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Geological events from Precambrian to Quaternary have played a very important role in producing magmatic rocks in Iran. However, magmatic rocks with the ages of Precambrian, early Cambrian and specially Tertiary are much more frequent (Aghanabati, 2004). In contrast, magmatism and plutonism in Iran with Paleozoic age considered to be very rare. Volcanic rocks with the age of Ordovician-Silurian have been reported from some restricted areas of Iran such as Soltan Meydan near Shahroud (Derakhshi and Ghasemi, 2015) and Abyaneh near Kashan (Ayati et al., 2011). Volcanic and volcanoclastic rocks from the North of Neyshabour extend with a linear trend from Garineh to Bojan. In the lack of geochronological data and on the basis of stratigraphical evidence, the age of Ordovician-Silurian has been suggested for these rocks. A detailed study on petrology and geochemistry of north Neyshabour volcanic and volcanoclastic rocks can help us reconstruct the evolution of Iran bed rock during the early Paleozoic Era. The aim of this study includes petrology and major and trace element geochemistry to present critical keys to obtain some knowledge about tectono-magmatic situation of Iran during the early Paleozoic Era, especially in the Binaloud structural zone. 

This study was carried out in two parts including field and laboratory works. Sampling and structural studies were carried out during field work. The petrographic studies were performed on 45thin and polished thin sections. Geological map for the study area was also prepared. Whole-rock chemical analysis of 7 samples for major, minor, trace and rare earth elements were performed at the ACME Laboratory in Canada, by using the 4AB1 method using ICP-MS and the major oxides of six basalt samples were analyzed by X-ray fluorescence (XRF) at the Zarazma Laboratory.

The study area is located in the Northeast of Iran 15 Km NE of Neyshabour city and 7 Km NE of Bojan village. The Bojan area consists of Paleozoic sedimentary rocks (Limestone, sandstone, Dolomite) and volcanic-volcanoclastic rocks (basalts, andesit-basalts, andesite, trachyte, agglomerate and tuff). Petroghraphic studies showed that major minerals in Bojan basalts are plagioclase, pyroxene and olivine and secondary and accessory minerals are apatite, ilmenite, magnetite, chlorite, calcite and epidote. The texture of the Basalts is porphyritic, glomeroporphyric and trachytic.Based on geochemical data, the TAS diagram shows that the Basalts fall within the fields of tephrite to trachyte and belong to alkaline series with sodic nature. MgO# is varied from 20.13 to 38.62 which can be interpreted on the basis of crystal differentiation in magma chamber. The low value of compatible elements such as nickel and descending trend of MgO versus SiO2 can clearly be explained in terms of olivine fractionation. In addition, the nearly constant ratios of incompatible elements such as Nb/Zr, Ce/Zr, La/Zr, and Rb/Zr in rocks with different SiO2 content can reveal the importance of primitive magma differentiation. In contrast, these ratios suggest that crustal assimilation plays no important role in changing primitive magma composition. Enrichment of LREE compared with HREE in the studied basalts can be explained by low degrees of partial melting. Chondrite-normalized REE patterns for basalts from the Bojan area show a very similar pattern with those from transitional - mildly alkalic basalts from the Eastern branch of the East African Rift. Spider diagram patterns for Bojan basalts normalized according to Thompson (1982) and Sun and Mc Donough (1989) show a clear enrichment of all trace elements compared with those from chondorite and primitive mantel. On the basis of tectonic setting discrimination diagrams the study area basalts fall in within plate alkaline domain. According to petrographical and geochemical data of Bojan volcanic rocks it can be concluded that magmatism in the Bojan area has been formed as a result of a cycle of within plate rifting when the Palaeo-Tethys Ocean started to open during the Ordovician-Silurian time. AcknowledgmentsThe Research Foundation of Ferdowsi university of Mashhad, Iran, supported this study (Project 3/50860, 08/09/ 2019). We thank the university authorities for funding. The authors also would like to thank Professor Gültekin Topuz at the Eurasian Institute of Earth Sciences, Istanbul Technical University (Turkey) for his kind support and valuable comments.

Abstract
The thick Jurassic fluvial coarse-grained sediments rest non-conformably on older metamorphic rocks to the northwest of Mashhad. Two sections, 300 and 400 m thick, were measured and studied through the Jurassic deposits.  In this unit, three facies assemblages, conglomerate, sandstone and shale, have been identified. They comprise eight lithofacies (Gcm, Gmg, Gmm, Sm, Sh, Sp, Fl, and Fm) and four architectural elements (Channel-fill element (CH), Sediment gravity flows (SG), Downstream–accretion element (DA), and Overbank fines (FF)). The orientation of the gravel particles indicates that the direction of the paleo-flow was from northeast to southwest. The presence of an erosive base, lens-shaped sediment bodies, and fining-upward sequences suggests a gravelly braided-river system that  deposited in a half-graben. Based on the results of petrological studies, subarkose, arkose, lithic arkose, sublitharenite, and litharenite are the main identified sandstone petrofacies. Also, based on the components of the sandstones, plutonic and metamorphic rocks have been identified as the source of sediments deposited in a humid climatic condition. In addition, the grain types suggest recycled orogen (RO), craton interior (CI), dissected arc (DA), and transitional continental (TC) tectonic settings of the study area during deposition.
Keywords: Conglomerate, Braided river, Paleotethys, Jurassic, Binalud, Iran
 
