New Permian Aliyak and Kariz Now Formations, Alborz Basin, NE Iran: Correlation with the Zagros Mountains and Oman

GEOLOGICAL JOURNAL Geol. J. (2014) Published online in Wiley Online Library (wileyonlinelibrary.com). DOI: 10.1002/gj.2599

New Permian Aliyak and Kariz Now formations, Alborz Basin, NE Iran: correlation with the Zagros Mountains and Oman

SAKINEH AREFI FARD1* and VLADIMIR I. DAVYDOV2,3 1Geology and Geophysics Department, TAMU, College Station, Texas, USA 2Permian Research Institute, Department of Geosciences, BSU, Boise, Idaho, USA 3Kazan (Volgan region) Federal University, Kazan, Russia

Two new Permian-aged formations ‘Kariz Now Formation’ and ‘Aliyak Formation’ are proposed for a 65–150 m-thick succession in the Kariz Now area, with the type section for both (79.5 m thick) located 9 km northeast of Aliyak village ca. 100 km southeast of Mashhad city, northeastern Iran. The lower Kariz Now Formation is composed of siliciclastics. The age of this Formation is poorly constrained but its correlation with the Shah Zeid Formation in the Central Alborz suggests a possible Asselian-Hermagorian age for the Kariz Now Formation, which implies a hiatus of Yakhtashian–mid Midian (Artinskian–mid Capitanian) age between the siliciclastics of the Kariz Now Formation and carbonates of the disconformably overlying Aliyak Formation. There is also the possibility of a potential correlation of this Formation with the Kungurian Faraghan Formation in the Zagros area. The succeeding Aliyak Formation is mostly composed of carbonate rocks capped by a thin basaltic lava flow. The Aliyak Formation is unconformably overlain by dolostones that are correlated with the Middle Triassic Shotori Formation. Samples were collected from the Kariz Now and Aliyak formations, but fossils were only recovered from the Aliyak Formation. These include calcareous algae, small foraminiferans, fusulinids, crinoid stems and brachiopods. The recovered fusulinid assemblage from the Aliyak Formation is consistent with that of the upper Capitanian Monodiexodina kattaensis–Codonofusiella erki and Afghanella schencki–Sumatrina brevis zones of the Zagros Mountains and with the upper part of the Ruteh Fm in the Alborz Mountains. Although not radiometrically dated, the basaltic lava flow most probably corresponds to similar basaltic lava flows occurring in the uppermost part of the Ruteh Formation in Central Alborz. Thus, the Permian in the studied region developed in a basin that extended westward as far as the Central Alborz. A late Capitanian age for the Aliyak Formation implies it correlates with the Capitanian KS5 in Al Jabal Al-Akhdar in Oman, with Aliyak Unit 5 potentially representing the Permian maximum flooding surface MFS P25. Copyright © 2014 John Wiley & Sons, Ltd.

Received 17 May 2014; accepted 11 July 2014

KEY WORDS lithostratigraphy; fusulinids; taxonomy; biostratigraphy; palaeogeography; microfacies; depositional environment; northeastern Alborz; Iran

1. INTRODUCTION We have studied the succession in the Kariz Now area, located near the easternmost tectonic boundary of the Alborz The E–W-trending Alborz Mountains extends laterally for Terrane, with the Sabzevar, Farah and Turan terranes about 2000 km in northern Iran, from the lesser Caucasus (Fig. 1). It has been considered a part of the Alborz or of Armenia and Azerbaijan in the northwest, to the Sabsevar terranes (Alavi, 1991; Aghanabati, 1993, 2004) Paropamisus Mountains of northern Afghanistan to the located south of the Palaeotethys Suture. In this study, we east (Fig. 1). These mountains contain the tectono- describe the stratigraphy of the Permian deposits and pro- stratigraphic record of the Alborz Terrane, also known as pose a palaeogeographic model of this poorly known region the ‘Alborz Block’ or ‘NW Iran Terrane’ (Fig. 1; Sengör, within the context of the surrounding regions. 1990; Alavi, 1991, 1996; see review in Ruban et al., This paper focuses on the Permian deposits in the Kariz Now 2007). The Alborz Terrane lies at the intersection of several area, which we propose to divide into two lithostratigraphic regional tectonic sutures and its boundaries and palaeo- units: a lower siliciclastic unit named the Kariz Now Formation tectonic history are complicated (Afshar-Harb, 1970, and the upper carbonate unit named the Aliyak Formation. We 1994; Alavi Naeini, 1972; Berberian et al., 1996; Zanchi document for the first time the details of the sedimentary and et al., 2009). volcanic rocks and precise taxonomy of calcareous algae and foraminiferans recovered in the limestones of the Aliyak *Correspondence to: S. Arefifard, Geology and Geophysics Department, Formation, and compare them to those in the Central Alborz fi TAMU, College Station, TX, USA. E-mail: sare [email protected] Mountains, Zagros, Oman and other regions.

Figure 1. (a) Main tectono-stratigraphic units of Iran, Caucasus and Afghanistan (adapted from Alavi, 1991; Aghanabati, 1993; Bagheri and Stampﬂi, 2008). Ag = Aghdarband tectonic window; Bb = Band-e-Bayan; BFTB = Baluchestan Fold Thrust Belt; Bj = Birjand ophiolitic mélange; BM = Binalud Mountains; DF = Doruneh Fault; EO = Erevan-Ordoband; Fa = Fariman; GS = Gorgan Schist; Jm = Jazmouriam; Kr = Kermanshah ophiolite; Ma = Masouleh; MZT = Main Zagros thrust belt; Na = Nain Ophiolitic mélange; Nz = Neyriz ophiolite; Pb = Posht-e-Badam Terrane; PBB = Posht-e-Badam Block; Sz = Sabzevar zone; UD = Uromieh-Dokhtar volcanic belt; YB = Yazd Block. (b) Enlarged map showing location of the Aliyak section, Kariz Now area. This ﬁgure is available in colour online at wileyonlinelibrary.com/journal/gj

