For Peer Review

Latest Tournaisian-late Viséan foraminiferal biozonation (MFZ8-MFZ14) of Valiabad area, northwestern Alborz

(Iran); geological implications

Journal: Geological Journal

Manuscript ID: GJ-14-0067

Wiley - Manuscript type: Research Article

Date Submitted by the Author: 19-Apr-2014

Complete List of Authors: Zandkarimi, Keyvan; Shahid Beheshti University, Earth science NAJAFIAN, BAHRAM; Shahid Beheshti University, Earth Science Vachard, Daniel; Université Lille 1, UMR 8217 Géosystèmes,

Keywords: Mobarak Formation; Valiabad; Alborz; Iran; foraminifers; ; , Early Carboniferous, biostratigraphy

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Latest Tournaisian-late Viséan foraminiferal biozonation

(MFZ8-MFZ14) of Valiabad area, northwestern Alborz

(Iran); geological implications

KEYVAN ZANDKARIMI1, BAHRAM NAJAFIAN

1, DANIEL VACHARD

2, MARYAMNAZ

BAHRAMMANESH3, and SEYED HAMID VAZIRI

4

1) Shahid Beheshti University, Tehran (Iran).

2) Université Lille 1, UMR 8217 Géosystèmes, Avenue Paul-Langevin, 59655 Villeneuve d’Ascq cédex (France).

3) Geological Survey of Iran, Azadi Square, Tehran (Iran).

4) Department of Geology, Faculty of Basic Sciences, North Tehran Branch, Islamic Azad University, Tehran

(Iran).

Correspondence to: Keyvan Zandkarimi, Shahid Beheshti University, Tehran (Iran)

Email: zandkarimykeyvan@yahoo.com

The Mobarak Formation in Valiabad area (northwestern Alborz, Iran), is composed of

bioclastic, ooidic and sandy limestone interbedded with black shale, and disconformably

underlain and overlain by the Cambrian Lalun and Permian Dorud formations, respectively. In

this study, 104 foraminiferal species belonging to 12 families and 33 genera were determined.

Among them, six genera and nine species are reported for the first time in Iran. Thanks to the

foraminiferal assemblages, eight local biozones can be correlated with the MFZ8 to MFZ14

zones of the Viséan stratotypes in Belgium. The Valiabad equivalents of these biozones are

essentially characterized by (1) Eoparastaffella ex gr. rotunda-Lysella cf. gadukensis; (2)

Eoparastaffella simplex-Lapparentidiscus bokanensis; (3) Ammarchaediscus; (4) Uralodiscus-

Glomodiscus; (5) Glomodiscus-Archaediscus-last Eotextularia diversa; (6) Pojarkovella-

Msitinia fallax-last Uralodiscus; (7) Mstinia bulloides-Pseudoendothyra; and (8) Howchinia

gibba-Howchinia bradyana-Tubispirodiscus attenuatus. Consequently, the Valiabad section

appears as one of the most complete Viséan sections in Iran. Some taxonomic precisions are

provided about the principal taxa. Biogeographically, the MFZ8-MFZ11 biozones are extended

to all the shelves of Palaeotethys, from Ireland to South China, and Urals oceans; nevertheless,

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due to the complete evolution of archaediscoids, they seem more related to the Perigondwanan

assemblages from Sinai and Taurus (including the Antalya Nappes); (2) the MFZ12

assemblage appears relatively endemic; and (3) the impoverished assemblages of the biozone

MFZ13-14 are again relatively cosmopolitan but have marked affinities with the Kazakhstan

Block. It is currently impossible to indicate precisely if these variations are related with a drift

of the Alborz to the north, or to a change of oceanic currents. Moreover, the double affinity

goes to show the narrowness of the Paleotethys in the future Iran during the Viséan.

Received ………….

KEY WORDS Mobarak Formation; Valiabad; Alborz; Iran; foraminifers; biostratigraphy; Early

Carboniferous.

1. INTRODUCTION

The Early Carboniferous deposits of the Alborz Ranges were first mentioned by Tietze (1877).

The historic background of the investigations about this Subsystem in Iran was summarized in

Gaetani (1968) and Vachard (1996). The Mobarak Formation was defined and subdivided into 4

informal members A, B, C and D, by Assereto (1963). Their brachiopods were first studied by

(Gaetani 1964, 1965 and 1968). The foraminifers of the Mobarak Formation were successively

analyzed by Bozorgnia (1973), Lys et al. (1978), Kalantari (1986), Vachard (1996), Ueno et al.

(1997), Devuyst (2006), Brenckle et al. (2009), and Falahatgar et al. (2012).

The Valiabad section (coordinates: N 36˚15’32”; E 51˚18’44”) is located south of Chalus

city (Figure 1). Despite of its very rich macrofossil content, the Mobarak Formation in this

section was not investigated for comprehensive palaeontological studies up to now.

Our biostratigraphical subdivisions in the Mobarak Fm of Valiabad are based on correlations

with the well-known Russian formations, the Belgian stratotypes and the British and Irish

parastratotypes, because the foraminiferal biostratigraphy of the Tournaisian and Viséan was

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actively studied in the former USSR (e.g., Rauzer-Chernousova, 1948a; Aizenverg et al., 1968,

1983; Grozdilova and Lebedeva, 1954; Ganelina, 1951, 1956, 1966; Durkina, 1959;

Rozovskaya, 1963; Maklina et al., 1993; Vdovenko, 2001; Kulagina et al., 2003; Kulagina,

2013) and then in Belgium (Conil and Lys, 1964; Mamet, 1974; Conil et al., 1991; Poty et al.,

2006), and finally in England, Scotland, and Ireland (Strank, 1981; Fewtrell et al., 1989; Conil

et al., 1980; Cózar and Somerville, 2004, 2012; Somerville and Cózar, 2005; Cózar et al.,

2008, 2010).

The Early Carboniferous outcrops in southern Belgium (Namur-Dinant Basin) and northern

France (Avesnois, Boulonnais) are used as worldwide references for Tournaisian and Viséan

stages of the Mississippian Subsystem, based on intensively studied foraminifers, conodonts,

and corals (Conil and Lys, 1964; Groessens, 1975; Poty et al., 2006). The biozonation of Poty

et al. (2006) permits to subdivide and correlate the latest Devonian to earliest Serpukhovian

interval of times. It was successfully used in Belgium, Ireland, Moravia, England, South China,

etc. (Devuyst, 2006; Devuyst and Kalvoda, 2007; Hance et al., 2011; Kalvoda et al., 2011).

The aims of this paper are: (1) to provide some new data about the principal foraminiferal

markers of the Mobarak Formation in the Valiabad section, (2) to establish its complete

biozonation, (3) to discuss the correlation of this local biozonation with the Belgium

biozonation of Poty et al. (2006), and (4) to establish the different palaeobiogeographical

affinities of the foraminiferal assemblages, in order to reconstruct the history of the Alborz as a

Perigondwanan and/or Cimmerian terrane.

2. PREVIOUS BIOSTRATIGRAPHICAL WORK

Early biostratigraphical and chronostratigraphical studies of the Mobarak Formation were

mainly based on macrofossils (e.g., Gaetani, 1964, 1965, 1968). As the conodont microfaunas

are rarely found (Ahmadzadeh Heravi, 1971; Ueno et al., 1997; Habibi et al., 2008); the

biostratigraphical studies of the Mobarak Formation are essentially based on foraminifers.

Bozorgnia (1973) published the first comprehensive paper about the foraminiferal microfaunas

from the western, central and eastern Alborz. He studied the Valiabad and Dozdehband

sections in western Alborz; the Geirud, Gaduk, Abnak, Mobarakabad and Aruh sections in

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Figure 1. Location of the Valiabad section and geological sketch map (modified from Vahdati,

1999).

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central Alborz, as well as the Peyghambaran, Kalariz and Khoshyeilagh sections in eastern

Alborz (Figure 2). Bozorgnia imposed definitively the name Mobarak for designating the Early

Carboniferous beds. He provided an excellent biozonation by comparison to the Belgian

stratotypes or their equivalents in the former USSR. Bozorgnia mentioned also that the top of

the Mobarak Formation becomes older towards the south-east across the Alborz Mountains,

and attributed this age discrepancy to differential uplift across the southern Alborz that started

in the late Viséan and continued into the Early Permian.

