Biostratigraphy of Late Triassic deposits in Central Iranian (Shams abad section in the south of Posht badam Block)

doi:10.21203/rs.3.rs-5297167/v1

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Biostratigraphy of Late Triassic deposits in Central Iranian (Shams abad section in the south of Posht badam Block)

https://doi.org/10.21203/rs.3.rs-5297167/v1

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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

Central Iranian Microcontinent (CEIM) (Takin, 1972)) includes Lut, Tabas and Yazd blocks (Davodzadeh and Schmidt, 1982). The page of Iran, which covers the entire area of middle, northern and southern Iran, According to the geological evidence, it was a part of the Cimmerian continent (Shengur, 1990) and middlee 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 and

gradual 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 (Ig, 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. 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 (Ig, 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, Yazd blocks, etc., 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.

Therefore, 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.

Geological Settings

The study area is a small part of the Central Iran (Ig. 1), part of middle Iran and limited from the north and northwest by the Daroneh fault (Great Desert fault), and 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 separate features, and the dynamics of the subcontinent are not the same.

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) (Ig. 1).

Shams abad region in the North West of the 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 is located within the 1:250000 Rafsanjan and 1:100000 Baghin geological maps and is located approximately 30 meters northwest of Shams abad village, which is identified by the geographic specification section base: (N: 56̊ 47̍ 28̎ ; E: 30̊ 20̍ 51̎ ).

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. samples were collected from the studied section.

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, and bivalves foraminiferal microfossils in the age range of Upper Triassic to Lower Jurassic (Ig. 2). Good sorted red quartz sandstone fragments are cemented by Fe at the top of Nayband Formation, overlain by sandstone and shale sediments of Ab-e-Haji Formation.

stratigraphic units:

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 thinly 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. whose description of them are as follow Ig. 2,3,4,5,6,7 The detailed description of these layers are:

Biostratigraphic studies in this research are based on foraminifera. The Nayband Formation consists of foraminifera, which, although they are not widely distributed, have a great variety. In the present studies, a total of 15 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 as following Ig. 8, Plates 1,2.

So far, no official zoning has been provided for the deposits of the Nayband Formation in the Upper Triassic age range. But due to features such as abundance, high diversity, as well as a significant number of the first appearance and the last appearance of the foraminifera fauna in the mentioned age range, the mentioned fauna can be part of the very important paleobiotic elements in terms of biostratigraphy in the sequences of the Nayband Formation. Determining geological age is a process. The lithological changes of the studied section can be related to the sedimentation and weather conditions and as a result overshadow the distribution of fossil fauna, their accumulations and the zoning 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

The biozonation of the Triassic range has been studied based on the pre-miniferous fauna, and in many cases, the global standard biozonation that can be used in different places has not been obtained, and in the age range of the Triassic, we are mostly faced with local pre-miniferous zoning and Of course, this also overshadows compliance. ased 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, 1978a, 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 paraminiferous zonation in the Triassic, and the reason for this is based on the aforementioned studies in different parts of the world, some taxonomic issues and flaws, poor calibration of the time range of the taxa used in zoning, and strict facies control. This is the distribution of foraminiferal taxa during the Triassic, and all these factors prevent the creation of a global standard zoning (Altiner et al., 2021).

Based on biostratigraphic studies, it is possible to understand the differences in different regions and identify specific fossil communities of each region. 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 out of 21 genera were identified, and their age ranges were studied and finally the age was determined based on this. The foraminifera of the Naiband formation in the studied section of Shahdad have a low abundance but at the same time a significant diversity. Families like: Permodiscidae, Turrispirilinidae, Ammodiscidae, Frondicularidae have the highest frequency in the sections studied in this research, and the most important foraminifers identified are:

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 range of expansion of these foraminifera is also shown in Fig. 8. As mentioned, no precise zoning has been done for these taxa and the sequence biozones studied are local and can be traced 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, whose description is as follows (Ig. 8 and Plates 1, 2):

1. (Interval zone A) Rectoglandulina tenuis Biozone: This biozone is between two horizons of the appearance of Rectoglandulina tenuis in the lower zone and Permodiscus minutus at the top of the zone. 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.