 
The Binalud Mountains form one of the most characteristic geological zones in northeastern Iran. Stöcklin (1968), Eftekhar-Nezhad and Behroozi (1991), and Alavi (1992) considered the Binalud Mountains as the continuation of the Alborz Mountains, but Nabavi (1976) interpreted them as an incremental unit between the Alborz and Central Iran based on the similarity of the Palaeozoic succession with that of Central Iran, and the similarity of the Jurassic and Cretaceous strata and of its folding style with the Alborz mountains. The Binalud Mountains consist mainly of sedimentary, igneous, and metamorphic rocks, among which Jurassic sediments have been deposited in many areas, resting unconformably on Palaeozoic and/or Triassic sedimentary and metamorphic rocks. According to the position of the strata and sparse biostratigraphic data, an Early to early-Middle Jurassic age is suggested for the study deposits (Wilmsen et al., 2009a). The purpose of the present study is to figure out the identification of lithofacies and interpretation of their depositional environments. In addition, the source rocks (possibly hidden or eroded) of the Jurassic siliciclastic rocks (NW of Mashhad), and the tectonic setting of the Binalud Mountains during deposition of this formation are evaluated based on petrographic analysis.
 
Material & Two sections (400 and 300 m thick) to the northwest of Mashhad were measured and sampled. In total, 200 samples of sandstone and conglomerate were collected. Twenty-three samples of sandstones and 20 conglomerates were selected for thin section preparation. Petrographic modal analyses were made using a Nikon Eclipse E400 polarizing microscope, with 500 point counts using the Gazzi-Dickinson method at the Islamic Azad University of Mashhad, Iran. Sandstones were classified following Folk (1980), and coarse-grained sediments were classified based on the Pettijohn classification (Pettijohn, 1975). A facies code modified from Miall’s (1996) classification was utilized, with G for conglomerate facies, S for sandstone facies, and M for mudstone facies. To measure paleocurrents, 695 imbricated clasts from conglomerate were measured in two sections and plotted on a rose diagram.
 
Discussion of Results & The Jurassic deposits in the study area are all siliciclastic and range in grain size from clay to pebbles. Based on field and laboratory studies, three facies assemblages, conglomerate (Gcm, Gmg, Gmm), sandstone (Sm, Sh, Sp), and shale (Fl, Fm) have been identified. Architectural elements are defined as CH, SG, DA, and FF. The paleoflow direction is consistent with the palaeoreconstructed position of the Jurassic deposits and indicates that sediment was transported from northeast to southwest.
The lack of any marine fossils and the abundance of plant fossils in the finer-grained parts clearly point to a non-marine setting. The conglomerates and pebbly sandstones can be interpreted as the fills of braided river channels in an alluvial fan system (Wilmsen et al. 2009a; Poursoltani et al. 2015, Poursoltani and Fursich 2020). Medium to coarse-grained sandstones with planar lamination and occasional trough cross-stratification can be interpreted as part of fluvial channel fills deposited during times of waning flow velocity. Fine to very fine-grained sandstones, some with plant fragments, interbedded with siltstones and mudstones represent overbank sediments. The mudstones and shales are floodplain deposits.
Petrographically, the sandstones are fine to medium-grained and grain-supported, with some coarse-grained and well-rounded components. Based on Folk’s classification (1980), the sandstones are predominantly subarkose, arkose, lithic arkose, sublitharenite, and litharenite. Based on the petrographic analysis of the Jurassic sandstones, plotted on the diagrams of Dickinson et al. (1983) and Yerino and Maynard (1984), craton interior, recycled orogen, quartzose recycled, mixed zone, and transitional continental are the main tectonic settings of the studied sediments. Basu’s diagram (Basu et al., 1985, with Qp, Qm u, Qm, nu) indicates that metamorphic rocks were the main source area of the deposits. In the Q–F–R ternary diagram of Suttner et al. (1981), the Jurassic sandstones plot in the field for plutonic and metamorphic source areas under humid climate conditions.
According to previous studies (Wilmsen et al., 2009a; Sheikholeslami and Kouhpeyma 2012) and the result of this study, the non-marine Jurassic succession was possibly related to the early Middle Jurassic Mid-Cimmerian Tectonic Event. Thus, we suggest that the Jurassic strata of the Binalud Mountains were deposited in a half-graben. This graben formed within the Cimmerian mountain belt and developed during a late phase of the Early Cimmerian Orogenic Event

The Binalud Mountains in the northeast of Iran is a limited structural unit between the central Iran, Kopet-Dagh, and Alborz Mountains, mainly considered as a southeastern extension of Alborz Mountains (Lammerer et al., 1983; Eftekhar-Nezhad & Behroozi, 1991; Alavi, 1992; Seyed-Emami & Schairer, 2011). Jurassic successions, which have very well extended outcrops in the eastern Alborz and Binalud Mountains, were the main topic of the publications by Seyed-Emami & Schairer (2010), Wilmsen et al. (2009a,b), Raoufian et al. (2011, 2014), Seyed-Emami and Raoufian (2017), Seyed-Emami et al. (2018). Dalichai Formation in the eastern Alborz and Binalud Mountains comprises a thickness of marl and marly limestone, with an abundance of ammonite fauna which is the most important characteristic of the formation in the Binalud Mountains. This fauna in the Alborz and Binalud has long been considered in different papers (e.g., Shafeizad et al., 2005; Seyed-Emami et al., 2008, 2013, 2015, 2018; Raoufian et al., 2011, 2014). In this research, an outcrop of Dalichai Formation in the Bāghi stratigraphic section, northwest of Esfarayen city, was lithostratigraphycally and biostratigraphically studied.