Lys et al. (1978) provided an additional documentation for the foraminifers and the

biozonation of the eastern Alborz. Vachard (1996) thanks to a compilation of the Bozorgnia’s

data and new field results revised the biozonation of the Mobarak Formation.

Recently, some classical sections provided new data. For example, the Tournaisian-Viséan

boundary was revised in the Gaduk section (Devuyst, 2006). Brenckle et al. (2009),

biostratigraphically, chronostratigraphically and palaeogeographically, completed the

knowledge of the Mobarak Formation in the Abnak and Abrendan sections. They assigned the

Mobarak Formation to the Tournaisian-early Viséan interval. Finally, Bahrammanesh et al.

(2011) carried out a detailed work on brachiopods from the Abrendan and Simeh Koh sections

in the central Alborz and confirmed the base of the Mobarak Formation as Tournaisisan in age.

Among the rare studies about the Valiabad section, we can notice that Bozorgnia (1973)

reported Archaediscus exiguus (now Nodosarchaediscus), A.conili (now Nodasperodiscus) A.

krestovnikovi, A. demaneti (now Nodosarchaediscus), A. stellatus (now Rugosoarchaediscus)

and Rezvannia et al. (2010) suggested a late Viséan to Serpukhovian age for the Member C of

the Mobarak Formation of Valiabad, based on solitary rugose corals.

3. GEOLOGICAL SETTING

Iran has a complex geological structure and is tectonically divided into several terranes.

Among these, the Alborz belt is a 1500 km-long mountain system extending from Azerbaijan

to Afghanistan, flanking in its central part to the southern coast of the Caspian Sea (Zanchi et

al., 2009a).

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It was suggested that the Alborz Mountain Chain developed relatively recently during a Late

Triassic collisional orogeny (Zanchi et al., 2009a). During the Late Palaeozoic times, it formed

the North Iran Block, whose boundary with Central Iran was located in south of the southern

foothills of the Alborz Belt (Zanchi et al., 2009b). From the Eo-Cimmerian orogeny to the Late

Tertiary-Quaternary intracontinental transpression, several subordinate tectonic events affected

the Alborz (Allen et al., 2003). The main tectonic evolution of the Alborz Mountain is thought

to be a result of the northward subduction of the Palaeo-Tethys and subsequent collision

between the Iranian Cimmerian microcontinent and Turan plate, southern part of Laurasia

(Alavi, 1991).

Zanchi et al. (2009a) divided the Alborz in two main portions that show a different structural

setting: western Alborz, forming the Talesh Mountains, and central-eastern Alborz, east of

Rasht. The studied area is located in northern part of central-eastern Alborz (Figures 1-2). It

shoud be mentioned that the so called Eastern, Central, Northern and Western Alborz

subdivitions were frequently used by many authers (e.g. Stöcklin, 1971; 1974; Alvi, 1991;

1996; Zanchi et al., 2006); however this division is however this division is apparently more

based on palaeogeographic positions than on structural differences (Aghanabati, pers. comm.;

October 2013).

The Northern Alborz is affected by sequences of nearly E-W-trending thrust faults and folds

(figure 1), which are dominant in the inner parts of the belt and decrese toward the Caspian

side as the external part. The evolution of this part is presumably because of the inversion of

pre-existent extensional faults (Vahdati, 1999) owing to the reactivation of grabens formed in

the foreland of the Late Triassic Eo-Cimmerian orogen, resulting from the accretion of the

Iranian block to Eurasia (Zanchi et al., 2006).

4. LITHOSTRATIGRAPHY OF VALIABAD

The Mobarak Formation was first described near the village of Mobarakabad in the central

Alborz, east of Tehran. The lithology of the type section, approximately 450 metres-thick is

mainly composed of black fossiliferous limestone with subordinate black marl, intercalated in

the lower part (Assereto, 1963). Overlying an emersion surface at the top of Cambrian Lalun

Formation, the Mobarak Formation, in the Valiabad section, consists of bioclastic and ooidic

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Figure 2. Skech map of the Alborz Mountains, with the important cities, the location of some key-sections (black circle), and the

present studied section of Valiabad (rectangular). The arrow shows the increasing age of the top beds of the Mobarak Formation

from SE to NW (modified from Brenckle et al., 2009). The key sections as follows: 1: Dozdehband; 2: Geirud; 3: Abnak; 4:

Mobarakabad; 5: Aruh; 6: Gaduk; 7: Shahmirzad; 8: Peyghambaran; 9: Simeh Koh; 10: Abrendan; 11: Kalariz; 12: Viru; 13:

Khoshyeilagh; 14: Kalate; 15: Nodeh-Sud.

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limestone alternating with black marl and sandstone which underlies disconformably the Early

Permian Dorud Formation. In Valiabad, the Mobarak Formation, more than 500 metres-thick

(Figure 3) is subdivided into four informal members as follows:

Member 1 (150 m)

The lowermost part of this member includes a few layers of grey, thick-bedded wackestone

without foraminifer followed by light grey, thick to very thick, bedded bioclastic grainstone

with some ooidic grainstone beds in basal part. The member includes the foraminiferal zones

MFZ8, MFZ9, and lower part of MFZ10 as defined by Poty et al. (2006).

Member 2 (123 m)

Light brown, thin-bedded sandy grainstone to packstone with crinoids, bryozoans and

palechinid radioles. This Member comprises the upper part of MFZ10, the MFZ11A subzone

and the lower part of MFZ11B subzone. Abundant large solitary rugose corals and rare

spiriferid brachiopods are present in this member.

Member 3 (146 m)

Light grey, medium- to thick-bedded bioclastic and ooidic grainstone interbedded with

sandstone and black shale. The bioclasts are constituted by foraminifers, and bryozoans. This

member encompasses the upper part of MFZ11B, MFZ12 and the lower part of MFZ13.

Member 4 (90 m)

Yellowish thin to medium bedded, bioclastic grainstone to packstone interbedded with black

shale. Abundant macrofossil including bryozoans, brachiopods and corals can be seen in this

member. The member includes the upper part of MFZ13 and MFZ14. The macrofossil genera

of this member are mainly composed of bryozoans (Fenestella, Prasopora and Dekayella),

brachiopods (Rhipidomella, Tolmatchoffia, Spinocarinifera, Lamellasothyris, Brachythyris,

Leptaena, Carteridina, Choristites, Marginatia, Schizophoria, Schellwienella and

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Perdiniocardinia), and corals (Kailingophyllum, Marzanophyllum, Hapsiphyllum,

Zaphrentoides and Syringopora).

5. MATERIALS AND METHODS

The best stratigraphical section was selected east of the Valiabad Village, and 127 rock

samples were collected. More than 350 thin sections were prepared by the first author as a part

of his postgraduate thesis. This material is registered under the numbers MZ1 to MZ127, and is

housed in the Palaeontological Museum of the Department of Earth Sciences, University of

Shahid Beheshti, Tehran (Iran). The thin sections were studied under polarized light with

Olympus BX51 polarizing microscope and the images have been taken in x10 objective. The

used classification of carbonate rocks is that of Dunham (1962), and the classification of the

Early Carboniferous foraminifers follows that of Hance et al. (2011) with slight modifications

(see Chapter 7 and Figure 4).

6. DEFINITIONS OF THE MFZ8-14 BIOZONES IN VALIABAD

In previous studied sections of the Mobarak Formation, probably because of either inadequate

sampling or unfavourable environments, the foraminifers were not discovered in the early units

of the formation, except for some earlandiid species (e.g., Bozorgnia, 1973; Vachard, 1996;

Ueno et al., 1997; Brenckle et al., 2009). However in Valiabad, some relatively rich

foraminiferal assemblages were found. These assemblages permitted a detailed biozonation

and comparison (Figures 3, 5) with the reference biozones MFZ8 to MFZ14 of Poty et al.

(2006).

