RESUMEN ABSTRACT Sedimentary Environment and Provenance Of

This is anopenaccess article undertheCCBY-NC-SAThis Universidad NacionalAutónoma de México. Peer Reviewing under the responsibility of 14,2020 Manuscript September accepted: Corrected manuscript received: August 25,2020 Manuscript received: March 16,2020 BSGM2021v73n1a140920 73 (1), A140920.http://dx.doi.org/10.18268/ Boletín de la Sociedad Geológica Mexicana, Formation, Tabas block, east-central Iran: from the Qadir member in the Nayband sandstones environment andprovenance of 2021, Sedimentary Harami, R.,Mahboubi,A., Zamaniyan, E.,Khanehbad,M.,Moussavi- How tocitethisarticle: [email protected] * Corresponding author:(M.Khanehbad) Square, Mashhad,Iran. Azadi Mashhad, ence, FerdowsiUniversity of 1 Ehsan bloque deTabas,centro-esteIrán Ambiente sedimentario yprocedenciade las areniscasdelmiembro Qadir de la FormaciónNayband, in theNaybandFormation,Tabasblock,east-centralIran Sedimentary environmentfrom Qadirmember and provenance the of sandstones license(https://creativecommons.org/licenses/by-nc-sa/4.0/) eateto Geology, Sci Faculty of Department of Zamaniyan 1 , Mohammad Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín - Khanehbad Provenance. environment,Sedimentary Triassic, Tabas Block, Keywords: Nayband Formation, Iranian Microcontinent. orogenyand Central inAlborz East coincided with the early Cimmerian Triassic, which nic activity at the end of subduction under Iran’s plate andvolca the Neotethys couldsuggest this deposit active continental margin conditions for rocks.igneous andsedimentary The the intermediate a probable source of also showed geochemicalThe diagrams was found to be rather medium to high. Alteration, the weathering rate Index of Chemical nental margin and because of re-cycling andactive conti enance of the geochemical data showed the prov to semi-humid conditions andplotting ering index (71%)indicated semi-arid tidal currents. chemical The weath of Member which isunder the impact environments were identified for Qadir front, andprodelta) andopen marine plain, proximal delta front, distal delta coastal plain,deltaic (includingdeltaic lithofacies, the and identification of regarding the field, laboratory studies, (Sr) /Sr (FI)andone coal facies. Also, lithofacies,grained includingFI,Fm,Fl facies includingSr, Sh, Sp, St, three fine- were identified as having four sandstone siliciclastic facies. siliciclastic facies The lithofacies, including carbonate and two tures, QadirMember consists of Based onfield evidence andfacies fea the deltaic and marine deposits. of environment, resulted inidentification the lithofacies andsedimentary of developed to agreat extent. Investigation Central Iran,has located inEast of Nayband Formation, Qadir Member of ABSTRACT 1,* , Reza Moussavi-Harami - - - - - /73(1)A140920/2021 1 en la identificación de los depósitos deltaicos en laidentificación de losdepósitos de la litofacies yelmedio sedimentario resultó medida. La investigación engran desarrollado ubicada eneleste del centro de Irán, seha El miembro Qadir de la FormaciónNayband, RESUMEN Procedencia. Tabas, Ambientesedimentario, Nayband, Triásico, Bloque Palabras clave: Formación microcontinente iraní centro-este. con la orogenia cimeria temprana enAlborz y el al finaldelTriásico,volcánica que coincidió Neotethys bajo la placa de Irány la actividad podrían sugerir la subducción de este depósito paracontinental activo condiciones del margen de rocas Las ígneas y sedimentarias intermedias. químicos también mostraron unafuenteprobable bastante media.lo alto. en geo Los diagramas de alteración, la tasa de meteorización resultó ser y,gen continental activo debido al índicequímico cos mostró la procedencia del reciclaje yelmar semihúmedas yeltrazado de losdatos geoquími química (71%)indicócondiciones semiáridas a de marea. Elíndicede meteorización corrientes Qadir que seencuentra bajo elimpacto. de las y ambientes marinos abiertos para elMiembro deltaico proximal, frente delta distal yprodelta) deltaica (incluida la llanura deltaica, frente litofacies, seidentificaron la llanura costera, los estudios de laboratorio yla identificación de facies de carbón. Además, con respecto al campo, fino, incluidas FI, Fm, Fl (Sr) /Sr (FI) yuna incluidas Sr, Sh, Sp, St, tres litofacies de grano siliciclásticas tenían cuatro facies de arenisca, y siliciclástico. Seidentificó que las facies de dos litofacies, incluidas facies de carbonato características de facies, Qadir Member consta y marinos. de campo y Basado enevidencia ,Asadollah Mahboubi 1 1 - - -

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation ABSTRACT Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation INTRODUCTION / GEOLOGICAL SETTING 1. Introduction 2 2 tary facies is a very facies is forgood basis tary sedimentology sedimen different areas.in cesses Investigation of environments sedimentation pro andinterpreting most important tools in identifying sedimentary the faciesisoneof sedimentary Examination of 1985). Accordingly, inaddition to petrography and for compositions (Dickinson, factors sedimentary the majorcontrolling is considered to be one of tectonic setting inson, 1985;Critelli, 1993).The and Suczek, 1979;Dickinson compositions andtheir provenance (Dickinson sandstone tectonic settings andthe relationships of sandstones isemployed to identify the analysis of Khanehbad rocks (Weltje, 2002;Weltje andVon Eynatten, 2004; rock up to the final deposition and burial history of the source initial erosion of of as interpretation andreconstructionpre-sedimentary history aswell provenance could be used to identify the tion of Zamaniyan Sabbagh Bajestani et al Ayaz‐Bozdag, 2011; Mishra and Sen, 2012; Zhang Quanren son andSuczek, 1979;Bhatia andCrook, 1986; been investigated by many researchers (Dickin siliciclasticrocks has nance, andcomposition of (Catuneanu, 2003). syn-sedimentation processes of the interpretation lithofacies greatare a helpin and identification of processesenvironments, sedimentary in thestudy cies are by controlled and formed sedimentation ronment (Aboumaria sedimentation processes envi inthe sedimentary facies associations characterize the alteration of size, texture, structures, and sedimentary while grain include that features sedimentological tifies 2010). Accordingly,(Flugel, iden faciesanalysis field studies, petrography, or geochemical analyses data including lithology environment isthe use of the sedimentary faciesandinterpret and determine the most important waysto identify 2000). One of sea-level global studies to interpret changes (Geel, / / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín lo h eaino tectonic setting, proveAlso, the relation of ., 2014; Fleming ., 2014;Fleming et al et al et al ., 2002;Tijani ., 2019),because the interpreta ., 2012a,2012b).Clastic modal et al et al et al ., 2018;Iqbal ., 2016,Fathy ., 2009).Since lithofa et al ., 2010;Ozkanand et al http://dx.doi.org/10.18268/BSGM2021v73n1a140920 ., 1983;Dick et al et al ., 2019; ., 2018; /73(1)A140920/2021 ------/73(1)A1409202021 2. GeologicalSetting ato Central Iranduring Late Triassic. part of eastern the paleogeography of reconstruction of geochemical methods. Ourresults canbe used for ies, petrography andmodalanalysisalongwith stud field the (Tabasthrough Iran Block) Central the Nayband Formation inthe east of Member of the Qadir of siliciclastic deposits provenance of environment the sedimentary and interpret and siliciclastic rocks. study This aimsto investigate the identify to tool effective an as used been have discriminant diagrams and the implementation of attention. Nowadays, the geochemical studies of the originalregion) hasalways been the center of tonic setting, source region, andpaleoweathering provenance (tec facies analyses, investigation of 1983; Aghanabati, 2006), which are from the (Bronifmanformation the have been recognized at the type section of Iran (Seyed-Emami, 2003). Five members part of distributed over a large area in central and eastern Triassic(Norian-Rhaetian) Nayband Formation is Naybandvillage; Aghanabati, Late 2006).The the NaybandMountain (the West of in southof been measuredtype sectionhas andintroduced tral Iran’sstructural zonesedimentary andthe in Cen 3000mwasdeposited of the thickness level rise, Nayband Formation (Late Triassic)with Early Cimmerian orogeny, the sea because of (Wilmsen Early Cimmerianto Middle Cimmerian orogeny between the two tectonic occurrences of formed tic rocks, causedthecoal-bearing sequences tobe coastal-continental basins, inaddition to siliciclas Late Triassicand Jurassic. time,At this theshallow Iran’san important role in forming in the geology the Middle to Late Triassic time played the end of Early Cimmerian at tectonic movementsThe of a complex (Aghanabati, structural history 2006). the CEIM witch hasexperienced and a part of Tabas Basin isan intra-continental depression Central East Iranian Microcontinent (CEIM). studyThe area is located in the central part of et al ,20a.Atrteocrec f., 2009a). After the occurrence of et al ., 1971;Kluyver et al ., - - - - the studied section (asterisk)inTabas BlockbetweenNaybandthe studied section and Kalmard-Kuhbanan C)Sequence position studiedonthe faults, Figure 1 Abshaleh (Saidi geological map of ParvadehCoalMinearea (by draw againof Korit (Moussavi-Harami and Ghaemi,2006)and Gharb-E-Shekasteh Nayband fault in the east and Kalmard-Kuhbanan structural zonesedimentary between the large Tabas Block islocated in Central Iran’sregion of the studied (Aghanabati,divisions 2006), part of Fürsich Rhaetian; Nützel Formationto Late goesback Triassic(Norian to Nayband 2005). Based on the studies, the age of andgastropodsechinoderms, (Fürsich brachiopods, sponges, subordinate elements of of rofauna, includingbivalves, corals, diverse groups Nayband Formation contains rich benthic mac e-Khan Member, and5- Qadir Member. The Member, 3-Howz-e-Sheikh Member, 4- Howz- base to the top: 1- Gelkan Member, 2- Bidestan A)Thegeneral mapofIran’s sedimentary structuralzone (adopted and changed from Motiei,1994),B) Thelocationof et al et al ., 2005).According toIran’sgeological ., 2004)geological mapswithascaleof1:100000). et al ., 2010;Cirilli Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín http://dx.doi.org/10.18268/BSGM2021v73n1a140920 et al ., 2005; et al ., - and fossiliferous limestone. includes sandstone, shale, siltstone, coal bearing lithology, it of (Figurethickness terms 1c)andin the central Parvadeh Coal 450 mof Mine has anticline of of flank southern the in Formation Tabas. Nayband Coal Mine zone inthe south of is located in the Parvadeh thisformation crops of the best out Tabas Blockandoneof vast area of outcropsFigures formation ina 1a and 1b). This Tabas Block; structural sub-blockof (subdivisions Nayband sedimentary and studied in the north of Tabasbeen measured andhas of south 80 Km locatedand 56°48’40”E)is (33° 00’21”N about band Formation inParvadeh Coal Mine section the Nay fault in the Qadir west.Member of The /73(1)A140920/2021 / 73(1)A140920/2021 3 3 - -