The base of the measured stratigraphic section is located in 37°11′45.34″ and 57°16′21.89″, 29 km northwest of Esfarayen city (Esfarayen to Jajarm route). After field studies, reviews of lithofacies in the field, and drawing the log, 540 in situ ammonite specimens were obtained from the section. They are kept in the Museum of the Geology Department at the Ferdowsi University of Mashhad. The biometric details of ammonite specimens, including the dimensions of the specimens, size, depth, and diameter of the umbilical area, the number, arrangement, and shape of ribs, marginal keels, nodes, suture lines, and apertural shape, have been studied. The studied ammonitic fauna are typically Northwest Tethyan and belongs to the Submediterranean Province with episodic Mediterranean and Subboreal affinities (Seyed-Emami et al., 2013). It reflects the relationship between these regions with other parts of the Paleotethys sidelines during the Jurassic time.

In the Baghi section, the Dalichai Formation unconformably overlies the siliciclastic Shemshak Formation and gradationally underlies the cliff-forming carbonate rocks of Lar Formation. The Dalichai Formation, with a thickness of 655 meters, is divided into ten separate informal members and is mainly composed of marls, limestone, and marly limestone. One of the most important features of the Dalichai Formation in this section is the abundance of ammonite fauna, especially in the lower half of the section. Due to the specific color, lithology, and abundance of ammonite fauna, the second member is a key member.Paleontological studies in this research is led to the determination of 96 species, 26 subgenera, 39 genera, 20 subfamilies, 14 families, and 6 superfamilies belonging to 3 suborders of Ammonitida. According to the mentioned assemblage, 17 standard biozones are recognized, consisting of Grantiana, Parkinsoni, Zigzag, Retrocostatum, Bullatus, Gracilis, Anceps, Coronatum, Athleta, Lamberti, Transversarium, Bifurcatus, Bimammatum, Planula, Platynota, Hypselocyclum, and Acanthicum. These biozones show the age of late Bajocian – late Kimmeridgian for the Dalichai Formation. The studied ammonitic assemblages are closely related to the other Middle-Late Jurassic fauna from Iran and further peri-Mediterranean regions, which correlates with the Sub-Mediterranean province.

The Binaloud Mountains, with an almost eastern-western trend, is extended from the Jajarm area in the Northern Khorasan to the Torbat-e-Jam region. In the Binalud zone, Jurassic succession in many places covered Paleozoic rocks and metamorphic assemblages, known as Mashhad Phyllite. Chaman-Bid Formation is one of the most famous Jurassic deposits in the northeastern. The studied sequence in the Ghroneh section is located at 43 kilometers north of Neyshabur and northeast of Ghroneh village (580 45' 36'', 360 45' 05''), respectively contains siliciclastic rocks of Kashafrud Formation, shale, marl, limestone, and sandstone beds of Chaman-Bid Formation, and thick to massif limestones of the Mozduran Formation. Most paleontological studies on the Chaman-Bid Formation are done based on ammonites (Majidifard, 2003, 2008; Raoufian et al., 2011, 2014; Seyed- Emami et al., 2013, 2018), palynomorphs (Mafi et al., 2014a,b), and more recently nannofossils by Amani et al. (2016). Based on calcareous nannofossils, the Early Bajocian–Early Berriasian age was suggested for the mentioned deposits in the Ghroneh section. In the present study, for the first time, ostracods of the Chaman-Bid Formation have been investigated. The present study introduces the Chaman-Bid Formation ostracods and compares this fauna within the calcareous nannofossils biozones.

  The thickness of the Chaman-Bid Formation in the studied section is 715 meters and consists of shale, marl, and limestone, interbedded with some sandstone beds. Sixty-four samples of the Chaman-Bid Formation with intervals of 10 to 15 meters were collected. 300 grams of each sample were soaked in water and hydrogen peroxide for 24 hours and washed in 30 and 60 mesh sieves. The residue was dried, and all ostracods in each sample were separated. The ostracods were studied with a Zeiss ZH55 microscope at 40x magnification and photographed in scanning electron microscopy (SEM) at the central laboratory of the Ferdowsi University of Mashhad.

Ostracoda is one of the most valuable crustaceans in paleontological and paleoecological studies. The remains of these small and microscopic crustaceans are widely distributed through Phanerozoic, and individuals belonging to this subgroup are characterized by their particular morphological and physical characteristics (Van Morkhoven, 1963). In the present study, 45 genera and 59 species of Ostracoda have been identified in the Chaman-Bid Formation in the studied section. Previous studies of Ostracoda have been compared with ammonite zones. The current study is important since there are no reports on Iran's Jurassic ostracods. Therefore, introducing ostracods and determining their age range is a significant objective of this study; however, their preservation is relatively poor. The study of the Chaman-Bid Formation ostracods in the Ghroneh section led to identifying of 59 species belonging to 45 genera. For relative age dating in the present study, calcareous nannofossils have been used and identified ostracods correlated with them. These assemblages have been compared with 12 previously reported nannofossil zones from the Ghroneh section. Nannofossil zones (Amani et al., 2016) belong to NJ9 to Early CC1 and confirm the age of Early Bajocian to Berriasian for the discussed ostracod assemblages.

