◄ Carnets Geol. 23 (6) ►
Outline:
[1. Introduction]
[2. Geological setting and lithostratigraph]
[3. Materials and methods]
[4. Gzhelian foraminifers in Iran]
[5. Pseudoacutella partoazari assemblage zone]
[6. Carbonate microfacies]
[7. Remarks on Pseudoacutella and Pseudonovella]
[8. Conclusions]
and ...
[Bibliographic references]
Department of Geology, Earth Sciences Research Center, Zahedan Branch, Islamic Azad University, Zahedan (I.R. Iran)
University Lille 1, UMR CNRS 8198 Evo-Eco-Paleo, SN5, 59655 Villeneuve d'Ascq
Cedex (France);
1 rue des Tilleuls, 59152 Gruson (France)
Published online in final form (pdf) on June 30, 2023
DOI 10.2110/carnets.2023.2306
[Editor:
Brian Pratt; technical editor: Bruno R.C. Granier]
A foraminiferal assemblage is reported from the Zaladou Formation in the Tabas Block (Shishtu Section), Central Iran. This assemblage comprises 16 species belonging to 14 genera, and encompasses the fusulinids Pseudoacutella partoazari, Grovesella tabasensis, Gr. aff. australis, Gr. sphaerica, Gr. sphaerica var. quadrata, Gr. cf. staffelloides, Schubertina sp., Schubertella sp., and the smaller foraminifers Eotuberitina sp., Lasiodiscus tenuis, Raphconilia cf. minor, R. multihelicis, R. modificata, Tetrataxis cf. parviconica, Globivalvulina ex gr. bulloides, Gl. graeca, Calcivertella heathi, Tansillites sp., Palaeonubecularia? sp., Hemigordiellina sp., Nodosinelloides longa, and N. longissima. The age of this assemblage is considered to be Gzhelian. The assemblage is dominated by the fusulinid Pseudoacutella partoazari with a low total diversity of smaller foraminifers. This assemblage is compared to similar assemblages in other parts of Iran and well as the USA. An evolutionary lineage of Pseudoacutella partoazari is also proposed. It is confirmed that Pseudonovella differs from Pseudoacutella by the periphery rounded-carinate (carinate in Pseudoacutella), pseudochomata less developed, and the type of coiling (Pseudoacutella is truly planispiral involute). Pseudonovella is suggested here as the ancestor of Pseudoacutella. This assemblage bears one unusual attribute, the overwhelming dominance of the fusulinid Pseudoacutella and the relatively low total diversity, compared with similar foraminifera from Alborz, Sanandaj-Sirjan, Sabzevar and central Iran, which present warm and humid conditions during the Late Carboniferous.
• Ozawainelloid;
• Pseudoacutella
partoazari;
• Gzhelian;
• Tabas Block;
• Central Iran
Yarahmadzahi H. & Vachard D. (2023).- Gzhelian (latest Carboniferous) Pseudoacutella partoazari foraminiferal assemblage from the Tabas Block (Central Iran).- Carnets Geol., Madrid, vol. 23, no. 6, p. 107-122.
À propos de l'association de foraminifères à Pseudoacutella partoazari du Gzhélien (Carbonifère terminal) du Bloc de Tabas (Iran central).- Une association de foraminifères de la Formation de Zaladou du Bloc de Tabas (coupe de Shishtu, Iran central) est décrite. Cette association comprend 16 espèces appartenant à 14 genres ; elle réunit les fusulinides Pseudoacutella partoazari, Grovesella tabasensis, Gr. aff. australis, Gr. sphaerica, Gr. sphaerica var. quadrata, Gr. cf. staffelloides, Schubertina sp., Schubertella sp., et les petits foraminifères Eotuberitina sp., Lasiodiscus tenuis, Raphconilia cf. minor, R. multihelicis, R. modificata, Tetrataxis cf. parviconica, Globivalvulina ex gr. bulloides, Gl. graeca, Calcivertella heathi, Tansillites sp., Palaeonubecularia? sp., Hemigordiellina sp., Nodosinelloides longa, and N. longissima. Cette association, dominée par le fusulinide Pseudoacutella partoazari et à faible diversité totale des petits foraminifères, est comparée à celles d'autres régions de l'Iran, ainsi qu'à celles des ÉUA. Son âge est considéré comme étant gzhélien. Durant le Carbonifère supérieur, elle serait le témoin de conditions plus chaudes et plus humides que celles enregistrées par les associations de l'Elbourz, de Sanandaj-Sirjan, de Sabzevar et de l'Iran central. Par ailleurs, une lignée évolutive de Pseudoacutella partoazari est proposée. Celle-ci confirme que Pseudonovella diffère de Pseudoacutella par sa périphérie carénée-arrondie (elle est carénée chez Pseudoacutella), des pseudo-chomata moins développés et son type d'enroulement (seul Pseudoacutella est réellement planispiralé involute). Toutefois, Pseudonovella pourrait même être l'ancêtre de Pseudoacutella.