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation GEOLOGICAL SETTING Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation GEOLOGICAL SETTING / MATERIALS AND METHODS / RESULTS 3. MaterialsandMethods Figure 2 4 4 gated for petrography. To analyze the sedimentary 3). After sampling, 86thinsectionswere investi Tabas (Figures 2and Mine sectioninthe south of been measured and studied in Parvadeh Coal has thickness Qadir Member with 450mof The used methods in sandstone classification with classification sandstone in methods used and Folk (1980),andwidely as the most common Pettijohn of classifications the using thesandstoneshave alsobeen determined of names The field. the in limestones label to used Also,condition. Grabau’s classification was (1904) thepaleo-oxygenation andunderstand determine Dill microfacies, standard determine to classification (2010) Flugel and facies, calcareous for sification petrofacies, Dunham(1962) was employed clas identify and label to used was classification (1980) 2006) were used to identify lithofacies, while Folk’s Miall(2000, faciescodesbyThe the methodof completely. deposits sedimentary cal changes of lithological features as well as lateral and verti structures, sample sedimentary geometrical and Qadir Member, ithasbeen attempted to facies of / / General landscape intheParvadehCoal Minearea,southof of QadirMember Tabas. section Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín et al . (1988) and Jones andManning(1994) for http://dx.doi.org/10.18268/BSGM2021v73n1a140920 et al ., 1987, /73(1)A140920/2021 - - - /73(1)A1409202021 4.1. LITHOSTRATIGRAPHY 4. Results X-ray spectrometer). PW1480 (Philips device fluorescence X-ray the byEast Amethyst analytical geological lab, using elements. sandstonesampleswere The analyzed majorandtrace chemicalto determine analysis (less than5percent), were selected forgeo XRF carbonate weathering and theleast amount of well-sorted sandstones, having the least rate of of Also, based on the thin sectionstudies, 10samples and Suczek,Dickinson 1985). 1979;Dickinson, andSuczek,method (Ingersoll 1979; Dickinson least 300 points per sample (Tables 1and 2) by the sandstone withat medium-grained 15 samplesof on data and detrital modes hasbeen performed particular importance, andthe modal analysis stone andcoallayers (Figures 2and3). fossiliferous lime sediments withintercalation of shaleandsandstone of mainly consists section is the Nayband Formation in this Qadir Member of - - geochemical analysis (arrowsign). Figure 3 Thelithostratigraphic column oftheQadirMember of theNayband Formation, representing thelocationofsamples for Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín http://dx.doi.org/10.18268/BSGM2021v73n1a140920 /73(1)A140920/2021 / 73(1)A140920/2021 5 5

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS 4.1.1. THEUNIT1 badland and2. steep slopewallsof unit (Sr and Sp)and horizontal lamination(Sh),F)convolute bedding, G)shale and sandstone alternation intheunit2,H)general viewand Figure 4 6 6 into two. to lithological features, Qadir divided Member is ate - Early Jurassic)(Figures 2and3).According tion (white sandstones andred-brown conglomer the Ab-Haji Forma sediments of coarse-grained with isdisconformable and the upper boundary Its lowercoveredis boundary section this in tary structures tary such ripple symmetrical markas to etc. along with abundant plant fossilsand sedimen Rhizocorallium trace fossilssuch as a wide range of thisunit is the presence of prominent feature of most theunit1.The coalat the topof layer of the unit 1with the unit 2 corresponds to the last numeroushematite concretions. contactof The unit 1 compared to the unit 2 isthe presence of the the unit 2, and the most important feature of and marlsthe unit1arein more expanded than bivalve, coral,etc.) and coal(Figure shale 2).The fossiliferous limestone (brachiopod, with layers of nating sandstone shale sedimentsandlight green alter of consists unit with 315mthickness This / / A-B)symmetricaltoasymmetrical ripple mark,C)herringbone, D)trough crossbedding and lamination,E)ripple cross bedding Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín , Planolites , Skolithos , Scolicia http://dx.doi.org/10.18268/BSGM2021v73n1a140920 Thalassinoides , Arenicolites /73(1)A140920/2021 - - - - /73(1)A1409202021 , , 4.1.2. THEUNIT2 4.2. FACIES ANALYSIS the form of badland and steep slopewallsinthe badlandandsteep of the form wellas feweras fossiltraces. often in unitis The coallayers andfossiliferous limestones absence of thisunit compared to unit 1 are the features of sandstone (Figure most distinctivegreen 4g). The shaleand alternating of composed lar tounit1,is and, simi 185meters of a thickness unit has This analysis. environmentdetail in the facies andsedimentary 4a, 4b, 4c,4d,4e and 4f) in and willbe discussed ripple cross-bedding, convolute bedding (Figure cross-bedding, lamination, trough cross-bedding, asymmetrical ripple mark, herringbone, planar facies. Siliciclastic facies were identified, consisting siliciclasticandcarbonate Member is composedof lithofacies, Qadir of 2006) alongwiththe analysis (2000, Miall of classifications lithofacies modified Based on the field studies and evidence as well as the field (Figure 4h). - Figure 5 4.2.1. SANDSTONE FACIES ASSOCIATION (Q: totalquartz; F: feldspar; R:rockfragment),C)litharenite, D)sublitharenite. characteristics. similarities in texture and lithological uniform by structures sedimentary and show relatively and St were identified.These facies were classified Sr, Sh,Sp,abundance andfour facies of sandstone relatively high lithofacies wereMedium grain of maturity (Figures 5a,5b, 5cand5d). litharenite to sublithareniteof petrofacies interms mature sub tomature and were alsoat arangeof and calcirudite (Table 1). Sandstone thinsections facies andcarbonate calcirudite facies including Fl of along withacoal-based (C) /(Fl)Sr and Fm,(Sr)Fl comprising facies grain fine- three and St four sandstonefaciesincludingSr, Sh,Sp and of A-B)Mineralogical classification ofthesandstones Qadir Member from inthePettijohn Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín http://dx.doi.org/10.18268/BSGM2021v73n1a140920 SANDSTONE FACIES (SR) 4.2.1.1. RIPPLEDLAMINATION ANDLAYERED formed under different flow regime conditions regime flow different under formed coastal environments are known asindicators of ripple marks ridges (Figure types of 6a).These metricripple marks withstraight andsinusoidal symmetrical andasym of various forms sence of this lithofacies isthe pre main characteristic of sublitharenite petrofacies. The and composed of good roundness andsorting, being submature grains, andthe sandstones show moderate to medium from to variesmainly fine sandstones the shows arelatively highabundance. size The of QadirMember and and well-known facies of identified the of one is facies sandstone Rippled (Longhitano /73(1)A140920/2021 et al / 73(1)A140920/2021 ., 2012).Also, direct-ridged ripple et al ., 1987 and1987 Folk (1980)diagrams ., 7 7 - -

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS Table 1. Summary of characteristics andTable 1.Summaryofcharacteristics interpretation ofsedimentarylithofacies(lithofaciescodesmodified after Miall;2000,2006). 8 8 Carbonate grained sandstone andfine Interbedded Coal sand, silt, clay) Fine Sandstone

Laminated Trough cross Laminated or wavy bedded Planar cross Fossiliferous Horizontally bedded or laminated limestone / - / Massive

Rippled Lithofacies bedded bedded rippled grained (fine Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Massive Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín

and

- -

- Fl Sr(Fl) Code Fm Sp Sh Sr Fl St ) C - / Sr)

