Sedimentary facies and sequence stratigraphy of the Asmari Formation at Chaman-Bolbol, Zagros Basin, Iran

Amirshahkarami, Mahnaz; Vaziri‐Moghaddam, Hossein; Taheri, Asghar

doi:10.1016/j.jseaes.2006.06.008

Cited by 87 publications

(48 citation statements)

References 36 publications

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“…shallow shelf lagoon ;Wilson 1975;Epting 1980;Flügel 1982). Almost similar foraminiferal facies were reported from the shelf lagoon or inner ramp environments in Iran (Vaziri-Moghaddam et al 2006;Amirshahkarami et al 2007;Rahmani et al 2009;Seyrafian et al 2011 andSajadi et al 2014), from NE Italy (Bassi et al 2007), from SE Turkey (Sirel 1996(Sirel , 2003 and from back reef environments in Iraq (Edgell 1997;Al-Banna 2004). In contrast to the Tuzlagözü section, the limestones enclosing the foraminiferal packstone-grainstone facies alternate with pelecypod bearing sandstone, fossiliferous (mainly ostracoda) siltstone with plant fragments, sandy conglomerate and evaporites and mudstones with planktonic foraminifera in the Egribucak section (Fig.…”

Section: Paleoenvironmental and Paleoecologic Interpretationssupporting

confidence: 59%

Planktonic and benthic foraminiferal biostratigraphy of the Middle Eocene–Lower Miocene successions from the Sivas Basin (Central Anatolia, Turkey)

Hakyemez¹,

Özgen-Erdem²,

Kangal³

2016

Geologica Carpathica

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Planktonic and benthic foraminifera are described from the Middle Eocene-Lower Miocene successions in the Sivas Basin, Central Anatolia. An integrated foraminiferal zonation provides new age assignments in terms of a great number of taxa for the studied sections. Four biostratigraphical intervals are first recorded based on the concurrent ranges of sporadically occurring but well preserved planktonic foraminiferal assemblages. The first interval characterized by the co-occurrences of Acarinina bullbrooki, Truncorotaloides topilensis and Turborotalia cerroazulensis is referable to the E11 Zone of late Lutetian-early Bartonian. An assemblage yielding Paragloborotalia opima accompanied by Globigerinella obesa forms a basis for the late Chattian O5 Zone. The successive interval corresponds to the late Chattian O6 Zone indicated by the presence of Globigerina ciperoensis and Globigerinoides primordius along with the absence of Paragloborotalia opima. The early Aquitanian M1 Zone can be tentatively defined based mainly on the assemblage of Globigerina, Globigerinella, Globoturborotalita and Tenuitella. The biostratigraphical data obtained from the benthic foraminifera assign the studied sections to the SBZ 21-22, SBZ 23 and SBZ 24 ranging in age from Rupelian to Aquitanian. The SBZ 23 and 24 are well constrained biozones by the occurrences of Miogypsinella complanata and Miogypsina gunteri, respectively, whereas the SBZ 21-22 defined by nummulitids and lepidocylinids in the Tethyan Shallow Benthic Zonation is characterized dominantly by peneroplids, soritids and miliolids in the studied sections. Benthic foraminiferal assemblages suggest different paleoenvironments covering lagoon, algal reef and shallow open marine whereas planktonic foraminifera provides evidence for relatively deep marine settings on the basis of assemblages characterized by a mixture of small-sized simple and more complex morphogroups indicative for intermediate depths of the water column.