• Ozawainelloïdes ;
• Pseudoacutella partoazari ;
• Gzhélien ;
• Bloc de Tabas ;
• Iran central
Upper Carboniferous (Gzhelian) strata in Iran are basically widespread in the Central Iran, Sabzevar tectonic zone, Alborz Mountains, and the Sanandaj Sirjan zone (e.g., Leven & Taheri, 2003; Leven & Gorgij, 2006, 2011a, 2011b; Gaetani et al., 2009; Alipour et al., 2013; Gorgij & Leven, 2013; Yarahmadzahi & Vachard, 2014, 2018, 2019; Badpa et al., 2011, 2014, 2015; Yarahmadzahi et al., 2016; Fassihi et al., 2014, 2017, 2020; Niko & Badpa, 2020; Jalali et al., 2021). In the northern Tabas Block (Ozbak Kuh mountains), these strata are defined as the Zaladou Formation. Fusulinids and smaller foraminiferal assemblages characterizing the latest Gzhelian were described in Zaladou Formation in central Iran (Leven & Taheri, 2003; Leven & Gorgij, 2006; Yarahmadzahi & Vachard, 2018; Jalali et al., 2021). In this paper, we review the geographic distribution, stratigraphic occurrence, and taxonomy of Pseudoacutella partoazari Yarahmadzahi & Vachard, 2014. We further make some considerations on the paleobiogeographic and phylogenetic characters of this species.
Upper
Carboniferous deposits of north Tabas Block is well exposed in the Ozbak Kuh
area (Stöcklin, 1971). Structurally, the Ozbak Kuh mountains, located in
the north of the Tabas Block, are part of Central Iran (Aghanabati,
2004). The Shishtu section is situated near the Shishtu village (Fig.
1A-C 
).
There, the Upper Carboniferous and Lower Permian foraminifera of the Zaladou
Formation were accurately studied (e.g.,
Leven & Taheri, 2003; Leven & Gorgij, 2006b;
Yarahmadzahi, 2011; Yarahmadzahi & Vachard, 2018; Jalali
et al., 2021). Lithostratigraphically,
this part of the Shishtu section corresponds to the Anarak Group including the
Zaladou (Gzhelian-Asselian) and Tigh e Madanu (Sakmarian)
formations. The Zaladou Formation unconformably overlies the Carboniferous (Moscovian)
Absheni Formation; it is approximately 60 m thick. The Tigh e Madanu
Formation is 100 m thick. The Zaladou Formation is clearly subdivided into
eight units (Fig. 2 )
from bottom to top:
Unit 1. (24.3 m) Gray, green and purple shale and brown, thin- and medium-bedded with interbedded green, thin-bedded microconglomerate and sandy limestone with bioclasts including smaller foraminifers, echinoderms and bryozoans;
Unit 2. (4.9 m) Gray, thin-bedded limestone. Small foraminifers, echinoderms, bryozoans and brachiopods were observed among bioclasts;
Unit 3. (5.6 m) Gray and brown, medium-bedded limestone and gray shale with bioclasts including smaller foraminifers and brachiopods;
Unit 4. (2.1 m) Gray
thick-bedded coral limestone (Fig. 3 );
Unit 5. (4.7 m) Gray and purple, thin and medium-bebded fusulinid limestone;
Unit 6. (3.8 m) Gray shale including very thin-bedded brachiopods limestone;
Unit 7. (6.8 m) Gray, medium- and thin-bedded limestone with bryozoans and echinoderms bioclasts;
Unit 8. (7.56 m) Gray and purple, thin- and thick-bedded fusulinid limestone with interbedded gray shale with bryozoans, echinoderms and smaller foraminifers.
|
Figure 1:
Geological setting of
the studied area, Ozbak Kuh region (Tabas Block, east-central Iran). A)
tectonic map of Iran (modified from Zanchi et
al., 2009). AA = Anatolian-Armenian Block; AMC = Anarak Metamorphic Complex;
KDF = Kopeh Dagh Foredeep; MZT = Main Zagros Thrust. B) geographic position
(star) of the Shishtu section. C) cross-section of Zaladou Fm. |
|
Figure 2:
Lithostratigraphic
column with the main species of Pseudoacutella partoazari in the Zaladou
Formation, Shishtu section, Ozbak Kuh region (Tabas Block, east-central
Iran). |
|
Figure 3:
Unit 5 photo and sampling location. |
The Pseudoacutella
partoazari assemblage described in this study was sampled 1.5 km to the east
of the village of Shishtu (GPS coordinates: 34°39'08.0"N
57°11'14.0"E) and 150 km to the northeast of the town of Tabas (Fig.
