I I

Policy Making Committee of the 4th YES Congress

Patronage: Mohammad Taghi Korehie

Members: (In alphabetic order)

Hamid Ashtari Bita Mirzapour

Marziyeh Esterabi Ashtiani Ali Najafi

Manouchehr Ghorashi

Raziyeh Lak

Local Organizing Committee of the 4th YES Congress

Local Organizing Committee

Chairperson: Marziyeh Esterabi Ashtiani

Members: (In alphabetic order)

Khatereh Aligholizadeh Hatam Sedigheh Jadavi

Mina Birjandi Zahra

Saba Dashti Chandanagh Amir Mohammad Mahboubi

Najmeh Davari Maryam Mehrdadian

Parvin Esmaili Marziyeh Rostami

Masoumeh Namvar Zeinab Sharifi Esmaili

Reyhaneh Fazli Mojgan Yaghoubi

Somayeh Habibi

Maryam Heidarian

Field Itinerary*

Day 1 (Tuesday, Aug. 29) Time Title 8:30 Moving to 14:30 Lunch in Kashan city 15:30 Tour in Kashan city

Day 2 (Wedneday Aug. 30) Approximate Activity time 10:00 Visiting the Permian-Triassic boundary beds, North of Shahreza 12:30 Lunch in city 15:00 Tour in Isfahan city

Day 3 (Thuesday Aug. 31) Approximate time Activity Solenoporacean algae Late Triassic warm water reefs, Disconformity (Late Devonian/ 8:25-12:00 Late Permian event), Angular unconformity ( Early Jurassic/Early Cretaceous movements)

2:00 Lunch in Mahalat 13:00 Moving to Tehran and Visiting the Qom Formation 17:30 Arriving in Tehran * Please note: Everyday wakeup time is 7:00 A.M., breakfast starts at 7:20 A.M., and departure for the field is at 8:00 A.M.

sponsors

Fig. 1: Tectonic map of showing geological provinces, ophiolites and faults

Geological Framework

The present day geological features of the Iranian plateau have developed through a long history of western Asian Tethyan realm, which may be summarized in the following stages:

1. Late Proterozoic consolidation and peneplanization of the basement in northern margin of Gondwana.

2. Deposition of Latest Neoproterozoic to Permian epicontinental rocks of predominantly sedimentary nature.

3. Separation and drifting of Cimmerian blocks from northern margin of Gondwana and their collision to the southern margin of Eurasia across the Tethys Ocean. This stage spanned in time between Late Permian to Late Triassic, and resulted in development of Neotethys, closure of the Paleotethys, and the Cimmerian orogeny.

4. Northeastward subduction of Neotethys under the Central Iran, and development of the Sanandaj-Sirjan metamorphic-magmatic belt as an active continental margin of the Central Iran between Jurassic and Cretaceous.

5. Ophiolite obduction on the passive margin of the Arabian plate and around the Central Iranian terranes, and magmatic arc and backarc development along the Urmia-Dokhtar belt during Late Cretaceous to Paleogene times.

6. Closure of the Neotethys Ocean and Zagros orogeny during Paleogene and Neogene times, and growth of the Iranian plateau.

Permian-Triassic boundary beds (transition from Paleozoic to Mesozoic)

Fig. 2: Satellite view of outcrop and field photographs of the Permian-Triassic boundary beds to the N of Shahreza.

Permian-Triassic boundary beds in Shahreza section

The -Shahreza region is well-known for their classic Permian-Triassic outcrops. Particularly the Abadeh section on the northern flank of the Hambast Mountain, about 60 km SW of Abadeh town and the Shahreza section, about 14 km NNE of Shahreza town has been studied in detail (e.g., IJRG, 1981). This region was located in the southern zone of the Cimmerian Sanandaj-Sirjan block as a part of northern shelf of the Neo-Tethyan Ocean (Stampfli and Borel, 2002). The lithological subdivision of the Permian strata of the entire region were refined by IJRG (1981), including the Surmaq Formation (units 1-3), the Abadeh Formation (units 4-5), and the Hambast Formation (units 6–7). The latter with a special focus on conodont- and ammonoid-based biostratigraphy as well as geochemistry of the Permian/Triassic boundary beds has been extensively studied (Richoz et al. 2010; Leda et al. 2014 for a review of earlier works and recent achievements). Unit 6 of the Hambast Formation is lithologically characterised by the alternation of shales and micritic grey limestone, following dark grey limestone beds of the Abadeh Formation (unit 5). The succession was subdivided with conodonts (Kozur, 2004; 2005) representing the entire Clarkina leveni and lowermost of the C. transcaucasica zones of the Dzhulfian (Wuchiapingian). The succeeding unit 7 is composed of thin-bedded greyish red nodular limestone with ammonoids, nautiloids, rare brachiopods, rugose corals, crinoid ossicles and fish-remains. The conodonts provided an age ranging from the C. transcaucasica to the Merrilina ultima - Stepanovites ?mostleri (= uppermost of C. hauschkei) zones, late Dzhulfian - top of Dorashmamian (e.g., Kozur, 2004; 2005). The Shahreza section has been investigated in several studies for facies and isotope geochemistry (Korte et al., 2004; Kozur, 2004, 2005, 2007; Heydari et al., 2008, 2013).