3 Medium fossiliferouslimestone, 5 grouped, set thickness generally generally, 1 Description; bedding features Oftenclay and very silt size: 5 Coal andcoaly mud: 5 Rippled sandinterbeds inmud - solitaryor grouped, 2 40 cm, planarand herringbone Oftensilt and very fine sand sometimes withtracefossils with trace fossils and planet Medium sand: set thickness 1 Medium sand: solitary, set Mediumsand: solitaryor - layers, with plant fossil size: 1 200 cm, Coarse http://dx.doi.org/10.18268/BSGM2021v73n1a140920 thickness generally thickness generally planet fossildebris - cross fine sand: set thicknesssand: setfine - 1500 cm - 2 cm2 layers, 3 - 200 cm; sometimes200 fossils layers - medium size: sometimes with 10 cm - bedding

-

- 20 cm, 250 cm set /73(1)A140920/2021 /73(1)A1409202021 -

25 cm

-

Siltstone Siltstone, litharenite Bioclast grainstone, Coal andclaystone Often litharenite Often Litharenite and and sometimes Petrofacies or sandy bioclast sublitharenite sublitharenite microfacies grainstone, Litharenite sometimes sometimes claystone litharenite -

claystone

,

bipolar paleo Depositionfrom traction current ripples movement: tidal channel bedforms (ripple or 2 in upper intertidal and proximal current: ripple with low indiceslow current: ripplewith Depositionfromsuspension on underconditions of lower flow Interpretation; sedimentary (5 Coastal orflood plainswamp top top of sandy bedforms and/or across low relief, abandoned underthe condition ofeither Alternation strong and weak deposit with input of input deposit with flood plains and distal delta Planar bedlower and upper upper lower or flowregime 3 flowin tidal flat: deposited - grouped tabular sets with Depositionfrom traction - Transverseand linguoid 7) related to7) relatedwave D dunes and interference currentstidal in flat flowsin intertidal Open marine tidal channel delta front processes sediment regime - front

currents represent

- - D dunes):

induced clastic

hematite pebble, C)Splithofacieswithherringbone cross-bedding, horizontal and ripple lamination,D)Fllithofacies, E)Fmlithofacies, Figure 6 BEDS (SH) 4.2.1.2. HORIZONTAL LAMINATION ANDSANDSTONE and silicacement types,respectively. with convexandbetween sand concave contact grains,J-K)Heavymineral include ofzirconand tourmaline, L-M-N) Calcite,hematite, sorted ModeratelyI) lithofacies. H) Carbonate lithofacies, (Sr) Fl / (Fl) Sr G) lithofacies,surfaceerosional andFm with lithofacies C F) otomtr Fgr b n aytae fplant to two(Figure meters 6b)andmanytraces of severalup centimeters layersof with athickness of verydelicate anassociation laminations that form tions horizontally. faciesare These thinlayersand bedding and lamina Member is the presence of Qadir the most important features of One of ripple marks (Dalrymple and river processes (tide andwave) alongwithbifurcated marine of performance the reflecting performance, tidal-flow of indicators are marks A) Sr lithofacies with asymmetrical ripple mark in the sandstone, B) Beds of horizontalsandstoneBedsofwith andin thesandstone,laminated B) (Sh) lithofacies asymmetrical ripplemark Sr with A) et al Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín ., 1992). http://dx.doi.org/10.18268/BSGM2021v73n1a140920 - SANDSTONE FACIES (SP) 4.2.1.3. PLANAR CROSS-BEDDED ANDHERRINGBONE lithofacies along withplanar cross- bedding and is identified facies sandstone prominent most The intoSrandSplithofacies.laterally transformed and low flow regimes (Lee and Chough, 2006) and lithofacies couldhave underhigh been formed litharenite to sublitharenite. This cies at a range of maturity from submature to mature with petrofa relatively good roundnessand sorting, textural with sand, medium to fine very from varies size remnants are visible amongtheir layers. grain The /73(1)A140920/2021 / 73(1)A140920/2021 9 9 -

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS grainstone facies. (marl and siltyshale)with thinlayers offossiliferous limestones intheprodeltaand openmarine, K)Coral pieces,L)Sandy bioclast G-I) beddingConvolute delta front,front, insandstonesintercalation F) in theproximal proximal delta ripple of mark with symmetrical E) fragments, fossil andplanet mark ripple cross-beddingandasymmetrical andherringbone, symmetrical C) Figure 7 10 10 Arenicolites Rhizocorallium jenese formed under low-flow regime conditions and conditions regime low-flow aremainly under and formed coarse-grained to fine-grained thisfaciesvaryfrom 2012; Davis, 2012).Grainsof nal environments (Tucker, 2001;Longhitano sedimentation in one-directional and bi-directio Sp sandstone facies. lithofacies represents This (Figureherringbone 6c),related with Sr, Sh,and (Strand, 2005). flat zone tidal the especially flow, oscillatory the an environmentin indicates deposition with inthislithofacies herringbones presenceThe of lithofacies varyfromlitharenite to sublitharenite. this from submature to mature. petrofacies The of textural maturity,of ranging and sortinginterms medium sand,having relatively good roundness to fine from range sizes grain their and degrees, Cross betweenbeddings show angles 5 and15 2-D ripples (Harms have been described by ripples as well mega as / / A) Bivalve fossil fragments impregnated with iron oxide in coastal plain sandstone, B) Tidal channel in the coastal plain part, in thecoastal channel Tidal plain sandstone,B) iron oxideincoastal with impregnated fragments fossil Bivalve A) Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín tracefossil,D)Coarsening upward cyclesof siltyshaleand sandstone in theproximaldelta front along withplanar , rhizocorallium irregular et al ., 1982; Therrien, 2006). ., 1982; Therrien, http://dx.doi.org/10.18268/BSGM2021v73n1a140920 and thalassinoides et al ., /73(1)A140920/2021 - /73(1)A1409202021 (MUDSTONE FACIES) 4.2.2. FINEGRAINEDFACIES ASSOCIATION (ST) 4.2.1.4. TROUGH CROSS-BEDDED SANDSTONE FACIES trace fossils intheproximal deltafront, trace J)Fine-grainsediments Chough, 2006). ripples with sinuous andcomplex crests (Lee and 3-D ripples andmega of migration racteristic of to Sr andShlithofacies. lithofacies ischa This is relatively mature incomposition andisrelated to relatively goodroundness andsorting, while it size.grain Texturally, medium to this facies shows moderate fine with cm 10 to up observed cross-bedding was 1. Trough unit of layers first the and can be onlyvisible to a limited extent in lithofacies isless abundantThis than other facies n opieapoiaey5%o thestudied approximatelyand comprise 50%of Qadir Member the lower and middle parts of in present often are lithofacies fine-grained The Planolites trace fossil alongfossil trace - SANDSTONE 4.2.4. FINEGRAINEDFACIES ASSOCIATION OF 4.2.3. COAL FACIES (C) MUD (FM) 4.2.2.2. FINE-GRAINED(FINESILT, CLAY), MASSIVE LAMINATED MUD(FL) 4.2.2.1. FINE-GRAINED(FINESAND, SILT, CLAY), tification, with its thickness reaching over 15 m in m reaching 15 over thickness its with tification, faciesisblackishdarkThis without any green stra anoxic conditions(for example: Davis, 2012). in thisfaciesindicates its formation color of green cases convolute bedding is alsoclearly visible. The often is blackishdark in color,green andinsome thislithofacies, which the most important features of of one is laminates parallel and fine very of presence The 6d). (Figure silt to sand fine-grained Qadir Member with very cies isvisible in parts of pended currents (Higgs sus under low-waterand asaresult conditions of which are mainlysilttoclay-sized,formed mostly fine-grains, of composed is facies mudrock This sequence (Figure 6d,6eand6f). studied the in identified were (C) coal and (Fm) withoutlaminations facies withlaminations (Fl), litho fine-grained mud and silty Three sequence. this group. These facies have been identified spo identified been have facies These group. this fall into Sr / (Sr) Fl rent lithofacies including(Fl) evidence, diffe and two studies field the on Based 2006). sequence in deltaic and river environments (Miall, floodplain the of part integral an as interpreted aregenerally facies) (coal Coals 6f). (Figure field very highorganic matter and dark color in the andFmfacies,observed having along withthe Fl from andis to about2meters afewcentimeters a coal layer varying of faciesisinthe form This affected gravityby low (Miall,2006). currents environments and river deltaic in floodplains as in water and in a low-energy environment such particles suspended of cates therapiddeposition indi lithofacies coal and fine-grained other with these facies along (Figure presence 6e). The of Qadir Member, andClithofacies andseenwithFl et al Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín ., 2012). This lithofa ., 2012).This http://dx.doi.org/10.18268/BSGM2021v73n1a140920 ------4.2.5. CARBONATE LITHOFACIES 4.3. PETROGRAPHY Zamaniyan these lithofacies (Longhitano forming sediments, fine-grained mud the above deposited sandstone sedimentswillbe coarse-grained energy, flow increased and times longer at versa lithofacies are attached to the ripples and vice Fl short time and low energy conditions, fine-grained Accordingly, time) will be formed. energy ina time) and mudrockhigh energy facies (at low systems. Therefore, intercalated(at sandstones by changes levels inenergy withinsedimentary (Figure 6g). In fact, the facies association is formed Member Qadir the of parts different in radically most frequent cement types, respectively (Figures than (less one percent). Calcite, hematite, andsilicaare the frequency insignificant very with 6k) (Figuressuch 6jand aszircon andtourmaline minerals are and heavy mica Accessory minerals fragments. and sandstone)afewmetamorphic rock sedimentary fragments (chert various types of 3, andmore than3components),plagioclase, and talline and polycrystalline quartz (including 2or sandstones include monocrys differentof types of theyare mature sub tomature. components The maturity, of in these samples islow andinterms clay (Figure amount of sand size 6i). The grains sorted with convex andconcave contactbetween coarse-grained, sub angular to sub rounded, poorly to to moderately fine often are samples stone 86thinsectionsshow that the sand studies of limestone and coal.Petrographic intercalations of shale and sandstoneswith area mainly of consists statedAs above, Qadir Member in the studied and removed. careous layers are laterally reduced inthickness reddish-brown (Figure cal 6h).These a colorof etc.) andsandy fossiliferousderm, limestone with bivalve, brachiopod, coral, gastropod, echino and include fossiliferous limestones (containing several to less than 1mthickness centimeters from layers in vary field the in lithofacies These et al /73(1)A140920/2021 / 73(1)A140920/2021 ., 2018). et al ., 2012; 11 11 - - - -

