain-Kohbanan fault in the east and the Posht badam fault in the west. The mountain range of the region is mostly northwest-southeast. The outcrops of the region are mostly Mesozoic units in the highlands and Cenozoic, Pliocene, and Quaternary in the desert. The Shams abad section (N: 56̊ 47̍ 28̎ ; E: 30̊ 20̍ 51̎ ) is located within the 1:250000 Rafsanjan and 1:100000 Baghin geological maps and is located approximately 30 km northwest of Shams abad village. 3. Material and Methods To establish the age dating and depositionsl environmental studies of the Nayband Formation, the Shams abad stratigraphic section was measured and sampled systematically, emphasizing lithology and facies changes and the characterization of sedimentary structures. 4. Discussion Lithostratigraphy Field studies on the Upper Triassic deposits in the studied area indicate that most of the studied area has an NW-SE trending fold and fracture zone. Lithological studies of the deposits of this section are based on field studies and microscopic studies of rocks and their microfacies results. The lithological characteristics of the studied section consists of 112 m thickness, mainly composed of medium to thin bedded olive green silty shales with gray sandstones interbeds and abundant corals, sponges, bivalves and foraminiferal fauna in the age range of Upper Triassic to Lower Jurassic (Fig. 2). Good sorted red quartz sandstone fragments are cemented by Fe at the top of the Nayband Formation, overlain by sandstone and shale sediments of Ab-e-Haji Formation. 5. Description of Shahdad stratigraphic section: The outcrop of the Nayband formation in this section, with a thickness of about 112 meters, is mainly composed of prograding carbonate rocks layers between shallow regressive shales and sandstones dominated by a deltaic-river environment. In its lower parts, iron staining can be seen contact with the equivalent unit of Shotori, which indicates a period of aridification and an erosional discontinuity between these two units. In the upper part of these deposits, there are medium to thin layered pea-colored to pale yellow-brown limestones alternate with olive-green shales, sometimes slightly silty to mostly gray to cream sandstones. In fact, the lower boundary of the outcrop begins with a discontinuity that is in contact with the upper parts of the Nayband or Howz Khan and Qadir formations and gradually reaches the sandstone-shale deposits belonging to the Lower Lias or Ab Haji. The detailed description of these layers are: 6. Biostratigraphy Biostratigraphical studies in this research are based on benthic foraminiferal fauna. Although the Nayband Formation foraminiferal fauna have a notable variety, but they are not widely distributed,. In the present study, a total of 23 species of 21 genera were identified and their presence intervals were also determined. The families Permodiscidae, Turrispirilinidae, Ammodiscidae, Frondicularidae, have a maximum abundance in this study and lead to the recognition of 8 biozones (Fig. 8, Plates 1,2). So far, no official biozonation has been provided for the deposits of the the Nayband Formation in the Upper Triassic age range. But due to some features such as abundance, high diversity, as well as a significant number of the first appearance and the last appearance of the mentioned fauna through upper Triassic, foraminifers can be part of the very important paleobiotic elements in terms of biostratigraphy in the sequences of the Nayband Formation. The lithological changes of the studied section can be related to the sedimentation and paleoclimatic conditions and as a result overshadow the distribution of fossil fauna, their accumulations and the biozonation position. Various authors such as: Zaninetti, 1976 ; Vachard and Fontaine, 1988 ; Altıner and Koçyiğit, 1993; Rettori et al., 1994; Rettori, 1995 ; Muttoni et al., 1996 ; Marquez, 2005; Kobayashi et al., 2006 ; Lehrmann et al., 2015; ; Luka Gale, 2012 In the present research the biozonation of the Triassic range which has been studied based on the foraminiferal fauna, the global standard biozonation that can be used in different parts of the world, has not been obtained in the studied region. Mostly we are faced with local foraminiferal biozonation and Of course, this also overshadows compliance. Based on the studies conducted in the Triassic basins of Europe or the Alps, including Spain, Bulgaria, Poland, Hungary, Switzerland, (Salaj, 1969 , 1978 ; Salaj et al., 1983 ; Salaj et al., 1988 ; Trifonova, 1978 a, b, 1992, 1993; Gazdzicki et al., 1975 ; Orovecz-Scheffer, 1987 ;)، and also some basins of Asia, including parts of Türkiye and the Caucasus (Zaninetti and Dağer, 1978 ; Efimova, 1991 ), none of the studies have led to the creation of a framework of foraminiferal biozonation in the Triassic, and the reason is based on the aforementioned studies in different parts of the world, some taxonomic issues and flaws, poor calibration of the age range of the taxa used in biozonation, and finally strict facies control. all of these factors prevent the creation global standard biozonation based on foraminiferal fauna through Triassic (Altiner et al., 2021 ). Based on biostratigraphic studies, it is possible to understand the differences in different regions and identify specific fossil communities and their faunal assemblages. In the studied area, considering that the lithological changes of Late Triassic deposits are directly related to the sedimentation and climatic conditions, as a result of the dispersion of the existing biological populations and biocenoses, they have undergone obvious changes in relation to the paleo-ecological developments. Based on the biostratigraphic studies, it is possible to identify the differences in the regions in general in the present study, 23 species of 21 genera were identified, and their age ranges were studied and finally the age has been determined. The foraminifera of the Nayband Formation in the studied section of Shahdad have a low abundance but significant diversity. Families such as Permodiscidae, Turrispirilinidae, Ammodiscidae, Frondicularidae have the highest frequency in the studied section, and the most important identified foraminifers are as follows: Triasina hantkeni Majzon, 1954. Angulodiscus cummunis Kristan, 1957, Tetrataxis nana , Morozova, 1949. Rectoglandolina tenuis , Bornemann, 1854. Trochammina almtalensis , Koehn-Zaninetti, 1969. Auloturtus Broennimanni , Salaj,1969. Glomospira minima , Michalík, J., Jendrejáková, O., & Borza, K. (1979). Ammodiscus parapriscus , Ho, 1959. Angulodiscus cummunis , Kristan, 1957. Agathammina oustroalpina , Kristan-Tollmann, Tollmann (Michalík, Jendrejá- ková 1978; Michalík 1978). Ophtalmidium exiguum , Koehn-Zaninetti, 1969. Involutina liassica , Jones, 1853.. Nodosaria sumatrensis , Lange, 1925. Lenticulina sp., Lamarck, 1804. Permodiscus praecommunis , Salaj, Borza & Samuel, 1983 . Turrispirillina minima , Pantić, 1967. Involutina liassica , Jones, 1853. Angulodiscus gaschei , Koehn-Zaninetti, L.; Brönnimann, P. (1968). Pilamminella falsofriedli , Salaj, Borza & Samuel 1983 . Robuloides sp., Reichel 1946 Dostomina alta , Kristan-Tollmann, 1960. Auloconus permodiscoides , Oberhauser, 1964. Salaj, Borza & Samuel, 1983 . regularis, Planiinvoluta The stratigraphic range of studied foraminifera is also shown in Fig. 8. As mentioned, no precise biozonation has been done for these taxa. the studied biozons are local and can be used to some extent in other blocks of the Central Iranian subcontinent. Fauna of foraminifera and systematics of Upper Triassic taxa have been introduced based on benthic foraminifera in the Tethys basin, in the southeast of the Alps, which can be referred to the studies of Luka Gale ( 2012 ). Therefore, according to the abundance and distribution of foraminifera in the studied sequence, biostratigraphic studies were conducted and led to the identification of 8 biozones as follows ( Fig. 8 and Plates 1, 2): 1. (Interval zone A) Rectoglandulina tenuis Biozone: Category: Interval zone Age: Late Norian Author: Rectoglandolina tenuis, Bornemann, 1854. Definition : Interval from first occurrence of Rectoglandulina tenuis to first occurrence of Permodiscus minutus , This biozone is between two horizons of the appearance of Rectoglandulina tenuis in the lower part of biozone and Permodiscus minutus at the top of the biozone. The presence of these species in the above interstitial zone indicates the age of the Norian. The accompanying species of this biozone are: Nodosaria nitidana , Nodosaria shablensis , This zone is up to 2 meters thick at the base of the Shamsabad section. 