Copyright © 2014 John Wiley & Sons, Ltd. Geol. J. (2014) DOI: 10.1002/gj NEW LOWER AND MIDDLE PERMIAN FORMATIONS, NE IRAN 2. LITHOSTRATIGRAPHY OF THE ALIYAK AND Locality and type section: The type section of this Formation KARIZ NOW FORMATIONS is sandstone beds in the Aliak Section located at latitude 35° 19′45″N and longitude 60°03′37″E(Figs.1and2). The Permian deposits at the Aliyak section in the Kariz Now area begin with quartz sandstones and are followed by Lithology and thickness: ThethicknessoftheKarizNow carbonate deposits including limestone and dolostone, and Formation varies from northwest to southeast in the study area terminate with a thin basaltic lava flow. Based on the lithologic from 30 to 60 m. In the type section, it is 39 m thick and con- characteristics of these deposits and their stratigraphic sists of the following two units, from the base upwards (Fig. 3): relations, two lithostatigraphic units were recognized: the • Unit 1 (29 m thick) Red, medium-bedded (12–14), lower siliciclastic unit defined as the Kariz Now Formation medium- to coarse-grained quartz sandstone with and the upper carbonate unit defined as the Aliyak Formation. small-scale cross-bedding and laminations. • Unit 2 (10 m thick) Red to orange, medium-bedded (12–15), medium- to fine-grained quartz sandstone with carbonate 2.1. ‘Kariz Now Formation’ cement, small-scale cross-bedding and laminations. Name: The proposed ‘Kariz Now Formation’ is named after Lower boundary and underlying formation: In the the Kariz Now Village, located 151 km southeast of studied area, the Kariz Now Formation overlies an undiffer- Mashhad City (Figs. 1 and 2). entiated Proterozoic–Lower Cambrian unit with an angular

Figure 2. Geological map of the Kariz Now area exhibiting the main structural features. This ﬁgure is available in colour online at wileyonlinelibrary.com/journal/gj

Figure 3. Stratigraphic log of the Aliyak Formation in Aliyak Section, Kariz Now area, NE Iran with some key foraminiferal taxa, A = undifferentiated Soltanieh–Barut formations, B = Proterozoic–Lower Cambrian, Sh. = Shotori Formation, Tr. = Triassic. This ﬁgure is available in colour online at wileyonlinelibrary.com/journal/gj

unconformity boundary (Figs. 4a, 4b and 4c). In the Alborz micaceous shales of the Soltanieh Formation and the Lower area, this undifferentiated unit is divided into the Proterozoic– Cambrian cherty, stromatolite-bearing recrystallized dolostone Lower Cambrian thick-bedded to massive, cherty interbedded with micaceous shales of the Barut Formation stromatolite-bearing dolostone with a few intercalations of (Figs. 3 and 4).

Copyright © 2014 John Wiley & Sons, Ltd. Geol. J. (2014) DOI: 10.1002/gj NEW LOWER AND MIDDLE PERMIAN FORMATIONS, NE IRAN Lithology and thickness: The thickness of the Aliyak For- mation varies from northwest to southeast across the study area, from 35 to 90 m, based on the geological map report of the Kariz Now area (Boubee de Gramont et al., 1979). The maximum thickness (90 m) is an estimate in an area affected by structural complication. In the type section, it is 40.5 m thick and consists of the following seven units, from the base upwards (Fig. 3): • Unit 1 (1 m thick) Grey, medium-bedded sandy dolostone. • Unit 2 (11 m thick) Dark grey, medium-bedded partly crystallized limestone with small foraminiferans, algae, brachiopods, crinoid ossicles and ostracods. • Unit 3 (11 m thick) Grey, medium- to thick-bedded, medium to coarse crystalline dolostone. • Unit 4 (2 m thick) Grey, medium-bedded limestone (wackestone–packstone) with fusulinids, small foraminiferans, algae, crinoid stems and/or ossicles, and brachiopods (Fig. 3, sample K30). • Unit 5 (1 m thick) Grey, medium-bedded algal limestone (wackestone). • Unit 6 (14 m thick) Dark grey, medium- to thick- bedded medium crystalline dolostone. • Unit 7 (0.5 m thick, Fig. 4d) Dark green basaltic lava flow that laterally extends for 6 km. The thickness varies from 0.2 to 1.5 m. Lower boundary and underlying formation: In the studied area the Aliyak Formation has an unconformable contact Figure 4. Aliyak Section, Kariz Now area, NE Iran, outcrop details: (a) and with the Kariz Now Formation. (b) quartz sandstones of the Kariz Now Formation, carbonates of the Aliyak Formation and dolostones of the undifferentiated Soltanieh–Barut forma- Upper boundary and overlying formation: The Aliyak tions looking towards the west and east, respectively; (c) dolostone of the Formation is unconformably overlain by massive dolostones undifferentiated Soltanieh–Barut formations; (d) dark grey basaltic lava that are correlated to the Middle Triassic Shotori Formation flow at the top of the Aliyak Formation and overlying Triassic rocks of the Shotori Formation. This figure is available in colour online at as reported in the geologic map report of the Kariz Now wileyonlinelibrary.com/journal/gj (Boubee de Gramont et al., 1979).

Upper boundary and overlying formation: The contact of 3. MICROFACIES DESCRIPTION AND the Kariz Now Formation with the overlying Aliyak Formation INTERPRETATION is most probably disconformable. No biostratigraphic information is available to constrain the age of the Kariz Now Forma- A total of 42 thin sections were prepared from collected samples tion, but correlation of these siliciclastic units with their in the Aliyak section, Kariz Now area and studied for equivalent siliciclastics in Alborz, Zagros and east-central Iran microfacies analyses. The result of the petrographic studies suggests that there is no continuous succession between the and microfacies analyses was the recognition of 5 microfacies Kariz Now and the Aliyak formations. for the Kariz Now and Aliyak formations. These microfacies can be arranged into two palaeoenvironmental belts. These include tidal flat sediments (quartz sandstone, sandy dolo- 2.2. ‘Aliyak Formation’ mudstone, dolosparite) and lagoon sediments (bioclastic wackestone–packstone, algal wackestone, bioclastic fusulinid Name: The proposed ‘Aliyak Formation’ is named after packstone–grainstone). Aliyak Village, located 103 km southeast of Mashhad City (Figs. 1 and 2). 3.1. Tidal flat sediments Locality and type section: The type section is proposed at Aliyak Section where the type section of the underlying The tidal flat facies in the Aliyak Formation are composed of Kariz Now Formation is located (Figs. 1 and 2). quartz sandstone, sandy dolomudstone and dolosparite.