The Kopeh Dagh and Binalud-Alla Dagh mountains are important structural elements located in the northeastern boundary of Arabia-Eurasia collision zone. Due to existence of large cities with a long history of civilization, there is a relatively rich body of data on historical seismicity in this area. Nonetheless, little adequate instrumental seismic data were available prior to this study. In this paper, we utilized the temporary China-Iran local seismic network data deployed in the area for 13 months. Based on this data, we determined 37 focal solutions through first motion polarity approach suggesting a combination of strike-slip, reverse and normal mechanisms. There is a significant concentration of epicenters and focal mechanisms around the eastern Alborz - Kopeh Dagh boundary along the Atrak River. The southern and western boundaries of the Binalud Mountains also show relatively high seismic activities. The Local magnitude (ML) of the events ranges from 3.5 to 4.9 with depths of up to 20 km, mostly concentrated at ~10 km. The principal stress axes and slip vectors obtained from the focal mechanisms agree well with kinematic state of main faults and tectonic regime of the area, confirming the seismogenic nature of these faults. In addition, they are consistent with right-lateral component of slip along thrust faults in eastern Kopeh Dagh and Binalud and both laft- and right-lateral motions in the central Kopeh Dagh.

Continuation of the compressional regime within the convergence zone between the Central Iran and Turan rigid blocks caused thrusting of old rock complexes over the recent sediments. As a result of multiple thrusts and folds, the area uplifted at the same time and the Binalud range have been shortened. This study attempts to evaluate the amount of shortening of the Binalud mountains by reconstruction of a balanced cross-section. Field data from the Dulat-Abad-Neyshbur transect, study of the geological units and décollements along the section, and the Move® software environment are used as the basis for this research. Based on these information, four tests were carried out for balancing the cross section in question. The first test, which used the arc and polygon method for the horizons and a listric fault without floor thrust, failed to display the deformed section. In the second test the section was drawn, however the deformed structure did not balance the section in the process of unfolding the fault bend folds. In the third and fourth tests, we used the kink method to restore the deformed state to an undeformed section. For the third test, deformation was proceeded from the hinterland, and in the process of restoration, a shortening of about 65% was revealed. The fourth test was proceeded from the foreland, and taking into account both the foreland uplifts and shortening, the amount of shortening of Binalud range was estimated to about 26%. The final structural model defined a thin-skinned fold and thrust belt which included fault-bend-folds with out-of-sequence and in sequence duplexes. Major décollement horizons defined in the region include: 1) shale horizons within the Silurian-Devonian rock units, 2) medium-bedded dolomite and limestone layers within the Bahram Formation, and 3) evaporitic layers in the Eocene sediments.

This study was conducted to determine the deformation pattern of the Mashhad metamorphic rocks which results from the convergence between Turan and Central Iran plates and closure of Paleotethys Ocean during Early Cimmerian event. The results of 2D and 3D strain analysis show that the maximum deformation is concentrated in the central part of the study area and most strain shape parameters (K) obtained from oriented samples are located within the flattening part of the Flinn diagram. Strain intensity parameter in most cases is less than 0.5 and a maximum strain occurred in the central part which is reduced towards the margins. This is the most characteristic of the typical shear zones in which, the maximum strain is concentrated on the central part. Calculated vorticity numbers is ranged between 0.2 to 1 indicating the presence of both pure shear and simple shear during a transpressional regional deformation.

In this research, Calcareous Nannofossils of the Chamanbid Formation in Ghoroneh section have been studied. The Ghoroneh stratigraphic section with 750 meters thickness is located at the Binalud Mountains, about 43 kilometers far in northwestward direction from Neyshabour city. In this study, 64 samples from Chamanbid Formation have been studied. Samples were prepared following a standard smear slide method (Bown, 1999). Calcareous nannofossils nomenclature follows the taxonomic schemes of Perch-Nielson (1985). In general, 27 genera and 49 species of the calcareous nannofossils have been recognized in this section. Calcareous nannofossils recorded in the Mesozoic strata are believed to be an appropriate means for biostratigraphic studies. Abbreviations used in this study are the FO (first occurrence) and the LO (last occurrences). Based on the zone maker of index taxa and their accociated assemblages, biozones NJ9-NJ18 from biozonation scheme of Bown et al. (1988) with the age of Early Bajocian to Jurassic-Cretaceous boundary and CC1 zone from Sissingh (1977) belongs to Early Berriasian, have been suggested for the studied sequence and the biozones are as follows:
Watznaueria britannica Zone: The first nannofossil unit recorded in this study is the NJ9 zone.This bio zone is recorded from the FO Watznaueria britannica to the FO of Stephanolithion speciosum. The age of this zone is Lower Bajocian.

Stephanolithion speciosum Zone: The second nannofossil unit recorded in this study is the NJ10 zone. This biozone is recorded from the FO Stephanolithion speciosum to the FO of Pseudoconus enigma. The age of this zone is Lower Bajocian to Upper Bajocian.