2. (Interval zone B) : Triassina hantkeni Biozone : This biozone is between two horizons of the appearance of Triassina hantkeni In the lower part of biozone and Tetrataxis nana at the top of the biozone. The presence of these species in the above interstitial zone indicates the Norian-Late Norian age. Other assemblage of this biozone include the following: Angulodiscus commonis , Nodosaria samatrensis , Permodiscus minutus. This biozone is up to 18 meters thick at the bottom of the Shams Abad section, and it ranges from 3 meters to 20 meters . Here, the only recognized biozone of the international standard that is important in determining the exact age of this biozone is the Triassina hantkeni Biozone, named by Louisette Zaninetti et al. And in northwestern Australia it has been identified as Late Norian-Early Rhaetian and is also defined throughout the Tethys realm: According to international stratigraphic rules: Triasina hantkeni defines Lat Norian - Lower Rhaetian Triasina hantkeni Biozone (Gazdzicki et al., 1979 ; Gazdzicki, 1983 ; Gazdzicki and Reid, 1983 ; Abate et al., 1984; Ciarapica and Zaninetti, 1985 ; Vachard and Fontaine, 1988 ) throughout the Tethys realm. Category: Interval zone Age: Late Norian Author: Triasina hantkeni , Majzon, 1954, Definition : Interval from first occurrence of Triasina hantkeni , to first occurrence of Tetrataxis nana , 3. (Concurrence rang zone A) : Turrispirillina minima Biozone : This biozone began with the appearance of Turrispirilina minima , in the lower part of biozone and the disappearance of Rectoglandulina tenuis above, it is clear that they have acted as a collision zone, so that the overlap of these species in the above collision zone indicates the late Norian - Early Rhaetian. This zone is 3 meters thick at the bottom of the Shams Abad section, and it ranges from 20 meters to 23 meters . Category: Concurence rang Zone Age: Early Rhaetian Author: Turrispirillina minima , Pantić, 1967. Definition : Interval from first occurrence of Turrispirillina minima to last occurrence of Rectoglandulina tenuis , 4. (Interval zone C) Ophtalmidium exigum Biozone : This biozone is between the two horizons of the appearance of Ophtalmidium exigum species at the top of the zone and the disappearance of Angludiscus communis . at the top of the zone. The presence of these species in the above interstitial zone indicates the posterior neuron - the highest part of the posterior neuron. Among the species associated with this biozone, the following can be mentioned: Triassina hantkeni , Turrispirilina minim a, Tetrataxis nana , Planiinvoluta regularis , This zone is up to 6 meters thick at the bottom of the Shams Abad section, and it ranges from 22 meters to 32 meters . Category: Interval zone Age: Early Rhaetian Author: Ophtalmidium exiguum , Koehn-Zaninetti, 1969. Definition : Interval from first occurrence of Ophtalmidium exiguum , to last occurrence of Angludiscus communis . 5. (Concurrence rang zone B) Angulodiscus communis Biozone : This biozone with the appearance of Involutina lissica at the bottom and its disappearance at the top along with Angulodiscus communis, Triassina hantkeni , it is clear that they represent a collision zone, so the overlap of these species in the above collision zone indicates the previous retina. This zone is up to 4 meters thick at the bottom of the Shams Abad section and includes the sequence from 29 meters to 32 meters . Category: Concurence rang Zone Age: Early Rhaetian Author: Kristan, 1957 Definition : Interval from first occurrence of Involutina lissica , to last occurrence of Angulodiscus communis. 6.(Interval zone D) Planiinvoluta regularis Biozone : This biozone is between two horizons of disappearance of Planiinvoluta regularis at the top of the zone and Angulodiscus communis It is specified at the bottom of the zone. The presence of these species in the above interstitial zone indicates the age of the Rhaetian. The accompanying species of this biozone are : Involutina liassica , and Triassina hantkeni , This zone is up to 37 meters thick in the middle of the Shams Abad section and it includes from 32 meters of sequence to 67 meters of it. Category: Interval zone Age: Middle Rhaetian Author: Planiinvoluta regularis , Salaj, Borza & Samuel, 1983 . Definition Interval from last occurrence of Planiinvoluta regularis , to last occurrence of Ammodiscus parapriscu s, 7. (Interval zone E) Duostomina alta Biozone : This biozone is between two horizons of the emergence of Duostomina alta species At the top of the zone and the disappearance of Planiinvoluta regularis It is specified below. The presence of these species in the above interstitial zone indicates the age of the Rhaetian. The accompanying species of this biozone is Nodosaria nitidana, Lenticulina Sabquadrata , This zone is up to 28 meters thick at the top of the Shams Abad section, and it ranges from 67 meters to 94 meters . Category: Interval zone Age: Middle Rhaetian Author: Dostomina alta , Kristan-Tollmann, 1960. Definition Interval from first occurrence of Dustomina alta , to last occurrence of Planiinvoluta regularis . 8. (Concurrence rang zone C) Tetrataxis nana Biozone : This biozone coincides with the appearance of Duostomina alta , In the lower part of zone and the disappearance of Tetrataxis nana , and or with the appearance of Trochammina almtalensis , Glomospira sinensis , it is clear above that they represent a collision zone, so the overlapping of these species in the above collision zone indicates the posterior retina. This zone is up to 20 meters thick at the top of the Shams Abad section, and it ranges from 94 meters to 112 meters . Formation. become The age range of all species is estimated based on available sources and articles until 2020. Category: Concurence rang Zone Age: Late Rhaetian Author: Tetrataxis nana , Morozova, 1949. Definition Interval Zone from last occurrence of Duostomina alta to last occurrence of Tetrataxis nana . Based on the identified biozones, the delay of the studied synapses in the Shams abad sections is suggested to be Late Norian-Early Rhaetian to Late Rhaetian. Thus, the studied section can be considered equivalent to the Howz Khan and Qadir members of the Nayband Formation. 