1B ). It
was collected from the middle part of Zaladou Formation, which is composed of
bioclastic limestone of medium- to thick-bedded, which in some cases emerges
from the rock (layer 16).
Taxonomic investigations were performed on 10 thin sections using a Leitz Wetzlar (Laborlux 11 pol) microscope. Photomicrographs were taken using Superior Statistical Analysis Pro (with version 9.0 of LIMDEP, 2008).
The material from Shishtu section is stored at the Earth Sciences Research Center, Islamic Azad University of Zahedan, Iran (collection numbers SH16a-j).
The Gzhelian fusulinids have been well studied in Iran (Gaetani et al., 2009; Leven & Taheri, 2003; Leven & Gorgij, 2006, 2011a, 2011b; Yarahmadzahi, 2011; Fassihi et al., 2019; Jalali, 2021).
Endemic fusuline species from Gzhelian in Iranian Plateau are noticeably rare in foraminiferal assemblages. Compared to similar fusuline assemblages in the Eastern European Platform, Iranian fusuline species are less diversified; still and all, Iranian fusulines have not been well studied. Furthermore, a large number of fusulinids reported from Iran belongs to Ruzhenzevites and Schwageriniformis species. In spite of their differences from typical specimens obtained from the Eastern European Platform, Iranian fusuline species have common components with the collections found in the northern part of the Tethys territory (Spain, Carnic Alps, southern Turkey, Darvaz, and Fergana).
Gzhelian fusuline assemblages which have been obtained from different tectonic blocks of Iran have specific regional characteristics (Leven & Gorgij, 2011). For instance, the fusuline complex from the Yazd Block is more diverse than the Tabas, Alborz, and Sanandaj-Sirjan Blocks. In addition, the genera Rauserites, Triticites, and Ruzhenzevites, which are found in all tectono-sedimentary blocks of Iran, are also found in the Yazd Block, in the lower part of the sequence Schwagerina genus and in the upper parts Ultradaixina, Schellwienia, Anderssonites, and Likharevites genera. In other blocks, either the stratigraphic intervals are absent or other fusulinids appear. Important and noticeable specimens include Anderssonites genus in Tuyeh Formation (Alborz zone) or Anderssonites and Schellwienia genera in Zaladou Formation (Tabas Block). In the Sanandaj-Sirjan zone, the fusuline complex is based on the abundance and diversity of Ruzhenzevites while this genus is less important in Yazd and Alborz blocks.
Gzhelian smaller foraminifers have been well studied in Iran (Vachard, 1996; Alipour et al., 2013; Yarahmadzahi et al., 2016; Fassihi, 2017; Fassihi et al., 2017, 2019, 2020; Fassihi & Shirezadeh, 2018; Yarahmadzahi & Vachard, 2018, 2019; Jalali et al., 2021).
|
Figure 4:
Gzhelian
small-shelled fusulines and smaller foraminifera list from Iran. |
Previous
studies on smaller foraminifers of Iran were more focused on Upper Carboniferous.
For instance, Gzhelian smaller foraminifers described until recently (Fig. 4 )
comprise:
In the Alborz Mountains:
Gadouk section (Yarahmadzahi et al., 2016). The Gzhelian smaller foraminifera in section are located in the Nodosinelloides shikhanica-Geinitzina primitiva Zone, and the accompanying foraminifera of this zone include Geinitzina ex gr. uralica.
In the Chaman-Saver area, Alipour et al. (2013) reported Gzhelian smaller foraminifera in two biozones:
A) Nodosinelloides potievskayae-Vervilleina bradyi Zone. The smaller foraminifers of this biozone are: Nodosinelloides potievskayae Mamet & Pinard, 1996, Palaeotextularia bella Lipina, 1949, Climacammina durabilis Konovalova, 1962, Cribrogenerina celebrata? Lin, 1978, C.? elegans (Möller, 1879, sensu Schellwien, 1898, emend. Vachard & Krainer, 2001), Tetrataxis conica Ehrenberg, 1854, T. hemiovoides? Morozova, 1949, T. lata Spandel, 1901, Tezaquina sp. 1, Vervilleina bradyi (Spandel, 1901), Nodosinelloides potievskayae Mamet & Pinard, 1996, N. cf. pinardae Groves & Wahlman, 1997, 'Nodosinelloides-Geinitzina transitional forms' sensu Groves, 2000, Geinitzina postcarbonica Spandel, 1901, Gr. ex gr. primitiva Potievskaya, 1962.