6.1. MFZ8: Eoparastaffella ex gr. rotunda-Lysella cf. gadukensis assemblage zone

This zone is characterized by the occurrence of Eoparastaffella ex gr. rotunda Vdovenko, 1971

and Lysella cf. gadukensis Bozorgnia, 1973 (samples MZ1-MZ12). These taxa are known in

MFZ8 from Ireland to South China (Hance et al., 2011). Devuyst (2006) emphasized the

importance of Lysella gadukensis in the Gaduk section of northern Alborz, in South China and

Ireland, as a marker of the biozone MFZ8 and base of MFZ9; Kalvoda et al. (2010; figs. 13.5,

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7-9) reported latest Tournaisian Lysella cf. gadukensis in the Mokrá quarry (Czech Republic);

Kalvoda et al. (2011, figs. 12.O, 13.H) illustrated other L. gadukensis of the Tournaisian-

Viséan boundary interval in Ireland and Kalvoda et al. (2012, figs. 15.I, M-O, 16.A-B, 19AA,

22I, 25O, 26A-J, 27K, N) in Great-Britain. The complete assemblage of the Valiabad’s MFZ8

biozone include Dainella cf. grandis Grozdilova and Lebedeva, 1978; Lysella cf. gadukensis;

L. sp. 2; Eoparastaffella ex gr. rotunda Vdovenko, 1971; E. cf. florigena (Pronina, 1963); and

E.macdermoti Devuyst and Kalvoda, 2007.

6.2. MFZ9: Eoparastaffella simplex-Lapparentidiscus bokanensis lowest occurrence zone

The base of the zone MFZ9 is everywhere characterized by the FO of Eoparastaffella simplex

Vdovenko, 1971 and the top of the zone coincides with the first occurrence of primitive

archaedisicds. These criteria are exactly registered in Valiabad from the samples MZ12 to

MZ31. Among the MFZ9 taxa in Valiabad can be mentioned: Eoparastaffella simplex lata

Vdovenko, 1971; E. interiecta Vdovenko, 1971; E. sp.; Endothyra ex gr. similis Rauzer-

Chernousova and Reitlinger in Rauzer-Chernousova et al., 1936; E. sp.; Omphalotis? sp.,

Forschia subangulata (Möller, 1879); Earlandia vulgaris (Rauzer-Chernousova and Reitlinger

in Rauzer-Chernousova and Fursenko, 1937); Lapparentidiscus bokanensis Vachard, 1980;

and L.? sp.

6.3. Ammarchaediscus lowest occurrence zone (MFZ10)

The base of this zone is characterized by the first occurrence of the primitive archaediscid

Ammarchaedisus sp. 1, and the top of this biozone is located just before the first occurrence of

Uralodiscus ex gr. rotundus (Chernysheva, 1948a) (samples MZ22 to MZ42). Hence, MFZ10

of Valiabad corresponds with MFZ10 of Belgium (Poty et al., 2006), because this latter zone

contains the first archaediscids prior to the appearance of Uralodiscus rotundus. Other taxa are

Ammarchaediscus cf. eospirillinoides (Brazhnikova in Brazhnikova et al., 1967);

Lapparentidiscus bokanensis; L. sp.; Mediocris cf. cupellaeformis (Ganelina, 1951); Cf.

Mediocris? liae Brenckle, 2004; Mediendothyra sp.; and Plectogyranopsis ex gr. convexa

(Rauzer-Chernousova, 1948b).

6.4. Uralodiscus-Glomodiscus lowest occurrence zone (MFZ11A)

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Characterized by the first occurrence of Uralodiscus ex gr. rotundus and last occurrence of

Uralodiscus sp. (samples MZ50-MZ57), the local subzone MFZ11A, like the lower MFZ11

subzone of Belgium (Poty et al., 2006) does not display any true Paraarchaediscus (see Figure

4). The MFZ11B was established in South China, as an assemblage zone of Pojarkovella sp. (a

genus whose FO in only known at the base of the MFZ12 in Belgium) with typical MFZ11

representatives. As Uralodiscus rotundus is not yet well-determined in South China (Hance et

al., 2011), the FO of Parachaediscus and then that of Conilidiscus were introduced as another

characteristic of the base of the MFZ11B (Okuyucu et al., 2013). As in Belgium (Hance,

1988), Ammarchaediscus, Glomodiscus (sensu Figure 4), and Planoarchaediscus are abundant

in MFZ11A, whereas Eostaffella appears at its top.

6.5. Glomodiscus-Archaediscus-Eotextularia diversa assemblage zone (MFZ11B)

The zone characterized by the first occurrence of large, advanced Glomodiscus sp. and that of

Archaediscus sp., and by the last occurrence of Eotextularia diversa (Chernysheva, 1948b)

(samples MZ51-MZ85). These bioevents occur in the upper MFZ11 of Belgium (Poty et al.,

2006). Eotextularia diversa and Mediendothyra wjasmensis (Ganelina, 1956) are present up to

the top of the MFZ11B suzone in Valiabad.

6.6. Pojarkovella-Mstinia fallax-Uralodiscus assemblage zone (MFZ12)

The next Valiabad zone is characterized by the first occurrence of Pojarkovella nibelis

(Durkina, 1959) at its base, whereas its summit is located below the first occurrence of Mstinia

bulloides (Mikhailov, 1939) emend. Dain, 1953 (samples MZ86-MZ97). By the richness in

Pojarkovella, encountered for the first time in Iran, this Valiabad zone is coeval with MFZ12

of Belgium (Poty et al., 2006) and Livian Substage of Western Europe. MFZ 12 exists also

within the Hunangjin Fm of South China (Hance et al., 2011).

Abundant Pojarkovella species (e.g., P. nibelis; P. wushiensis (Li, 1991) emend. Brenckle,

2004 and P.? ketmenica Simonova and Zub, 1975 (enclosure in Figure 3)) have been identified

in this interval. They are generally reported for the first time in Iran. Auxilliary forms as

Koskinotextularia cf. cribriformis Eickhoff, 1968 appear a few meters above the base of the

local MFZ12. This latter records also the first occurrence of some genera such as Omphalotis,

Endothyranopsis, Consobrinella, Permodiscus and Pirletidiscus, as well as the last occurrence

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of Planoarchaediscus and Uralodiscus. Mstinia Dain, 1953 emend. Pille, 2008 (=

Haplophragmella = Nevillella = Nevillea of the authors) appears precoceously, because the

first specimens observed in western Europe and Kazakhstan have their FO in the V3bβ =

MFZ13 (Vachard, 1977), and have generally their acme in the biozone MFZ14 (= Cf6γ)

(Aizenverg et al., 1968; Conil et al., 1981; Conil and Paproth, 1983; Somerville et al., 1992;

Cózar, 2001; Brenckle and Milkina, 2003). The Nevillea mentioned in the lower part of the

biozone MFZ10 in Ireland (Kalvoda et al., 2011) are not illustrated, and eventually rather

correspond to Pseudolituotubella (e.g., in Malakhova, 1975), Rectopravina Vachard, Haig and

Mory (2014), or even to atypical Haplophragmina. Similarly, the not illustrated Mstinia sp. of

Kulagina et al. (2003, text-fig. 6 p. 179) are probably Pseudolituotubella during their FAD. In

contrast, the lower/middle Visean Haplophragmella tetraloculi of Pronina (1963, p. 134, pl. 2,

fig. 11, pl. 3, fig. 1) belong to Lituotubella ex gr. glomospiroides Rauzer-Chernousova.

Moreover, some typical Mstinia tetraloculi (under the generic name of Nevillella) were

illustrated in the Holkerian (an equivalent of the biozone MFZ12) of England by Fewtrell et al.

(1989, pl. 3.5. 3-4), who indicated an Arundian-Asbian (i.e., MFZ11-MFZ14) complete range

for the genus in England. Similarly, Mstinia cordobensis (Cózar, 2001) has a late Holkerian to

Asbian (MFZ12-MFZ1) range in southern Spain (Cózar, 2001).

6.7. Mstinia bulloides-Pseudoendothyra assemblage zone (MFZ13)

The base of the next Valiabad zone is marked by the first occurrence of Mstinia bulloides,

whereas the top of the zone is placed below the first occurrence of Howchina gibba (Howchin,

1888) (samples MZ98-MZ113). In this interval, the genera Pseudoendothyra, Archaediscus,

Consobrinella, Nodosarchaediscus and Tetrataxis entered for the first time in the Valiabad

section; however, the main guides of MFZ13: Neoarchaediscus, Vissariotaxis, and bilamellar

Palaeotextularioidea are absent in Valiabad.

