The present study focuses on stratigraphy of the Permo-Triassic boundary in the Haftad Gholleh in the east Arak and north of the Mahallat, which is located in central Iran. This boundary is an erosional unconformity or disconformity and as in other Iranian sequences related to the Permian contains dolomitic limestone and shale and sandstone that is disconformably located below the Triassic sequence. A detailed measured stratigraphic section has provided conodonts for the Permian–Triassic boundary (PTB) sequences at the studied area. Three conodont zones have been recognized, wich place the PTB in this section by precise biostratigraphy. The of the most upper Permian sequence belongs to the Guadalupian. The Triassic sequence consists of vermiculate limestone layers with colored shale interbeds that belong to the Early triassic therefore, the unconformity at the of Permo-Triassic boundary is a hiatus of about 10 million years

Mostafa Yousefirad

Earth Sciences Research Journal

Yousefirad, Mostafa

Universidad Nacional De Colombia - Repositorio Institucional UN

EARTH SCIENCESRESEARCH JOURNALEarth Sci. Res. SJ. Vol. 17, No. 1 (June, 2013): 61 - 65Using conodont elements to distinguish Permian-Triassic boundary  disconformity near Haftad Gholleh, central IranMostafa Yousefirad1, Somayeh Ghanbari2 and Mahnaz Parvanehnejad Shirazi21Department of Geology, Faculty of Earth Sciences, Payam-e-Noor University, Iran2Department of Geology, Faculty of Earth Sciences, Payame Noor University, Shiraz, Iran  Email: mostafa.yousefirad@yahoo.com Mobile: 00989125700730PALEONTOLOGYThe present study focuses on the stratigraphy of the Permian-Triassic boundary in the Haftad Gholleh area in eastern Arak and north of  Mahallat,located in central Iran. This boundary of erosional uncon-formity or disconformity and as in other Iranian sequences related to the Permian period, contains dolomitic limestone and shale and sandstone disconformably located below the Triassic sequence. A detailed measured stratigraphic section has provided conodonts from the Permian–Triassic boundary (PTB) sequences in the area being studied. Three conodont areas have been recognied which place the PTB in this section by precise biostratigraphy. One of the most upper Permian sequences belongs to the Guadalupian period. The Triassic sequence consists of vermiculate limestone layers with coloured shale inter beds belonging to the Early Triassic period; unconformity at the Permian-Triassic boundary therefore represents a hiatus of about 10 million years.El presente estudio se enfoca en la estatigrafía del Límite Pérmico-Triásico en el área de Haftad Gho-lleh, al este de Arak y al norte de Mahallat, centro de Irán. Este límite de discordancia erosiva, al igual que en otras secuencias iraníes relacionadas al período Pérmico, contiene calizas dolomías, esquistos y areniscas discordantes localizadas debajo de la secuencia Triásica. En una medida estratigráfica deta-llada del área de estudio se encontraron conodontas del Límite Pérmico-Triásico (PTB, por sus siglas en inglés). Se reconocieron tres áreas de conodontas, lo que ubica esta sección del PTB como bioesta-tigráfica precisa. Una de las secuencias superiores del Pérmico pertenece al período Guadalupiense. La secuencia Triásica consiste en calizas con capas vermiculitas coloreadas de esquisto que pertenecen al período Triásico temprano. La discordancia del Límite Pérmico Triásico, entonces, representa un lapso cercano a los 10 millones de años.Key words: Conodont, Haftad Gholleh, Permian-Triassic, stratigraphy.Palabras clave: Conodont, Haftad Gholleh, Permian-Triassic, stratigraphy.RecordManuscript received: 08/10/2013Accepted for publication: 02/04/2013ABSTRACTRESUMENIntroductionThe end of the Palaeozoic period and the beginning of the Mesozoic saw the greatest of all extinctions in the Phanerozoic causing mass morta-lity in the marine environment (up to 96% of species, 83% of genera