7. Conclusion The biostratigraphic study of the Nayband Formation in the Shams abad section, located in the south of the Posht Badam block, shows the organisms such as algae, corals, bivalves, sponges, cephalopods, gastropods, blemenites and foraminifers, and their distribution has varied depending on changes in water circulation, salinity, oxygen levels and other local conditions. As a result of biozonation studies in this region, 21 species out of 15 genera of benthic foraminifera have been identified. Based on this, the number of 5 Interval Zone ( Rectoglandulina tenuis, Triassina hantkeni , Ophtalmidum exigum , Angulodiscus communis, Planiinvoluta regularis ) and 3 Concurrence Zone Turrispirillina minima , Involutina liassica , Duostomina alta , have been identified in the Upper Triassic deposits. Based on the identified biozones, the age range of the studied sequences has been suggested to the late Norian-late Rhaetian, which is equivalent to the Howz Khan and Qadir members of the Nayband Formation in Central Iran. These foraminifera are found together with sponges, corals, bivalves, algae, and sometimes bryozoans and brachiopods, which indicates the shallowness of its sedimentary environment. Based on the studied biozonations, the basin of these deposits is similar to the most of the Triassic Tethys sedimentary basins, especially in North America and Europe, and finally in the northern territory (Boreal), including China, due to having diaster forms. 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(1977). in cooperation with the staff of the Geological Survey of Iran. Stratigraphic lexicon of Iran. Geological Survey of Iran report No . 18. 376p. Rettori, R., (1994). Replacement name Hoyenella, gen. n. (Triassic Foraminiferida Paleontologica Italiana , v. 33, p. 341-343.. Rettori, R., (1995). Foraminiferi del Trias inferiore e medio della Tetide: Revisione tassonomica, stratigrafia ed interpretazione filogenetica: Université de Genève, Publications du Département de Géologie et Paléontologie 18, 147 p. Trifonova, E., (1978b). Foraminifera zones and subzones of the Triassic in Bulgaria II. Ladinian and Carnian: Geologica Balcanica , v. 8, no. 4, p. 49- 64.. Trifonova, E., (1978)c, New Foraminifera species from the Lower and Middle, Triassic in Bulgaria: Comptes Rendus de l’Académie Bulgare des Sciences v. 31, p. 1151-1154. Trifonova, E., (1992). Taxonomy of Bulgarian Triassic Foraminifera. I. Families Psammosphaeridae to Nodosinellidae: Geologica Balcanica , v. 22, p. 3-50.. Trifonova, E., 1993. Taxonomy of Bulgarian Triassic Foraminifera. II. Families Endothyriidae to Ophthalmidiidae: Geologica Balcanica , v. 23, p. 19- 66. Vachard, D., and Fontaine, H., (1988). Biostratigraphic importance of Triassic, Foraminifera and algae from South-East Asia : Revue de Paléobiologie, v. 7, p. 87- 98. Vaziri Moghadam, H., Taheri, A., and Kimiagary, M. (2005). Principles of stratigraphy. Isfahan University. Iran. Press. Issue 273. 310. Zaninetti, L., and Brönnimann, P., (1975). Triassic Foraminifera from Pakistan. Rivista Italiana di Paleontologia , v. 81, p. 257–280. Zaninetti, L. 1976, Les foraminifères du Trias. Essai de synthèse et correlation entre les domains mésogéens European et asiatique: Rivista Italiana de Paleontologia , v. 82, p. 1-258. Zaninetti, L., and Dağer, Z., (1978). Biostratigraphie intégrée et paléoecologie du Trias de la peninsula de Kocaeli (Turquie): Eclogae Geologicae Helvetiae, v. 71, p. 85-104. Zaninetti, L., Martini, R., and Dumont, T. (1992). Triassic foraminifers from sites 761 and 764, Wombat Plateau, northwest Australia. Geology . DOI:10.2973/odp.proc.sr.122.173.1992Corpus ID: 73604277. Plates Plates 1-2 are available in the Supplementary Files section. Additional Declarations No competing interests reported. Supplementary Files Plates.docx Cite Share Download PDF Status: Posted Version 1 posted You are reading this latest preprint version Research Square lets you share your work early, gain feedback from the community, and start making changes to your manuscript prior to peer review in a journal. As a division of Research Square Company, we’re committed to making research communication faster, fairer, and more useful. We do this by developing innovative software and high quality services for the global research community. Our growing team is made up of researchers and industry professionals working together to solve the most critical problems facing scientific publishing. Also discoverable on Platform About Our Team In Review Editorial Policies Advisory Board Help Center Resources Author Services Accessibility API Access RSS feed Manage Cookie Preferences © Research Square 2026 | ISSN 2693-5015 (online) Privacy Policy Terms of Service Do Not Sell My Personal Information {"props":{"pageProps":{"initialData":{"identity":"rs-5840499","acceptedTermsAndConditions":true,"allowDirectSubmit":true,"archivedVersions":[],"articleType":"Research Article","associatedPublications":[],"authors":[{"id":406176052,"identity":"cf9974dc-6fc6-4d6a-8061-c9d567666845","order_by":0,"name":"Nooshin Hadadi","email":"","orcid":"","institution":"Islamic Azad University","correspondingAuthor":false,"prefix":"","firstName":"Nooshin","middleName":"","lastName":"Hadadi","suffix":""},{"id":406176053,"identity":"7a909190-32f4-4b05-972c-5ff4c67a9f51","order_by":1,"name":"Massih Afghah","email":"data:image/png;base64,iVBORw0KGgoAAAANSUhEUgAAAZAAAAAyAQMAAABI0h/eAAAABlBMVEX///8AAABVwtN+AAAACXBIWXMAAA7EAAAOxAGVKw4bAAABAklEQVRIiWNgGAWjYLCCxAYGfgb2xoYDHyoYGAyI1SLZwHP44MMZZ4jVwgjSIpGWbMzbRoQW3fbjjz883GEnIe+QYybBO++wvDl78wGGHxXbcGoxOwNUmXgmWcLwwBkzCclthw139hxLYOw5cxu3lgM5bAyJbcx1ho09ZhKG2w4zbriRY8DM2IZHy/nnjz8kttVLGDbzAK2bc9iesJYbCQYSiW2HJeTZ2JINDjYcTiRCyxug4W3HJQx4mA8+bDiWnrzhzLGEg3j9cj798cefbdUS8vMfNhz+U2Ntu+F488EHPypwa4EDgwNgqhlMHiCsHgjkG8BUHVGKR8EoGAWjYGQBAAljZJI5FdcDAAAAAElFTkSuQmCC","orcid":"","institution":"Islamic Azad University","correspondingAuthor":true,"prefix":"","firstName":"Massih","middleName":"","lastName":"Afghah","suffix":""}],"badges":[],"createdAt":"2025-01-16 09:23:22","currentVersionCode":1,"declarations":"","doi":"10.21203/rs.3.rs-5840499/v1","doiUrl":"https://doi.org/10.21203/rs.3.rs-5840499/v1","draftVersion":[],"editorialEvents":[],"editorialNote":"","failedWorkflow":false,"files":[{"id":74918291,"identity":"01624ff7-9297-4769-9fad-90bf558f42cc","added_by":"auto","created_at":"2025-01-28 10:16:04","extension":"png","order_by":1,"title":"Figure 1","display":"","copyAsset":false,"role":"figure","size":383924,"visible":true,"origin":"","legend":"\u003cp\u003e(a) Structural and geographic framework of Iran shows the main sutures, structural units and geographic areas after Stöcklin (1968) and Nezafati (2006);\u003c/p\u003e\n\u003cp\u003e(b) Location of the studied area in the southern part of the Central Iranian microcontinent situated in the south of Lut, Tabas, Posht badam and Yazd blocks (after Aghanabati, 2004);\u003c/p\u003e\n\u003cp\u003e(c) Tectonic and structural position of the studied area and Shamsabad section;\u003c/p\u003e\n\u003cp\u003e(d) widespread extension of the Nayband Fm. in Central Iran (modified from Seyed-Emami, 1971)\u003c/p\u003e","description":"","filename":"1.png","url":"https://assets-eu.researchsquare.com/files/rs-5840499/v1/607d009250a9233e39cfa53a.png"},{"id":74916578,"identity":"dcbe2d90-6e63-4ece-b5d8-ccd0e389abca","added_by":"auto","created_at":"2025-01-28 10:08:03","extension":"png","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":82515,"visible":true,"origin":"","legend":"\u003cp\u003eThe general position of the stratigraphic Cheshmeh gaz sections in the south of the Posht badam block\u003c/p\u003e","description":"","filename":"2.png","url":"https://assets-eu.researchsquare.com/files/rs-5840499/v1/81803b92141c988c3806cbbe.png"},{"id":74918282,"identity":"30fe80ba-6b8e-46d2-8768-177c5b8d0476","added_by":"auto","created_at":"2025-01-28 10:16:03","extension":"png","order_by":3,"title":"Figure 3","display":"","copyAsset":false,"role":"figure","size":526296,"visible":true,"origin":"","legend":"\u003cp\u003eGeological map of the studied area (taken from the 1:100,000 geological map of Baghin) and the location of the studied section\u003c/p\u003e","description":"","filename":"3.png","url":"https://assets-eu.researchsquare.com/files/rs-5840499/v1/44fcbdfdd72933296151ee5d.png"},{"id":74918280,"identity":"c42e727d-c950-4c17-89f2-99a4215926a0","added_by":"auto","created_at":"2025-01-28 10:16:02","extension":"png","order_by":4,"title":"Figure 4","display":"","copyAsset":false,"role":"figure","size":287761,"visible":true,"origin":"","legend":"\u003cp\u003eOverview of Shamsabad stratigraphic section outcrop and Contact between Nayband formation with Shotory and Ab-e-Haj formations.