6.8. Howchinia gibba-H. bradyana-Tubispirodiscus attenuatus lowest occurrence zone

(MFZ14)

The base of the zone coincides with the first occurrence of Howchinia gibba (Howchin, 1888);

the top is marked by the last occurrence of Howchinia bradyana (samples MZ114-MZ127),

and correlates with MFZ14 of Belgium. Other characteristic taxa in Valiabad are Archaediscus

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acuminatus (Marfenkova, 1983), A. moelleri Rauzer-Chernousova, 1948c, A. krestovnikovi

Rauzer-Chernousova, 1948d; Nodosarchaediscus demaneti (Conil and Lys, 1964), and

Endostaffella parva (Möller, 1879). Two index taxa of late Viséan foraminifers including

Howchinia bradyana and Tubispirodiscus attenuatus are reported here for the first time in Iran.

The latter species, as revised below, is another typical species of our biozone.

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Figure 3: Stratigraphic log of the Valiabad section showing the distribution of foraminiferal taxa.

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Figure 3: Continued.

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7. REMARKS ON THE FORAMINIFERAL CLASSIFICATION ADOPTED HERE

7.1. Archaediscids

The archaediscids are one of the most useful foraminiferal groups for subdividing the Viséan

Stage due to evident evolutionary lineages and the acquisition of new characters in short period

of time (e.g., Pirlet and Conil, 1974; Brenckle et al., 1987; Vachard, 1988, Laloux, 1988;

Brenckle and Grelecki, 1993; Hance et al., 2011). A relatively complete pattern of Viséan

archaedisicids is obvious in the studied section, and of great importance for the detailed

biozonation of the Mobarak Formation.

Hance et al. (2011) recognized 2 main lineages of archaediscoids. Their common ancestor is

the pseudoammodiscoid, planispirally, involute, dark-walled, microgranular genus

Lapparentidiscus, the FAD of which is probably located in the upper MFZ9 zone, as its FO in

Valiabad (Arefifard and Vachard, unpublisheds data). We suggest here that Lapparentidiscus

generated 2 lineages of primitive archaediscoids, but relatively different of those reconstructed

by Hance et al. (2011): (1) a planispirally coiled lineage with successively Ammarchaediscus-

Viseidiscus-Uralodiscus; whereas Ammarchaediscus gives rise to oscillating coiling with

Planoarchaediscus which has no particular descendence; (3) Uralodiscus gives various stages

of Glomodiscus (@ Glomodiscus, @ Melarchaediscus, @ Propermodiscus?) which in turn

generate probably all the other archaediscoids of the concavus, concavo-angulatus, angulatus,

tenuis and pseudo-miliolid stages (Figure 4); independently it gives the stage Conilidiscus, also

without descendence.

In Ammarchaediscus and primitive Planoarchaediscus, the evolved, pseudo-fibrous, clear,

external layer is reduced to an umbilical plug. In Viseidiscus and evolved Planoarchaediscus,

the clear layer remains very poorly developed but covers entirely the internal dark,

microgranular layer. In Uralodiscus and Glomodiscus (@ Melarchaediscus), the pseudofibrous

layer becomes the most developed and the inner layer is reduced to buttresses (Figure 4); after

that the inner dark layer is very reduced and finally disappears. Each stage can give rise to

diverse stellate genera; i.e. with basal nodosities occluding more or less completely the

chamber (Figure 4). These forms, diversified in the central Alborz (Bozorgnia, 1973), are rare

in our material, and principally represented by some Nodosarchaediscus.

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ARCHAEDISCIDS TAXONOMY

EVOLUTIONARY

STAGES

planispiral

(entirely or

dominantly)

no planispiral

(e.g., oscillating,

sigmoidal, or bimorphic)

stellate genera

pseudo-miliolid

stage - Eosigmoilina Brenckleina

tenuis stage

Browneidiscus - -

angulatus-tenuis

stage Betpakodiscus - Kasachstanodiscus

angulatus stage Tubispirodiscus

Tubispirodiscus? (to

emendate)

Asteroarchaediscus

Neoarchaediscus

Planospirodiscus

Nodasperodiscus

concavo-angulatus

stage Pirletidiscus

Archaediscus Rugosoarchaediscus

Permodiscus

concavus stage

- Paraarchaediscus Nodosarchaediscus

involutus stage

Uralodiscus (@

Conilidiscus)

Glomodiscus (@

Propermodiscus)

-

ogival-buttresses

stage

Uralodiscus

(@ Uralodiscus)

Glomodiscus (@

Melarchaediscus)

- Glomodiscus (@

Glomodiscus)

parallel flanks Viseidiscus evolved Planoarchaediscus

-

plug stage Ammarchaediscus primitive Planoarchaediscus -

pseudoammodiscoid

ancestor Lapparentidiscus - -

Figure 4. Generic definitions of the names of archaediscoids used in this work according to

Brenckle et al., 1987; Vachard, 1988, Hance et al., 2011, and Vachard and Moix (unpublished

data); slightly modified.

In the lineage of Archaediscus, successively appeared three genera, very similar or at least very

transitional: Tubispirodiscus, Betpakodiscus and Browneidiscus (see Cózar et al., 2008 and

Figure 4).

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For many authors, Ammarchaediscus can be interpreted as a synonymous of Viseidiscus sensu

Brenckle et al. (1987). However, Hance et al. (2011) demonstrated that Viseidiscus, as defined

by its type species Archaediscus primaevus Pronina, 1963 differs from Ammarchaediscus

(sensu stricto) and corresponds in fact to Leptodiscus Conil and Pirlet in Pirlet and Conil,

1974. As this name is preoccupied, Viseidiscus is a prioritary name, but Ammarchaediscus and

Viseidiscus are distinct (Hance et al., 2011).

Primitive and evolved Planoarchaediscus were named Brunsiarchaediscus and

Nudarchaediscus, respectively, by Pirlet and Conil (1974, 1977), but these names are difficult

to use because the selected type species do not correspond exactly to the definitions of the taxa.

Then, in the evolution of the archaediscoids, appears the family Archaediscidae with four

evolutive stages of Archaediscus: involutus; concavus; concavo-angulatus; and angulatus),

Pirletidiscus Vachard, 1988, Permodiscus Dutkevich in Chernysheva, 1948a, and

Tubispirodiscus Browne and Pohl, 1973 emend. Cózar et al., 2008 (= Betpakodiscus

Marfenkova, 1983 of the authors) and finally, the Eosigmoilinidae whose the coiling is

planispiral evolute or pseudo-miliolid (Figure 4).

Another family (Asteroarchaediscidae) or multiple derivations of each stage of development

(hypothesis suggested by Vachard, 1988) can generate diverse stellate genera (Figure 4).

We have seen the important presence of Tubispirodiscus attenuatus in MFZ14. This taxon was

initially described under the generic name of Propermodiscus Miklukho-Maklay, 1953. This

latter genus encompasses in fact various species of Paraarchaediscus Orlova, 1955;

Glomodiscus, and Archaediscus (@ involutus) and differs strongly from Tubisprodiscus by the

test entirely involute and the strong development of the inner black layer.

Propermodiscus acuminatus forma tipika (misspelling for: typica) Marfenkova, 1983,

described by the same author in he same publication, is for us completely different and

corresponds to an Archaediscus at the concavus stage, probably Archaediscus stilus Grozdilova

and Lebedeva in Grozdilova, 1953. According to Brenckle and Grelecki (1993),

Tubispirodiscus attenatus might be synonym of Archaediscus krestovnikovi compressa

Vdovenko in Brazhnikova et al., 1967. Nevertheless, the latter species is smaller (D = 0.256

mm; width = 0.057 mm; h = 0.029-0.031 mm) and has more whorls (7.5). Therefore, it

corresponds for us to a distinct species. Besides contrary to the recommendation of Brenckle

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and Grelecki (1993), if the two species are synonym, the name compressa would have priority

upon attenuatus.

7.2. Lasiodiscids

Krainer and Vachard (2002) proposed some characters for the Viséan species of Howchinia.

The most useful character is the number of whorls; they also considered 7-8 whorls for H.

gibba, 9-12 for H. bradyana, and 13-14 for H. longa. We followed these criteria in this work.

7.3. Tetrataxis spp.

Tetrataxis elegans, T. exornatus, and T. pallae, three species created in Belgium by Conil and

Lys (1964), correspond to some specimens of our study. Occurring simultaneously in Belgium

and Iran, they are only considered as a unique group, of high and broad Tetrataxis, with 7-8

whorls and with an apical angle of less than 90°.