and 55% of families) (Sepkoski, 1990; Raup, 1991) and a nearly equally large loss of life on land (Erwin, 1993). Important P/T boundary sections are located in Iran (NW, NE and Central Iran, Alborz region, belonging to the Iranian Plate, and the Zagros fold belt, belonging to the Arabian Plate), Oman, Southern China, Japan, Pakistan, Afghanistan, Turkey, Greenland, Austria, Italy, South Africa and Antarctica. The Permian sea’s last regression period occurred at the end of this system, which is why the upper boun-dary of the Permian strata in Iran is commonly discontinuous but has a type of parallel unconformity (disconformity). Nevertheless, evidence of continuous sedimentation from the Permian to Triassic been reported in many regions of Iran (Julfa, Kandovan, Amol, Shahreza and Abadeh). The recommended, but somewhat controversial, chronostratigraphical Per-mian scale is summarised here, according to Jin et al., (1997) and Wardlaw (1999), but correlated with Leven’s alternative classification (Leven, 1992; Kotlyar and Pronina, 1995). The names Midian (eventually Abadehian) for Capitanian, Dzhulfian for Wuchiapin-gian and Dorashamian for Changhsingian have been preferred concerning Iran’s stratigraphy (Fig. 1).Due a lack of macroscopic and microscopic fossils, especially Fora-minifera, some uncertainties in conodonts’ biostratigraphy have not been studied and clarified. This research thus attempts to study conodonts, the Figure 1. Permian-Triassic boundary in different areas of Iran (Aghanabati, 2004)Mostafa Yousefirad, Somayeh Ghanbari and Mahnaz Parvanehnejad Shirazidisconformity interval and the Permian-Triassic boundary’s paleoecology in the area being studied.2. Geological settingThe Haftad Gholleh area is a small part of central Iran, located bet-ween volcanic belts at Urmia Kerman Sanandaj Sirjan. The Soltanieh Do-lomites, Zagun, Lalun, Mila and Permian sequence deposits in the region are known as Palaeozoic facies. Soltanieh grey dolomite is overlain by a green to red shale formation containing little sand and mica, becoming converted locally into fine-grained sandstone. Shale thickness varies from 100 to 200 metres (Zagun formation). Overlying the shale are about 50 metres of dense, hard lightcoloured quartzite sandstone which has been assigned to the Lalun Formation. This formation is overlain by light to dark dolomite containing coral, sand and crinoids, having less than 100 m thickness.The dolomite gradually changes from bottom to top from light grey to light green limestone, bearing trilobite fragments; such dolomite and limestone are assigned to the Mila Formation. This different kind of facies (Permian) is located directly on older formations. No Ordovician to Carboniferous sequences thus occurred in the area being studied. Permian deposits are mainly dolomite. In some locations, the base consists of Lalun sandstone. The base of the Permian deposits in some parts is calcareous shale associated with red sandstone and conglomerate. Permian lithology mainly consists of thick bedded dolomite (light grey) (Fig. 2).LithostratigraphyThe Upper Permian sedimentary sequence in the area being studied included limestone continuing with dolomite; limestone has been assig-ned to the Jamal Formation. All deposits were isoclinal, indicating marine transgression in the studied area (Permian). One sequence, having several meters of shale and sandstone, lacking fossils, had such adistinctive colour that it could be applied as a key bed. There were several metres of thin to medium-bedded Claraia vermicular limestone inter-bedded with coloured shale above the key bed; this belonged to the Early Triassic, based on a stu-dy of conodont fragments. It has thus been concluded that Early Triassic deposits in the study area consisted of two parts: clastic (lower part) and carbonate (upper part), generally being equivalent to the Shotori Forma-tion. The carbonate part included dolomite inter-bedded