Fig. 3: Columnar section of the Permian-Triassic boundary beds at Shahreza with carbon isotope records (Korte et al., 2004, and new data).

Kashan city (Long history of sustainable living near a desert)

Fig. 4: Tourist attractions in Kashan

The etymology of the city name comes from the Kasian, the original inhabitants of the city, whose remains are found at Tapeh Sialk dating back 9,000 years; later this was changed to "Kashian", hence the town name. Between the 12th and the 14th centuries Kashan was an important centre for the production of high quality pottery and tiles. In modern Persian, the word for a tile (kashi) comes from the name of the town. Kashan is divided into two parts, mountainous and desert. In the west side, Kashan is cited in the neighbourhood of two of highest peaks of Karkas chain, Mount Gargash to the southwest of Kashan (the home of Iran national observatory, the largest astronomical telescope of Iran) and Mount Ardehaal in the west of Kashan, also known as "Damavand of

Kashan" and the highest peak of Ardehaal mountains (end part of Karkas chain in central Iran). In the east side of the city Kashan opens up to the central desert of Iran which the city is famous for. Kashan is also known for Maranjab Desert and located near the namak lake (or salt lake). Today Maranjab and the surrounding Shifting Sands is a popular destination at the weekends. Kashan was also a leisure vacation spot for Safavi Kings. Bagh-e Fin (), specifically, is one of the most famous gardens of Iran. This beautiful garden with its pool and orchards was designed for Shah Abbas I as a classical Persian vision of paradise. The original Safavid buildings have been substantially replaced and rebuilt by the Qajar dynasty although the layout of trees and marble basins is close to the original. The garden itself however, was first founded 7000 years ago alongside the Cheshmeh-ye-Soleiman. The garden is also notorious as the site of the murder of Mirza Taghi Khan known as Amir Kabir, chancellor of Nasser-al-Din Shah, Iran's king in 1852 (Wikipedia, 2014).

Tappeh Sialk

Fig. 5: Tourist attractions in Tappeh Sialk

The Sialk ziggurat was built around the 3000 BC. A joint study between Iran's Cultural Heritage Organization, the Louvre, and the Institut Francais de Recherche en Iran also verifies the oldest settlements in Sialk to date back to 5500–6000 BC.

Sialk, and the entire area around it, is thought to have originated as a result of the pristine large water sources nearby that still run today. The Cheshmeh ye Soleiman ("Solomon's Spring") has been bringing water to this area from nearby mountains for thousands of years. The Fin garden, built in its present form in the 17th century, is a popular tourist attraction. It is here that the kings of the Safavid dynasty would spend their vacations away from their capital cities. It is also here that Piruz Nahavandi (Abu-Lu'lu'ah), the Persian assassin of Caliph Umar, is buried (Wikipedia, 2014).

Isfahan city (architecture and handicrafts in the Safavid capital)

Fig. 6: Safavid architecture in Isfahan.

The Isfahan city emerged gradually over the course of the Elamite civilization (2700-1600 BCE) under the name of Aspandana, and continued its life as a major city through Median, Achaemenid and Sassanid empires. Its strategic location at the intersection of the ancient roads to Susa and made it an ideal candidate to house a standing army, ready to march against at any moment. One etymological theory argues that the name 'Aspahan' derives from the Pahlavi for 'place of the army'.

In 1598 Shah Abbas the Great moved his capital from Qazvin to the more central and Persian Isfahan, called Ispahān in early New Persian, so that it wouldn't be threatened by his arch rival, the Ottomans. This new importance ushered in a golden age for the city, with architecture, prestige, and Persian culture flourishing.

During the time of Shah Abbas and on Isfahan was very famous in Europe, and many European travelers made an account of their visit to the city, such as Jean Chardin. This all lasted until it was sacked by Afghan invaders in 1722 during the Safavids heavy decline. Today Isfahan, the third largest city in Iran, produces fine carpets, textiles, steel, and handicrafts. Isfahan has one of the largest steel-producing facilities in the entire region, as well as facilities for producing special alloys(Wikipedia, 2014).