B) Calcitornella heathi-Nodosinelloides sp. Zone. The following smaller foraminifers are associated: Diplosphaerina inaequalis (Derville, 1931), Tuberitina sp., Raphconilia damghanica Alipour & Vachard in Alipour et al., 2013, R. modificata (Potievskaya, 1962), Climacammina cf. durabilis Konovalova, 1962, C. ex gr. elegans (Möller, 1879), C. sp., Deckerella laheei Cushman & Waters, 1928, D. tenuissima Reitlinger, 1950, Tetrataxis aff. baschkirica Morozova, 1949, T. lata Spandel, 1901, T. minuta Morozova, 1949, T. paraconica Reitlinger, 1950, T. parviconica? Lee & Chen in Lee et al., 1930, T. planulata? Morozova, 1949, Globivalvulina bulloides (Brady, 1876), Gr. aff. pergrata Konovalova, 1962, Calcivertella sp., Calcitornella heathi Cushman & Waters, 1928, Hemigordius/Rectogordius transitional forms, Nodosinelloides bella (Lipina, 1949), N. longissima (Suleimanov, 1949b), N. ex gr. longissima (Suleimanov, 1949b), N. longa (Lipina, 1949), N. netchajewi (Cherdyntsev, 1914), N. sp., and Langella aff. lepida (Lin, 1984).
In the Sanandaj-Sirjan zone:
In the Vazhnan Formation, the Gzhelian smaller foraminifera have been well studied (Yarahmadzahi & Vachard 2019), in two biozones:
A) Monotaxinoides melanogaster Zone, where the assemblage includes the following taxa: Monotaxinoides melanogaster (Yarahmadzahi & Vachard, 2019), Turrispiroides cf. microsphaerica (K.V. Miklukho-Maklay, 1968), Endothyra lipinae Morozova, 1949, Bradyina lucida Morozova, 1949, B. lepida Reitlinger, 1950, Tetrataxis cf. subconica Morozova, 1949, T. ex gr. lata Spandel, 1901, Pseudonovella aff. carbonica Grozdilova & Lebedeva, 1950, Pseudoacutella aff. partoazari Yarahmadzahi & Vachard, 2014, and Grovesella ex gr. tabasensis Davydov & Arefifard, 2007.
B) Raphconilia spp., Protonodosaria spp., Nodosinelloides spp., and Rectogordius? minimus Zone. This assemblage encompasses the following taxa: Eotuberitina reitlingerae A.D. Miklukho-Maklay, 1958, Diplosphaerina inaequalis (Derville, 1931), Turrispiroides ex gr. roessleri (E. Schmid, 1867), Asselodiscus primitivus Mamet & Pinard, 1992, Raphconilia modificata (Potievskaya, 1962), R. minor (Pinard & Mamet, 1998), R. cf. pararecta (Pinard & Mamet, 1998), R. sp., Endothyra lipinae Morozova, 1949, Bradyina lepida Reitlinger, 1950, B. sp., Deckerella sp., Climacammina sp., Palaeotextulariidae indet., Spireitlina ex gr. conspecta (Reitlinger, 1950), Tetrataxis cf. subconica Morozova, 1949, T. aff. parviconica Lee & Chen, 1930, T. aff. planulata Morozova, 1949, T. sp., Globivalvulina cf. celebrata Zamilatskaya, 1969, Gl. ex gr. bulloides (Brady, 1876), Gl. ex gr. pulchra Reitlinger, 1950; Gl. cf. kantharensis Reichel, 1946; Gl. aff. granulosa Reitlinger, 1950, Gl. sp., Pseudonovella sp., Pseudoacutella aff. partoazari Yarahmadzahi & Vachard, 2014, Grovesella ex gr. tabasensis Davydov & Arefifard, 2007, Calcitornella? sp., Orthovertella verchojanica Sosipatrova, 1970, Hemigordius sp., H.? sp., Rectogordius minimus (Yarahmadzahi & Vachard, 2019), Protonodosaria spp., Nodosinelloides shikhanica (Lipina, 1949), N. talimuensis (Han, 1984), N. cf. netschajewi (Cherdyntsev, 1914), N. cf. subquadrata (Lipina, 1949), N. cf. pinardae Groves & Wahlman, 1997.
In the Tabas area (Central Iran):
The Zaladou section (Yarahmadzahi & Vachard, 2018) exhibits two biozones of the Gzhelian.