\u003c/p\u003e","description":"","filename":"4.png","url":"https://assets-eu.researchsquare.com/files/rs-5840499/v1/abe3ca4783f37da14ccbe6a1.png"},{"id":74916568,"identity":"ee904b89-7984-45dd-bb5d-ed7a957670fa","added_by":"auto","created_at":"2025-01-28 10:08:03","extension":"png","order_by":5,"title":"Figure 5","display":"","copyAsset":false,"role":"figure","size":390274,"visible":true,"origin":"","legend":"\u003cp\u003eContact between Nayband and Shotori formations, view towards the northeast\u003c/p\u003e","description":"","filename":"5.png","url":"https://assets-eu.researchsquare.com/files/rs-5840499/v1/4875e1c93a6d0e6849afbf68.png"},{"id":74916592,"identity":"a1db6e2c-d6d4-440b-8264-2f8f30617234","added_by":"auto","created_at":"2025-01-28 10:08:04","extension":"png","order_by":6,"title":"Figure 6","display":"","copyAsset":false,"role":"figure","size":465360,"visible":true,"origin":"","legend":"\u003cp\u003eContact between Nayband Formation and Ab Haji, view to the northeast\u003c/p\u003e","description":"","filename":"6.png","url":"https://assets-eu.researchsquare.com/files/rs-5840499/v1/234a0cb07a7662056d2d5281.png"},{"id":74916631,"identity":"58c72111-5dd0-4170-928a-ac89fc8efff9","added_by":"auto","created_at":"2025-01-28 10:08:06","extension":"png","order_by":7,"title":"Figure 7","display":"","copyAsset":false,"role":"figure","size":430477,"visible":true,"origin":"","legend":"\u003cp\u003e\u003cstrong\u003eStratigraphic column of the Nayband Formation in the Shams Abad section.\u003c/strong\u003e\u003c/p\u003e","description":"","filename":"7.png","url":"https://assets-eu.researchsquare.com/files/rs-5840499/v1/10ba2c9e180481d6236d84e7.png"},{"id":74918283,"identity":"e3bbf57b-6dfc-45af-8a86-993c296ffcaf","added_by":"auto","created_at":"2025-01-28 10:16:03","extension":"png","order_by":8,"title":"Figure 8","display":"","copyAsset":false,"role":"figure","size":342084,"visible":true,"origin":"","legend":"\u003cp\u003e\u003cstrong\u003eStratigraphic range chart of the Nayband Formation in the Shams Abad section.\u003c/strong\u003e\u003c/p\u003e","description":"","filename":"8.png","url":"https://assets-eu.researchsquare.com/files/rs-5840499/v1/1452c4d1ab69d41cc3e8d1b5.png"},{"id":74920156,"identity":"58767b23-5694-45b2-9fde-c0ca496e3a39","added_by":"auto","created_at":"2025-01-28 10:32:10","extension":"pdf","order_by":0,"title":"","display":"","copyAsset":false,"role":"manuscript-pdf","size":3839767,"visible":true,"origin":"","legend":"","description":"","filename":"manuscript.pdf","url":"https://assets-eu.researchsquare.com/files/rs-5840499/v1/39d3e609-7064-4f66-badc-1d5100a9ff1c.pdf"},{"id":74919258,"identity":"78876936-83da-4dba-9f5b-7333ff4af445","added_by":"auto","created_at":"2025-01-28 10:24:04","extension":"docx","order_by":1,"title":"","display":"","copyAsset":false,"role":"supplement","size":2443193,"visible":true,"origin":"","legend":"","description":"","filename":"Plates.docx","url":"https://assets-eu.researchsquare.com/files/rs-5840499/v1/0edbade1eea32ab2c49c6b03.docx"}],"financialInterests":"No competing interests reported.","formattedTitle":"\u003cp\u003eBiostratigraphy of Late Triassic deposits, based on foraminiferal fauna in the Central Iran Zone (Posht badam Block) \u003c/p\u003e","fulltext":[{"header":"1. Introduction","content":"\u003cp\u003eCentral Iranian Microcontinent (CEIM) () includes Lut, Tabas and Yazd blocks (Takin, 1972; Davodzadeh and Schmidt, 1982). According to the geological evidence, the sheet of Iran, which covers the entire area of ​​central, northern and southern parts of Iran, was a part of the Cimmerian continent (Shengur, 1990). Central and northern Iran were separated from the northern edge of the Gondwana supercontinent and pushed northward during the Permian and Triassic periods due to the action of rifting, simultaneously with the subsidence andgradual closing of the Paleotethys oceanic basin and the collision of the Iranian plate with the southern edge of the Eurasian supercontinent or the Turan Plate at the beginning of the Late Triassic (Shtoklin, 1974), the orogeny event of the early Simmerian and the formation of the Simmerid Mountains were established (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e\u003cb\u003e)\u003c/b\u003e.\u003c/p\u003e \u003cp\u003eAt the front of the rising mountains of Simmerid and along with the simultaneous dynamic tectonics of sedimentation, a thick series of siliceous-clastic rocks related to alluvial plains, marshes, coastal and sea environments has been deposited, which is called Shemshak Group (Aghanbati, 1998; Seyid Emami. et al., 2001). The Shemshak Group is actually a large\u003c/p\u003e \u003cp\u003estructural-sedimentary cycle that is limited by the Early Cimmerian (Norian) and Middle Cimmerian (Middle Bajocian) events (Aghanbati, 1998). The homogeneity and adaptation of rock strata facies of Shemshak group (Norian to Lower Bajocian) in central and northern Iran shows that the Iranian plate has acted as a continuous and integrated area during this cycle.\u003c/p\u003e \u003cp\u003eThe Upper Triassic deposits of the Nayband Formation are distributed over a large area from different provinces such as Yazd, Khorasan, Isfahan, Arak and Kerman (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e), (Seyed-Emami, 2003; Aghanabati, 2004).\u003c/p\u003e \u003cp\u003eIn fact, the breaking of the Iranian plate into several structural and sedimentary units such as Lut, Tabas, Posht Badam and Yazd blocks has been done in relation to the Middle Cimmerian event at the end of the early Bajocian (Seied Emami and Alavi Naini, 1990). Among the three Simrid events, it has had the greatest impact on the tectonics of central and northern Iran. As a result, after the middle Cimmerian event in the early Bajocian, which caused the Iranian plate to break into several structural pieces or blocks, tectonic unrest has intensified in it.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003efinally, during the following periods, in the Middle and Late Jurassic, numerous tectonic movements, in the form of block movements along with frequent global fluctuations of sea water, played a decisive role in the sedimentation pattern of the region and it has created various stratigraphic facies, whose time regulation and correspondence of stratigraphy with each other in the past has led to many inadequacies and ambiguities in the geological in perception and interpretation of the region (Shtoklin et al., 1965).\u003c/p\u003e \u003cp\u003eAfter this event in the Late Bajocian, another structural-sedimentary cycle (Mago Group) begins, which ends with the Late Cimmerian event at the end of the Jurassic and the beginning of the Early Cretaceous. During this cycle, especially in the microcontinent of Central Iran, due to a combination of tractional, traversal and rotational movements and general block movements in connection with numerous tectonic movements (Seyed Emami et al., 2004), various series of different lithostratigraphy facies related to continental, evaporite, marsh, coastal, shallow to deep marine sedimentation environments have been formed. Determining the correlation of stratigraphy and their compatibility with each other requires very detailed geological and paleontology studies.