Pseudoconus enigma Zone (NJ11(: This zone spans the interval from the FO of Pseudoconus enigma to the FO of Ansulasphaera helvetica. The age of this zone is Upper Bajocian to Upper Bathonian

Ansulasphaera helvetica Zone )NJ12(: This zone spans the interval from the FO of Ansulasphaera helvetica to the FO of Stephanolithion bigotii bigotii. The age of this zone is Upper Bathonian to Callovian.

Stephanolithion bigotii bigotii Zone )NJ13(: This zone spans the interval from the FO of Stephanolithion bigotii bigotii to the FO of Stephanolithion bigotii maximum. The age of this zone is Callovian.

Stephanolithion bigotii maximum Zone: The NJ14 zone spans the interval from the FO of Stephanolithion bigotii maximum to the LO of Stephanolithion bigotii maximum. The age of this zone is Callovian to Lower Oxfordian.

Cyclagelosphaera margerelii Zone )NJ15(: This zone spans the interval from the LO of Stephanolithion bigotii maximum to the FO of Stephanolithion brevispinus. The age of this zone is Lower Oxfordian  to Upper Kimmeridgian.

Stephanolithion brevispinus Zone (Nj16): This zone spans the interval from the FO of Stephanolithion brevispinus to the FO of Stephanolithion atmetos. The age of this zone is Upper Kimmeridgian to Lower Volgian.

Stephanolithion atmetos Zone (NJ17): This zone spans the interval from the FO of Stephanolithion atmetos to the LO of Stephanolithion atmetos. The age of this zone is Lower Volgian to Middle Volgian.

Watznaueria fossacincta Zone: The NJ18 zone spans the interval from the LO of Stephanolithion atmetos  to ?. The age of this zone is Middle Volgian to Jurassic/Cretaceous boundary. The detail study of Chamanbid Formation at the Binalud Mountains, based on calcareous nannofossils, enables the subdivision of the studied deposits into biozones NJ9-NJ18 from biozonation scheme of Bown et al. (1988) with the age of Early Bajocian to Jurassic-Cretaceous boundary and CC1 zone from Sissingh (1977) belongs to early Berriasian, have been suggested for the studied sequence.

It is very important to use geomorphometric indices to detect active tectonics. The parameters related to the drainage network are the angle of connection of the rivers. And quantitative assessment can help to identify the active tectonics, earth science researchers. Kopet Dagh -Hezarmasjed Geological Unit and Aladagh - Binalood is one of the most active geological units in Iran. In this research four basins were selected to evaluate the role of tectonics in the cross-flow angle of the rivers.Baghrood and Bojan Basin in Aladagh-Binalood Zone and Zavin and Sharrood Basins in Kopet Dagh -Hezarmasjed Construction Zone .In this way, were used cross-flow angle (CA), branching index (R), basin asymmetric percentage index (PAF) and mountain front elevation index (Smf).Also, cross-flow angle calculation showed that the highest amount in Zavin watershed is 73/67 degrees and the lowest amount in Baghrood Basin is 59.5 degrees.Which indicates changes in the flow paths of the streams, such as the capture of the river and, consequently, tectonic movements in the slope Khor anticline.Also, the calculated values of (R) (Smf) and (PAF) indicate that most tectonic species of Kopet Dagh basins are compared to the Binalod mountain basins.

The siliciclastic Padeha Strata (Middle Devonian), in the Binalud, 108 metres thick, in the Bujhan area, rests unconformably on Ordovisian basalts. This strata conformably overlain by carbonate rocks of the Sibzar Formation (Middle Devonian). The one stratigraphic section was logged graphically, and 98 fresh sandstone samples were systematically collected, from which 63 thin sections were made. Petrographic modal analyses were made using a Nikon E400 Pol microscope, with 500 point counts on 63 selected samples using the Gazzi-Dickinson method to identify grain and cement types and proportions. Porosity was estimated from counts of 500 points in each of 22 thin sections prepared separately with blue epoxy. Six polished thin sections were studied to determine the composition of mineral components. The Scanning Electron Microscope (SEM) used was a LEO 1450 VP at an acceleration voltage of 30.00 kv. Luminescence characteristics of the same sandstone suite were studied using a conventional hot-cathode cathodoluminescence (HCL) microscope (model HC4-LM).
Discussion and Based on field and Laboratory studies, 3 association facies, sandstone, dolostone and shale have been identified. The sandstones are fine- to medium-grained and grain-supported, with some coarse-grained and well-rounded components. Based on angularity, sorting, and matrix content, most sandstones are mature and submature. Detrital grains are quartz, predominantly monocrystalline quartz with subordinate polycrystalline quartz, K-feldspar and plagioclase, lithic grains, and accessory minerals and micas. Lithic grains are mainly metamorphic and sedimentary. Dense-minerals include opaques, zircon and tourmaline, dispersed. The sandstones have a compositional range from quartzarenite, subarkose and little bit of arkose.
The Padeha sandstones experienced diagenetic events that included cementation, alteration, compaction and fracturing, dissolution and replacement and porosity. The predominant cement is silica and carbonate (dolomite, calcite, ankerite and siderite), iron oxide, clay minerals (kaolinite, illite and chlorite), with minor authigenic minerals such as appetite. The silica is typically non-luminescent, and mainly occurs as syntaxial overgrowths on detrital quartz grains; reddish rims of very fine-grained material that probably include clay and iron oxides mark the contacts between authigenic and detrital quartz. Silica also forms pore-filling cement in primary pores. The cements occupy inter- and intragranular spaces, form veins and fill fractures, and vary from microcrystalline to coarsely crystalline in the case of calcite. Iron oxide cement is present throughout the Padeha sandstones as an alteration product and cement. Clay minerals are less than other type of cements, but illite and kaolinite are the main clay minerals cement in Padeha sandstones. Authigenic minerals mainly fill fracturs and pores. The sandstones show variable degrees of mechanical and chemical compaction, which is particularly prominent where early cements are lacking. Grain contacts include elongate and concavo-convex, point contacts in rare cases, and sutured contacts that indicate intergranular pressure solution and deformation at a more advanced stage. Quartz and feldspar grains have been intensively fractured but the fractures have been largely healed through silica cementation, allowing the grains to maintain their integrity. This was evident using SEM and CL techniques, which show that the majority of grains contain fractures. Dissolution is prominent in the sandstones. Detrital K-feldspar, quartzand carbonate cement all show evidence of partial to complete dissolution. In feldspars, the proportion of voids is variable, with dissolution prominent along cleavages and fractures.
Based on two-dimensional estimates from thin sections, the mean porosity is 4.7%, and maximum 14.4% for 22 samples from the formation as a whole, with little apparent upward change. The bulk of the porosity is secondary. Pores formed mainly through dissolution of K-feldspar and carbonate cement, and as open fractures within grains.
Based on petrological and geochemical studies, minor diagenetic events in the eodiagenetic stage include cementation (calcite, dolomite and iron oxide) and rarely fracturing. Mesodiagenetic events were dominated by cementation (silica, dolomite, calcite, iron oxide components, clay minerals), compaction, intra-grain microfractures, alteration of unstable clasts, dissolution and replacement, pressure solution, and rarely formation of apatite. Minor telodiagenetic events include dissolution and cementation (dolomite, ankerite, siderite, iron oxide and rarely kaolinite). The bulk of the porosity is secondary, with an average of 4.7%, which is the result of dissolution and fractures