Oligo- Miocene Qom Formation

Fig. 7: Satellite view, facies and field photographs of Qom formation.

Qom Formation deposits are widespread at the north-eastern coast of the Tethyan Seaway & Reuter et al., 2008) and ranged from the Early Oligocene to the Early Miocene (St ِ cklin) Setudehina,1991). The Qom Foramtiondeposits including marine limestone and marls with gypsum and siliciclasticsis contrasting in lithology and color with the red beds of the underlying Lower Red Formation (Oligocene) and overlying Upper Red Formation (Miocene). Furrer and Soder (1955) defined the lower and upper limits of the Qom Formation and alsosubdividedthe Qom Formation deposits into six members, from bottom to top including “a(basallimestone), b(sandy marls), c (alternating marls and limestone), d(evaporites), e(green marls) and f(top limestone)”. Soder (1959)subdivided the c member into four subunits as c1-c4 Bozorgnia (1965) proposed ten members for the Qom Formation and introduced the oldest member of the Qom Formation in Kashan area in name “unknownmember” with Rupelian age.

Fig. 8: Stratigraphic log of the Qom Formation (Karevan et al. 2014)

Solenoporacean algae (Late Triassic warm water reefs)

Fig. 9: Satellite view and outcrop of Solenoporacean algae in Dambelini 1 section.

Late Triassic (?Rhaetian) algae-dominated reef

Senowbari-Daryan et al. (2008) described two endemic, reef-building red algae of the family Solenoporaceae, Solenopora rectangulata and Parachaetetes dizluensis. Most likely they come from the Rhaetian interval of the Nayband Formation, exposed at the Dambelini Mountain NE of Esfahan. These algae build reef structures or patches are up to 17 m thick and occur in association with other reef-building organisms including foraminifers, sponges, corals, etc. Such solenoporacean reef structures appear to be unique as the main reef-building organism; up to now, elsewhere in the world, solenoporaceans have only been found as minor components of reefs or reef-like structures. A foraminiferal association in the reef includes several new taxa, which were also described recently by Senowbari-Daryan et al. (2010).

Morphologically, both algae can be discriminated in the field by their thalli and particularly by their branching pattern. Solenopora rectangulata has smaller and multi-branched thalli, the branching angle rised up to 90° giving the appearance of a fir-tree. Parachaetetes dizluensis is characterized by large and finger like multi-branched thalli.

Fig. 10: Stratigraphic log of the Nayband Formation and overlying Lower Jurassic rocks (after Senowbari-Daryan et al., 2008). Arrow indicates the solenoporacean horizon.

Angular unconformity (Early Jurassic/Early Cretaceous movements)

Fig. 11: Satellite view and outcrop of Jurassic-Cretaceous angular unconformity in the Dambelini Mountain.

Jurassic–Early Cretaceous stratigraphy and Late Cimmerian tectonic unconformity

The major tectonic angular unconformity (~30°), illustrated here at the middle part of the succession is an evidence of intense tectonic activity, already well-known as Late Cimmerian event across the Central-East Iran Microcontinent and the Sanandaj-Sirjan Block (Fürsich et al. 2009; Wilmsen et al., 2009, 2010, 2015). These are probably related to the closure of small oceanic basins surrounding the central Iranian blocks/terranes.

There is a set of pinkish-red polymict pebble-boulder conglomerate and sandstone beds. Its stratigraphic position between the underlying “Shemshak” Group deposits including sandstone, shale with limestone beds (Late Triassic to Middle Jurassic) and overlying mid- Early Cretaceous strata suggested an age range from Late Jurassic (?) to the Early Cretaceous. Rare ammonites of Toarcian/?Aalenian age were found in the limestone unit immediately below the unconformity level.

Above the unconformity level, the siliciclastic unit is followed by thick bedded, cliff- forming micritic carbonates with abundant orbitolinid foraminifera and rudists representing a large-scale shallow-marine carbonate platform system. It can be assigned to a Late Barremian (?) to Aptian age.

Disconformity (Late Devonian/Late Permian event)

Fig. 12: Satellite view and outcrop of Devonian-Permian disconformity in Chahriseh section.