\u003c/p\u003e"},{"header":"2. Geological settings","content":"\u003cp\u003eThe study area is a small part of the Central Iran Zone (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e). Extensive structural-sedimentary disparities have caused the Central Iran subcontinent to be divided into the Lut block, Tabas block, Kalmard block, Posht Badam block, and Yazd block (Aghanbati, 2004) (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe studied zone which limited from the north -northwest by the Daroneh fault (Great Desert fault), from the east by the Nehbandan, and from the southwest by Nain - Dehshir - Baft fault. The structural pattern of this subcontinent is the type of blocks separated by major faults, each of them has separated features, and the dynamics of the subcontinent are not the same.\u003c/p\u003e \u003cp\u003eThe studied Shams abad region in the NW Kerman, is located in the southern part of the Posht badam block, which is located between the Nain-Kohbanan fault in the east and the Posht badam fault in the west.\u003c/p\u003e \u003cp\u003eThe mountain range of the region is mostly northwest-southeast. The outcrops of the region are mostly Mesozoic units in the highlands and Cenozoic, Pliocene, and Quaternary in the desert. The Shams abad section (N: 56̊ 47̍ 28̎ ; E: 30̊ 20̍ 51̎ ) is located within the 1:250000 Rafsanjan and 1:100000 Baghin geological maps and is located approximately 30 km northwest of Shams abad village.\u003c/p\u003e"},{"header":"3. Material and Methods","content":"\u003cp\u003eTo establish the age dating and depositionsl environmental studies of the Nayband Formation, the Shams abad stratigraphic section was measured and sampled systematically, emphasizing lithology and facies changes and the characterization of sedimentary structures.\u003c/p\u003e"},{"header":"4. Discussion","content":"\u003cp\u003e \u003cb\u003eLithostratigraphy\u003c/b\u003e \u003c/p\u003e \u003cp\u003eField studies on the Upper Triassic deposits in the studied area indicate that most of the studied area has an NW-SE trending fold and fracture zone. Lithological studies of the deposits of this section are based on field studies and microscopic studies of rocks and their microfacies results.\u003c/p\u003e \u003cp\u003eThe lithological characteristics of the studied section consists of 112 m thickness, mainly composed of medium to thin bedded olive green silty shales with gray sandstones interbeds and abundant corals, sponges, bivalves and foraminiferal fauna in the age range of Upper Triassic to Lower Jurassic (Fig.\u0026nbsp;2). Good sorted red quartz sandstone fragments are cemented by Fe at the top of the Nayband Formation, overlain by sandstone and shale sediments of Ab-e-Haji Formation.\u003c/p\u003e"},{"header":"5. Description of Shahdad stratigraphic section:","content":"\u003cp\u003eThe outcrop of the Nayband formation in this section, with a thickness of about 112 meters, is mainly composed of prograding carbonate rocks layers between shallow regressive shales and sandstones dominated by a deltaic-river environment. In its lower parts, iron staining can be seen contact with the equivalent unit of Shotori, which indicates a period of aridification and an erosional discontinuity between these two units. In the upper part of these deposits, there are medium to thin layered pea-colored to pale yellow-brown limestones alternate with olive-green shales, sometimes slightly silty to mostly gray to cream sandstones.\u003c/p\u003e\n\u003cp\u003eIn fact, the lower boundary of the outcrop begins with a discontinuity that is in contact with the upper parts of the Nayband or Howz Khan and Qadir formations and gradually reaches the sandstone-shale deposits belonging to the Lower Lias or Ab Haji.\u003cstrong\u003e\u0026nbsp;\u0026nbsp;\u003c/strong\u003eThe detailed description of these layers are:\u003c/p\u003e"},{"header":"6. Biostratigraphy","content":"\u003cp\u003eBiostratigraphical studies in this research are based on benthic foraminiferal fauna. Although the Nayband Formation foraminiferal fauna have a notable variety, but they are not widely distributed,. In the present study, a total of 23 species of 21 genera were identified and their presence intervals were also determined.\u003c/p\u003e\n\u003cp\u003eThe families Permodiscidae, Turrispirilinidae, Ammodiscidae, Frondicularidae, have a maximum abundance in this study and lead to the recognition of 8 biozones (Fig. 8, \u003cstrong\u003ePlates 1,2).\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eSo far, no official biozonation has been provided for the deposits of the the Nayband Formation in the Upper Triassic age range. But due to some features such as abundance, high diversity, as well as a significant number of the first appearance and the last appearance of the mentioned fauna through upper Triassic, foraminifers can be part of the very important paleobiotic elements in terms of biostratigraphy in the sequences of the Nayband Formation. The lithological changes of the studied section can be related to the sedimentation and paleoclimatic conditions and as a result overshadow the distribution of fossil fauna, their accumulations and the biozonation position. Various authors such as:\u003c/p\u003e\n\u003cp\u003eZaninetti, \u003cspan class=\"CitationRef\"\u003e1976\u003c/span\u003e; Vachard and Fontaine, \u003cspan class=\"CitationRef\"\u003e1988\u003c/span\u003e; Altıner and Ko\u0026ccedil;yiğit, 1993; Rettori et al., 1994; Rettori, \u003cspan class=\"CitationRef\"\u003e1995\u003c/span\u003e; Muttoni et al., \u003cspan class=\"CitationRef\"\u003e1996\u003c/span\u003e; Marquez, 2005; Kobayashi et al., \u003cspan class=\"CitationRef\"\u003e2006\u003c/span\u003e; Lehrmann et al., 2015; ; Luka Gale, \u003cspan class=\"CitationRef\"\u003e2012\u003c/span\u003e\u003c/p\u003e\n\u003cp\u003eIn the present research the biozonation of the Triassic range which has been studied based on the foraminiferal fauna, the global standard biozonation that can be used in different parts of the world, has not been obtained in the studied region. Mostly we are faced with local foraminiferal biozonation and Of course, this also overshadows compliance. Based on the studies conducted in the Triassic basins of Europe or the Alps, including Spain, Bulgaria, Poland, Hungary, Switzerland, (Salaj, \u003cspan class=\"CitationRef\"\u003e1969\u003c/span\u003e, \u003cspan class=\"CitationRef\"\u003e1978\u003c/span\u003e; Salaj et al., \u003cspan class=\"CitationRef\"\u003e1983\u003c/span\u003e; Salaj et al., \u003cspan class=\"CitationRef\"\u003e1988\u003c/span\u003e; Trifonova, \u003cspan class=\"CitationRef\"\u003e1978\u003c/span\u003ea, b, 1992, 1993; Gazdzicki et al., \u003cspan class=\"CitationRef\"\u003e1975\u003c/span\u003e; Orovecz-Scheffer, \u003cspan class=\"CitationRef\"\u003e1987\u003c/span\u003e;)، and also some basins of Asia, including parts of T\u0026uuml;rkiye and the Caucasus (Zaninetti and Dağer, \u003cspan class=\"CitationRef\"\u003e1978\u003c/span\u003e; Efimova, \u003cspan class=\"CitationRef\"\u003e1991\u003c/span\u003e), none of the studies have led to the creation of a framework of foraminiferal biozonation in the Triassic, and the reason is based on the aforementioned studies in different parts of the world, some taxonomic issues and flaws, poor calibration of the age range of the taxa used in biozonation, and finally strict facies control. all of these factors prevent the creation global standard biozonation based on foraminiferal fauna through Triassic (Altiner et al., \u003cspan class=\"CitationRef\"\u003e2021\u003c/span\u003e).