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS 4.4. SEDIMENTARY ENVIRONMENT Table 2.Frameworkparametersof detritalmodes(Ingersoll and Suczek,1979). 12 12 plain, while deltaic facies include 1-Delta plain, ofcoastal, deltaic and marine. Coastal facies include coastal associations facies three of tification iden the to led Member Qadir in identified facies et al synsedimentation (Kumar of to the interpretation significantly contributes lithofacies of recognition tions prevailinghence,basin; inthe sedimentary lithofacies based on the condi of the formation regimes flow result in altered environments sedimentary in and sedimentation changes specific while in environments, operate that cesses Lithofacies are controlled bypro sedimentary 5b, 5c,and5d). litharenite to sublitharenite (Figures 5a, a range of (Tableanalysis 2and3),sandstonesamplesare at (1980) and according to the data plot from modal Pettijohn of the diagrams sandstones have very low clay content, based on 6l, 6m,and6n).Also, given that Qadir Member / / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín ,20;Ctnau 03.Aayi fthe ., 2007;Catuneanu,of 2003).Analysis Qm non Qpq2 Qm un Qpq>3 Lsm Qpq Cht RF Qp Lv Lc Qt Ls Lt K Q L F P

-

3

Polycrystalline quartzose (or calcedonic) lithic Total (Qm non +Qm andun) Qpq used forclassification (Qm + Qpq) Carbonate (reworked fossils and limeclasts include mudstone) rock Total unstable rock fragments andchert +(L Cht)(Folk, 1974 et al Unstable (siliciclastic)lithic fragments (Lv + Ls +Lsm) ., 1987andFolk http://dx.doi.org/10.18268/BSGM2021v73n1a140920 Total siliciclastic lithic fragments (L+ Qp) Non Volcanic Undulouse monocrystallinequartz Total quartzose grains (Qm+ Qp) Metasedimentary rock fragments - Qpq2 Qpq>3 crystal units per grain crystalper Qpq>3 units Total feldspar grains +(P K) undulouse monocrystallinequartz Sedimentary rock fragments Polycrystalline quartz - plagioclase feldspar metavolcanic rock fragments Potassium feldspar - 3 crystal3 units per grain classification) /73(1)A140920/2021 - - - /73(1)A1409202021 (Folk, 1974) fragments Chert 4.4.1. COASTAL PLAIN

moderate to good rounding andsorting along with these sediments with fabric of coarse-grained Interpretation: m witherosional base. 1.2 0.4mandawidthof channels of with adepth and color with fossillighter green traces of visible in the field as white to lightgray to a slightly fossilfragments and plant particles.facies is This the bivalve horizontal laminations with some of ripple marks, cross-bedding, herringbone and symmetrical thissectionmainly of consist tures of showing a fining upwards. struc The sedimentary thickness, 4to9m layersmedium sandstone of with thinto grains mediumto slightly coarse of Description: in more detailbelow. open marine environment, which will be discussed the include facies finally, marine and Prodelta, 4- 2- Proximal delta front, 3- Distal delta front, and

Scolicia

fragments (Qpq+ Cht)

. Its most significant features are tidal are features significant most Its .

This facies association composed is This

Mediumto the moderately

Arenicolites - 4.4.2. DELTA PLAIN Table 3.Modalanalysisdataand detritalmodesof 15selectedsandstone samplesfrom Qadir Memberof theNayband Formation.

Qpq 2 Qm non Qpq ˃Qpq 3

Sample

Lsm Qpq

Cht No. (Sr lithofacies), herringbone (Sp lithofacies) with a (Sr lithofacies), herringbone symmetrical ripple mark structures sedimentary sometimes mass laminationssometimes mass and intercalations facies isalso visible as verythin horizontal and sediments this shale with organic (coal) facies. stratificationThe of and silt fine-grained of mainly Description: ments (Gingras sedi zone flat tidal the with associated strongly is of effect fossil the of identification the that so 7c) (Figure zone flat tidal the in formation Scolicia theherringbone, the other the presencehand, of coastal environments (Zamaniyan in tidal to their formation cates the conditions of indi currents reciprocal reflect that waves metric ripplesandsym structures suchas intermittent of ronments (Figures 7a and 7b). In fact, the presence marginal seasaswell as shallow envi of sections thisfaciesinshallow of indicate the formation the tidal channels surface andthe presence of stratified the at fragments bivalve and plant few RF Qp Lv Lc Qt Ls Lt K Q L F P - 3 , and

105 230 230 171 59 33 66 59 P 0 2 0 0 7 0 7 2 0 7 0

Arenicolites

The deltaic composed facies is The 110 110 28 35 28 28 10 82 35 P et al 0 3 0 0 0 0 0 3 3 0

., 2011).

36.5 226 220 188 39 41 32 26 P 0 2 0 0 7 0 7 2 8 0 6 traces fossil indicates their Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín

181 181 160 10 21 85 10 21 21 12 40 40 P 0 0 0 0 0 0 0

http://dx.doi.org/10.18268/BSGM2021v73n1a140920

117 110 49 78 42 35 17 68 60 et al P 0 5 0 0 7 0 7 5 9 7

., 2018). On

157.2

Arenicolites

41 65 62 52 35 25 17 27 10 17 P 0 4 0 0 6 0 6 4

141 156 148 175

83 83 75 13 35 65 P 0 0 4 8 0 4 0 0 0 - - - -

177.3

4.4.3. PROXIMAL DELTA FRONT 53 65 71 71 49 49 17 19 22 P 0 4 7 0 0 7 0 0 4 Interpretation: Interpretation: with thecoalfacies. many plant remnants associated the presence of anditsmostimportant featurethan 15meters is the delta plain varies from 5to more the facies of thinsandstoneandsiltstone.of thickness The of upwards.part this have Sandstonesin mainly fining becoming cycles, sandy and shale-silty ral Description: et al vegetation,clastic material including (Zamaniyan inmarshyenvironments formed withabundant sediments inthisfaciesindicates thatbeen it has fine-grained and remnants plant of presence The Rhine-Meus Rivers: Kosters, 1989;Bos, 2010). and the Mississippi example, the delta plains of (Fielding and Frank, 2015;Higgs the delta-coastal plain tributaries of and marshes withinthe interdis considered assedimentsformed currents in a low-energy environment, they canbe fine-grained with suspended muda result as sedimentsdeposited of association their and layers

182.3

117 53 89 78 53 42 20 11 25 P 0 0 0 0 0 0 0 0 0 ., 2018).

304.5

121 127 122 48 48 43 11 74 P 0 0 6 4 5 0 6 0 0 0 /73(1)A140920/2021 / 73(1)A140920/2021 hsfce scmoe fseve facies iscomposed of This

329.2

135 135 37 95 37 37 20 98 P 0 0 0 0 0 0 0 0 0 0 ie h xsec fcoal Given the existence of