7.4. Pojarkovella spp. and pojarkovellids

Abundant Pojarkovella species (e.g., P. nibelis, P. wushiensis) have been discovered in our

study. Such diversity is mentioned for the first time in Iran. Another, probably new, genus of

pojarkovellids is associated with the true Pojarkovella; this genus appears almost planispiral

and consequently resemble the misinterpreted Viséan “Millerella” of Conil and Lys (1964) and

“Eostaffella parastruvei” of Conil and Lys (1964) and Bozorgnia (1973).

7.5. Eoparastaffella spp.

We have followed for this group the classification of Devuyst and Kalvoda (2007) who have

already described and illustrated in Iran: E. interiecta (pl. 1, fig. 2), E. cf. interiecta (pl. 3, fig.

19), and E. macdermoti (pl. 3, fig. 3).

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8. DISCUSSION

We compare the biostratigraphical results of the present paper with foraminiferal zone of Poty

et al. (2006) as well as with equivalent Western Europe Substages. The introduced

foraminiferal zones correlate with the MFZ8 to MFZ14 biozones, and consequently with upper

Ivorian, Moliniacian, Livian, and Warnantian Substages of the stratotypic areas (Figure 5).

8.1. Tournaisian

In some Alborz sections, Bozorgnia (1973) and Vachard (1996) indicated that the Tournaisian

is complete with three biozones: Earlandia minor Zone (MFZ1 of Poty et al., 2006);

Septabrunsiina krainica Zone (MFZ2-MFZ5); and Eotextularia diversa Zone (MFZ6-MFZ8).

In Valiabad, the transgressive Tournaisian beds resting on the Cambrian Lalun Formation are

latest Tournaisian (MFZ8 biozone) in age, because their foraminiferal assemblages are similar

to those analyzed by Devuyst (2006) in the Gaduk section of central Alborz (especially, due to

the presesence of relatively primitive species of Eoparastaffella and the absence of

Eoparastaffella simplex, the FAD of which is characteristic of the Visean base). Furthermore,

the Tournaisian biozone in Valiabad corresponds most probably to the upper part of MFZ8

because neither Darjella monilis nor Elevenella parvula were observed, and because these two

foraminifers are limited to the lower part of MFZ8 of Gaduk (Devuyst, 2006, fig. 5.10).

The “Kosvinsky” of Brenckle et al. (2009) in the Abrendan section is clearly also MFZ8 in

age; the MFZ9 is probably present in the last beds of this section (not illustrated in the log of

Brenckle et al., 2009, text-fig. 8 p. 56), because of the presence of an Eoparastaffella of the

group simplex illustrated by these authors (pl. 5, fig. 11). Similarly the Dainella chomatica

zone of Vachard (1996) contains also probably the two biozones MFZ8 and MFZ9.

It is to notice that the Eoendothyranopsis sp. sensu Ueno et al. (1997, pl. 1, figs. 11-12) is in

fact an Eoparastaffella sp. of the biozones MFZ8 or MFZ9.

8.2. Moliniacian (early Viséan)

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Our biozone MFZ9 is characterized by the appearance of Eoparastaffella simplex at its base

and the appearance of a primitive archaediscid Ammarchaediscus at the base of the following

zone MFZ9. Between its lower and upper limits, MFZ9 does not contain characteristic forms.

Figure 5. Correlation of the subdivisions used in this study.

In the MFZ 9 of Valiabad, the succession of Endothyra ex gr. similis, Omphalotis? sp., and

Mediendothyra might correspond to a primitive lineage among the omphaltin endothyrids.

Forschia appears precociously, only 10 m above the base of the biozone; moreover some

Forschiella were mentioned near the base of the Viséan in Czech Republic (Kalvoda et al.,

2010, fig. 13.3) or even in MFZ8 in Ireland (Kalvoda et al., 2011, fig. 11G). The taxa

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Plectogyranopsis ex gr. convexa and Cf. Mediocris? liae may also be used as local

subordinate markers. The top of the MFZ9 in Valiabad is characterized by the FO (and

possibly, the FAD) of Lapparentidiscus bokanensis. The FO of Eostaffella (notably, E.

nalivkini) in the MFZ9 of Belgium was not observed in Valiabad.

The zone MFZ10 is characterized by primitive archaediscids; especially Ammarchaediscus sp.

1 and A. cf. eospirillinoides; this latter being probably transitional to Planoarchaediscus.The

filiation with Lapparentidiscus suggested by Vachard (1988) is confirmed here due to the

discovery of Lapparentidiscus in the top of MFZ9.

Conil et al. (1991) characterized the biozone Cf4β by the appearance of Glomodiscus, rapidly

followed by the entry of “Rectodiscus” (= Uralodiscus). The biozone Cf4γ was indicated as

that of the appearance of Archaediscus. Poty et al. (2006) considered Uralodiscus rotundus as

characteristic of the MFZ11. Okuyucu et al. (2013) have considered the FAD of

Paraarchaediscus as the marker of the base of the zone MFZ11B. Consequently, the MFZ10

corresponds exactly to our subdivision in Valiabad, but the Cf4β corresponded only to the

upper part of this zone and to the lower part of the MFZ11A. Finally, the MFZ11B corresponds

to the lower part of the Cf4γ.

The biozone MFZ11 is the acme zone of Uralodiscus. MFZ11A is characterized by the

assemblage of Uralodiscus, Glomodiscus, Ammarchaediscus sp. 1, A. sp. 2, and

Planoarchaediscus cf. rigens, whereas the true Archaediscus appear in MFZ11B, with an

obvious transition between Glomodiscus sp. 3 and Archaediscus (stage involutus) ex gr.

convexus. MFZ11B is relatively thick in our section; it contains many archaediscids in open

nomenclature of the genera Archaediscus (stage involutus and stage concavus),

Planoarchaediscus, and Glomodiscus. Contrary to Belgium, the last Eoparastaffella are

limited to the base of MFZ11A and the first true Eostaffella appear in this subzone. Similarly,

in both areas, Eotextularia diversa disappears at the base of MFZ12.

The assemblages of the biozone MFZ11 (late Moliniacian) are apparently widespread in

Alborz, after re-interpretation of the literature (Bozorgnia, 1973; Jenny, 1977; Stampfli, 1978;

Lys et al., 1978; Meissami et al., 1978; Vachard, 1996; Brenckle et al., 2009).

In the Abnak section, the Member “C” of Brenckle et al. (2009) maybe begins before the

MFZ11A Zone; the Member “D” is almost entirely MFZ11A in age due to the appearance of

Uralodiscus (samples 1066-806). The MFZ11B appears evidently in the sample 807 with the

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first Pojarkovella (this taxon is indicated as doubtful by Brenckle et al., 2009; probably

because the section is transverse but this illustrated specimen belongs unquestionably to

Pojarkovella). Therefore, we find here the character indicated by Hance et al. (2011) as

characteristic of the MFZ11B biozone: i.e., the appearance of rare Pojarkovella, prior to the

abundance and diversity of this genus at the base of MFZ12. Apparently, this biozone MFZ12

is not present in the section of Brenckle et al. (2009) due to the absence of true Pojarkovella

nibelis.

Similarly, in the Tarim (NW China), in the Wushi section studied by Brenckle (2004), the

lower limit of the biozone MFZ12 can be emplaced in the sample 7 showing the appearance of

Pojarkovella nibelis and P. wushiensis. Moreover, a P. sp. is mentioned in the sample 3; that

is, for us, an evidence of the presence of the MFZ11B subzone in Tarim. In this study of

Brenckle (2004), we can also remark that the probable equivalent of the biozone MFZ12 is

located between his samples 7 and 19. In the Tarim’s sample 20, appears the marker of the

biozone MFZ13; i.e., the genus Vissariotaxis Mamet, 1970 which unfortunately has not been

found in our study.