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Section: Paleoenvironmental and Paleoecologic Interpretationssupporting

confidence: 59%

Planktonic and benthic foraminiferal biostratigraphy of the Middle Eocene–Lower Miocene successions from the Sivas Basin (Central Anatolia, Turkey)

Hakyemez¹,

Özgen-Erdem²,

Kangal³

2016

Geologica Carpathica

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“…The distal middle shelf facies types are differentiated from the proximal middle shelf ones by the greater amount of micritic matrix and an increase in the flatness and size of the perforate foraminifera. High taxonomic diversity of perforate foraminifers, corallinaceans, echinoids, bryozoans, mud micrite matrix as well as the stratigraphic position suggests the deposition of facies 2 in a shallower slope environment (Amirshahkarami et al, 2007). The abundance of deep living larger foraminifera (large and flat nummulitids and lepidocyclinids) and the presence of typical open marine skeletal fauna including echinoids and corallinaceans suggest sedimentation in the middle shelf's oligophotic zone (Geel, 2000;Bassi et al, 2007;Brandano et al, 2009).…”

Section: Discussionmentioning

confidence: 99%

Facies analysis and sequence stratigraphy of the Asmari Formation in the northern area of Dezful Embayment, south-west Iran

Zoeram¹,

Vahidinia²,

Mahboubi³

et al. 2013

Studia UBB Geologia

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Abstract. This paper deals with the sequence stratigraphy of the Oligocene (Rupelian-Chattian)-Early Miocene (Burdigalian) Asmari Formation based on microfacies analysis of the sediments in the Ghale Nar Oilfield, central area of Zagros fold-thrust belt. Fourteen facies types typical for upward shallowing trend from open marine (MF 1-3), to shoal (MF 4-5), semi-restricted and restricted lagoon , and finally to near-shore lagoon (MF 13-14) depositional environments were identified. Based on the environmental interpretations, we reconstructed a homoclinal ramp mainly represented by its inner and middle sectors. Facies types MF 4-14 are characterized by the occurrence of large and small porcelaneous benthic foraminifera representing a shallow-water setting of an inner ramp influenced by wave-and tide-related processes. MF1 (Pabdeh Formation), and 2-3 with planktonic, large and small hyaline benthic foraminifera represent between fair weather wave base (FWWB) and storm wave base (SWB). Four third-order depositional sequences were recognized. In order to better correlate the identified sequences with those pre-defined of the Asmari Formation in the Dezful Embayment and the Izeh zone that are chronologically well-known, we use their number instead of their name. Sequence 2 mainly consists of an open marine environment in the base, followed by semi-restricted to restricted lagoonal facies. Sequences 36 are characterized by semi-restricted to restricted lagoonal facies. Moreover, the regional relative sea-level change curves correlate well with the global sea-level change curves.

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“…In microfacies C 2 the presence of intraclast, coated grains and good sorting is a sign of shoal environment [11]. Skeletal fragments like bryozoan, relating to shoal environment can also be seen in C 3 microfacies [8] [21] [34]. This environment causes a separation between lagoon and open marine environments.…”

Section: Discussionmentioning

confidence: 99%

Facies Interpretation, Depositional Environment and Sequence Stratigraphy of the Sartakht Formation in the Bakhshi Section, Located in Kalmard Block, East-Central Iran

Emraninasab¹,

Adabi²,

Majidifard³

et al. 2016

OJG

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B. H. Emraninasab et al. 315HST system tracts, separated from each other by MFS. Sartakht formation rocks in Bakhshi section are deposited in a low-angle homoclinal ramp, mostly in the inner ramp, located in the south of Paleotethys Ocean. The depositional sequence identified in Sartakht formation points to the age of middle Permian, conforming to middle Absaroka II supersequence. The upper erosional boundary between Sartakht and Hermez formations conforms to the global-scale sea level fall.

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Sedimentary facies and sequence stratigraphy of the Asmari Formation at Chaman-Bolbol, Zagros Basin, Iran

Cited by 87 publications

References 36 publications

Planktonic and benthic foraminiferal biostratigraphy of the Middle Eocene–Lower Miocene successions from the Sivas Basin (Central Anatolia, Turkey)

Planktonic and benthic foraminiferal biostratigraphy of the Middle Eocene–Lower Miocene successions from the Sivas Basin (Central Anatolia, Turkey)

Facies analysis and sequence stratigraphy of the Asmari Formation in the northern area of Dezful Embayment, south-west Iran

Facies Interpretation, Depositional Environment and Sequence Stratigraphy of the Sartakht Formation in the Bakhshi Section, Located in Kalmard Block, East-Central Iran

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