115 107 107 337

45 45 45 62 P 0 0 2 0 0 0 0 2 0 0 0

125 130 130 103 349

27 27 27 11 P 0 0 3 0 0 0 3 0 0 0 et al

120 114 114 354

11 52 41 41 16 73 11 P ., 2012) (For 0 5 0 0 0 5 0 0

379.2

48 93 92 92 39 39 12 53 P 0 4 0 0 9 0 9 4 0 0 13 13 - -

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS Figure 8 14 14 seen aslaminating anddiagonal as well as thin sand layer’sis up to thickness 0.5 mandcanbe also presentding is a very in limited range. The ments (Figure 7d). Small scale trough cross-bed ripple markswith relatively abundant plantfrag cross-bedding, symmetricalandasymmetrical low-angle planar cross-bedding andherringbone dding suggests that sediments have been affected been have sediments that suggests dding small-scale trough cross-be limited expansionof tidal currents. Also, indicators of performance cross-beddingherringbone canbeconsidered as ripple markswith straight ridge and low angle symmetricalandasymmetrical presenceThe of in the delta front area (Carlos and Ronland, 2008). facies this of sedimentsindicate the formation of along with relatively good roundnessand sorting plant fossils the delta plain and alsothe presence of Interpretation: identified withlow abundance (Figure 7e). ciated with bioturbation in thisassemblage were and siltyshale. trace fossils The of ripple layers with intercalations withinthe shale / / Reconstruction ofpaleoenvironment fortheQadirMember of Nayband Formation(notscale). Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Lcto fthesefaciesbelow Location of http://dx.doi.org/10.18268/BSGM2021v73n1a140920 Planolites asso /73(1)A140920/2021 - - - - /73(1)A1409202021 4.4.4. DISTAL DELTA FRONT ihaudneo shalesediments, thispart is high abundance of with convolute bedding (Figure 7f).Duetothe medium to thin and horizontal stratification along nes to calcareousof sandstonewithathickness sandsto darkcolor withintercalations gray of blackish in sediments fine-grained silty and shale Description: Zamaniyan front section(Bayet-Goll and Carvalho, 2017; the proximal delta can alsoprovide evidence of of the trace fossils presenceand Plint, 1992). The of (Walkerfluctuations environmental and waves by exhibit inthis small-scale regular alternations Interpretation: were identifiedinthisfacies. (Figure(Figures 7i) 7gand7h),Thalassinoides Trace fossilsof front, which hasmore sandstone alternations. the delta well separated from the upper part of Planolites along with et al Ti ati anycmoe fpart is mainlycomposedof This ., 2018). Rhizocorallium Jenese, Rhizocorallium The shale-siltstone layers The Thalassinoides and Skolithos Skolithos - 4.4.5. PRODELTA Figure 9 7j). These sediments contain insignificant interca insignificant contain sediments These 7j). identifiable in Qadir the Member unit (Figure 1 of scattered with low planar laminations that are constitute the prodelta facies inthispart and are grains the of fining upward with sediments ined Description: theprodelta. of facies final the into changes gradually facies This (Fielding and Frank, 2015;Zamaniyan inthe distal delta frontindicate facies formation convolute bedding and scattered bioturbation of the proximal over delta front alongwiththe presence sediments fine-grained of dominance The bed (Bayet-Gollsedimentary and Carvalho, 2017). from organisms suspendedmaterial and vity of and trace fossilsof proximal delta front sediments. presence The of sediments, the layers are well separated from the fine-grained of abundance the given and, facies Different parts ofthedeltaicenvironment Different ofQadirMember parts inthelower unit. Thalassinoides The shale-silty and marl fine-gra marl and shale-silty The Rhizocorallium Jenese in thisfacies indicates the acti Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín http://dx.doi.org/10.18268/BSGM2021v73n1a140920 , Rhizocorallium et al ., 2018). - - - , 4.4.6. OPENMARINE particles (Einsele, 2000). suspended prodelta of during the rapid deposition marine facies canindicate sedimentation in the and shalesedimentstheir accompanying marl and Dries, 1998). Also, the large volume of open marine(Tovaglieri and George, 2014;Cotter the prodelta to parts of conditions inthe deeper with anoxicassociated conditions with low energy mud sedimentsindicate environmental nance of fossil evidence, and the domi fabric, the absence of Interpretation: cross bed. times withsymmetricalripple strata and low-angle sandstoneandthin-layer siltstone, some lations of chiopod skeletal fragments larger than 2mmin the bivalve andbra comprises about 50-70% of facies This sediments. prodelta fine-grained with facies andobservablebioclast grainstone along fied in the 1 and 2 units (mostly unit 1), containing Qadir Member were identi Marine sediments of /73(1)A140920/2021 / 73(1)A140920/2021 Tepeec flaminar presence The of 15 15 - - - -

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation RESULTS Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION 4.5. GEOCHEMISTRY Figure 10 16 16 3.5% Fe TiO 1.48% Na 78.53% SiO contain an average of are presented in Tables sandstones 4and5.These sandstonesinthe study area and trace elements of major resultsThe associated of with the analysis Formation and itsvarious sections. the Nayband the Qadir Member of model of tary Montenegro (Cadjenovic south of been reported inthe Yudova basin, sedimentary Read, 1985)andfacies similarto this have also 2010; the open marine (Flugel, shallower parts of skeletal particles indicate facies with coarse-grained environments inhigh-energy cate formation while indi 2004) and Read, (Coffey particles siliciclastic subangular with very low mud andthe presence of facies along grainstone presence(2010). The of and belong to facies belt No. 7andSMF11 Flugel environment energy high a in wave’seffect the of facies are aboveand l).These deposited the surface gastropod, etc.) are less than 10%(Figure 7k derm, size, while other skeletal fragments (coral,echino / / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Figures 8and9show the proposed sedimen Thechemicalcomposition of QadirMember sandstones plotted onthediagram 1975). (Pettijohn, 2 , 0.06%MnO, 0.96CaO, 0.07%P 2 O 2 3 O, 1.1%MgO, 1.04%K lo h aiso oxides are cal . Also, the ratios of http://dx.doi.org/10.18268/BSGM2021v73n1a140920 et al 2 , 9.65% Al ., 2008). 2 O, 0.41% 2 O 5 and 2 O 3 - - - - , /73(1)A140920/2021 /73(1)A1409202021 5.1. THESOURCE ROCK TYPE 5. Discussion indicates that the sediments mayhave been derived quartz grains monocrystalline dominance of The arkose (Figure 10). sandstones include sublitharenite and slightly sub classification, Pettijohn’s(1975) on Based 1.01%). Compositional Variability or ICV (averageof Alteration orCIA(average 71.26)andIndex of Na (average 10.03%), K culated and presented in Table 4: SiO hematite cement, as well as iron oxide bearing Fe rocks.mafic volcanic and minerals, opaque rutile, TiO amount of (albite). The Na amount of spar (microcline), mica, andclay minerals. The and K Al feldspar, andclayminerals. amountsof The silica could be often provided by the quartz, chert, bad from source agranitic (Basu 2 O 2 O + K et al 3 canalsobe related to heavyminerals and 2 a erltdt h rsneo k-feld be relatedO can tothepresence of ,21a 02) h oreo existing source., 2012a,2012b).The of 2 O (average 2.52%), Chemical Index 2 O is mainlyrelated to Na-feldspar 2 O/Na 2 et al 2 O (average 0.67%), is largely related to ., 1975;Khaneh 2 /Al 2 2 O O - - - 3 3 Table 5.Traceelement(ppm)concentrations inthesandstones of Qadir Member (Note: N=notdetected). Alteration, ICV: Index ofCompositionalVariability). concentrations inthesandstonesTable 4.Majorelement(oxide%wt) of Qadir Member (LOI: Loss ofignition,CIA: Chemical Index of Sample Sample Ni/Co V/Cr Fe Al Na MnO MgO TiO P CaO SiO No. K ICV CIA LOI Cu Nb Rb SO Zn Co Th Ba Pb Ce Cr Zr No. Cl Ni Sr V Y U 2 2 2 2 O 2 O O

O

O

3

2 5 2

3 3

P 33 0.41 560 199 371 112 65.44 87.77 5.3 P 33 36 56 38 74 16 31 24 74 38 1.15 1.56 0.15 2.04 0.05 0.89 0.05 0.34 1.32 4.83 N N 3 2 0.2 0.6

P 40 72.22 82.65 391 147 203 4.5 P 40 1.02 2.52 2.99 0.09 0.94 0.08 0.22 0.48 1.21 1.38 7.28 32 39 42 62 72 85 35 36 35 N N N 1 8 2 0

P 84 1.47 56.83 85.64 130 319 184 3.2 P 84 1.27 1.85 1.82 2.14 0.06 1.48 0.08 0.13 0.72 1.46 4.82 58 61 42 17 23 25 58 17 10 17 35 N 0.1 7 3 Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín

http://dx.doi.org/10.18268/BSGM2021v73n1a140920 P 157.2 P 157.2 P 0.66 70.24 79.71 537 130 1.14 0.02 3.61 0.09 1.19 0.04 0.43 0.94 1.45 1.34 8.19 10 68 45 78 37 75 60 97 50 38 30 67 N 2.8 1 6 5

P 177.3 P 177.3 P 0.58 50.97 80.78 238 145 9.4 2.68 0.06 3.55 0.11 0.21 0.44 1.02 1.31 5.51 4.05 0.15 74 58 64 13 56 47 36 33 24 87 35 1.7 N N 5 0

P 223.8 P 223.8 P 1522 10.81 75.95 79.02 3.69 0.09 138 103 276 106 4.98 0.13 0.34 0.06 1.09 1.34 1.44 0.94 3.03 0.05 57 62 48 13 34 29 74 0.5 N 6 1 2 6

P 329.2 P 329.2 P 13.87 72.93 80.03 3.57 1.13 103 126 131 406 134 4.47 0.27 0.07 1.65 1.56 1.54 0.77 2.73 67 32 61 50 14 69 14 45 11 44 89 0.1 0.6 N 0

/73(1)A140920/2021 P 349 P 349 / 73(1)A140920/2021 14.77 72.45 79.96 4.54 1.27 126 197 132 498 127 3.89 0.08 0.15 0.02 0.69 1.67 1.35 1.88 0.69 2.82 57 68 59 50 11 75 52 13 29 95 N 8 0