8.3. Livian (middle Viséan).

The base of MFZ12 is characterized by a massive appearance of Pojarkovella spp. Hence, it is

the exact equivalent of the biozone MFZ12. As in South China, the genus Uralodiscus is still

present in this zone. True Archaediscus (stage concavo-angulatus) karreri Brady, 1873 are

present, as well as Koskinotextularia cribriformis. Concomitantly, appears Mstina fallax which

was most traditionally considered a late Visean taxon (see above). No local markers indicate

clearly the top of this zone. Possible candidates might be the disappearance of Uralodiscus

rotundus, the appearance of Permodiscus vetustus Dutkevich in Chernysheva, 1948a, or that of

Pirletidiscus sp. We have finally selected the appearance of Mstinia bulloides as the indicator

of the base of MFZ12, because in Western Europe and Russia, this taxon is generally well

represented in the late Viséan.

Our MFZ12 biozone shows therefore a great diversity of the genus Pojarkovella with P.

nibelis, P. wushiensis and P.? ketmenica and possible new related genera, as soon as its base.

Almost all these taxa are mentioned for the first time in Iran as P? ketmenica. A new genus of

pojarkovellids is similar to Pojarkovella by its wall structure, but devoid of axis deviations and

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almost planispiral, and consequently difficult to distinguish from Eoendothyranopsis Reitlinger

and Rostovceva in Reitlinger, 1966, Pseudoendothyra Mikhailov, 1939 or Eostaffella Rauzer-

Chernousova, 1948d. The smaller species like P.? ketmenica appear morphologically similar to

P. nibelis as well as Euxinita Conil and Dil in Conil et al., 1980. If we cannot find a difference

between the wall structures, we will admit that Pojarkovella and Euxinita are synonym as

proposed by Reitlinger (1981) but discussed by Cózar (2002) and Okuyucu and Vachard

(2006).

8.4. Warnantian (late Viséan)

The endemism of MFZ13 microfaunas does not permit an accurate comparison with the

MFZ13 biozone of Poty et al. (2006). Hence, the local MFZ13 is included between the

appearance of Mstinia bulloides and that of Howchinia gibba. The local other biomarkers are

Nodosarchaediscus and large Tetrataxis spp. It is to notice that Brenckle et al. (1987)

suggested that Nodosarchaediscus did not exist, whereas Brenckle et al. (2009) denominated

Kasachstanodiscus the abundant and unquestionable Nodosarchaediscus of the Alborz

Mountains. We consider Kasachstanodiscus and Nodosarchaediscus as very different (Figure

4). The upper part of this biozone is characterized, as in Belgium, by the appearance of

Pseudoendothyra.

The last zone, MFZ14, is easy to characterize due to the appearance of Howchinia gibba and

H. bradyana, as well as that of Endostaffella parva. This zone corresponds therefore to the

MFZ14 (V3bγ) of Belgium. This division is relatively well-known in all the Alborz

(Bozorgnia, 1973; Jenny, 1977, p. 7, figs. 3-4; Lys et al., 1978, pl. 1, figs. 13-25; Vachard,

1996).

Another interesting species of MFZ14 is Tubispirodiscus attenuatus (see above and below).

Compared with the MFZ14 of Belgium, the MFZ14 of Valiabad is poorly diversified and its

total assemblage of 5taxa is entirely indicated in this paragraph.

9. GEOLOGICAL IMPLICATIONS

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9.1. Diachronism of the top of the Mobarak Formation

It seems that the top of the Mobarak Formation becomes increasingly younger from southeast

to northwest (Brenckle et al., 2009). For example, the Mobarak Fm at Abrendan and Abnak

sections in the south side of our Valiabad section terminated at late Tournaisian and early

Viséan respectively. The Dozdehband section, nearly situated at the North of the Valiabad

section, exhibits a Mobarak Fm that terminates in the latest Viséan (MFZ15 or V3c in

Belgium) (Bozorgnia, 1973; Vachard, 1996). Foraminiferal data indicate almost the same age

for the top of the Valiabad section, and strongly confirm the regional studies that concluded

that the top of the Mobarak Formation becomes younger in a northwestern direction across the

Alborz Mountains (e.g., Bozorgnia, 1973; Brenckle et al., 2009). As indicated by Bozorgnia

(1973), this age discrepancy might be attributed to differential uplifts across the Alborz that

started in the late Viséan and continued into the Early Permian. Concerning the late Viséan, a

more precise age can be suggested here; indeed, the biozone MFZ13 (former V3bα-V3bβ) due

to its relative paucity in foraminifers can appear as a period of tectonic instability, preventing

the migrations and/or the development of stable biotopes. Furthermore, the exact datation of

MFZ13 might be re-discussed; alternatively, this subzone can be still MFZ12 or yet upper

MFZ13 in age. Consequently, tectonic movements and no-deposition episods might occur

during the interval of time equivalent of the lower MFZ13 in northern Alborz, and/or during

the MFZ12 in central Alborz due to (1) the end of the Mobarak deposits, (2) the apparent

absence of Pojarkovella, in this area. Other geodynamical implications can be found according

to the foraminiferal assemblages and the palaeobiogeography, especially, as a possible

explanation for a narrowing of the northern branch of the Palaeotethys, starting as soon as the

late Viséan, prior to the Eo-Cimmerian suturation.

9.2. Data of the Valiabad foraminifers

The principal biogeographic foraminiferal indexes for the latest Devonian-late Viséan period

(Hance et al., 2011) seem to be: Quasiendothyra kobeitusana (Rauzer-Chernousova, 1948d),

Eoparastaffella spp., Uralodiscus spp., Pojarkovella spp., and Tubispirodiscus spp. The

ostracod Cryptophyllus is also important (Vachard et al., in press).

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The important biostratigraphical marker of the northern border of the Palaeotethys,

Quasiendothyra kobeitusana (Rauzer-Chernousova, 1948d), characteristic of the latest

Devonian DFZ7 biozone is not mentioned in Alborz (the specimen illustrated by Kalantari,

1986, pl. 17, fig. 1 is misinterpreted and corresponds most probably to Praedainella Hance,

Hou and Vachard, 2011); nevertheless, (1) the lithology of the outcrops of this age is totally

unfavourable with red sandstone, red shale, quartzite, and dolomitic sandstone (e.g., Weddige,

1984; Ueno et al., 1997); (2) one specimen of this species has been found in Central Iran

(Bagheri and Stampfli, 2008, pl . 1, fig. A).

The genus Eoparastaffella has migrated, during the biozones MFZ11B and MFZ12, along the

northern shelf of Palaeotethys, the Ural shelves, and rare areas of the southern shelf of the

Palaeotethys (Southern France: Vachard, 1977; Southern Turkey: Altiner, 1981; Alborz:

Bozorgnia, 1973, Vachard, 1996; Brenckle et al., 2009; this study). It remains totally absent in

Northern Africa (from Morocco to Sinai), and from North America, because, as indicated by

Devuyst (2006), the so-called forms of this subcontinent belong in fact to Eoendothyranopsis.

Pojarkovella, although known in Palaeotethys (from Ireland to South China) and Urals (from

south to north), has its maximal diversification in Tajikistan (Simonova and Zub, 1975), South

China (Hance et al., 2011), and Iran (this study).

The radiation of the primitive archaediscids seem appear in a Sinai (Egypt)-Antalaya (southern

Turkey) (Vachard and Moix, in press) but the first maximal diversification of archaediscids

occur probably in the area Kazakhstan (Marfenkova, 1978, 1983, 1991)-Afghanistan (Vachard,

1980; Vachard and Montenat, 1996)-Alborz (this study). Uralodiscus has probably the same

distribution than Eoparastaffella, although it is very rare in South China, and begins to attain

the southern border of the Palaeotethys, in central Morocco (Vieslet, 1983; Vachard and Fadli,

1991) and eastern Egypt (Sinai: Omara and Conil, 1965; Brenckle and Marchant, 1987). The

presence of late Viséan Tubispirodiscus attenuatus in Valiabad, confirms privilegiate

relationships with Kazakhstan, although this species has then migrated, during the early

Serpukhovian, in Belgium, England, Scotland, Ireland, Spain and Morocco (Cózar et al., 2008;

Cózar, pers. communication, July 2012).

Cryptophyllus disappears in the northern border of the Tethys, concomitantly with the

Hangenberg event; i.e. at the latest Devonian (Vachard et al., 2014) or earliest Carboniferous

(Devuyst et al., 2005); but it find a refuge in the Perigondwanan territories up to the upper

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MFZ 12 (= V3a). This latter age was precisely obtained in Valiabad by Bozorgnia (1973); that

seems indicate that the Alborz is still Perigondwanan in this period.