  The siliciclastic Lalun Strata (Early Cambrian), in the Binalud zone, with thickness of 70 metres in the Chenar area, rests with an fault contact on the Early Cambrian sedimentary rocks (Soltaniyeh dolomite). This strata overlain with erosional surface by Eocene conglomerates. The upper part of this strata contains sandstone that compare with upper sandstone unit of other parts (Porsoltani et al., 2014; Poursoltani and Ghotbi Ravandi, 2015). This formation is red to reddish-brown in color, and mostly purple. The one stratigraphic section was logged graphically, and 67 fresh sandstone samples were systematically collected, and 50 thin sections were made. Petrographic modal analyses were done using a Nikon Eclipse E400 Pol microscope, with 500 point counts on 20 samples. Four polished thin sections were studied to determine the composition of mineral components. The Scanning Electron Microscope (SEM) used was a LEO 1450 VP at an acceleration voltage of 30.00 kv. Based on field and laboratory studies, two facies association including sandstone and shale have been identified. The sandstones are fine- to medium-grained and grain-supported, with some coarse-grained and well-rounded components. Based on angularity, sorting, and matrix content, most sandstones are mature and submature. Detrital grains are quartz, predominantly monocrystalline quartz with subordinate polycrystalline quartz, K-feldspar and plagioclase, lithic grains, and accessory minerals and micas. Lithic grains are mainly metamorphic (quartzite) and sedimentary (sandstone and chert), with a few volcanic grains. Heavy minerals include opaques, zircon and tourmaline, scattered or present as a thin laminae. The sandstones have a compositional range from quartzarenite to subarkose and sublitharenite (Folk, 1980). The Lalun sandstones experienced diagenetic events that included compaction, fracturing and cementation. The predominant cement is silica, but some samples contain considerable proportions of carbonate, iron oxides and clays cements, with minor authigenic minerals. The silica is typically non-luminescent, and mainly occurs as syntaxial overgrowths on detrital quartz grains; reddish rims of very fine-grained material that probably include clay and iron oxides mark the contacts between authigenic and detrital quartz. Silica also forms pore-filling cement in primary pores, and large volumes of cement lie along primary and secondary fractures (McBride, 1989; Friis et al., 2010). The cements occupy inter- and intragranular spaces, form veins and fill fractures, and vary from microcrystalline to coarsely crystalline in the case of calcite. Iron oxide cement is present throughout the Lalun Formation as an alteration product and cement. Clay minerals present less than other type of cements, but illite and kaolinite are the main clay minerals cement in Lalun sandstones (Ketzer et al., 2005). Dissolution is prominent in the sandstones. Detrital K-feldspar, quartz, volcanic rock fragments, and carbonate cement all show evidence of partial to complete dissolution. In feldspars, the proportion of voids is variable, with dissolution prominent along cleavages and fractures. The sandstones show variable degrees of mechanical and chemical compaction, which is particularly prominent where early cements are lacking (Mansurbeg et al., 2008). Grain contacts include elongate and concavo-convex, point contacts in rare cases, and sutured contacts that indicate intergranular pressure solution and deformation at a more advanced stage. Quartz and feldspar grains have been intensively fractured but the fractures have been largely healed through silica cementation, allowing the grains to maintain their integrity (Milliken, 1989; Dickinson and Milliken, 1995). This was evident using SEM and CL techniques, which show that the majority of grains contain fractures. Based on petrological and geochemical studies, it is interpreted that diagenetic history of the Lalun sandstones can be related to early, deep burial and late stages (Abdel Wahab, 1998; Salem et al., 2005). Based on petrogragpic studies of upper sandstone units of the Lalun Formation, in Binalud Zone, compaction, fracturing and cementation (mainly silica) are the most important diagentic events of these sandstones. The cements occupy inter- and intragranular spaces, form veins and fill fractures, and vary from microcrystalline to coarsely crystalline. The sandstones show variable degrees of mechanical and chemical compaction, which is particularly prominent where early cements are lacking. Quartz and feldspar grains have been intensively fractured but the fractures have been largely healed through silica cementation, allowing the grains to maintain their integrity. According to diagenetic events, diagenetic history for the Lalun sandstones, in study area, is related to early, deep burial and late stages. Keywords: Diagenesis; Lalun Formation; Early Cambrian; Binalud. Reference
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In this paper, the feedback or interaction between tectonic and surface processes in the Binaloud Mountains and Neyshabour plain has been investigated. To achieve this, we have used topographic data, recorded earthquake data provided by the Geophysical Institute of Tehran University (Mashhad center) and field surveying results. Surface processes affect the propagation of tectonic thrust wedges in orogenic belts. In regions tectonic processes have led to an increase in the surface slopes due to development of mountain highs, surface processes will justify the uplifted areas by smoothing the slopes, eventually shedding off a massive load of clastic sediments into the foreland basin. Because of their huge weight and volume, these sediments prevent the forward propagation of the wedge and therefore increase the accumulation rate of stress in the orogenic wedge. Also the increase of fault-plane dips in the orogenic wedge will make the slip along the fault planes hard or even impossible. Formation of out-of-sequence faults and back-rotation of preexisting thrust faults may be considered as results of these accumulated stresses. North Neyshaboor thrust fault is a later or secondary structure and can be considered as an out-of-sequence thrust because it cuts other thrust sheets and limbs of folds. Our research shows that the high volume of Paleogene/Neogen sediments in the Neyshabour foreland basin has prevented the forwards (southwestward) propagation of the Binaloud mountain range as the orogenic wedge. Releasing of the accumulated forces has therefore led to the development of the North Neyshaboor out-of-sequence fault and back-rotation of former thrust faults.