P 379.2 P P 379.2 12.67 76.56 79.68 1.32 3.14 0.02 0.18 0.02 0.55 1.44 1.18 1.61 0.68 2.44 103 146 239 120 5.7 90 34 19 46 57 10 61 48 16 26 89 N 8 0

P 422 P 422 13.76 70.94 78.22 5.09 0.09 0.66 0.07 0.59 1.65 1.19 1.52 0.82 4.14 0.01 4.42 0.92 102 971 101 102 143 65 47 75 62 14 69 46 11 54 99 N 8

Average Average 71.26 78.53 40.25 133.2 311.6 129.4 1.01 2.79 0.22 0.07 0.96 0.06 0.41 1.04 1.48 9.65 4.93 0.81 85.7 57.2 29.6 44.9 45.4 42.9 66.3 3.5 1.1 9.1 4.6 0.5 56 36 7

17 17

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION and McLennan, 1985). Figure 11 18 18 unchangeable during weathering, transformation clay phases(Dabard, 1990;Getaneh,2002). Fe 02) h ao lmnso Qadir sandstones major elements of 2012b). The the carbonate particles (Khanehbad MgOandCaObe provided can by the source of calcite cement and skeletal fragments; presence of CaO is largely in relation to the the amount of cement, and dolomite, of inthe form presence of MgO is inrelation to the minerals. amount of The ihcnetaino TiO concentrationhigh of phyllosilicates (especially illite) inawaythat the TiO tion, the low amountsof diagenetic processes (Salehi carbonate during minerals with calcium depletion the lack of CaO can depict low concentration of to thepetrographycorresponding data. very The sodiumfeldspar which is to the lower ratio of Na of depletion than UCC.The MgO, CaO, Na Al According to the plotted diagram, (UCC; Taylor andMcLennan,1985)(Figure 11). were compared withthe upper continental crust / / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín 2 Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Normalization of major oxides of Qadir Member sandstones in comparison with the upper continental crust (UCC; Taylor (UCC; crust uppercontinental the in comparisonsandstones with Member Qadir of oxides majorNormalization of O Considering that aluminum oxide is almost 3 , andAl 2 O 2 O, andTiO 3 masteeitneo more meansthe existence of 2 et al 2 , CaO, MgO, K are significantly less significantly are 2 could be due to http://dx.doi.org/10.18268/BSGM2021v73n1a140920 ., 2014). In addi 2 O canbe related et al 2 O ., 2012a, 3 , FeO, 2 O, O, /73(1)A140920/2021 - /73(1)A1409202021 n h muto SiO ing the amount of point regarding Al trend (reverse) withthe Al other hand, CaO and SiO 2006; Khanehbad aluminosilicate (Pettijohn clay minerals, especially indicate the presence of eemnn h oreo sedimentsandpresent the source of determining calcite(Das ations of alter diagenetic and secondary as the presence of CaO could bereferred to reverse relationshipof et-Goll and Hosseini Barzi, 2011). In addition, the textural maturity in the given(Bay compositions more-quartz phases andhigh to the presence of oxide (less than 5%) decreases. couldbe due This neadfeunyo these oxides withthe Al ance andfrequency of TiO Fe 12. Elements of other major oxides have been presented in Figure Al El-Gohary, amounts of 2008). The major elements (Getaneh, and 2002; Akarish with other and alsocomparison comparisons ogy and, diagenesis, it can be used asafactor for lithol The trace element’sThe canbe used to pattern 2 show apositive trend withAl 2 O et al 2 O 3 et al andSiO 2 3 h muto aluminum , the amount of ., 2012a, 2012b). On the , K ., 2006). et al 2 2 O, MgO, Na represent a negative 2 O ., 1987; Das 2 3 is that is byincreas Te significant The . 2 O 3 2 . Compli O 2 3 O, and versus et al 2 O ., - - - - - 3

Figure 12 Investigating thechanges ofmajoroxides versusAl Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín http://dx.doi.org/10.18268/BSGM2021v73n1a140920 2 O 3 intheQadirMember sandstones. /73(1)A140920/2021 / 73(1)A140920/2021 19 19

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION Figure 13 20 20 muto Al amount of a positivein sandstonesdepict relationship with the trace elements (Co,The Nb, Ni, Rb, V, Th, and Y) proportionsdifferent (Salehi in cantly varysignifi rocks source felsic and mafic the of rocks mentary (Von Eynatten sedi about the provenanceuseful information of from and the middle to low-rank metamorphic Qadir Member was largely the source rock of (Tablemodal analysis 2 and3) on thisdiagram, located smallvertices.in the sandstone Basedon non-undulatory andundulatory quartz were more than 3 were located in large vertices, while or 2to 3 crystals According to this diagram, sandstones. the provenancetals to interpret of quartzcrys latoryextinction andthe number of Basu ish andEl-Gohary, 2008;Zaid,2015). Al these elements with increasing of the amount of / / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín 2 Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín TheQadirMember sandstones source rock based onBasu O 3 sostepeec fclay minerals(Akar showsthe presence of et al (95 sddfeettpso undu of types different used (1975) 2 O 3 , presented in Table 5. Increasing et al http://dx.doi.org/10.18268/BSGM2021v73n1a140920 ., 2003),because et al ., 2014). /73(1)A140920/2021 - - - - - /73(1)A1409202021 et al ., 1975diagram. this diagram shows granite to granodiorite source to granodiorite shows granite this diagram TiO the of On the other hand, based on the diagram 14b), which represent provenance. sedimentary ous, provenance andquartz sedimentary (Figure igne felsic igneous, intermediate igneous, mafic of ranges four in sediments differentiate to used Roser and Korsch is also (1988) function diagram The 14a). (Figure rocks mafic and granite around extent around and a lesser extent granodiorite Qadir Member sandstones wasplotted to a great and felsicsource rocks,intermediate the setting for Al ment of due to the place the Schieber (1992) diagram, slightly plutonic rocks(Figure 13). Also, basedon conducted by heavyminerals plotted in aninter (Figure 14c). It shouldbe noted that the zircon is igneous rocks the felsic igneoustointermediate the sandstones have been often plotted around ZrversusTiO rocks. of Basedonthe diagram 2 versusAl 2 O 3 against TiO against 2 O 3 , the range of sandstones on sandstones , therange of 2 for separating basic, 2 - - - , (-1.22×K Discriminant function1:(-1.773×TiO TiO with compared Figure 14 5.2. DEPOSITIONAL ANDTECTONIC SETTING diagrams Al + (1.426×K fsediments, the P of To environments the depositional determine the Nayband Formation. rockbe proposedcan for theQadirMemberfrom igneous source andintermediate the sedimentary rock (Figure 14d). Thus, based on these diagrams, felsic source intermediate represents the nature of samplesaround illite and smectite placement of - (FeO+MgO), according to Hayashi Al of 2015). Indiagram and the mineral’s hostismainlyzircon (Zaid, mediate igneous source rock(Paikaray 2 O%) +(-9.09).Discriminant function 2:(0.445×TiO Investigating the Qadir Member sandstones source rock based on different diagrams. A) The ratio of Al rock basedondifferentMember sandstonessourceThe ratio InvestigatingtheQadir diagrams.A) 2 O %) +(-6.861).C)TiO O 2 O 3 -(CaO +Na 2 (Schieber, 1992), B) Discriminant plot for sandstones using major elements oxides (Roser and Korsch, 1998). andKorsch, (Roser oxides elements sandstonesusingmajor for plot Discriminant B) 1992), (Schieber, 2 O+K 2 2 O)-(FeO +MgO)(Hayashi O 5 2 (wt.%) versus Zr (ppm) bivariate diagram (Paikaray (wt.%)versusZrbivariate (ppm) 2 (wt%) andAl O Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín 3 2 - (CaO+Na %) +(0.607×Al http://dx.doi.org/10.18268/BSGM2021v73n1a140920 et al et al 2 2 O O+K 2 O et al ., 1997, 3 ., 2008) 3 (wt%) %) +(0.76×Fe 2 %) +(0.07×Al ., 1997). 2 O) 2 O 2 O 3 (T)%)+(-1.5×MgO%)(0.616×CaO%)+ (0.509×Na 3 %) +(-0.25×Fe ated during lateconditions Triassictime (Tables restrictedoccurred in shallowoxygenmarine in Qadir Member environments. of deposition The havedeposits been originated in shallow marine Member (Figure Qadir Member 15b). Then, theQadir of settings depositional marine-fluvial plot (Dhannoun andAl-Dlemi, 2013) asshallow drawnfrom V (ppm)-Al2O3 (wt%)bivariate (Norian toRhaetian). Also, Similar results were to lower biologic activity during the latest Triassic phosphorous due further indicate lower values of plotted in shallow marineenvironmentswhich the Qadir Member were sandstone samples of Al-Dlemi, 2013). Figure 15a indicates that most bivariate areand used (Dhannoun diagram et al 2 O /73(1)A140920/2021 ., 2008), D)Drawingthedata intheternary ., / 73(1)A140920/2021 3 (T)%)+(-1.142×MgO %)+(0.432×Na 2 O 3 major oxides major 2 O%) + 2 O %) 21 21 -

