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Refinements in Biostratigraphy, Chronostratigraphy, and Paleogeography of the Mississippian (Lower Carboniferous) Mobarak Formation, Alborz Mountains, Iran

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Refinements in Biostratigraphy, Chronostratigraphy, and Paleogeography of the Mississippian (Lower Carboniferous) Mobarak Formation, Alborz Mountains, Iran GeoArabia, v. 14, no. 3, 2009, p. 43-78 Mississippian (Lower Carboniferous) Mobarak Formation, Iran Gulf PetroLink, Bahrain Refinements in biostratigraphy, chronostratigraphy, and paleogeography of the Mississippian (Lower Carboniferous) Mobarak Formation, Alborz Mountains, Iran Paul L. Brenckle, Maurizio Gaetani, Lucia Angiolini and Maryamnaz Bahrammanesh ABSTRACT Detailed sampling of limestones from the Mobarak Formation at the Abrendan and Abnak measured sections in the eastern and central Alborz Mountains, northern Iran, yielded a diverse assemblage of Tournaisian – Lower Visean (Mississippian/ Lower Carboniferous) calcareous microfossils (foraminifers, algae, incertae sedis). The Abrendan locality contains Tournaisian foraminifers in the upper part of the formation that correlate to the Ivorian and upper Courceyan – lower Chadian substages of western Europe and the Kosvinsky Horizon of the Russian Platform. Brachiopods confirm a Tournaisian age for the lower part of the Mobarak, which lacks age-diagnostic calcareous microfossils. Lower Visean foraminifers at Abnak provide good correlation to the western European Moliniacian and Arundian substages and the Russian Bobrikovsky Horizon. Synthesis of foraminiferal data from this and other published reports indicates that the top of the Mobarak Formation becomes increasingly older across the Alborz to the southeast, caused most likely by Pennsylvanian (Upper Carboniferous) exposure and erosion in the south followed by a latest Pennsylvanian – Early Permian transgression from the north. The microbiota at both sections and the macrofossils at Abrendan show close affinity to the warm-water Paleo-Tethyan Ocean, seemingly contradicting Early Mississippian paleomagnetic reconstructions placing the Alborz region at 45–50° South latitude. The discrepancy is not resolvable at this time, but the answer may lie in the circulation of Paleo-Tethyan currents to the south along the Gondwanan shelf, rather than to repositioning the Alborz region to the northern side of the Paleo-Tethyan Ocean. INTRODUCTION The Mississippian (Lower Carboniferous) Mobarak Formation of Assereto (1963) is a mixed carbonate-siliciclastic marine unit that crops out in an arcuate pattern along the flanks of the EW- trending Alborz Mountains of northern Iran (see location map in Bozorgnia, 1973, and Figure 1). The present definition of the formation (Stepanov, 1971; Bozorgnia, 1973) includes most Tournaisian and Visean rocks (Figure 2) that Assereto (1963, 1966) initially placed in the Mobarak and partly time-equivalent Geirud formations (Figure 3); the distinction between his two formations is based on lithologic differences that still require a more detailed stratigraphic nomenclature. Initial attempts at dating and locally correlating the Mobarak focused on macrofossil studies (see historical reviews in Gaetani, 1968; Stepanov, 1971; and Vachard, 1996) based primarily on brachiopod and coral occurrences. Most published microfossil investigations appeared in the latter part of the last century and concentrated on identifications and age interpretations of calcareous foraminifers, as will be explored further herein. Conodonts, another potentially useful microfossil group within the Mobarak (Ahmadzadeh Heravi, 1971; Ueno et al., 1997; Habibi et al., 2008), have yet to be examined in detail throughout the Alborz region. The objectives of this paper are to (1) provide new information on the distribution of calcareous microfossils (foraminifers, algae, and incertae sedis) from the Abrendan (eastern Alborz) and Abnak (central Alborz) measured sections located in Figure 1, (2) relate their occurrences to those published in previous Alborz foraminiferal studies, (3) comment on their relationship to other biotas within 43 Downloaded from http://pubs.geoscienceworld.org/geoarabia/article-pdf/14/3/43/4567073/brenckle_43-78.pdf by guest on 02 October 2021 Brenckle et al. 52º 54º Gonbad-e-Qabus 0 N 50 Caspian Sea km 13 Aliabad 11 Fazelabad 12 14 Gorgan Chalus Sari 1 Amol 10 P UPPER VISEAN 9 TO Abrendan Figure 4 Damghan Figure 6 36º 2 3 LOWER VISEAN 36º Abnak TOP 34°E 38° 42° 46° 50° 54° 58° 38°N TURKEY Caspian 38° 6 Sea 4 7 Karaj Firuzkuh 8 CYPRUS SYRIA Figure 1 34° LEBANON IRAN 34° 5 Med IRAQ N Sea 0 300 JORDAN 30° KUWAIT km 30° TEHRAN Semnan Gulf URNAISIAN of P TO Suez TO BAHRAIN 26° 26° QATAR EGYPT Gulf of 52º 54º Arabian UAE Oman Shield 22° 22° SAUDI OMAN SUDAN Red ARABIA Sea Figure 1: Mobarak foraminifer localities in the Alborz Mountains: Arabian 18°34° 38° 42° 46° 50° 54° Sea (1) Dozdehband (Bozorgnia, 1973; Pirlet and Conil, 