Copyright © 2014 John Wiley & Sons, Ltd. Geol. J. (2014) DOI: 10.1002/gj S. AREFI FARD AND V. I. DAVYDOV 3.1.1. Quartz sandstone dense; i.e. with no porosity. Medium- to fine-grained, mode- This facies is typified by red to orange, medium-bedded rate to well-sorted, sub-rounded to rounded mono-crystalline (12–15 cm thick), medium- to coarse-grained quartz arenite quartz grains represent about 10% to 15% of the rock. No relic with occasional lithoclasts (chert). Quartz grains occur as of the original fabric is present in this facies. The size of the monocrystalline with rare polycrystalline grains. Monocrystalline dolomite rhombs ranges between 5 and 16 μm(withamean quartz grains mainly show unit extinction. Quartz grains are gen- of 11 μm). This facies occurs in Unit 1 of the Aliyak erally moderately to well-sorted, rounded to sub-rounded and Formation in the studied section (Fig. 5d). show straight to concavo-convex grain contacts. Quartz grains form 90% of this facies. This facies encompasses units 1 and 2 3.1.3. Dolosparite of the Kariz Now Formation of the studied section (Fig. 5a). This facies consists of grey to dark grey, medium- to thick From the base to the top of this clastic unit, the sandstone cement beds (25–35 cm thick) and includes anhedral dolostone crys- changes, as it begins with siliceous overgrowth cement and then tals with non-planar faces which have a xenotopic fabric. changes to a carbonate cement (Figs. 5b, c). The size of the dolomite crystals ranges from 62 to 270 μm (with a mean of 170 μm). Although in some rare thin 3.1.2. Sandy dolomudstone sections relics of original allochems (including rare crinoid Grey, medium beds (14 cm thick) of dolostone are characteris- stems and brachiopod shell fragments) are present, the orig- tic for this facies in the field. Dolostone crystals are fully inal sedimentary textures in the dolosparites of the Aliyak Formation are not preserved in most cases. This facies is observed in units 3 and 6 of the Aliyak Formation of the studied section (Fig. 5e).

3.1.3.1. Interpretation. The dominance of monocrystalline quartz grains in quartz sandstone indicates that the sediments may have been derived from a granitic source (Basu et al., 1975; Suttner et al., 1981) or from older quartzitic deposits that were exposed as the result of the uplift in the interior part of the craton (Potter, 1986). According to preliminary petrographic evidence of these quartz sandstones, such as the absence of unstable grains (feldspars) and presence of well-rounded quartz grains, it can be suggested that recycling of sedimentary successions had led to the maturity of these sandstones. The high compositional and textural maturity in these quartz arenites, as well as cross-bedding and laminations indicate a high-energy depositional environment for this facies. Vertical grading of the quartz arenite to herringbone cross-bedding, and a vertical association of the clastic facies with carbonate tidal facies, point to sedimentation in a shallow supratidal to an upper intertidal environment. Considering the texture and size of crystals in dolomudstones and the presence of more than 10% to 15% quartz grains, the dolostones of the Aliyak Formation were formed under near-surface low temperature conditions (Gregg and Shelton, 1990; Hopkins, 2004; Machel, 2004). The absence of skeletal grains and the presence of quartz grains imply a landward position of this facies. The dolosparites probably formed at relatively high temperatures (80–120 °C) (see Narkiewicz, 2009) and replace limestones Figure 5. Photomicrographs of facies types of the Kariz Now Formation (a–c) and Aliyak Formation (d–h): (a) quartz sandstone, sample K-1; (Gregg, 1988; Gregg and Shelton, 1990; Dorobek et al., (b and c) carbonate-cemented quartz sandstone, samples K-7, K-11; (d)sandy 1993; Reinhold, 1998). Based on the presence of scattered dolomudstone, sample K-15; (e) dolosparite, sample K-26; (f) bioclastic – quartz grains and rare relics of skeletal grains, as well as wackestone packstone, sample K-17; (g) algal wackestone, sample K-31; ﬂ (h) bioclastic fusulinid packstone–grainstone, sample K-30. This ﬁgure is its position below lagoonal facies, a tidal at setting is likely available in colour online at wileyonlinelibrary.com/journal/gj for this facies.

Copyright © 2014 John Wiley & Sons, Ltd. Geol. J. (2014) DOI: 10.1002/gj NEW LOWER AND MIDDLE PERMIAN FORMATIONS, NE IRAN 3.2. Lagoonal sediments sedimentation in a shallow supratidal to an upper intertidal environment. In these sandstones as the rate of siliciclastic input The lagoonal sedimentary deposits are composed of a bioclastic in the depositional environment decreased, and conditions for fusulinid packstone–grainstone and an algal wackestone. the deposition of the carbonates increased, carbonate cement replaced siliceous overgrowth cement between quartz grains. – 3.2.1. Bioclastic wackestone packstone According to the microfacies distribution of the Aliyak For- – This facies contains dark grey, medium-bedded (15 17 cm mation in the Kariz Now area, the inner portion of a thick) limestones with skeletal grains including small fora- homoclinal ramp (Read, 1985; Einsele, 1992; Burchette and miniferans (Agathammina, Hemigordius and Baisalina), Wright, 1992; Ahr, 1998) is suggested for its depositional en- dasycladacean algae, brachiopods, crinoid stems and ostra- vironment. The inner ramp comprises the zone above the fair- cods. There is quartz, which is a minor allochem (less than weather wave-base (FWWB). Inner ramp lagoon and sabkha 5% presence). Recrystallization is observable in some skele- deposits comprise evaporites and a wide range of mud-, tal grains. Allochems were cemented by micrite and have wacke- and packstone with a restricted faunal spectrum partially micritized boundaries. This facies occurs in Unit 2 (Burchette and Wright, 1992). The Aliyak Formation is com- of the Aliyak Formation of the studied section (Fig. 5f). posed of five lithofacies types. The tidal flat facies shows rare bioclastic allochems suggestive of the restricted environment 3.2.2. Algal wackestone during the deposition of sandy dolomudstones and – Grey, medium beds (12 13 cm thick) mark this facies in the dolosparites. As sea level rose it increased carbonate input. fi eld. This mud-rich microfacies includes only gymno- The transgressive carbonate facies is composed of bioclastic codiacean algae which are cemented by micrite. The algal wackestone–packstone, algal wackestone and bioclastic fusuli- grains are relatively intact. This facies occurs in Unit 5 of nid wackestone–packstone representing restricted and semi- the Aliyak Formation of the studied section (Fig. 5g). restricted lagoonal environments.