Binalud watershed is located, South-East of Mashhad, that geologically, is a part of Binalud zone. Binalud watershed contanis three subbasins, which among them, Bazeh-Hour subbasin has been studied. Climatology, Bazeh-Hour area is arid and semi-arid, and, so, due to the various geological units, the chemical composition and the quality of the water has been changed, so, the type of water is sulfuate and chloride. Additionally, in terms of agriculture and human drinking is also acceptable. Thus sedimentology studies, along Bazeh-Hour river shows that three main factors, sudden changes of slope, entrance of minor channels and seasonal flood events, caused the sediments fabric variation, and parameters changing, such as sorting, skewness and kurtis. So, sedimentology and petrology studies show that the most sediments are very poor sorted, platykurtic and fine skewed, and basic and ultrabasic rocks are the main source of Bazeh-Hour deposits. Although, based on field studies, three facies associations are recognized, that consist four gravely facies, Gmm, Gmg, Gcm and Gci, two sandy facies, Sh and Sl, and three mud facies, Fm, Fr and Fl, and four structural elements, SG, HO, LS and FF are identified. In according to Bazeh-Hour river facies associations and structural elements, three depositional models, gravely bradied rivers with gravity flows, sandy meandering river and fining grain meandering river are suggested.

The Middle Jurassic scilisiclastic doposit has a good exposure in the East of the Binaload Zone and composed of conglomerate, sandstone and high amounts of fine grained sediments. The lower and upper boundaries of section are sharp respectively with Mashhad phylite and limestone. In this study lithofacies analysis in order to interpretation depositional environment and the origin of tectonic setting of Jurassic silisiclastic deposits in Binaload Zone were investigated in Baze hoz section, soth of Mashhad. Relying on the facies characteristics and stratal geometries the silisiclastic succession are divided into 10 lithofacies in the 160 meter thick. lithofacies are classified into 4 categories including coarse grain (Gcm,Gmm,Gh,Gp), medium grain (Sh, Sr,Sm), fine grain (Fl,Fm) and biochemical (C). Based on the following evidence, the Jurassic silisiclasic sediments have been deposited in Delta river system: Sedimentary facies: coarsening upward deposit, coal deposite, Leave fossils, syneresis crack and unidirectional sedimentary structures such as ripplemark, cross bedding, lack of Bi-directional structure. Petrographic studies led to the identification 6 petrofacies conglomerate and sandstone. Plotted data on Qt, F, L diagram, indicate recycled orogene for this deposits. Also plot data on Basu and Q, F, L diagrams, respectively shows low to medium grade metamorphic and hiumid climatic condition for sandstones of Jurassic sediments for these deposits at the time of formation. According to Turan and Iran clash pages and closing the Paleo-Tethys Sea in NE Iran Jurassic sediments in the study area composed of erosion of upland areas. These results indicate a wet weather conditions.