1977); (2) Geirud ERITREA YEMEN 14° 14° SOCOTRA (Bozorgnia, 1973; = Jajerud section of Lys et al., 1978); (3) Abnak (Stepanov, ETHIOPIA1971; Bozorgnia,Gulf of Aden 1973; Pirlet and Conil, 1977; this paper); (4) Mobarakabad (Bozorgnia, 1973; Meissami et al., 1978); (5) Aruh (Bozorgnia, 1973); (6) Gaduk (Bozorgnia, 1973; Devuyst, 2006; Devyust and Kalvoda, 2007); (7) Shahmirzad (Bozorgnia, 1973; Ueno et al., 1997; Habibi et al., 2008); (8) Peyghambaran (Bozorgnia, 1973); (9) Abrendan (this paper); (10) Kalariz (Bozorgnia, 1973); (11) Kalate (Lys et al., 1978); (12) Viru (Lys et al., 1978); (13) Nodeh-Sud (Lys et al., 1978); (14) Khoshyeilagh (Bozorgnia, 1973). For localities above the uppermost dashed line, the top of the Mobarak Formation terminates in the Upper Visean; for those between the dashed lines the top of the Mobarak ends in the Lower Visean; and for those below the lowermost dashed line the top does not extend above the Tournaisian. See Figures 2 and 3 for stratigraphic terminology used in this paper. International Belgian British Russian Subsystem Series Stage Substage Substage Horizon Figure 2: Chrono- stratigraphic Brigantian Venevsky terminology Warnantian Mikhailovsky used in this upper V2b-V3c Asbian Aleksinsky paper, showing Middle Visean correlation Livian Holkerian Tulsky between Arundian Bobrikovsky international and lower V1a-V2a Moliniacian Mississippian Chadian Radaevsky regional Paleo- (part) Kosvinsky Tethyan units. upper Tn3a-c Ivorian The position of Kizelovsky the base of the Tournai- Cherepetsky Moliniacian Lower Courceyan sian Upinsky substage follows lower Tn1b-Tn2 Hastarian the emendation Malevsky of Poty et al. Gumerovsky (2006). 44 Downloaded from http://pubs.geoscienceworld.org/geoarabia/article-pdf/14/3/43/4567073/brenckle_43-78.pdf by guest on 02 October 2021 Mississippian (Lower Carboniferous) Mobarak Formation, Iran the Paleo-Tethyan Realm, and (4) discuss their implication for regional and global paleogeography. Representative microfossils from the two measured sections are illustrated on Plates 1-12 and supplemental information on macrofossil occurrences (mostly brachiopods) and their significance is also included. This study developed from a project on Pennsylvanian (Upper Carboniferous) – Early Triassic stratigraphy in the Alborz (Gaetani et al., 2009) that was part of the Middle East Basin Evolution Programme (MEBE). The sections were sampled because of their relevance in establishing regional stratigraphic relationships at the Mississippian – Pennsylvanian boundary. BIOSTRATIGRAPHY AND CHRONOSTRATIGRAPHY Foraminifers Foraminifers are the primary calcareous microfossil group used to correlate and date the Mobarak Formation, but little was done prior to the pioneering paper of Bozorgnia (1973). He described and illustrated the microfauna from numerous outcrop sections (Figure 1) and established a zonal scheme to correlate across the Alborz Mountains. His research showed the value of foraminifers in elucidating the local chronostratigraphy, e.g., identifying diachroneity along the top of the Mobarak, and also showed the feasibility of long-distance correlation by relating the assemblages to the better known Dinantian sequences in Belgium. Despite this promising start, only a few follow-up investigations have been published. Pirlet and Conil (1977) provided additional taxonomic information on the Dozdehband and Abnak sections as did Meissami et al. (1978) for the Mobarakabad area. Lys et al. (1978) published a generalized range chart and selected microfossil illustrations from localities in the central and eastern Alborz (Figure 1). In an excellent summary of progress to date, Vachard (1996) refined Bozorgnia’s foraminiferal zonal scheme by incorporating data from both published reports and dissertations (Jenny, 1977; Stampfli, 1978), and Kalvoda (2002) utilized this information in his analysis of the paleobiogeography of the Alborz region. Ueno et al. (1997) related the foraminiferal succession at the Shahmirzad section to major lithologic units in the Mobarak Formation, and Devuyst (2006) identified taxa within the Tournaisian – Visean boundary beds at the Gaduk section (Figure 1). Bozorgnia (1973) and Vachard (1996) established a credible zonal and chronostratigraphic framework but did not show the sample-by-sample distribution of individual taxa within the Mobarak Formation. Without that information, a high-resolution chronostratigraphy, now promoted by the Carboniferous Subcommission and by others to standardize series, stage and substage boundaries, cannot be Stepanov Bozorgnia Wendt et al. Stage/Age Assereto (1963, 1966) (1971) (1973) (2005) "D" member Visean Mobarak Mobarak Mobarak Mubarak "C" member Limestone Formation Formation Limestone "B" Tournaisian member Geirud Formation Khoshyeilagh "A" Geirud Khoshyeilagh Geirud Formation Famennian member Formation Formation Formation Figure 3: Name changes to strata assigned originally by Assereto
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