3.2.3. Bioclastic fusulinid packstone–grainstone This facies is composed of grey, medium-bedded (14–16 cm 5. BIOSTRATIGRAPHY OF THE ALIYAK thick) limestones and includes diverse fauna dominated by FORMATION fusulinids, brachiopods, crinoid stems/ossicles, dasyclad algae and small foraminiferans. Peloids represent a minor We collected and studied 27 samples from the Aliyak constituent. This facies is observed in Unit 4 of the Aliyak Formation in the Aliyak Section (Fig. 3). The fossil content Formation of the studied section (Fig. 5h). in the Aliyak Formation includes calcareous algae (samples K-16, K-27, K-30 and K-31), small foraminiferans (samples 3.2.3.1. Interpretation. The bioclastic wackestone–packstone K-16, K-20 and K-30), fusulinids (sample K-30), brachio- was deposited in a lagoonal environment that was protected pods and crinoid stems. The fusulinid fauna was recovered from the waves. Shallow near-shore and lagoonal environ- from only one stratigraphic level at 64 m above the base of ments down to a depth of 50 m are characterized by miliolid the section. The fusulinid-bearing bed is a bioclastic foraminifers (Flügel, 2010). The relatively low diversity of packstone–grainstone that yielded 26 algal, fusulinid and normal marine fauna and the high proportion of micritic small foraminiferan taxa, recovered from 61 thin-sections mud of the algal wackestone suggest that deposition was identified at generic and species level. The thin sections con- in a quiet water and lagoonal environment (Nichols, taining the figured specimens of fusulinids, algae and small 1999). During the Late Permian, gymnocodiaceans were foraminiferans are housed in the University of Iowa Paleon- important sediment producers in shallow, low to moderate tology Repository, USA (collection SUI 132563-132613). energetic shelf seas (Flügel, 2010). The coarse grain size For the chronostratigraphy, we have adopted in this paper and relatively high biodiversity in bioclastic fusulinid the Tethyan Time Scale, as it is the most applicable to the wackestone–packstone indicate that it was deposited mainly study area, and also shows the approximate correlation to in a sheltered lagoonal environment near shoals with an the Global Time Scale (Wardlaw et al., 2005). The identified open marine circulation under low to moderate energy. algae, small foraminiferans and fusulinids are shown in Figs. 6 and 7.

4. DEPOSITIONAL MODEL 5.1. Calcareous algae The depositional setting of the Kariz Now Formation can be Dacycladacean and gymnocodiacean algae found in the described as a shoreline. The only lithofacies recognized in Aliyak Formation (samples K16, K27, K30 and K31) this Formation is quartz sandstone that represents include Epimastopora sp. (Figs. 6.1 and 6.2), Mizzia sp.