\u003c/p\u003e\n\u003cp\u003eBased on biostratigraphic studies, it is possible to understand the differences in different regions and identify specific fossil communities and their faunal assemblages. In the studied area, considering that the lithological changes of Late Triassic deposits are directly related to the sedimentation and climatic conditions, as a result of the dispersion of the existing biological populations and biocenoses, they have undergone obvious changes in relation to the paleo-ecological developments.\u003c/p\u003e\n\u003cp\u003eBased on the biostratigraphic studies, it is possible to identify the differences in the regions in general in the present study, 23 species of 21 genera were identified, and their age ranges were studied and finally the age has been determined. The foraminifera of the Nayband Formation in the studied section of Shahdad have a low abundance but significant diversity. Families such as Permodiscidae, Turrispirilinidae, Ammodiscidae, Frondicularidae have the highest frequency in the studied section, and the most important identified foraminifers are as follows:\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eTriasina hantkeni\u003c/em\u003e Majzon, 1954. \u003cem\u003eAngulodiscus cummunis\u003c/em\u003e Kristan, 1957,\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eTetrataxis nana\u003c/em\u003e, Morozova, 1949. \u003cem\u003eRectoglandolina tenuis\u003c/em\u003e, Bornemann, 1854.\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eTrochammina almtalensis\u003c/em\u003e, Koehn-Zaninetti, 1969. \u003cem\u003eAuloturtus Broennimanni\u003c/em\u003e, Salaj,1969.\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eGlomospira minima\u003c/em\u003e, Michal\u0026iacute;k, J., Jendrej\u0026aacute;kov\u0026aacute;, O., \u0026amp; Borza, K. (1979).\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eAmmodiscus parapriscus\u003c/em\u003e, Ho, 1959. \u003cem\u003eAngulodiscus cummunis\u003c/em\u003e, Kristan, 1957.\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eAgathammina oustroalpina\u003c/em\u003e, Kristan-Tollmann, Tollmann (Michal\u0026iacute;k, Jendrej\u0026aacute;- kov\u0026aacute; 1978; Michal\u0026iacute;k 1978). \u003cem\u003eOphtalmidium exiguum\u003c/em\u003e, Koehn-Zaninetti, 1969. \u003cem\u003eInvolutina liassica\u003c/em\u003e, Jones, 1853..\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eNodosaria sumatrensis\u003c/em\u003e, Lange, 1925. \u003cem\u003eLenticulina\u003c/em\u003e sp., Lamarck, 1804.\u003c/p\u003e\n\u003cp\u003e\u003cem\u003ePermodiscus praecommunis\u003c/em\u003e, Salaj, Borza \u0026amp; Samuel, \u003cspan class=\"CitationRef\"\u003e1983\u003c/span\u003e.\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eTurrispirillina minima\u003c/em\u003e, Pantić, 1967. \u003cem\u003eInvolutina liassica\u003c/em\u003e, Jones, 1853.\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eAngulodiscus gaschei\u003c/em\u003e, Koehn-Zaninetti, L.; Br\u0026ouml;nnimann, P. (1968).\u003c/p\u003e\n\u003cp\u003e\u003cem\u003ePilamminella falsofriedli\u003c/em\u003e, Salaj, Borza \u0026amp; Samuel \u003cspan class=\"CitationRef\"\u003e1983\u003c/span\u003e. \u003cem\u003eRobuloides\u003c/em\u003e sp., Reichel 1946\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eDostomina alta\u003c/em\u003e, Kristan-Tollmann, 1960. \u003cem\u003eAuloconus permodiscoides\u003c/em\u003e, Oberhauser, 1964.\u003c/p\u003e\n\u003cp\u003eSalaj, Borza \u0026amp; Samuel, \u003cspan class=\"CitationRef\"\u003e1983\u003c/span\u003e. \u003cem\u003eregularis, Planiinvoluta\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003eThe stratigraphic range of studied foraminifera is also shown in Fig.\u0026nbsp;8. As mentioned, no precise biozonation has been done for these taxa. the studied biozons are local and can be used to some extent in other blocks of the Central Iranian subcontinent.\u003c/p\u003e\n\u003cp\u003eFauna of foraminifera and systematics of Upper Triassic taxa have been introduced based on benthic foraminifera in the Tethys basin, in the southeast of the Alps, which can be referred to the studies of Luka Gale (\u003cspan class=\"CitationRef\"\u003e2012\u003c/span\u003e). Therefore, according to the abundance and distribution of foraminifera in the studied sequence, biostratigraphic studies were conducted and led to the identification of 8 biozones as follows (\u003cstrong\u003eFig.\u0026nbsp;8\u003c/strong\u003e and Plates 1, 2):\u003c/p\u003e\n\u003cdiv class=\"Heading\"\u003e\u003cstrong\u003e1. (Interval zone A) \u003cem\u003eRectoglandulina tenuis\u003c/em\u003e Biozone:\u003c/strong\u003e\u003c/div\u003e\n\u003cp\u003eCategory: Interval zone\u003c/p\u003e\n\u003cp\u003eAge: Late Norian\u003c/p\u003e\n\u003cp\u003eAuthor: \u003cem\u003eRectoglandolina tenuis, Bornemann, 1854.\u003c/em\u003e Definition : Interval from first occurrence of \u003cem\u003eRectoglandulina tenuis\u003c/em\u003e to first occurrence of \u003cem\u003ePermodiscus minutus\u003c/em\u003e,\u003c/p\u003e\n\u003cdiv class=\"BlockQuote\"\u003e\n \u003cp\u003eThis biozone is between two horizons of the appearance of \u003cem\u003eRectoglandulina tenuis\u003c/em\u003e in the lower part of biozone and \u003cem\u003ePermodiscus minutus\u003c/em\u003e at the top of the biozone. The presence of these species in the above interstitial zone indicates the age of the Norian. The accompanying species of this biozone are: \u003cem\u003eNodosaria nitidana\u003c/em\u003e, \u003cem\u003eNodosaria shablensis\u003c/em\u003e, This zone is up to \u003cstrong\u003e2 meters\u003c/strong\u003e thick at the base of the Shamsabad section.\u003c/p\u003e\n\u003c/div\u003e\n\u003cp\u003e\u003cstrong\u003e2. (Interval zone B)\u003c/strong\u003e : \u003cstrong\u003eTriassina hantkeni\u003c/strong\u003e \u003cstrong\u003eBiozone\u003c/strong\u003e: This biozone is between two horizons of the appearance of \u003cem\u003eTriassina hantkeni\u003c/em\u003e In the lower part of biozone and \u003cem\u003eTetrataxis nana\u003c/em\u003e at the top of the biozone. The presence of these species in the above interstitial zone indicates the Norian-Late Norian age. Other assemblage of this biozone include the following: \u003cem\u003eAngulodiscus commonis\u003c/em\u003e, \u003cem\u003eNodosaria samatrensis\u003c/em\u003e, \u003cem\u003ePermodiscus minutus.\u003c/em\u003e This biozone is up to 18 meters thick at the bottom of the Shams Abad section, and it ranges from 3 meters \u003cstrong\u003eto 20 meters\u003c/strong\u003e.\u003c/p\u003e\n\u003cp\u003eHere, the only recognized biozone of the international standard that is important in determining the exact age of this biozone is the \u003cem\u003eTriassina hantkeni\u003c/em\u003e Biozone, named by Louisette Zaninetti et al. And in northwestern Australia it has been identified as Late Norian-Early Rhaetian and is also defined throughout the Tethys realm:\u003c/p\u003e\n\u003cp\u003eAccording to international stratigraphic rules:\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eTriasina hantkeni\u003c/em\u003e defines Lat Norian - Lower Rhaetian\u003c/p\u003e\n\u003cp\u003e\u003cem\u003eTriasina hantkeni\u003c/em\u003e Biozone (Gazdzicki et al., \u003cspan class=\"CitationRef\"\u003e1979\u003c/span\u003e; Gazdzicki, \u003cspan class=\"CitationRef\"\u003e1983\u003c/span\u003e; Gazdzicki and Reid, \u003cspan class=\"CitationRef\"\u003e1983\u003c/span\u003e; Abate et al., 1984; Ciarapica and Zaninetti, \u003cspan class=\"CitationRef\"\u003e1985\u003c/span\u003e; Vachard and Fontaine, \u003cspan class=\"CitationRef\"\u003e1988\u003c/span\u003e)\u003c/p\u003e\n\u003cp\u003ethroughout the Tethys realm.