A) Hemigordius spirilliniformis Bradyina cf. samarica subzone with: Bradyina cf. samarica Reitlinger, 1950, Globivalvulina celebrata Zamilatskaya, 1969, and Hemigordius spirollinoformis Wang, 1982, Eotuberitina reitlingerae Miklukho Maklay, 1958.
B) Raphconilia modificata Globivalvulina spp. Subzone including: Eotuberitina reitlingerae, Raphconilia (angulata stage) cf. minor Pinard & Mamet, 1998, R. (angulatus stage) cf. permiensis Pinard & Mamet, 1998, R. (concavus stage) modificata Potievskaya, 1962, Planoendothyra persica Yarahmadzahi & Vachard in Yarahmadzahi et al., 2016, Globivalvulina celebrata Zamilatskaya, 1969, Gl. ex gr. graeca Reichel, 1946, Gl. pulchra Reitlinger, 1950, Ammovertella sp., Cornuspira? sp., and Protonodosaria teretra Crespin, 1958.
In the section of Shishtu, Jalali et al. (2021) reported for first time the Rectogordius abundance zone, which contains Rectogordius iranicus Alipour & Vachard in Alipour et al., 2013, R. iranicus gadukensis Yarahmadzahi & Vachard, 2018, R. minimus Yarahmadzahi & Vachard, 2019, R. minimus shishtuensis Yarahmadzahi & Vachard in Jalali et al., 2021, and R. iranicus ozbakensis Yarahmadzahi & Vachard in Jalali et al., 2021.
Pseudoacutella was created by Vachard et al. (2013) from Cedro Peak (New Mexico, USA) and Pseudoacutella partoazari was found for first time by Yarahmadzahi and Vachard (2014) from Central Alborz (Gadouk section).
The Pseudoacutella partoazari assemblage consists of 16 species belonging to 14 genera: the fusulinids Pseudoacutella partoazari, Grovesella tabasensis, Gr. aff. australis, Gr. sphaerica, Gr. sphaerica var. quadrata, Gr. cf. staffelloides, Schubertina sp., Schubertella sp., and the smaller foraminifers Eotuberitina sp., Lasiodiscus tenuis, Raphconilia cf. minor, R. multihelicis, R. modificata, Tetrataxis cf. parviconica, Globivalvulina ex gr. bulloides, Gl. graeca, Calcivertella heathi, Tansillites sp., Palaeonubecularia? sp., Hemigordiellina sp., Nodosinelloides longa, and N. longissima.
Pseudoacutella partoazari (Yarahmadzahi & Vachard, 2014,
Figs. 5
- 6 ) is an advanced
species of this genus, which is characteristic of the Gzhelian to Asselian
deposits (i.e., the
Carboniferous-Permian boundary interval) throughout the Tethys region (e.g.,
Yarahmadzahi & Vachard, 2014, 2016, 2018, 2019; Yarahmadzahi
et al., 2016; Fassihi et
al., 2020). P. partoazari was first reported from Gadouk
section (Central Alborz), and later found in Asselian limestones of Zaladou
section (Yarahmadzahi & Vachard, 2018) and Banarizeh and
Tang-e-Darchaleh sections in Sanandaj-Sirjan zone (Fassihi et
al., 2020) and found in Gzhelian strata of Asad Abad section in
Sanandaj-Sirjan zone (Yarahmadzahi & Vachard, 2019).