Figure 7. Fusulinids from the Kariz Now Formation, Aliyak Section, Kariz Figure 6. Middle Permian fusulinids, small foraminiferans and calcareous Now area, NE Iran. (1) Pseudokahlerina implexa Sosnina, 1968, ×0.1, K30- algae from the Aliyak Section in Kariz Now area. The collection stored in 25a, SUI 132591; (2-3) Pseudokahlerina sp., ×0.1, (2) K30-52a, SUI the University of Iowa Paleontology Repository (SUI); (1–2) Epimastopora 132592, (3) K30-48b, SUI 132593; (4) Kahlerina sp., ×1, K30-24a, SUI sp., ×0.5, (1) K30-40b, SUI 132562, (2) K30-28a, SUI 132563; (3-5) Mizzia 132594; (5–6) Dunbarula sp., ×0.1, (5) K30-28a, SUI 132595, (6) K30- sp., ×1, (3) K30-34a, SUI 132564, (4) K30-26a, SUI 132565, (5) K30-6a, 47a, SUI 132596; (7–8) Dunbarula kitakamiensis Choi, 1970, (7) ×0.5, SUI 132566; (6) Pseudovermiporella? sp., ×0.5, K30-40a, SUI 132567; K30-56a, SUI 132597, (8) ×0.1, K30-48c, SUI 132598; (9–10) Ogbinella (7) Permocalculus sp., ×1, K31-1, SUI 132568; (8 and 9) Gymnocodium avushensis (Chedija)(in Kotlyar et al., 1983), (9) ×0.5, K30-26b, SUI sp., ×0.2, (8) K-16-12, SUI 132569, (9) K-16-8, SUI 132570; (10) 132599, (10) ×1, K30-27a, SUI 1322600; (11) Toriyamaia laxiseptata Permocalculus? sp., ×1, K-27-1, SUI 132571; (11–12 and 21) Kanmera, 1956, ×1, K30-7a, SUI 132601; (12–16) Codonofusiella erki Globivalvulina sp., (11) ×0.5, K-20-1, SUI 132572, (12) ×0.1, K-16-9, Rauser-Chernousova, 1965, ×0.5, (12) K30-56b, SUI 132602, (13) ×01, SUI 132573, (21) ×0.1, K-30-40c, SUI 132582; (13–15) Agathammina K30-23, SUI 132603, (14) ×0.5, K30-25a, SUI 132604, (15) ×0.5, sp., (13) ×0.1, K-16-1, SUI 132574, (14) ×0.1, K-30-42a, SUI 132575, K30-42b, SUI 132605, (16) ×0.5, K-30-2a, SUI 132606; (17–18) (15) ×0.5, K-30-58a, SUI 132576; (16) Pseudomidiella sp., ×0.1 K-16-2, Pseudodunbarula dzhagadzurensis (Chedija, 1983), (17) ×0.5, K-30-47a, SUI 132577; (17) Hemigordius planus Pronina, 1988, ×0.1, K-30-16-1- SUI 132607, (18) K-30-23b, SUI 132608; (19–22) Verbeekina heimi 2a, SUI 132578; (18) Hemigordius sp., ×0.1, K-16-1-1, SUI 132579; (19 Thompson and Foster, 1937, ×1, (19) K30-6a, SUI 132609, (20) K30-20a, and 20) Tansilites? sp., (19) 0.1 K-16-6, SUI 132580, (20) ×0.1, K-16-11, SUI 132610, (21) K30-34a, SUI 132611, (22) K30-55a, SUI 132612; SUI 132581; (22 and 23) Baisalina pulchra Reitlinger, 1965, ×0.1, (22) (23–24) Sumatrina annae Volz, 1904, ×1, K30-44a, SUI 132613. This K30-48a, SUI 132583, (23) K30-5b, SUI 132584; (24) Postendothyra sp., figure is available in colour online at wileyonlinelibrary.com/journal/gj ×0.1, K30-40, SUI 132585; (25–28) Staffella suborientalis Rozovskaya, 1963, ×0.5, (25) K30-55a, SUI 132586, (26) K30-14a, SUI 132587, (27) K30-43a, SUI 132588, (28) ×1, K-30-4a, SUI 132589; (29) Langella sp., 5.2. Small foraminiferans ×0.1, K-30-2-2a, SUI 132590. This figure is available in colour online at wileyonlinelibrary.com/journal/gj The small foraminiferans in the Aliyak Formation are relatively few compared to the Central Alborz and Zagros regions (Gaetani et al., 2009; Davydov and Arefifard, 2013). – (Figs. 6.3 6.5), Pseudovermiporella? sp. (Fig. 6.6), The eight genera are Globivalvulina (Figs. 6.11, 6.12 Permocalculus sp. (Fig. 6.7), Permocalculus? sp. (Fig. 6.10), and 6.21), Agathammina (Figs. 6.13–6.15), Pseudomidiella and Gymnocodium sp. (Figs. 6.8 and 6.9). The depth range (Fig. 6.16), Hemigordius (Figs. 6.17 and 6.18), Tansilites? of dacycladacean algae normally extends from just below (Figs. 6.19 and 6.20), Baisalina (Figs. 6.22–6.23), Postendothyra low tide to about 30 m (Wray, 1977). Gymnocodiaceans (Fig.6.24),andLangella (Fig. 6.29). The stratigraphic distribu- are often associated with dasycladaceans and presumably tion of important species of small foraminiferans and fusulinids occupied a similar shelfal environment (Elliott, 1958). are described below.