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION 22 22 etnto rvdsabte nesadn fdestination provides of a better understanding cycles the origin and and that is why of the orogeny determination about data significant ment El-Gohary, 2008). In fact, the sandstones docu source rockand (Akarish distance, andtype of controlled bythe diagenetic processes, transport is sandstones 4 and5).Also,of thecomposition h rgn hs fEarly Cimmerian inthe the orogeny phase of broad extensional retro-arc zone, concurrent with limited volcanic activity in the arc and the very Formation andNayband Formation) and also and Late Triassic between (the Boundary Shotori middle Cimmerian orogeny of inthe boundary the Early tectonic activities andoccurrence of theses sandstones. results These canbe due to the active for continental margin canbe interpreted Roser andKorsch (Figure 15e), (1986)diagram margin (Figure 15d).Inaddition, based onthe few samples are plotted on the passive continental are plotted onthe active continental margin anda the samples shows thatdiagram the majority of Qadir Member sandstones on the Bhatia (1983) the elements in sandstones. Plotting the data of major gin based onthe geochemical criteria of continental margin, andpassive continental mar nental island arcs, oceanic island arcs, active conti basinsinto fourthe sedimentary types of and Korsch (1986)divided the tectonic setting of particles (Tucker, 2009). these recyclingtransport, and/or sedimentary of setting,could showdepositional highenergy long with polycrystallinein comparison inthe samples quartz monocrystalline and existencequency of on the transitional recycled (Figure fre 15c). The quartzose recycled and a few sampleswere plotted was sandstones Suczek, 1979),the provenance of and Qm-F-Lt (Dickisnon diagram in the ternary sandstones(Table 2 and3) the of modal analysis majorprovenance. Conducting various typesof to sandstones terrigenous the of compositions Suczek (1979)andDickenson geochemical data (Tableand 2 and3).Dickinson using the and modal analysis ber is interpreted al the tectonicstatus andtheir development (Shi / / ,21) h etncstigo QadirMem tectonicsetting of ., 2016).The Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín On the other hand,Bhatia (1983)andRoser et al http://dx.doi.org/10.18268/BSGM2021v73n1a140920 ., 1983related et /73(1)A140920/2021 - - - - - /73(1)A1409202021 5.3. SOURCE AREAWEATHERING uigwahrn eut ndpeino alkali during weathering results of indepletion igneousrocks and Resentini, 2016). Alteration of and tectonic setting (Bauluz be changedcan byweathering the sourcein region asource region and such asthe composition of controlledenous sediments is with various factors terrig andchemical composition of Mineralogy 2009a; Zamaniyan et al Fürsich 2002; Borel, and Stampfli 1974; Stöcklin, Early Cimmerian; for example, occurrence of Central-East IranianMicrocontinent (CEIM;the Al SiO the amount of Based onthe Suttner and Dutta (1986) diagram, the rocks(Khanehbad of to humid weather which intensifies the weathering weathering can be due sitional site. rate This of source region and during transport to the depo rocksis shows in the chemical weathering of 4), according to which, mediumto rather a high 71.26%(Table50.97 to 80.03 withanaverage of CIAfrom Qadir Member ranges from the rate of Young, 1982). Considering the given calculations, humid climateand (Nesbitt conditions and warm cold climate conditions, while high CIAsuggests alteration and anddry lowsuggests amountof low tohigh;ranging from 50to 100. Low CIA and wasrelated to the chemical alteration from low, CIAwas mediumandhigh amountof The CIA following formula: (Nesbitt and Young, 1982)andcalculated by the Alterationused (CIA)was ing, ChemicalIndex of chemical weather2011). To identifytherate of unmovable ones (Bayet-Goll Barzi, and Hosseini movable oxides such asCaO, K the rocks isoften calculated by the ratio of ing of 2004; Osae Al enrichment of and alkalineearth elements andpreferential 2 O =[Al ., 2005;Fürsich 3 +K 2 O 2 O+Na 3 /(Al et al ,20) h itr fweather of history ., 2006). The 2 2 O O was used asanother O was weather 2 O 2 3 aanttettlpretg f the total percentage against of et al +CaO+Na 3 insediments(Garcia et al ., 2019). ., 2009;Wilmsen et al et al 2 O+K ., 2012a, 2012b). ., 2000;Garzanti 2 O andNa 2 O)]*100 2 et al et al O to ., ., - - - - using majorelements oxides(Bhatia, 1983).Discriminant function1:(-0.0447×SiO classificationDiscrimination function plot analysis D) 1979), (Dickinson andSuczek, analysis Modal on the sandstonesbasedMember (Dhannounplots and Al-Dlemi,2013)refer shallow marineand fluvialenvironments for QadirMember, of C)Thetectonicsetting Qadir +(0.208×FeO%) + (-3.082×MnO%) + (0.140×MgO%) + (0.195×CaO%) + (0.719×Na + (0.195×CaO%) + (0.140×MgO%) + (-3.082×MnO%) + +(0.208×FeO%) Figure 15 (-0.117×Na 2: (-0.421×SiO based on study by Cirilli Tabas climate. implyingamoistwarm However, flora studies by Sajjadi climaticthis situationalso supported is bypalyno semi-humid for the given samples (Figure 16a) and weather conditions are specified to be semi-arid to sandstones. the Plotting our data on thisdiagram, to identifythe chemical maturity of performance A) P 2 O%) +(-1.840×K 2 %) +(1.988×TiO 2 O 5 -Al 2 O 3 (Dhannoun and Al-Dlemi,2013)showingB) V-Al oftheQadirMember,settings shallowmarinedepositional 2 O%) +(7.244×P 2 %) +(-0.526×Al et al Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín et al . (2015) in southeastern southeastern . (2015)in . (2005) on the Nay http://dx.doi.org/10.18268/BSGM2021v73n1a140920 2 O 5 2 %). E) Tectonic setting diagramforsetting Sandsones%). E)Tectonic of QadirMember (Roserand Korsch, 1998). O 3 %) +(-0.551×Fe 2 O - - 3 %) +(-1.610×FeO%) +(2.720×MnO%)(0.881×MgO) +(-0.907×CaO%) 2 enance region. the Accordingdiagram, tothis prov chemical weathering and compositionof sample’salong with the compositions change of (Paikaray Al of diagram recorded. CIAvalues plotted The the triangle on (tropical tosubtropical)and warmer is conditions band Formation, achange from humidto drier O%) + (-0.032×K + O%) 2 %) +(-0.972×TiO et al /73(1)A140920/2021 2 / 73(1)A140920/2021 2 O%) + (7.510×P + O%) ., 2008) suggest the change., 2008)suggest the in O 3 -CaO+Na 2 %) +(0.008×Al 2 O 5 2 %). Discriminant function Discriminant %). O -K 2 O 3 %) +(-0.267×Fe 2 O orA-CN-K 2 O 23 23 2 3 O %) - 3