|
Figure 5: Pseudoacutella partoazari
assemblage from the upper Gzhelian of the Zaladou Fm. Sample SH 16 (Scale bar
= 0.1 mm). 1-21) Pseudoacutella
partoazari (Yarahmadzahi & Vachard,
2014); 22-26) Globivalvulina
graeca (Reichel); 27-34) Globivalvulina
ex gr. bulloides
(Brady); 35-36) Raphconilia cf. minor
(Pinard &
Mamet); 37) Raphconilia multihelicis (Pinard
& Mamet); 38)
Raphconilia modificata; 39) Lasiodiscus tenuis
(Reichel). |
|
Figure 6:
Pseudoacutella partoazari assemblage
from the upper Gzhelian of the Zaladou Fm. Sample SH 16 (Scale bar = 0.1 mm). 1)
Nodosinelloides longissima (Suleimanov); 2) Nodosinelloides longa (Lipina);
3-4) Hemigordiellina sp.; 5) Palaeonubecularia? sp.; 6) Calcivertella
heathi (Cushman & Waters); 7-9) Eotuberitina
sp.; 10) Raphconilia multihelicis (Pinard & Mamet);
11) Tansillites sp.; 12-16
Grovesella tabasensis (Davydov & Arefifard); 17-19)
Grovesella aff. australis
(Thompson
& Miller); 20-22) Grovesella sphaerica
(Suleymanov); 23) Grovesella sphaerica quadrata (Ivanova); 24)
Grovesella
cf. staffelloides (Suleymanov); 25-27) Schubertina
sp.; 28) Schubertella sp.; 29-32) Tetrataxis cf. parviconica (Lee
& Chen). |
Grovesella tabasensis (Davydov & Arefifard, 2007) was first identified from the Upper Sakmarian deposits of the Chili Formation in the Kalmard block, later reported from Upper Pennsylvanian-Lower Permian of Alborz, Sanandaj-Sirjan and Central Iran (Yarahmadzahi et al., 2016; Yarahmadzahi & Vachard, 2019; Fassihi et al., 2020), Lower Permian of Nevada (Davydov, 2011) and Texas (Lucas et al., 2011), Afghanistan, and Darvaz (Davydov & Arefifard, 2007). Middle Permian of NW Iran (Ebrahim-Nedjad et al., 2015). Gr. aff. australis was first described from the Lower Permian of South America, Maracaibo Basin (Thompson & Miller 1949), and Slovenia (Ramovš & Kochansky-Devidé, 1965); it resembles the Moscovian species of the genus Eoschubertella bluensis, E. mosquensis and E. texana (see Groves, 1991). Grovesella sphaerica (Suleimanov, 1949) and Gr. cf. staffelloides (Suleimanov, 1949) described from upper Asselian and Sakmarian in the Urals-Arctic, Tethys and Kalmard area in Central Iran (Davydov & Arefifard, 2007). Gr. quadrata (Ivanova, 2000), Recently, they have been found in the Gzhelian-Asselian sequence of the Sabzevar tectonic block, the Ahuban Mountains, north of Kashmar.
Globivalvulina graeca (Reichel, 1946) described and identified from middle-upper Gzhelian of the Zaladou section in central Iran (Yarahmadzahi & Vachard, 2018), Lower Permian of Slovenia (Kochansky-Devidé, 1970), Armenia (Akopian, 1974) and South China (Lin et al., 1990); it is common in Middle Permian and widespread in all the Palaeo-Tethys and Neo-Tethys: Greece, Italy, Austria, Tunisia, Hungary, Slovenia, Croatia, Montenegro, Turkey, Armenia, Iran (e.g., Kuh-e Jamal: Jenny-Deshusses, 1983b) and Murgabian, Midian and Djulfian of Maku (Ebrahim Nejad et al., 2015). Gl. ex gr. bulloides is reported from Serpukhovian, Bashkirian to uppermost Permian, cosmopolitan. Recently, it was described from Gzhelian-Asselian of Central Iran (Yarahmadzahi & Vachard, 2019, Fassihi et al., 2020) and Alborz (Yarahmadzahi et al., 2016).
Hemigordiellina sp. is complicate and controversial. The small glomospiroid porcelaneous tests were attributed to Hemigordiellina sp. by Gaillot and Vachard (2007).
Eotuberitina sp. is cosmopolitan, Silurian-Devonian, with an acme in Carboniferous- Permian, rare in lowermost Triassic (Vachard, 2016).
Raphconilia cf. minor, R. multihelicis, and R. modificata have a Gzhelian-Kungurian age, but are additionally considered as rare in Roadian, Wordian, and lower Capitanian strata and very rare in upper Capitanian and Wuchiapingian strata (Altıner, 1988; Vachard et al., 2017). Cosmopolitan distribution and relatively widespread in America (Pinard & Mamet, 1998; Vachard et al., 2017). Discovered in the middle-upper Gzhelian to middle-upper Asselian of Iran (Alipour et al., 2013; Yarahmadzahi et al., 2016; Yarahmadzahi & Vachard, 2018, 2019; Fassihi, 2020).
Tetrataxis cf. parviconica was first described by Lee and Chen in Lee et al., 1930. Later found in deposits on Moscovian-lower Permian of the Paleotethys and Panthalassa (Ueno & Nakazawa, 1993). Recently, this species has been reported in Iran from Abshani Formation (Leven et al., 2006) of Moscovian age; Vazhnan Formation in Sasandaj- Sirjan zone of Sirjan (Yarahmadzahi & Vachard, 2019; Fassihi et al. 2020) of Gzhelian age and from Emarat in Alborz (Alipour et al., 2013) of late Ghzelian age.