Copyright © 2014 John Wiley & Sons, Ltd. Geol. J. (2014) DOI: 10.1002/gj NEW LOWER AND MIDDLE PERMIAN FORMATIONS, NE IRAN Baisalina pulchra Reitlinger, 1965 (p. 65, pl. 1, Figs. 15–18) was Ogbinella avushensis (Chedija) (in Kotlyar et al., 1983, identified in sample K30. This species has been reported from the p. 130–131, pl. 2, Figs. 4–6) is known from the upper Hemigordius–Discospirella assemblage zone in the Permian suc- Midian–Dzhulfian (Capitanian–Wuchiapingian) in NE Iran cessions in NW Iran (Shabanian et al., 2006), in the Midian lime- and Transcaucasia. The studied material consists of one stoneinCrimea(Kotlyaret al., 1989), in Upper Permain subaxial and one axial section (Figs. 7.9 and 7.10). carbonates of Saudi Arabia (Hughes, 2009), and in the Derbent Limestone in Turkey (Turhan et al., 2004). It is suggestive of a Toriyamaia laxiseptata Kanmera, 1956 (p. 252–255, pl. 36, Midian (late Wordian–Capitanian) age. The studied material con- Figs. 1–14) was first described from uppermost Permian sists of one subaxial and one axial section (Figs. 6.22 and 6.23). limestone in Japan. It is also known to occur in the lower Yakhtashian (Artinskian–lower Kungurian) Motomura Hemigordius planus Pronina, 1988 (p. 55–56, Fig. 2.10): The Formation of Japan (Ueno, 1992), Yakhtashian–Bolorian beds below and above the fusulinid-bearing horizon in the Aliyak (Artinskian–Kungurian) of south Afghanistan (Leven, 1997), Formation Section are dolostone and dolomitic limestone that Kubergandian (lower Roadian) of north Afghanistan (Leven, only bear remnants of brachiopods and crinoid stems. In one 1997), and Yakhtashian–Bolorian (Artinskian–Kungurian) sample (K16), rare smaller foraminifers occur, for instance Bagh-e Vang Formation in east-central Iran (Leven and Vaziri Hemigordius sp. and Hemigordius planus Pronina. The latter Moghaddam, 2004). The studied material consists one subaxial species is also known from the Transcaucasus and indicates a section (Fig. 7.11). Guadalupian (middle Permian) age. The studied material consists Codonofusiella erki Rauser-Chernousova, 1965 was of one axial section (Fig. 6.17). described from lower Dzhulfian (lower Wuchiapingian) in Postendothyra sp. was described from upper Maokou in Guangxi, Transcaucasia (Rosovskaya and Rauser-Chernouzova, 1965, S. China (Lin, 1984) and from the Yabeina globosa Zone in the p. 141–142, pl. 3, Figs. 16 and 17; pl. 5, Figs. 3–5), and the Kaize, Central Japan (Kobayashi, 2006). It is also reported from Midian (upper Wordian–Capitanian) limestone (Unit 6) in Khoja the top of KS6 in Oman (Forke et al., 2012) (Fig. 6.24). Murod in south Afghanistan (Leven, 1997). It has also been recovered from the upper Midian (Capitanian) Monodiexodina 5.3. Fusulinids kattaensis Biozone in the Il-e Beyk section in the Zard Kuh Staffella suborientalis Rozovskaya, 1963 (p. 137, pl. 1, Figs. 6 area, Iran (Davydov and Arefifard, 2013), in the Sa’ad and and 7) is known from the Guadalupian (Middle Permian) in Arqov formations in the Levant (Orlov-Labkovsky, 2004), NE Iran, Afghanistan (Leven, 1997) and South China (Sheng, and from the sixth fusulinid assemblage zone in the Crimea 1956). The studied material consists of several nearly axial limestone of probable Dzhulfian (Wuchiapingian) age (Kotlyar sections (Figs. 6.25–6.28). et al., 1999). The studied material consists of five subaxial sections (Figs. 7.12 to 7.16). Dunbarula kitakamiensis Choi, 1970 (p. 314–316, pl. 8, Figs. 1–6) was originally described from the Midian (upper Pseudodunbarula dzhagadzurensis (Chedija) (in Kotlyar Wordian–Capitanian) uppermost portion of limestone of the et al., 1983, p. 133–134, pl. 5, Figs. 7, 10, 14–16, 18) is southern Kitakami Mountains, northeast Japan. It was later known from the upper Midian–Dzhulfian (Capitanian– reported from the upper Midian (Capitanian) Lepidolina Wuchiapingian) of NE Iran and the Transcaucasus. The multiseptata Zone in the Kitakami Mountains, Japan (Minato studied material consists of one oblique and one subaxial et al., 1978), and from the Midian (upper Wordian–Capitanian) section (Figs. 7.17 and 7.18). in central and northern Afghanistan (Leven, 1997). The studied material consists of two axial sections of Dunbarula Verbeekina heimi Thompson and Foster, 1937 (p. 137, kitakamiensis Choi (Figs. 7.7 and 7.8) and Dunbarula sp. pl. 23, Figs. 1–3; pl. 24, Fig. 4; pl. 25, Figs. 5 and 6) is (Figs. 7.5 and 7.6). one of the most age-diagnostic species recovered in the section and it was originally described from the upper part Pseudokahlerina implexa Sosnina, 1968 (in B.P. Markovski, of the Middle Permian Yanghshin Limestone in Sichuan, p. 107, pl. 26, Figs. 1 and 2) is known in NE Iran and eastern China. This species is also reported from Middle Permian Russia. It is indicative of the Midian (upper Wordian–Capitanian). limestones in Chios, Greece (Kahler, 1987), from the middle The studied material consists of one axial section (Fig. 7.1). to upper Murgabian (lower Wordian) Afghanella schencki Zone in the Surmaq Formation in Abadeh, Iran (Kobayashi Pseudokahlerina sp. It has been reported from Midian lime- and Ishii, 2003), and Murgabian (upper Roadian–lower stones of Bulola, zone of Bamian, North Afghanistan (Leven, Wordian) Verbeekina heimi Sub-Zone in the Akiyoshi lime- 1997) and also Midian carbonates in the Western Sakarya Com- stones in Japan (Minato et al., 1978). posite Terrane, Geyve Area, Turkey (Turhan et al. 2004). The In the Yangshin limestones of China, Verbeekina heimi studied material consists of two axial sections (Figs. 7.2 and 7.3). Thompson and Foster is associated with Sumatrina annae

Copyright © 2014 John Wiley & Sons, Ltd. Geol. J. (2014) DOI: 10.1002/gj S. AREFI FARD AND V. I. DAVYDOV Volz, Schubertella simplex Lange and Schwagerina sp. (Gaetani et al., 2009). It was considered (Gaetani et al., 2009) (Thompson and Foster, 1937). In the Afghanella schencki that these taxa broadly indicate an Asselian-Hermagorian age. Zone in Abadeh other fusulinid species such as Afghanella No biostratigraphic information is available to constrain sumatrinaeformis (Gubler), Sumatrina annae Volz, Skinnerella the age of the Kariz Now Formation. abadehensis Kobayashi and Ishii and Parafusulina tarazi Because of its palaeogeographic position within the same Kobayashi and Ishii, along with Verbeekina heimi Thompson basin as Alborz, the Kariz Now most probably correlates and Foster have been reported (Kobayashi and Ishii, 2003). with Shah Zeid in Central Alborz. This correlation suggests Afghanella schencki Thompson has been found from the upper a disconformity between the Kariz Now and Aliyak Midian (Capitanian) in the Zagros region (Davydov and formations that corresponds to the interval between the Areﬁfard, 2013) and was also recovered from the Akiyoshi Yakhtashian- to mid Midian (Artinskian to mid Capitanian). Limestone as one of the associations of Verbeekina heimi Alternatively, the Kariz Now Formation could be a lateral (Minato et al., 1978). The studied material consists of three equivalent of the lower part of the Ruteh Formation, imply- parallel sections and one subaxial section (Figs. 7.19 to 7.22). ing that it is of Murgabian (Upper Roadian–Upper Wordian) age and correlates with KS6 (Khuff sequence 6, the Middle Sumatrina annae Volz, 1904 (p. 182, Fig. 28) is widespread Permian to Lower Triassic Khuff Formation in the Arabian in the upper Neoschwagerina to Yabeina Zone of China and Platform and its time equivalent, the Saiq Formation and Japan (Ozawa, 1925; Chen, 1956; Xiao et al., 1986; Leven, the lower part of the Mahil Formation in Oman can be 1993), and in the upper Murgabian–Midian (Wordian– subdivided into six or seven third-order sequences). In Capitanian) strata of NE Iran, Turkey and Afghanistan addition, a possible correlation of the Kariz Now Formation (Kahler and Kahler, 1979; Leven, 1997; Kobayashi and with the Kungurian Faraghan Formation (Fig. 8) in the Ishii, 2003). It has recently been reported from the Midian Zagros region (Ghavidal-Syooki, 1988, 1993) implies a (upper Wordian–Capitanian) limestone of the southern disconformity between the Kariz Now and Aliyak formations Baoshan Block, China (Huang et al., 2009). Sumatrina annae and the existence of a hiatus of Kubergandian to mid Midian Volz is widely known from upper Murgabian–Midian (Roadian to mid Capitanian) age. (Wordian–Capitanian) of the entire Tethys (Volz, 1904; Further studies in regard to the dating of the Kariz Now Minato et al., 1978; Leven, 1997; Kobayashi and Ishii, Formation and sedimentological analyses to determine the 2003; Turhan et al., 2004). The studied material consists of provenance of these sandstones are necessary to fully under- one subaxial section (Figs. 7.23 and 7.24). stand the geologic history of this important region.