The effects of the Mid-Cimmerian event in the Binalud Mountains can be investigated in the Mashhad Phyllite around Mashhad and in the Aghdarband Group in the Aghdarband area. In the Eastern Binalud, this event acted in prehnite-pumpellyite to lower greenschist facies and influenced the Shemshak group, which deposited as a post Early Cimmerian molasse blanket in a Rhaetian–Lias back-arc basin. The result is transformation of these sediments into the slate, phyllite and metasandstone. Tight to open folds, axial plane foliations and crenulation folds with NW-SE trending are the Mid-Cimmerian deformational structures. Due to the lower grade of metamorphism and deformation, there isn’t any important effect of this event on the rocks, which were previously deformed and metamorphosed by the Early Cimmerian event. The exhumation and erosion of deformed rocks by the Early and Mid-Cimmerian events generated the intramontane basins in the internal part of the eastern Binalud Mountains. In the Aghdarband area, this event is characterized by folding of the Sina Formation from the Aghdarband Group, which is unconformably overlain by the Kashafroud Formation.

Binaloud Mountains formed during collision of Iran and Turan plate in the Late Triassic time and caused shortening of the sedimentary cover because of Cimmerian and Alpine orogeny. The thrust sheets with different generations formed as a results of the Binalood and Alborz fold- thrust belts. Northeast of Iran that was already south coast of the divergent margin of the Paleothetys Ocean at this time، has become a marine foreland basin as a result of this colliding and bending of lithosphere. Stratigraphical column of foreland basin usually is made up of a few upward coarsening and shallowing sequences that each of them represents a step loading and removal times of the lithosphere beneath the basin. The first generation of thrust faults began with thrusting of Mashhad sheet (Paleothetys remnants) over the Shemshak Formation that is syn-orogenic with Cimmerian orogeny. As a result of erosion of mountains، large amounts of siliciclastic deposits transported to foreland basin in southern parts and the Middle Jurassic conglomerate and sandstone layers of Aghonj formation and siliciclastic beds of Ferizee are deposited. These sequences show upward coarsening and thickening with flow direction to the south. Alpine movements began during the Mid-Cretaceous time، and caused the formation of the second generation thrusts of Binalud fold-thrust belt، uplift، erosion and transport of siliciclastic material with upward coarsening and thickening (Foreland basin) of Paleogene. These sequences represent depositions in different parts of the alluvial fans with movement towards the south. Third generation thrusting related to Late Alpine movements caused regression of sea water to the south and creation of lagoon in foreland basin. Evaporate sediments at the base of Neogene clastic sequence is the result of such a process. Uplift of the foreland basin deposits due to new thrusting activity and erosion of them caused transportation of large amounts of siliciclastic sediments into the foreland basin and creating upward coarsening and thickening sequence of Neogene to the present.

The Dalichai Formation is among marine deposits in Jurrasic period that has a geographic expansion in north of Iran. In order to palynological studies in eastern part of the Binaloud Mountains an outcrop of this formation, in the bar village was selected. The thickness in bar village section is 255 meters includes dark gray shales. The study of 112 slides of 28 samples taken from this formation showed that the most of the samples contain palynomorphs specifically dinoflagellates. 53 species belonging to 27 genera of dinoflagellates were identified. According to dinoflagellates, a middle Jurassic age was determined for the Dalichai Formation in the Bar village section. Based on the study of three main groups of phytoclasts, marine palynomorphs and amorphic organic matters and result of the statistical studies of different factors, sedimentary environment of the Dalichai Formation in studied section was open marine basin with shallow and low oxygen condition.

Miocene silisiclastic sediments in Binalood zone consist of three lithofacies group including gravelly (Gmm، Gcm، Gci، Gh، Gt، Gp)، sandy (St، Sm، Sh، Sp، Ss، Sl) and muddy (Fm، Fl). Gravelly lithofacies are generally massive and mainly consist of volcanic and sedimentary lithic in different size. Sandy lithofacies are composed of litharenite and feldespathic volcanicarenite and rock fragments are almost volcanic as well as minor amounts of sedimentary and metamorphic rock fragments. Based on red color، absence of marine fossils، present of unimodal planar and trough cross bedding in a fining upward cycles، lithofacies analysis and architectural elements، these sedimentary rocks deposited in braided river and alluvial fan as well as playa. Based on geochemistry and petrographic data، parent rocks for these sediments، are probably felsic and intermediate igneous rocks with recycled orogen that originate in active continental margin.

Binalud Mountain Ranges is a thin skinned fold- thrust belt that is formed during Cimmerian (Late Triassic) and Alpine (Mezozoic- Cenozoic) orogenies as a consequent of collision between Iran and Turan plates. Structurally، this fold–thrust belt were consists of several thrust sheet and thrust faults. Thrust faults are verging S-SW and younger to the south. In order of ageing and their characteristics، thrust faults can be divided into three systems. The first (older) system consists of ductile thrust faults with antiformal stack duplex geometry. The second one includes ductile-brittle thrust faults. Thrust faults in this system cut and emplaced older thrust system and show hinterland dipping duplex geometry. The third (younger) system includes quaternary thrust faults in the south foothills of Binalud Mountain Ranges. Thrust faults in this system are brittle and are probably members of an S-vengeance leading imbricate fan. Based on forland stratigraphic models، syn-orogenic clastic assemblages in post Triassic stratigraphic column are used for determination of the age of generation and activity of thrust systems. On the basis of this study، first system is a result of Cimmerian and early Alpine orogenies، while the second one formed due to middle Alpine orogeny and third system is formed during late Alpine orogeny.