Stratigraphic and geographic range of Schubertella sp. is distributed globally within the tropics-subtropics and known from Moscovian to Wordian (Rauzer-Chernousova et al., 1951; Skinner & Wilde, 1966; Leven, 1998a, 1998b; Davydov, 2011). Stratigraphic and geographic range of Schubertina sp. is distributed globally within the tropics-subtropics. It has been documented in the upper lower Bashkirian, in the Urals (Sinitsyna & Sinitsyn, 1987), Donets Basin (Manukalova-Grebenyuk et al., 1969) and Timan-Pechora (Nikolaev, 2005) and lower Atokan (upper Bashkirian) in North America (Groves, 1986, 1991). The upper range of Schubertina sp. is not clear at the moment (Davydov, 2011). Some forms that can be considered as Schubertina sp. are reported from Wordian (lower Midian), Capitanian (upper Wordian) and Lopingian (Skinner & Wilde, 1966; Leven, 1998a).
Pseudoacutella have been found in different microfacies from the Upper Carboniferous (Gzhelian)
and Lower Permian (Asselian-Sakmarian) of Iran. Yarahmadzahi & Vachard
(2014) and Yarahmadzahi et al.
(2016) suggested that Pseudoacutella partoazari associated with oncoid,
bryozoan, brachiopod, fusulinida (schwagerinids) and smaller foraminifers
characterizes a shoal sub-environment facies (Fig. 7A ), Such environments
and lithologies include mostly representatives of the genera Geinitzina sp.,
Globivalvulina sp., Pseudovidalina sp., Nodosinelloides
sp., Schubertella sp., Biwaella sp., Triticites sp., Tumefactus
sp., Pseudoschwagerina sp., Zellia sp., and Praepseudofusulina
sp. (Leven & Yarahmadzahi, 2020). Recently, Yarahmadzahi
& Vachard (2018) suggested a shoal sub-environment for bioclastic,
schwagerinid, brachiopod grainstone containing smaller foraminifers with a
microgranular and hyaline wall, such as Pseudonovella sp., Bradyina
sp., Globivalvulina sp., Raphconilia sp., Protonodosaria
sp. and Grovesella sp., from the Zaladou section in the Tabas block,
central Iran Zone (Fig. 7B ).
Yarahmadzahi and Vachard
(2019) reported Pseudoacutella partoazari in the shoal sub-environment
of the Asad Abad section in Sanandaj-Sirjan zone. They observed Pseudoacutella
together with smaller foraminifers, especially with Bradyina sp., Rectogordius
sp., Raphconilia sp., Nodosinelloides sp., Grovesella sp.,
and Endothyra sp. in the shoal sandy bioclastic schwagerinid brachiopod
grainstones (Fig. 7C ).
In the
present study, Pseudoacutella is found out in the shoal sub-environment
in bryozoan, brachiopod and echinid grainstone with smaller foraminifera such as
Globivalvulina sp., Hemigordiellina sp., Eotuberitina sp., Raphconilia
sp., Lasiosdiscus sp., Calcivertella sp., Tansillites sp., Palaeonubecularia?
sp., Nodosinelloides sp., Grovesella sp., Schubertina sp., Schubertella
sp. and Tetrataxis sp. (Fig. 7A-D ).
|
Figure
7:
Photomicrographs
of carbonate facies of the Zaladou Formation of the Shishtu Section in Ozbak Kuh
Mountain, in northeast Tabas Block, Iran: A) bryozoan, brachiopod,
fusulinida tests (schwagerinids)
and smaller foraminifer grainstone
with Pseudoacutella
partoazari in the Emarat Formation (Yarahmadzahi
& Vachard, 2014;
sample DH 6); B) bioclastic, schwagerinid, brachiopod grainstone containing smaller foraminifers with a
microgranular and hyaline wall with Pseudoacutella partoazari in
the Zaladou Formation in the Zaladou section (Yarahmadzahi
& Vachard, 2018,
sample CPH 28); C) sandy, bioclastic, schwagerinid, brachiopod grainstone with Rectogordius
in the Vazhnan Formation (Yarahmadzahi
& Vachard, 2019;
sample Vaa 3); D) bryozoan,
brachiopod and echinid grainstone with smaller foraminifera with Pseudoacutella
partoazari in the Zaladou Formation (this study; sample SH 16). |
Pseudoacutella is regarded as a junior synonym of Pseudonovella by Ueno (2022) with the following arguments: Pseudoacutella shares basic morphological features with the type species of Pseudonovella: Novella (Pseudonovella) irregularis Kireeva, 1949, such as a slender lenticular shell with 3-3.5 volutions and a large spherical proloculus relative to the shell size. Ueno (2022) suggests also that Pseudonovella and Pseudoacutella have similar stratigraphic ranges and occur commonly in the Bashkirian and Moscovian. This author, finally, admits only some subtle differences (sic) between these two genera, such as the shape of the periphery and the feature of chamber involution at umbilical regions. Furthermore, it is noticeable that Pseudonovella was previously considered as a subgenus of Eostaffella by Villa et al. (2021) including Ueno himself among the co-authors; hence, considered as having a coiling and growth different of Pseudonovella sensu stricto.