Consequently, many communications of microfaunas seem occur in the perimeter Alborz,

Kazakhstan, Tajikistan, Southern Turkey (Taurus), and South China. The explanation can be

either a system of marine currents in the centre of the Palaeotethys or close contacts between

these territories due to a narrower Palaeotethys. Affinities between foraminifers of South China

and Alborz have been underlined by Gaillot and Vachard (2007) and Brenckle et al. (2009).

Due to these movements of the northern Palaeotethys, the northern Alborz can remained

subsident and constitute some depocenters during the late Viséan-Serpukhovian, whereas the

southern Alborz can be yet emerged and submitted to no-deposition and/or erosion. The

eastern Alborz remains a marine carbonate platform during all the Middle Pennsylvanian

(Jenny, 1977; Jenny et al., 1978; Stampfli, 1978; Lys et al., 1978; Vachard, 1996; Gaetani et

al., 2009).

10. CONCLUSIONS

Early Carboniferous foraminiferal assemblages from the Valiabad section, situated in the

Northern Alborz (Iran) are examined in this contribution. 104 species have been found, which

have allowed the identification of seven Formaniferal zones, based mainely on Poty´s (1974)

zonal scheme, showing zones MFZ8 (late Tournaisian): Eoparastaffella ex gr. rotunda-Lysella

cf. gadukensis assemblage zone; MFZ9-MFZ11 (early Viséan): Eoparastaffella simplex-

Lapparentidiscus bokanensis lowest occurrence zone, Ammarchaediscus lowest occurrence

zone, Uralodiscus-Glomodiscus lowest occurrence zone and Glomodiscus-Archaediscus-

Eotextularia diversa assemblage zone; MFZ12-MFZ14 (upper Viséan): Pojarkovella-Mstinia

fallax-Uralodiscus assemblage zone, Mstinia bulloides-Pseudoendothyra assemblage zone;

and Howchinia gibba, Howchinia bradyana, Tubispirodiscus attenuatus lowest occurrence

zone.

In this study, nine species of Viséan foraminifers including Archaediscus koktjubensis,

Tubispirodiscus attenuatus, Consobrinella consobrina, Koskinotextularia cribriformis,

Permodiscus vetustus, Pirletidiscus sp., Pojarkovella nibelis, P? ketmenica and Mstinia fallax

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are reported for the first time in Iran; and the majority of our archaediscids and pojarkovellids,

which remain in open nomenclature, correspond probably also to new taxa.

Many communications of microfaunas seem to be existed between Alborz, Kazakhstan,

Tajikistan, Taurus, and South China. The explanation can be either privilegied currents in the

centre of the Palaeotethys or strong connections between these territories due to a narrower

Palaeotethys. The assemblages discovered during this study seem to indicate that the Alborz

has, from the the MFZ8 to MFZ11 (i.e., during the Moliniacian) the Alborz has dominantly

relations with Sinai, Taurus, and Antlaya Nappes; i.e., the southern margin of the Palaeotethys;

and, inversely, from MFZ2 to MFZ14 (i.e., Livian and Warnantian), the relations are more

with the northern marign and especially with the Kazakhstan. This suggests that (1) the

Palaeotethys is a narrow ocean during the Visean in this area; (2) a tectonic event occurs

between the MFZ11 and MFZ12; (3) it generates an inversion of the palaeogeographic

relations, either by a new system of oceanic currents, or by a translation to the north of the

Alborz, and possibly a modification of this status of Perigondwanan marinal area into a

Cimmerian terrane, although no phases of rifting and/or oceanic drift is directly known.

This narrowness of the pre-Permian Tethys is also evidenced by some olistostromes of Central

Iran which contains Perigondwanan elements as well as North-Tethyan elements (Bagheri and

Stampfli, 2008; Berra et al., 2014) thanks to the determination of foraminifers by D. Vachard

and brachiopods by L. Angiolini.

ACKNOWLEDGEMENTS

We acknowledge the cooperation of Mr Hassanpour, Mr Divdar, Mr Kamali and Mr Eslami, and

University students for the help in the field work. We thank Dr Pedro Cózar and Profesor

Edouard Poty for providing bibliographic references. We are grateful to Profesor Ian Somerville

for correcting a first draft of this paper. A first draft of our paper was submitted to Dr Luc Hance

and Dr Pedro Cózar. This version was revised by XXXXX and YYYY.

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FIGURES CAPTIONS

Figure 1. Location of the Valiabad section and geological sketch map (modified from Vahdati,

1999).

Figure 2. Sketch map of the Alborz Mountains, with the important cities, the location of some

key-sections (black triangles), and the studied section of Valiabad (rectangle). The arrow shows

the progressively younger top beds of the Mobarak Formation from SE to NW (modified from

Brenckle et al., 2009).

Figure 3. Stratigraphic log of the Valiabad section showing the distribution of foraminiferal

taxa.

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Figure 4. Generic definitions of the names of archaediscoids used in this work according to

Brenckle et al., 1987; Vachard, 1988, and Hance et al., 2011; slightly modified.

Figure 5. Correlation of Belgian Substages and biozonations, established in this study.

Figure 6. Foraminifers of the Valiabad section (Lower Carboniferous Mobarak Formation).

Scale bars = 500 µm for figs. 1-16, 250 µm for 17-29 and 1000 µm for figs. 30-38. Spl =

Sample number.

1. Dainella cf. grandis Grozdilova and Lebedeva in Sultanaev et al., 1978, Spl. MZ11; 2.

Lysella cf. gadukensis Bozorgnia, 1973, Spl. MZ11; 3, 4. Lysella sp. 2, Spl. MZ11; 5-7.

Eoparastaffella ex gr. rotunda Vdovenko, 1971, Spl. MZ11; 8. Eoparastaffella macdermoti

Devuyst and Kalvoda, 2007, Spl. MZ12; 9. Dainella sp., Spl. MZ12; 10, 11. Eoparastaffella

cf. florigena (Pronina, 1963), Spl. MZ12; 12. Eoparastaffella simplex lata Vdovenko, 1971,

Spl. MZ13. 13, 14, 15. Eoparastaffella simplex simplex Vdovenko, 1971, Spl. MZ13; 16.

Eoparastaffella interiecta Vdovenko, 1971, Spl. MZ13; 17. Endothyra ex gr. similis (Rauzer-

Chernousova and Reitlinger in Rauzer-Chernousova et al., 1936), Spl. MZ81; 18. Endothyra

sp., Spl. MZ101; 19. Lapparentidiscus? sp., Spl. MZ15; 20. Omphalotis? sp., Spl. MZ15; 21,

22, 23. Pseudoammodiscoid indet. 21: Spl. MZ15, 22, 23: Spl. MZ23; 24, 25. Lapparentidiscus

bokanensis Vachard, 1980, Spl. MZ30, MZ44; 26. Cf. Mediocris? liae Brenckle, 2004, Spl.

MZ30; 27, 33. Ammarchaediscus sp.1, Spl. MZ31, MZ47; 28, 29. Ammarchaediscus cf.

eospirillinoides (Brazhnikova in Brazhnikova et al., 1967), Spl. MZ44, MZ47; 30. Forschia

subangulata (Möller, 1879), Spl. MZ16; 31, 32. Earlandia vulgaris (Rauzer-Chernousova and

Reitlinger in Rauzer-Chernousova and Fursenko, 1937); Spl. MZ27, MZ37; 34-35.

Ammarchaediscus sp. 2. Spl. MZ49, MZ50; 36-38. Glomodiscus sp. 1, Spl. MZ56, MZ 57.

Figure 7. Foraminifers of the Valiabad section (Lower Carboniferous Mobarak Formation).

Scale bar =250 µm. Spl = Sample number.

1. Lapparentidiscus? sp., Spl. MZ49; 2. Eoparastaffella sp., Spl. MZ50; 3-6. Uralodiscus ex

gr. rotundus (Chernysheva, 1948a), Spl. 50; 7. Uralodiscus cf. sumsariensis (Skvortsov, 1965),

Spl. MZ51; 8, 9. Glomodiscus cf. praeconvexus (Bozorgnia, 1973), Spl. MZ51; 10,11.

Mediocris mediocris (Vissarionova, 1948b), Spl. MZ54, MZ64, MZ104; 12, 13.