\u003c/p\u003e\n\u003cp\u003eCategory: Interval zone\u003c/p\u003e\n\u003cp\u003eAge: Late Norian\u003c/p\u003e\n\u003cp\u003eAuthor: \u003cem\u003eTriasina hantkeni\u003c/em\u003e, Majzon, 1954, Definition : Interval from first occurrence of \u003cem\u003eTriasina hantkeni\u003c/em\u003e, to first occurrence of \u003cem\u003eTetrataxis nana\u003c/em\u003e,\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003e3. (Concurrence rang zone A)\u003c/strong\u003e: \u003cstrong\u003eTurrispirillina minima\u003c/strong\u003e \u003cstrong\u003eBiozone\u003c/strong\u003e: This biozone began with the appearance of \u003cem\u003eTurrispirilina minima\u003c/em\u003e, in the lower part of biozone and the disappearance of \u003cem\u003eRectoglandulina tenuis\u003c/em\u003e above, it is clear that they have acted as a collision zone, so that the overlap of these species in the above collision zone indicates the late Norian - Early Rhaetian. This zone is 3 meters thick at the bottom of the Shams Abad section, and it ranges from 20 meters \u003cstrong\u003eto 23 meters\u003c/strong\u003e.\u003c/p\u003e\n\u003cp\u003eCategory: Concurence rang Zone\u003c/p\u003e\n\u003cp\u003eAge: Early Rhaetian\u003c/p\u003e\n\u003cp\u003eAuthor: \u003cem\u003eTurrispirillina minima\u003c/em\u003e, Pantić, 1967. Definition : Interval from first occurrence of \u003cem\u003eTurrispirillina minima\u003c/em\u003e to last occurrence of \u003cem\u003eRectoglandulina tenuis\u003c/em\u003e,\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003e4. (Interval zone C)\u003c/strong\u003e \u003cstrong\u003eOphtalmidium exigum\u003c/strong\u003e \u003cstrong\u003eBiozone\u003c/strong\u003e: This biozone is between the two horizons of the appearance of \u003cem\u003eOphtalmidium exigum\u003c/em\u003e species at the top of the zone and the disappearance of \u003cem\u003eAngludiscus communis\u003c/em\u003e. at the top of the zone. The presence of these species in the above interstitial zone indicates the posterior neuron - the highest part of the posterior neuron. Among the species associated with this biozone, the following can be mentioned: \u003cem\u003eTriassina hantkeni\u003c/em\u003e, \u003cem\u003eTurrispirilina minim\u003c/em\u003ea, \u003cem\u003eTetrataxis nana\u003c/em\u003e,\u003c/p\u003e\n\u003cp\u003e\u003cem\u003ePlaniinvoluta regularis\u003c/em\u003e, This zone is up to 6 meters thick at the bottom of the Shams Abad section, and it ranges from 22 meters \u003cstrong\u003eto 32 meters\u003c/strong\u003e.\u003c/p\u003e\n\u003cp\u003eCategory: Interval zone\u003c/p\u003e\n\u003cp\u003eAge: Early Rhaetian\u003c/p\u003e\n\u003cp\u003eAuthor: \u003cem\u003eOphtalmidium exiguum\u003c/em\u003e, Koehn-Zaninetti, 1969. Definition : Interval from first occurrence of \u003cem\u003eOphtalmidium exiguum\u003c/em\u003e, to last occurrence of \u003cem\u003eAngludiscus communis\u003c/em\u003e.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003e5. (Concurrence rang zone B)\u003c/strong\u003e \u003cstrong\u003eAngulodiscus communis\u003c/strong\u003e \u003cstrong\u003eBiozone\u003c/strong\u003e: This biozone with the appearance of \u003cem\u003eInvolutina lissica\u003c/em\u003e at the bottom and its disappearance at the top along with \u003cem\u003eAngulodiscus communis, Triassina hantkeni\u003c/em\u003e, it is clear that they represent a collision zone, so the overlap of these species in the above collision zone indicates the previous retina. This zone is up to 4 meters thick at the bottom of the Shams Abad section and includes the sequence from 29 meters \u003cstrong\u003eto 32 meters\u003c/strong\u003e.\u003c/p\u003e\n\u003cp\u003eCategory: Concurence rang Zone\u003c/p\u003e\n\u003cp\u003eAge: Early Rhaetian\u003c/p\u003e\n\u003cp\u003eAuthor: Kristan, 1957 Definition : Interval from first occurrence of \u003cem\u003eInvolutina lissica\u003c/em\u003e, to last occurrence of \u003cem\u003eAngulodiscus communis.\u003c/em\u003e\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003e6.(Interval zone D)\u003c/strong\u003e \u003cstrong\u003ePlaniinvoluta regularis\u003c/strong\u003e \u003cstrong\u003eBiozone\u003c/strong\u003e: This biozone is between two horizons of disappearance of \u003cem\u003ePlaniinvoluta regularis\u003c/em\u003e at the top of the zone and \u003cem\u003eAngulodiscus communis\u003c/em\u003e It is specified at the bottom of the zone. The presence of these species in the above interstitial zone indicates the age of the Rhaetian. The accompanying species of this biozone are : \u003cem\u003eInvolutina liassica\u003c/em\u003e, and \u003cem\u003eTriassina hantkeni\u003c/em\u003e, This zone is up to 37 meters thick in the middle of the Shams Abad section and it includes from 32 meters of sequence \u003cstrong\u003eto 67 meters\u003c/strong\u003e of it.\u003c/p\u003e\n\u003cp\u003eCategory: Interval zone\u003c/p\u003e\n\u003cp\u003eAge: Middle Rhaetian\u003c/p\u003e\n\u003cp\u003eAuthor: \u003cem\u003ePlaniinvoluta regularis\u003c/em\u003e, Salaj, Borza \u0026amp; Samuel, \u003cspan class=\"CitationRef\"\u003e1983\u003c/span\u003e.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eDefinition\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eInterval from last occurrence of \u003cem\u003ePlaniinvoluta regularis\u003c/em\u003e, to last occurrence of \u003cem\u003eAmmodiscus parapriscu\u003c/em\u003es,\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003e7. (Interval zone E)\u003c/strong\u003e \u003cstrong\u003eDuostomina alta\u003c/strong\u003e \u003cstrong\u003eBiozone\u003c/strong\u003e: This biozone is between two horizons of the emergence of \u003cem\u003eDuostomina alta\u003c/em\u003e species At the top of the zone and the disappearance of \u003cem\u003ePlaniinvoluta regularis\u003c/em\u003e It is specified below. The presence of these species in the above interstitial zone indicates the age of the Rhaetian. The accompanying species of this biozone is \u003cem\u003eNodosaria nitidana, Lenticulina Sabquadrata\u003c/em\u003e, This zone is up to 28 meters thick at the top of the Shams Abad section, and it ranges from 67 meters \u003cstrong\u003eto 94 meters\u003c/strong\u003e.\u003c/p\u003e\n\u003cp\u003eCategory: Interval zone\u003c/p\u003e\n\u003cp\u003eAge: Middle Rhaetian\u003c/p\u003e\n\u003cp\u003eAuthor: \u003cem\u003eDostomina alta\u003c/em\u003e, Kristan-Tollmann, 1960.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eDefinition\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eInterval from first occurrence of \u003cem\u003eDustomina alta\u003c/em\u003e, to last occurrence of \u003cem\u003ePlaniinvoluta regularis\u003c/em\u003e.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003e8. (Concurrence rang zone C)\u003c/strong\u003e \u003cstrong\u003eTetrataxis nana\u003c/strong\u003e \u003cstrong\u003eBiozone\u003c/strong\u003e: This biozone coincides with the appearance of \u003cem\u003eDuostomina alta\u003c/em\u003e, In the lower part of zone and the disappearance of \u003cem\u003eTetrataxis nana\u003c/em\u003e, and or with the appearance of \u003cem\u003eTrochammina almtalensis\u003c/em\u003e, \u003cem\u003eGlomospira sinensis\u003c/em\u003e, it is clear above that they represent a collision zone, so the overlapping of these species in the above collision zone indicates the posterior retina. This zone is up to 20 meters thick at the top of the Shams Abad section, and it ranges from 94 meters \u003cstrong\u003eto 112 meters\u003c/strong\u003e. Formation. become The age range of all species is estimated based on available sources and articles until 2020.\u003c/p\u003e\n\u003cp\u003eCategory: Concurence rang Zone\u003c/p\u003e\n\u003cp\u003eAge: Late Rhaetian\u003c/p\u003e\n\u003cp\u003eAuthor: \u003cem\u003eTetrataxis nana\u003c/em\u003e, Morozova, 1949.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eDefinition\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eInterval Zone from last occurrence of \u003cem\u003eDuostomina alta\u003c/em\u003e to last occurrence of \u003cem\u003eTetrataxis nana\u003c/em\u003e.