We re-illustrate here (Table 1) the differences indicated by Vachard et al. (2013) and confirm that Pseudonovella differs from Pseudoacutella by the periphery rounded-carinate (carinate in Pseudoacutella), pseudochomata less developed, and the type of coiling (Pseudoacutella is truly planispiral involute). Pseudonovella is suggested here as the ancestor of Pseudoacutella.
Table 1: Morphologic and hypothetically phylogenetic evolution of Millerellinae. Abbreviations: ex gr. = ex gregae (Latin) = of the group (modified from Vachard et al., 2013).
| MILLERELLINAE | PERIPHERY | INVOLUTE AND THEN EVOLUTE |
ENTIRELY EVOLUTE |
| Advanced | Carinate | Pseudoacutella | Eostaffella ex gr. dolixa-fragilis |
| Horse shoe | Pseudonovella | Novella | |
| Rounded | Plectomillerella | Seminovella | |
| Millerella | |||
| Primitive | Rounded | Eostaffella ex gr. pseudostruvei | Zellerinella |
Even if these characters may appear subtle, they are at the base of the traditional distinction between Millerella and Eostaffella. We remember that Eostaffella Rauzer-Chernousova, 1948, and Millerella Thompson, 1942, were independently created and remained the children of the Cold War. We remember also that the Eostaffella of the U.S.A. were named Paramillerella by Thompson (1951) and, finally, that the genera Eostaffella and Millerella, initially synonymized by Ginkel (1965) were, in a second time, subdivided by this author (Ginkel, 2010) in several dozens of genera and subgenera.
At first glance, Pseudoacutella might be considered as a subgenus of Eostaffella, as proposed by Villa et al. (2021) because it is more similar to the millerellids than the eostaffellids. That is also the case for Pseudonovella. It differs from Eostaffella because it arises from a different lineage; nevertheless, the convergence and homeomorphy are almost perfect.
The initial mutation of Pseudonovella into Pseudoacutella seems to have taken place in the Donbass basin (Ukraine) during the deposit of the upper Bashkirian I limestone. Nevertheless, migrating Pseudoacutella are biostratigraphic markers for the lower Desmoinesian and/or the Atokan-Desmoinesian boundary interval in North America (Vachard et al., 2013).
The emendation of Pseudonovella by Maslo and Vachard (1997) is used here for defining this latter genus, because the subsequent emendation of Ginkel (2002) seems less consistent with the generotype characters. If we can admit the text of Ginkel (2002) and his analysis of Pseudonovella sp. 1, we believe that the other taxa analyzed by him (Pseudonovella sp. 2 to sp. 6) correspond more to Millerella or Seminovella, at least in the sense of Rauzer-Chernousova et al. (1951) and Ginkel (1987).
Pseudonovella differs from Novella by less evolute terminal whorls; consequently, Novella pulchra (sensu Leven, 1998, Pl. 1, fig. 5) is a Pseudonovella and not a Novella. Pseudonovella differs from Millerella and Seminovella by the coiling concomitantly evolute and enveloping, smaller pseudochomata and the periphery rounded-carinate (rounded in Millerella and Seminovella). It differs from Pseudoacutella by the periphery rounded-carinate (carinate in Pseudoacutella), pseudochomata less developed, and the type of coiling (Pseudoacutella is truly planispiral involute). Pseudonovella is suggested here as the ancestor of Pseudoacutella.
A foraminiferal assemblage, of 14 genera and 16 species, is reported from the Zaladou Formation in the Tabas Block (Shishtu Section), Central Iran.
The age of this assemblage is interpreted herein as Gzhelian (= latest Carboniferous).
This assemblage shows an overwhelming dominance of Pseudoacutella and relatively low total diversity, compared with similar foraminifera from Alborz, Sanandaj-Sirjan, Sabzevar and central Iran, which presents warm and humid conditions during the Late Carboniferous.
Pseudoacutella was recently regarded as a junior synonym of Pseudonovella. However, we confirm here the differences between the two genera, and conclude that Pseudonovella really differs from Pseudoacutella by the periphery rounded-carinate (carinate in Pseudoacutella), pseudochomata less developed, and the type of coiling (Pseudoacutella is truly planispiral involute).
Pseudonovella is suggested here as the ancestor of Pseudoacutella.
We are grateful to Ali Jalali and Ehsan Ajoodani-Feizabad for help to field work in this article. Thanks also to the referees, Ian Somerville and Brian Pratt, for their useful comments.
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