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Ammarchaediscus sp. 3, Spl. MZ54; 14-16. Glomodiscus oblongus (Conil and Lys, 1964), 14:

Spl. MZ 54, 15: Spl. MZ 57, 16: Spl. MZ 58; 17. Eostaffella sp., Spl. MZ 55; 18.

Ammarchaediscus sp. 4, Spl. MZ 55; 19. Ammarchaediscus sp. 5, Spl. MZ 56; 20.

Planoarchaediscus sp. 1, Spl. MZ 56; 21. Glomodiscus sp. 2, Spl. MZ 56; 22, 23. Uralodiscus

sp., Spl. MZ 57; 24. Glomodiscus sp. 3, Spl. MZ 59; 25. Archaediscus (involutus stage) sp.,

Spl. MZ 60; 26. Brunsia? sp., Spl. MZ 59, 27. Archaediscus (involutus stage) ex gr. convexus

Grozdilova and Lededeva, 1954, Spl. MZ 59; 28. Glomodiscus sp.4, Spl. MZ 61; 29.

Glomodiscus sp.4, Spl. MZ 62; 30. Archaediscus sp., Spl. MZ 62; 31. Ammarchaediscus sp. 6,

Spl. MZ 71; 32. Ammarchaediscus sp. 7, Spl. MZ 72; 33. Planoarchaediscus sp. 3, Spl. MZ

65; 34. Archaediscus (involutus stage) cf. pulvinus (Conil and Lys, 1964), Spl. MZ 75; 35.

Archaediscus (concavus stage) ex gr. chernousovensis Mamet, Choubert and Hottinger, 1966,

Spl. MZ 62; 36. Archaediscus (involutus stage) sp., Spl. 61; 37. Endothyra ex. gr. bowmani

(Phillips, 1846), Spl. MZ 79; 38. Archaediscus stage ?? ex gr. stilus (Grozdilova and Lebedeva

in Grozdilova, 1953), Spl. MZ 80; 39, 40. Eotextularia diversa (Chernysheva, 1948b), 39: Spl.

MZ 79, 40: Spl. MZ 84; 42. Mediendothyra wjasmensis (Ganelina, 1956), Spl. MZ 79.

Figure 8. Foraminifers of the Valiabad section (Lower Carboniferous Mobarak Formation).

Scale bar = 500 µm for figs. 1-33 and 1000 µm for figs. 37-39. Spl = Sample number.

1-5. Pojarkovella wushiensis (Li, 1991), 1, 2: Spl. MZ 85, 3, 4: Spl. MZ 86, 5: Spl. MZ 87. 6-

20. Pojarkovella ex gr. nibelis (Durkina, 1959), 6: Spl. MZ85, 7-20: Spl. MZ87; 21-30. n.

Genus., Spl. MZ 87; 31. Pojarkovella sp., Spl. MZ 86; 32, 33. Koskinotextularia ex gr. bradyi,

Spl. MZ89; 34. Koskinotextularia cf. cribriformis Eickhoff, 1968, Spl. MZ 92; 35. Omphalotis?

sp., Spl. MZ 86; 36-39. Mstinia fallax (Rauzer-Chernousova and Reitlinger in Rauzer-

Chernousova et al., 1936) Spl. MZ89.

Figure 9. Foraminifers of the Valiabad section (Lower Carboniferous Mobarak Formation).

Scale bar =250 µm for figs. 1-34 and 500 µm for figs. 35-40. Spl = Sample number.

1,2. Pojarkovella? ketmenica Simonova and Zub, 1975, Spl. MZ 85; 3. Omphalotis? sp., Spl. MZ

86; 4. Endothyra paraprisca Rozovskaya, 1963, Spl. MZ 86; 5, 6. Uralodiscus abnakensis

(Bozorgnia, 1973), Spl. MZ 86; 7. Planoarchaediscus aff. rigens (Conil and Lys, 1964), Spl. MZ

86; 8. Archaediscus mixtus (Conil and Lys, 1964), Spl. MZ 86; 9. Archediscus karreri (Brady,

1873), Spl. MZ 90; 10. Archaediscus koktjubensis (rauzer-Chernousova, 1948d), Spl. MZ 93; 11.

Uralodiscus rotundus (Chernysheva, 1948a), Spl. MZ 93; 12. Permodiscus vetustus Dutkevich in

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Chernysheva, 1948a, Spl, MZ 96; 13. Planoarchaediscus cf. contiguus (Omara and Conil, 1965),

Spl. MZ 93; 14, 15. Pirletidiscus sp , 19: Spl. MZ 97, 20: MZ 98; 16, 17. Kasachstanodiscus sp.,

Spl. MZ 99; 18-20. Nodosarchaediscus tchalussensis (Bozorgnia, 1973), Spl. MZ 99; 21, 22.

Nodosarchaediscus demaneti (Conil and Lys, 1964), 27: Spl. MZ 107, 28: MZ 116; 23.

Archaediscus moelleri (Rauzer-Chernousova, 1948c), Spl. MZ 110; 24. Archaediscus

acuminatus (Marfenkova, 1983), Spl. MZ 116; 25. Tetrataxis pallae (Conil and Lys, 1964), Spl.

MZ 109; 26. Tetrataxis palaeotrochus (Brady, 1876), Spl. MZ 107; 27, 28. Archaediscus

krestovnikovi (Rauzer-Chernousova, 1948d), Spl. MZ 112; 29, 30. Howchinia gibba (Möller,

1879), 29: Spl. MZ 114, 30: Spl. MZ 116; 31. Howchinia bradyana (Howchin, 1888), Spl. MZ

121; 32. Endostaffella parva (Möller, 1879), Spl. MZ 119. 33, 34. Tubispirodiscus attenuatus

(Marfenkova, 1978), 33: Spl. MZ 121, 34: Spl. MZ 119; 35, 36. Consobrinella sp., Spl. MZ 96,

37, 38. Consobrinella consobrina (Lipina, 1948), 37: Spl. MZ 104, 38: Spl. MZ 107; 39. Mstinia

bulloides (Mikhailov, 1939), Spl. MZ 98; 40. Tetrataxis acuta Durkina, 1959, Spl. MZ 108.

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. Location of the Valiabad section and geological sketch map (modified from Vahdati, 1999). 362x386mm (120 x 120 DPI)

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Skech map of the Alborz Mountains, with the important cities, the location of some key-sections (black circle), and the present studied section of Valiabad (rectangular). The arrow shows the increasing age of the top beds of the Mobarak Formation from SE to NW (modified from Brenckle et al., 2009). The key sections as follows: 1: Dozdehband; 2: Geirud; 3: Abnak; 4: Mobarakabad; 5: Aruh; 6: Gaduk; 7: Shahmirzad; 8: Peyghambaran; 9: Simeh Koh; 10: Abrendan; 11: Kalariz; 12: Viru; 13: Khoshyeilagh; 14: Kalate; 15:

Nodeh-Sud. 859x457mm (120 x 120 DPI)

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Stratigraphic log of the Valiabad section showing the distribution of foraminiferal taxa. 929x677mm (120 x 120 DPI)

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933x681mm (120 x 120 DPI)

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Generic definitions of the names of archaediscoids used in this work according to Brenckle et al., 1987; Vachard, 1988, Hance et al., 2011, and Vachard and Moix (unpublished data); slightly modified.

309x311mm (120 x 120 DPI)

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Correlation of the subdivisions used in this study.

429x355mm (120 x 120 DPI)

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Foraminifers of the Valiabad section (Lower Carboniferous Mobarak Formation). Scale bars = 500 µm for figs. 1-16, 250 µm for 17-29 and 1000 µm for figs. 30-38. Spl = Sample number

472x645mm (60 x 60 DPI)

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Foraminifers of the Valiabad section (Lower Carboniferous Mobarak Formation). Scale bar =250 µm. Spl =

Sample number

463x634mm (120 x 120 DPI)

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Foraminifers of the Valiabad section (Lower Carboniferous Mobarak Formation). Scale bar = 500 µm for figs. 1-33 and 1000 µm for figs. 37-39. Spl = Sample number

466x647mm (120 x 120 DPI)

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Foraminifers of the Valiabad section (Lower Carboniferous Mobarak Formation). Scale bar =250 µm for figs. 1-34 and 500 µm for figs. 35-40. Spl = Sample number.

464x645mm (120 x 120 DPI)

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