6.2. Aliyak carbonates: Units 1 to 6 6. CORRELATIONS OF THE ALIYAK AND KARIZ Gaetani et al. (2009) presented a comprehensive study of the NOW FORMATIONS Pennsylvanian (late Carboniferous) to Early Triassic formations in the outcrops of the Central Alborz Mountains 6.1. Kariz Now Formation: Units 1 and 2 between 51°E and 55°E (Fig. 1). The Guadalupian (middle Our studies suggest close proximity of the Permian deposits Permian) is represented by the Ruteh Limestone Formation in the Kariz Now region with Permian successions in Central (Assereto, 1963) (Figs. 8 and 9). It consists of a relatively Alborz (Fig. 8). In the latter region, the Ruteh Formation uniform blanket of packstones and wackestones, typically overlies the uppermost Carboniferous (Gzhelian) and Lower 150–250 m thick, and attains a thickness of 300–600 m near Permian (Asselian-Hermagorian) Dorud Group. The Group the Caspian Sea (Sussli, 1976; Gaetani et al., 2009). Crippa is divided, from the base-up, into the Toyeh, Emarat, and Angiolini (2012) documented the brachiopod fauna of Ghosnavi and Shah Zeid formations (Gaetani et al., 2009). the Ruteh Formation and concluded that the formation is The youngest Shah Zeid Formation is of particular interest Wordian–Capitanian (late Murgabian–Midian). The Ruteh as a possible correlative to the Kariz Now Formation. It Formation thus correlates with Guadalupian KS6 and KS5 consists mainly of reddish, whitish and vari-coloured in: (1) the lower part of the Dalan Formation in the Il-e Beyk siliciclastics that overlie the carbonates of the Ghosnavi Section in the High Zagros (Davydov and Areﬁfard, 2013), Formation. The siliciclastics attain a thickness of 97.5 m at and (2) the Wordian–Capitanian limestones of the upper part the Dorud locality, and exceed 160 m at the Emarat section. of the Saiq Formation in Al-Jabal al-Akhdar, Oman In the latter area, the topmost white quartz-arenites include (Koehrer et al., 2010; Al-Husseini and Koehrer, 2013). dark-grey mudstones, 10 m-thick, and contain a small Gaetani et al. (2009) noted that fusulinids are scarce in the brachiopod fauna including Acosarina aff. juresanensis Ruteh Formation whereas small foraminiferans are common, (Chernyshev) and Cancrinella cancriniformis (Chernyshev). in contrast to our observations in the studied region. In the Talar At Dorud, only Neochonetes (Neochonetes) sp. is present Rud and Qezelqaleh sections in Central Alborz (Fig. 10), the

Figure 8. Correlation of Guadalupian and Lopingian (middle and upper Permian) sections in Iran. Tabas Block (Leven and Vaziri Moghaddam, 2004), Central Alborz (Gaetani et al., 2009), Kariz Now (this study), Zagros (Davydov and Arefifard, 2013), northeast Oman (Koehrer et al., 2010; Forke et al., 2012). upper part of the Ruteh Formation yielded upper Murgabian– and Afghanella schencki–Sumatrina brevis zones of the Midian (Wordian–Capitanian) Chusenella padangensis Zagros region of late Capitanian age (Davydov and (Lange) together with Yangchienia haydeni Thompson. In other Arefifard, 2013). This assignment implies a correlation of Alborz sections of the Ruteh Formation, fusulinids such as the carbonates of the Aliyak Formation to upper KS5 Schubertella sp., Minojapanella sp., Codonofusiella sp., (MFS P25) in the High Zagros (Davydov and Arefifard, Nankinella sp. and Staffella sp. were also reported (Gaetani 2013) and in Al-Jabal al-Akhdar in Oman (Koehrer et al., et al., 2009). The presence of Yangchienia hydeni and 2010; Al-Husseini and Koehrer, 2013). Codonofusiella sp. definitely establishes a Midian age for the The fusulinid assemblages in the Ruteh Formation in the formation (Kotlyar et al., 1989; Leven, 1998). Central Alborz generally differ from those in the Aliyak The fusulinid assemblage recovered from sample K30 in Formation. Just a few taxa are common, such as Unit 5 of the Aliyak Formation is consistent with an assign- Minojapanella sp., Codonofusiella sp., advanced Yangchienia ment to the Monodiexodina kattaensis–Codonofusiella erki and rare staffellids. The dissimilarity may be due to significant