\u003c/p\u003e\n\u003cp\u003eBased on the identified biozones, the delay of the studied synapses in the Shams abad sections is suggested to be Late Norian-Early Rhaetian to Late Rhaetian. Thus, the studied section can be considered equivalent to the Howz Khan and Qadir members of the Nayband Formation.\u003c/p\u003e"},{"header":"7. Conclusion","content":"\u003cp\u003eThe biostratigraphic study of the Nayband Formation in the Shams abad section, located in the south of the Posht Badam block, shows the organisms such as algae, corals, bivalves, sponges, cephalopods, gastropods, blemenites and foraminifers, and their distribution has varied depending on changes in water circulation, salinity, oxygen levels and other local conditions. As a result of biozonation studies in this region, 21 species out of 15 genera of benthic foraminifera have been identified. Based on this, the number of 5 Interval Zone (\u003cem\u003eRectoglandulina tenuis, Triassina hantkeni\u003c/em\u003e, \u003cem\u003eOphtalmidum exigum\u003c/em\u003e, \u003cem\u003eAngulodiscus communis, Planiinvoluta regularis\u003c/em\u003e) and 3 Concurrence Zone \u003cem\u003eTurrispirillina minima\u003c/em\u003e, \u003cem\u003eInvolutina liassica\u003c/em\u003e, \u003cem\u003eDuostomina alta\u003c/em\u003e, have been identified in the Upper Triassic deposits. Based on the identified biozones, the age range of the studied sequences has been suggested to the late Norian-late Rhaetian, which is equivalent to the Howz Khan and Qadir members of the Nayband Formation in Central Iran. These foraminifera are found together with sponges, corals, bivalves, algae, and sometimes bryozoans and brachiopods, which indicates the shallowness of its sedimentary environment.\u003c/p\u003e \u003cp\u003eBased on the studied biozonations, the basin of these deposits is similar to the most of the Triassic Tethys sedimentary basins, especially in North America and Europe, and finally in the northern territory (Boreal), including China, due to having diaster forms. The mentioned basin, together with Triassic Balkan Carpathian and Alpine basins, was located in the passive southern margin of the Paleotethys, or in other words, in the southern margin of the Eurasian plate.\u003c/p\u003e"},{"header":"References","content":"\u003col\u003e\n \u003cli\u003eAdams, T.D. and Bourgeois, F., (1967). Asmari Biostratigraphy. \u003cem\u003eIranian Oil Operation Companies\u003c/em\u003e, Geological and Exploration Division, Report. No. 1074: 6-11.\u003c/li\u003e\n \u003cli\u003eAghanbati, S. A. 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Biostratigraphie int\u0026eacute;gr\u0026eacute;e et pal\u0026eacute;oecologie du Trias de la peninsula de Kocaeli (Turquie): \u003cem\u003eEclogae Geologicae Helvetiae,\u003c/em\u003e v. 71, p. 85-104.\u003c/li\u003e\n \u003cli\u003eZaninetti, L., Martini, R., and Dumont, T. (1992). Triassic foraminifers from sites 761 and 764, Wombat Plateau, northwest Australia. \u003cem\u003eGeology\u003c/em\u003e. DOI:10.2973/odp.proc.sr.122.173.1992Corpus ID: 73604277.\u003c/li\u003e\n\u003c/ol\u003e"},{"header":"Plates","content":"\u003cp\u003ePlates 1-2 are available in the Supplementary Files section.\u003c/p\u003e"}],"fulltextSource":"","fullText":"","funders":[],"hasAdminPriorityOnWorkflow":false,"hasManuscriptDocX":true,"hasOptedInToPreprint":true,"hasPassedJournalQc":"","hasAnyPriority":true,"hideJournal":true,"highlight":"","institution":"","isAcceptedByJournal":false,"isAuthorSuppliedPdf":false,"isDeskRejected":"","isHiddenFromSearch":false,"isInQc":false,"isInWorkflow":false,"isPdf":false,"isPdfUpToDate":true,"isWithdrawnOrRetracted":false,"journal":{"display":true,"email":"[email protected]","identity":"researchsquare","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":true,"externalIdentity":"","sideBox":"","snPcode":"","submissionUrl":"/submission","title":"Research Square","twitterHandle":"researchsquare","acdcEnabled":true,"dfaEnabled":false,"editorialSystem":"","reportingPortfolio":"","inReviewEnabled":false,"inReviewRevisionsEnabled":true},"keywords":"Late Triassic deposits, Nayband formation, Posht badam block, Central Iran, Kerman","lastPublishedDoi":"10.21203/rs.3.rs-5840499/v1","lastPublishedDoiUrl":"https://doi.org/10.21203/rs.3.rs-5840499/v1","license":{"name":"CC BY 4.0","url":"https://creativecommons.org/licenses/by/4.0/"},"manuscriptAbstract":"\u003cp\u003eIn order to conformity of the sedimentary environment and biological fauna of Late Triassic deposits in each of blocks of the Central Iran, including Lut, Tabas, Posht badam and Yazd blocks, as well as to study the tectonics of the region, were selected sever sections in these blocks, including one section It was studied in the south of \u0026nbsp;Posht badam block in Kerman region, this section is located in the northwest of Kerman city, and Between the Kohbanan and Posht badam faults. The studied section with a thickness of 112 meters is mostly composed of shale, sandstone and limestone. it has many fossils including Bivalves, Sponges, Corals, Bryozoa, Microgastropods and Cephalopods, especially Belemnite, which generally shows the presence of Late Triassic sediments (Norian-Rhaetian) in this area. According to the identified index foraminifera, 8 interval \u0026amp; Concurrence rang biozones Including \u0026nbsp;5 interval Zone\u003cem\u003e Rectoglandulina tenuis, Triassina hantkeni\u003c/em\u003e, \u003cem\u003eOphtalmidum exigum\u003c/em\u003e,\u003cem\u003e Angulodiscus communis, Planiinvoluta regularis \u003c/em\u003eand 3 Concurrence rang Zone \u003cem\u003eTurrispirillina minima\u003c/em\u003e, \u003cem\u003eInvolutina liassica\u003c/em\u003e, \u003cem\u003eDuostomina alta,\u003c/em\u003e were recognized in the Upper Triassic deposits. Based on the identified biozones, the age of the studied sequences, Late Norian - Early Rhaetian, Middle Rhaetian, Until the end of the Triassic, Late Rhaetian to the beginning of Lias is suggested that they are formation considered equivalent to the members of Howz Khan and Qhadir members from the Nayband Formation in central Iran.\u003c/p\u003e","manuscriptTitle":"Biostratigraphy of Late Triassic deposits, based on foraminiferal fauna in the Central Iran Zone (Posht badam Block)","msid":"","msnumber":"","nonDraftVersions":[{"code":1,"date":"2025-01-28 10:07:56","doi":"10.21203/rs.3.rs-5840499/v1","editorialEvents":[{"type":"communityComments","content":0}],"status":"published","journal":{"display":true,"email":"[email protected]","identity":"researchsquare","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":true,"externalIdentity":"","sideBox":"","snPcode":"","submissionUrl":"/submission","title":"Research Square","twitterHandle":"researchsquare","acdcEnabled":true,"dfaEnabled":false,"editorialSystem":"","reportingPortfolio":"","inReviewEnabled":false,"inReviewRevisionsEnabled":true}}],"origin":"","ownerIdentity":"96146b12-68d2-4c68-9e8e-34f5fe994100","owner":[],"postedDate":"January 28th, 2025","published":true,"recentEditorialEvents":[],"rejectedJournal":[],"revision":"","amendment":"","status":"posted","subjectAreas":[],"tags":[],"updatedAt":"2025-01-28T10:07:57+00:00","versionOfRecord":[],"versionCreatedAt":"2025-01-28 10:07:56","video":"","vorDoi":"","vorDoiUrl":"","workflowStages":[]},"version":"v1","identity":"rs-5840499","journalConfig":"researchsquare"},"__N_SSP":true},"page":"/article/[identity]/[[...version]]","query":{"redirect":"/article/rs-5840499","identity":"rs-5840499","version":["v1"]},"buildId":"8U1c8b4HqxoKbykW_rLl7","isFallback":false,"isExperimentalCompile":false,"dynamicIds":[84888],"gssp":true,"scriptLoader":[]}