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,

2. (Interval zone B) : Triassina hantkeni Biozone: This biozone is between two horizons of the appearance of Triassina hantkeni In the lower zone and Tetrataxis nana at the top of the zone. The presence of these species in the above interstitial zone indicates the Norian-Late Norian age. Other examples of this biozone include the following: Angulodiscus commonis, Nodosaria samatrensis, Permodiscus minutus. This zone 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 zone 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 minima, 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 Above, 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 parapriscus,

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 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.

The biostratigraphic study of the Naiband formation in the Shams abad section, located in the south of the Posht Badam block, shows that the existing animals (algae, corals, bivalves, sponges, cephalopods, gastropods, blemenites and foraminifera) are more than the types found in They are found in shallow marine environments and light-influenced areas, and their distribution has varied depending on changes in water circulation, salinity, and oxygen levels. As a result of biozone studies in this area, 21 species out of 15 genera of benthic foraminifera have been identified. Based on this, the number of 5 intermediate biozones (Rectoglandulina tenuis, Triassina hantkeni, Ophtalmidum exigum, Angulodiscus communis, Planiinvoluta regularis Interval Zone) and 3 overlapping or collision zones (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 is suggested to be 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 zoning, the basin of these deposits is similar to 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 land.

Author Contribution

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Plate 1 and 2 are available in the Supplementary Files section.

No competing interests reported.

Plate1.png
Plate 1 - a/ Ophtalmidium exiguum, in examples no. 5,8, 9, 18 Axial section in ig. 3 b/ Duostomina alta, 16,18 Transvers section c/ Planiinvoluta regularis, 6, 9, 15 Longitudinal section d,t/ Lenticulina sabquadrata, 2, 10, 17, 18 Axial and Tangential section e/ Nodosaria sumatrensis, 9,11,18 and f/ Nodosaria nitidana, and r/ Nodosaria shablensis, 16,17, 18 Longitudinal section h/ Rectoglandulina tenuis, 1,7 Longitudinal section g/ Glomospira sinensis., 18 Axial section m/ Permodiscus planidiscoides, 4,6 Axial section j/ Triassina hantkeni, 2,10 Transvers section s/ Urnulinella andrusovi 6,7 Axial section in ig. 3 k/ Tetrataxis nana, 5,18 Axial section m/ Permodiscus planidiscoides, 4,6 Axial section l/ Turrispirillina minima, 6,9,10,18 Axial section i,n,o/ Angulodiscus communis, 6,7 Axial section p/ Trochammina almtalensis, 18 Axial section q/ Involutina liassica, 9,10 Axial section
Plate2.png
Plate 2 - a,t,q / Duostomina alta, Transvers section in examples no. 16,18 in ig. 3 c/ Turrispirillina minima, 6,9,10,18 Axial section d/ Nodosaria dipartitan, and s,r/ Nodosaria nitidana, Longitudinal section e,w,x/ Tetrataxis nana, 5,18 Longitudinal section f/ Angulodiscus communis Axial section 6,7 g,u/ Rectoglandulina tenuis, 6,7 Longitudinal section k,h/ Triassina hantkeni, Transvers section p/ Algae debries (Acicularia sp.), Longitudinal section b,l/ Permodiscus minutus, 1,10,17,18 Axial section m/ Involutina liassica, Axial section 9,10 i/ Glomospirella facilis, 18 Axial section v/ Lenticulina sabquadrata, 2,10,17,18 in ig. 3 o/ Double valved bivalve, Axial section

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Biostratigraphy of Late Triassic deposits in Central Iranian (Shams abad section in the south of Posht badam Block)

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Abstract

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1. Introduction

2. Geological settings

3. Material and Methods

4. Discussion

5. Description of Shahdad cutting

6. Biostratigraphy

7. Conclusion

Declarations

Author Contribution

References

Plate 1 and 2

Additional Declarations

Supplementary Files

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Version 1