Figure 9. Middle to Late Permian stratigraphic correlation from Central and Eastern Alborz to Kariz Now along a NW–NE transect, emphasizing the difference between lithological units of the Ruteh and Aliyak formations. Green line indicates the rifting event that has been evidenced by basaltic lava flows in both the Alborz and Kariz Now regions. See Fig. 3 for explanation of facies. Vertical lines indicate a hiatus. This figure is available in colour online at wileyonlinelibrary. com/journal/gj variations in palaeobathymetry and/or palaeoenvironment flooding interval, potentially denoted as Permian MFS P25 across the Alborz region (Fig. 9). The depositional setting of (Sharland et al., 2004) in Al-Jabal al-Akhdar in Oman the Ruteh Formation was deeper water, as reflected by its (Koehrer et al., 2012; Al-Husseini and Koehrer, 2013). micritic to wackestone facies, and includes sparse colonial ThelateMurgabian–Midian (Wordian–Capitanian) Ruteh rugose corals in life position (Gaetani et al.,2009).The carbonates in Central Alborz may therefore represent a deeper-water setting may have been associated with colder more complete succession with a longer duration than that temperatures, which would explain the poor occurrence of of the relatively thin upper Capitanian carbonates of the fusulinids. In contrast, the Aliyak Formation was deposited Aliyak Formation. The carbonates underlying and overly- in shallow and warmer waters as indicated by abundant fusu- ing Aliyak Unit 5 are not dated but are probably of linids. Lithologically, the Aliyak Formation is composed Guadalupian (middle Permian) age based on their strati- mainly of limestone, dolostone and dolomitic limestones with graphic position and regional correlation with the Ruteh a few beds of fusulinid-bearing packstone–grainstone near its Formation in the Central Alborz Mountains. upper part. This kind of lithology has not been reported for the Ruteh Formation in any of its known exposures from the 6.3. Aliyak basaltic lava flows: Unit 7 Alborz area (Fig. 10). Another possible difference between the Ruteh and In the area to the north of the Elika–Nesen Belt in the Alborz Aliyak formations may be related to the chronostratigraphic Mountains (Figs. 9 and 10), tuffaceous layers and basaltic range of the Guadalupian (middle Permian) transgression in lava flows are intercalated with sedimentary rocks in the northern Iran. The deposition of the Ruteh Formation may uppermost part of the Ruteh Formation, have started earlier in the Central Alborz with KS6 biostratigraphically dated as late Midian (Capitanian) (Wordian third-order sequence in the upper part of the Saiq (Gaetani et al., 2009). The basaltic lava rocks are up to Formation). In contrast, the late Capitanian Aliyak Forma- 150 m thick and become much thinner eastwards. They oc- tion may only correlate with upper KS5 (Capitanian third- cur above Unit 5 of this formation. However, it seems that order sequence in the upper part of the Saiq Formation). they occupy the same stratigraphic position as basaltic lava Aliyak Unit 5 may correspond to a Capitanian maximum flows in Central Alborz. The basaltic lava flows (Unit 7) in

Figure 10. Middle Permian palaeogeographic map for Central Alborz and most eastern extensions of the Alborz Terrane showing localities with recorded Wordian–Capitanian Ruteh and Aliyak formations outcrops (adopted from Gaetani et al., 2009, with some modifications), Do = Dorud; El-Ne = Elika–Nesen; Qe = Qezelqaleh; Ru = Ruteh; TaR = Talar Rud. Enlarged map (zoom-in) shows the NE-part of the NW-Iran Terrane (modified from Ruban et al., 2007, Fig. 11). This figure is available in colour online at wileyonlinelibrary.com/journal/gj

Kariz Now may therefore be latest Capitanian, based on displacement in the Late Permian–Early Triassic. The correlation with basaltic lava flows in the Central Alborz large flood basalts are also reported from the top of the Mountains. Correlation of the Ruteh and Aliyak volcanics Capitanian Maokou Formation in Sichuan province and implies a regional latest Guadalupian tectonic event considered as a possible factor in the extinction event of extended along the northern margin of the Alborz Terrane, the end-Guadalupian (Lai et al., 2008). More investigations possibly related to rifting of the Iranian terranes across the are needed to understand the main cause of these basaltic Palaeotethys Ocean (Muttoni et al., 2009; Fig. 9). lava flows. Precisely constraining the age of the basaltic lava flows will require radiometric dating. However, in previous works it has been mentioned that the Iranian microplate 7. LATE PERMIAN–EARLY TRIASSIC HIATUS AT was already drifting far from Gondwana prior to the KARIZ NOW Capitanian (Muttoni et al., 2009; Gaetani et al., 2009). Recently, Angiolini et al. (2013) in their palaeogeographic In the Central Alborz Mountains, above the Ruteh Forma- reconstruction and interpretation of the mid-Permian tion, the Lopingian (upper Permian) is represented by the successions suggested that Iran seems to have not moved continental sediments of the Qeshlaq Formation to the east much in the Middle Permian relative to its large and southeast, and limestones and shales of the Nesen

Copyright © 2014 John Wiley & Sons, Ltd. Geol. J. (2014) DOI: 10.1002/gj S. AREFI FARD AND V. I. DAVYDOV Formation to the northwest (Gaetani et al., 2009; Fig. 9). In were parts of the same large basin that extended at least from the type area, near Bear Gully, the Nesen Formation is Central Alborz in the west to the Kariz Now region in the east. nearly 130 m thick. The lower part of the formation consists The basaltic lava ﬂows in both regions probably indicate a widely of shale interbedded with marly limestone, ca.70mthick, exhibited rifting event near the post-Capitanian tectonic event. and the upper part is dominantly bioclastic wackestone (Gaetani et al., 2009). The formation thins towards the south. The Qeshlaq Formation consists of arenite and ACKNOWLEDGEMENTS siltstone, and attains a maximum thickness of approxi- mately 80 m. The Qeshlaq and Nesen formations are over- We acknowledge the support of the U.S. National Science lain by the Lower and Middle Triassic Elika Formation, Foundation grants EAR-1004079 and EAR-0746107. which consists of alternating limestone, dolostone and do- We deeply appreciate the input of Dr Al-Husseini who pro- lomitic limestone. In the Kariz Now area, the uppermost vided important references and made many valuable com- Capitanian is overlain by the Middle Triassic Shotori For- ments and suggestions. We are indebted to Dr Thomas mation, and the hiatus between these two formations corre- Olszewski for discussing stratigraphic problems in Iran and sponds to the Lopingian (Late Permian) and Early Triassic for improving the English in our manuscript. The authors and correlates to the Nesen and Qeshlaq formations in the thank the reviewers Dr Lucia Angiolini and Dr Daniel Central Alborz. Vachard for their constructive comments on this paper. Fur- ther, we wish to thank editor Prof. Ian D. Somerville for the very careful editing of the ﬁnal draft. 8. CONCLUSIONS

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