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION 24 24 reduce and weathering procedure changes toward weatheringK-feldspars proceeds, potassiumions (Plagioclase), and as the feldspars by alteration of ering, sodium,andpotassiumionsare removed weath of stages first the throughout since 2011) with A-CN side (Bayet-Goll Barzi, and Hosseini procedure parallel a has weathering of stages first uesuc ok r ulo silicate minerals with ture source rocksare full of that ICV(>1) suggests the imma high value of weathering reduces and the increases, the value of thisindex ing, inother words, when the value of weather indexinversely is related to the value of this ICVvalue that The suggests the value of ICV geochemistry. relationship The isasfollows: source rock based on major elements of types of ICV couldbeemployed toidentifyandseparate ation (CIA; Cox Alter Variability (ICV) andChemical Index of Compositional relationshipbetween Index of source rockbycan beassessed compositions the Etesampour active continental margin (Zamaniyan by the sediments affected have which conditions tectonic in the semi-arid to semi-humid weather these results show rather unstable condition of in contour Al smectite and illite and to a lesser extent range of Given that the samples have been plotted in the weathering happened has in the source area. the contour Al ber sandstones while not drawing the samples in a rather severe weathering for the Qadir Mem in thecontourAl smectite and illite and less plotted in the range of samplesare thesandstone often the diagram, on A (Nesbitt and Young, 1984).Plotting these data these elements toward the vertex movement of K the value of is, inadvanced weathering, anobviousdrop in Al / / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín 2 Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín O The relationshipThe between weathering and =(Fe 3 composition (Paikaray composition 2 O 3 +K et al 2 2 O+Na 2 2 O O O emerges withthe composition ., 2019). 2 3 et al O 3 -Pl, it can be concluded that -K 3 -Pl (Figure 16c). This depicts -Pl depicts (Figure 16c).This 2 O+CaO+MgO+TiO 2 ., 1995;Potter O indicates that no severe et al http://dx.doi.org/10.18268/BSGM2021v73n1a140920 ., 2008).That et al et al ., 2005). 2 )/Al ., 2019; 2 O 3 /73(1)A140920/2021 - - - - - /73(1)A1409202021 5.4. PALEO-OXYGENATION CONDITION Lee (2002), theQadirfromMember sandstones the CIA basedonthe method of against diagram bythe alteration. Besides, byplotting the ICV indicating that the minerals have been less affected clay minerals, theseto form sandstones turity of (Table 4) which represents sub maturity to imma the Qadir Member sandstones wasabout 1.01 1995; Cullers, average 2000).The ICV value for and muscovite show values < 0.84 (Cox typical alteration products such askaolinite, illite, and pyroxenes show ICVvalues >0.84,whereas erals such asplagioclase, K-feldspars, amphiboles, source rock(Cox lesser ICV(<1) value, themore mature willbethe any clay minerals. Onthe other hand, the lack of et al 2005; Bayet-Goll and Carvalho, 2017;Zamaniyan by oxidant conditions (For examples: Fürsich environments,coastal and where they areaffected mation (Qadir Member) have settled in deltaic the Nayband For that of the siliciclastic deposits Tablein 5.Ontheothernewstudiesshowhand, ments. for ratios samples These were determined these sandstoneswereoxic in deposited environ 4.93, which thissectionis showsthat of sandstones and Manning, average 1994).The Ni/Co ratio for suboxicsuggests andanoxic environments (Jones cates oxidizing environments, whereas ratio >5 in oxic conditions. Also, the Ni/Co ratio <5 indi indicating thatwere thesesandstones deposited Qadir Member 0.81 (Tableis 5), of sandstones and Manning, average 1994).The V/Cr ratio for values more <2 suggest oxidizing(Jones conditions b). Ratios >2 indicate anoxic conditions, while studies (Dill paleo-oxidationmany in an indexbeen usedas of ancient sediments. V/Cr ratio The has dition of the paleo-oxygenationto understand authors con Geochemical data have been used by various ate igneousrocks (Figure16b). intermedi Nayband Formation show a source of ., 2019). et al ., 1988;Khanehbad et al ., 1995).Rock-forming min et al ., 2012 et al et al ., ., ------Figure 16 5.5. PALEOGEOGRAPHY the A-CN-K triangular diagram(Paikaray (Cox CIA against diagram dual ICV B) semi-humidweather, to semi-arid f cliin s tl udr icsin (Şengör discussion under al still is collision of Sheikholeslami, 2016). However, the precise age al Schmit, 1983; Stampfli and Borel, 2002; Zanchi (Berberian and King, 1981;Davoudzadeh and following the Late Triassic Neotethyan subduction and collided assic with Laurasia and Turan plates Paleotethysby moving northward duringthe Tri closure of the to led It Borel, 2002). and (Stampfli duringthe Early Gondwana Permian margin of and Alborz,separated from the northeastern Microcontinent Mountains (CEIM), northwestern Central-East Iranian Iranian plate is made of ., 1988;Alavi ., 2009;Wilmsen Investigation and procedure of Qadir Membersandstones weathering. A)TheSuttnerand Dutta(1986)dualdiagramsuggest et al et al ., 1997;Seyed-Emami, 2003; ., 2010;Cifelli Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín et al http://dx.doi.org/10.18268/BSGM2021v73n1a140920 ., 2008) (Ka: Kaolinite, Sm: Smectite, IL:Pl: Plagioclase,Gr:Granite, K-F: K-Feldspar). Illite., 2008)(Ka:Kaolinite, Sm:Smectite, et al ., 2013; et et - et al i fIranplate and thisevent reduced compres gin of Neotethys mar subduction started at the southern During the Late Triassic time (Norian-Rhaetian), sitional-marine environments (Shahrabi, 1999). tran the Nayband Formationof tooktheform and inthe Rhaetian time, the Qadir Member from 1000m of withthethickness iments were formed coastal and marine conditions, the sand-silty sed Tabas, inthe Iran), the strongly depressed blockof Central Formation fromgroup theShemshak of first the as Formation (Nayband time Norian the Middle Cimmerian (Fürsich between two tectonic events: Early Cimmerian and Late Triassicto the Middle Jurassichas happened the cycle sedimentary Golonka, 2004).The of sion of the Iran Plate with subsequent formation the Iran Plate with subsequent formation sion of ., 1995) suggest the intermediate igneous rock source,C) intermediaterockigneous the suggest 1995) ., /73(1)A140920/2021 / 73(1)A140920/2021 et al ., 2009). During 25 25 - - - -

Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION Sedimentary environment and provenance of sandstones from the Qadir member in the Nayband Formation DISCUSSION model (nottoscale; CEIM, Iranian Central-East Microcontinent)(modifiedafter Wilmsen the of phases representingimportant slices time Different (A-C) Iran Plate. the evolution of Triassic middle-late in Iran andthe Orogeny model fortheCimmerianandBarrieris indicatedasterisk onb,C)Geodynamic after 2008)and Vrielynck,thestudyarea byawhite oftheLate Triassic(MiddleNorian-Rheatian)palaeogeographic sketches for the Early CimmerianOrogenyontheIranPlate(modified Figure 17 26 26 / / Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín Boletín de la Sociedad Geológica Mexicana Geológica Sociedad la de Boletín A) Geodynamic model of late Triassic for the Cimmerian Orogeny in Iran, (modified after Stampfli and Borel, 2002), B) 2002), Borel,andStampfli(modified after in Iran, Cimmerian Orogeny the for Triassic late of model Geodynamic A) http://dx.doi.org/10.18268/BSGM2021v73n1a140920 /73(1)A140920/2021 /73(1)A1409202021 et al ., 2009b). 6. Conclusion retro-arc zone (Salehi activity inthe arc andthe verybroad extensional and Talbot, 2006) caused the limited volcanic Neotethysbeneathsubduction SWIran(Ghasemi Wilmsen (Figure17c:be also suggested geodynamicmodel; Triassicasia and Turan period could at the end of Qadir Member, while Iran’sof collisionwithEur tethysunder Iran’ssubduction plate for sandstones and Korsch (1998)diagrams, couldimply Neo conditions, based on the Bhatia (1983) and Roser On the other hand, the active continental margin 2005; Sajjadi ported and other studies (for example: Cirilli semi-arid climateabove discussed condition sup is 2008)). and Vrielynck, semi-humidto Accordingly, of ourinterpretation Barrier after (modified sketchesand Borel, 2002) and palaeogeographic (Figures17a and 17b: geodynamic model (Stampfli 25°-30°North locatedIran was Latitude in of et al theseaontoIranPlate (Wilmsen of gression extensional basins and trans (Nayband Basin) of trough cross-bedding, and different trace fossils, trace different and cross-bedding, trough ripples, cross-bedding,herringbone as typesof upward cycles structures and sedimentary such fining of presence The marine. open the of parts plain, proximal delta front, distaldelta front, Prodelta and shallow delta plain, coastal of tification iden the to led Member Qadir the in identified facies calcarenite and calcirudite.of Analysis of facies, together with carbonate facies inthe size lithofa fine-grained three and onecoal(C) / (Fl)Sr Fm,(Sr)Fl Fl, cies of St, and Sp Sh, Sr, of facies including four medium to coarse-grained identification the in resulted section studied the in analysis field Faciesand 2. and 1 units into limestone, anddivided layers andthin-layers of sediments along siliciclastic with the coal made of mainly is 450m (Late Triassic)of with athickness the Nayband Formation Qadir Member of The 2019, Etesampour ., 2009b; Fürsich et al ,20b.As,tesalwageo ., 2009b). Also, the shallowof angle et al ., 2015;Zamaniyan et al et al et al ., 2019). ., 2018; Zamaniyan Boletín de la Sociedad Geológica Mexicana Mexicana Mexicana Geológica Geológica Sociedad Sociedad la la de de Boletín Boletín ., 2005). In that period, http://dx.doi.org/10.18268/BSGM2021v73n1a140920 et al ., 2019). et al et al ., ., ------References Acknowledgements and volcanic activityinthe Central-East Iranian time which concurrent with the was orogenyphase Late Triassic that couldberelated to the period of Iran’s plate with Turansubduction andcollisionof event (the Middle and Late Triassic), Neotethys the Late Cimmerian to the tectonic activities of active continental could berelatedmargin. This the recycling provenance andtectonic setting of modal and geochemical the The analysis depicts slightly subarkose withthe medium-well sorting. show thattic deposits theyare sublitharenite and siliciclas open marine. Also, geochemical data of the tide-dominated delta and shallow partsof Qadir Member sediments inthe of deposition along with coalandcarbonate facies, all suggest Aboumaria, K., Zaghloul, M.N., Battaglia, M., improved ourmanuscript significantly. reviewers for their review and comments that would liketoacknowledge the two anonymous Boletín de la Sociedad Geológica Mexicana. We able from suggestions Dr. Ali Bahrami, editor of valu the for Thanks studies. field during facilities Parvadeh Coal Company (TPCCO) for providing (research code: 3/38412), Iran. We thank Tabas Geology, Mashhad Ferdowsiof University of M.S. thesisandwassupported by the Department the senior author’s researchThis represents part of ited inoxic environments. paleo-oxygenationwere these sandstones depos to semi-humidclimatic conditions. Also, basedon are sediments affected these gests semi-arid the by weatheringrather is whichmedium tohigh, sug chemical of coefficient The section. studied the igneous rocksfor and intermediate is sedimentary source rock geochemical data, thecombination of Microcontinent (CEIM). Also, according to the Tangier Peninsula Rif, Morocco): (Northern from marine formations the Quaternary of processes2009, Sedimentary andprovenance Loiacono, F., D., Puglisi, Aberkan,M.H., /73(1)A140920/2021 / 73(1)A140920/2021 27 27 - - - -

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