Late Devonian mixed siliciclastic−carbonate sequence and Late Devonian/Middle Permian unconformity

The Late Devonian sedimentary sequence in the Chahriseh region (ca. 55 km northeast of Isfahan), was first examined in the 1970s (e.g., Djafarian and Brice, 1973; Zahedi, 1976). In recent years, this fossiliferous section was the most interesting locality featured in several paleontological investigations (e.g., Brice and Kebriaee, 2000; Hairapetian et al., 2000, 2006, 2008, 2016; Hairapetian and Burrow 2016; Mistiaen et al., 2000; Mistiaen and Gholamalian, 2000; Gholamalian, 2007; Webster et al., 2007; Hairapetian and Ginter, 2009). The succession commences with a few meters of shallow water carbonates, gradating into thick siliciclastics and shallow water carbonates alternating with shale beds, ranging from the early Frasnian to the late Famennian (Yazdi et al., 2000; Gholamalian, 2003). The Late Devonian strata (late Famennian expansa Zone) are unconformably overlain by a Middle- Late Permian mixed carbonate-siliciclastic sequence (e.g., Yazdi et al., 2000). This erosional hiatus marked in the field by a discontinuity level with scours (upper right photograph) and palaesol (Wendt et al., 2005). It is also known as “Hercynian unconformity”, which is already well-recorded on the most of Iranian terranes (e.g., Wendt et al., 2002, 2005) and maybe related to the onset of Hercynian events (e.g., Berberian and King 1981). Alternatively it may have resulted from deformation originated in an early pre-subduction compressional phase along the northern Gondwana margin of the Paleotethys (outer margin of Cimmeria), before it started rifting in the Middle Permian (Sharland et al., 2001; Ruban et al., 2007).

Based on some shallow water conodonts, the age of the basal carbonate beds is determined as the Middle falsiovalis to hassi zones (Turner et al., 2002). Some diagnostic miospores and acritarchs confirmed an early Frasnian age for these beds by (Ghavidel-Syooki, 2001). Associated faunas are diverse representatives of fish micro-remains including thelodont, acanthodian, placoderm, chondrithyhyan and actinopterygian taxa (Hairapetian et al. 2006, 2008, 2016)

Shallow water and/or near shore conodonts, belonging to the icriodid-polygnathid biofacies were recovered from the upper part of the succession (Hairapetian and Ginter, 2009). Characteristic conodont species are: Icriodus cornutus I. deformatus deformatus, I. deformatus asymmetricus, I. multicostatus multicostatus, I. alternatusalternatus, I. alternatus helmsi, Pelekysgnathus. serradentatus and Polygnathus brevilaminus. Such an assemblage indicates a time span from the Middle to Late triangularis zones. The icriodid species occur in much greater abundance than polygnathids here. These thin to medium- bedded limestones, alternating with dark grey shales, are dominated by brachiopods, mostly rhynchonellids and to lesser degree with fish macro-remains and ostracods. In the overlying levels, samples from mollusc-brachiopod grainstones yielded Icriodus alternatus alternatus, I. cornutus, Pelekysgnathus inclinatus, Polygnathus communis communis and Mehlina sp. The co-occurrence of these polygnathid and icriodid species in both levels indicates an age not older than the Middle crepida Zone and not younger than Upper crepida Zone. Thus, the most probable age range lies within the Middle through Upper crepida zones.

From mid-Famennian horizons, Icriodus cornutus, Pelekysgnathus inclinatus, Polygnathus bouckaerti, P. communis communis, P. lanceolus, P. semicostatus, Mehlina sp. were collected. The most important species, Polygnathus bouckaerti and Icriodus cornutus, can suggest a time span from the rhomboidea through to Upper marginifera zones (Hairapetian and Ginter 2009). Abundance of Polygnathus and Icriodus species with the absence of Famennian deep water forms (e.g., Palmatolepis and Ancyrognathus) are typical characters of shallow shelf conodont palaeocommunities.

Several conodont species were retrieved from the upper part of the section. They include Clydagnathus ormistoni, Polygnathus delicatulus, P. communis communis, P. communis collinsoni, P. semicostatus, Bispathodus bispathodus, Mehlina strigosa and Branmehla inornata indicative of the Lower expansa Zone (see also Gholamalian, 2003; Yazdi et al., 2000). The lithology of this unit commences with sandy limestones and grades to marly limestones. The wackestone/mudstone matrixes are dominated by rich assemblages of brachiopods (mostly spiriferids and strophomenids; Djafarian and Brice, 1973), crinoid ossicles and bryozoans. There also occur the rare occurrences of trilobite Phacops (Omegops) cornelius and large shell fragments of cyrtoclymeniid ammonoids (Feist, Yazdi and Ghobadipour in Mistiaen et al., 2000; Becker et al., 2004; Korn et al., in prep.).

Fig. 13: Simplified stratigraphic column of the Chahriseh section (modified from Hairapetian and Ginter, 2009).

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