with coloured shale. There were few fossils in the sequence. Based on the stratigraphic situation, lithological similarities and lithocorrelation, it has been assigned to the Anisian age Shotori Formation (Figs. 3 and 4).BiostratigraphyApart from the studied section’s base part (related to the Permian rock sequence) having few benthic foraminifera, other layers in the studied rock sequence were very poor in terms of fossil content (foraminifera). Biolo-gical biozoning studies were thus based on conodont elements in the stu-died section’s complete rock sequence. elements in the studied section were biozoned according to standard Kozur biozonation (1977). Conodont elements known from Permian time would be as follows: Hindeodus mi-nutes, Streptognathodus barskovi, Sweetognathus whitei, Neostreptognathodus pequopensis, Hindeodus excavates and Merrillina divergens.Conodont elements known to be related to the Triassic age would be as follows: Prioniodella Prioniodellides, Hindeodella multihamata, Hindeo-della nevadensis, Lonchodina nevadensis, Hindeodella triassica, Ligonodina triassica, Diplodella lautissima, Pachycladina oblique, Hadrodontina anceps, Figure 2. The studied area’s geological setting Ellisonia triassica, hibardella subsymmertica, Parachirognathus geiseri, Prio-niodella decrescens, Enantiognathus bitortus, Chirognathus sp., Xaniognathus sp., and Anchiognathudos sp. (Fig. 5).Pachycladina oblique (Staesch), posterior view, X90, early Triassic (early Triassic) - 1Sweetognathus whitei (Rhodes), lateral view, X80, middle Permian (Guadalupian) - 2Hindeodella nevadensis (Muller), lateral view, X80, early Triassic (early Triassic) - 3Hindeodus minutes (Ellison), lateral view, X80, upper Permian - 4Hindeodella multihamata (Huckriede), lateral view, X95, middle Triassic (Anisian) - 5Chirognathus sp., lateral view, X80, early Triassic (Scythian) - 6Neostreptognathodus pequopensis (Behnken), outer view, X80, upper Permian - 7Ligonodina triassica (Muller), lateral view, X80, early Triassic (early Triassic) - 8Enantiognathus bitortus (Bender), outer view, X120, early Triassic (early Triassic) - 9 - 10Hindeodella triassica (Muller), lateral view, X80, middle Permian - lower Triassic - 11Hindeodus excavatus (Behnken), lateral view, X150, middle Permian (Guadalupian) - 12Streptognathus barskovi (Kozur), lateral view, X80, middle-upper Per-mian - 13Xaniognathus sp., lateral view, X80, lower Triassic - 14Prioniodella prioniodellides (Tatge), lateral view, X120, middle Triassic (Anisian) - 15Lonchodina nevadensis (Muller), lateral view, X110, early Triassic (early Triassic) - 16Merrillina divergens (Bender & Stopple), lateral view, X80, (Guada-lupian) - 17Parachirognathus geiseri  (Clarck), lateral view, X95, (early Triassic - Anisian) - 18Ellisonia triassica (Muller), lateral view, X80, early Triassic (early Trias-sic). - 19Following precise paleontological studies, including conodont re-cognition and taxonomy regarding samples from the studied section, each fossil’s biozone was identified on the Table showing the extent of fossils, based on their presence in each rock sample. Two assemblage zo-nes and one acrozone for Permian deposits and two assemblage zones for Triassic deposits were identified based on the emergence, decline and ex-panding stratigraphic accumulation index for conodonts having known elements.4.1. Neostreptognathodus pequopensis - Hindeodus minutes as-semblage zone The start of this base’s biozone was consistent with the occurrence of Neostreptognathodus pequopensis conodont genus and species and its end with the occurrence of Merrillina divergens conodont genus and species. Conodont elements contained in this biozone were assigned to the fo-llowing: Hindeodus minutes, Hideodus excavatus, Sweetognathus whitei, Hindeodella triassic and Neostreptognathodus pequopensis.Figure 3. Studied section near Haftad GhollehUsing conodont elements to distinguish Permian Triassic boundary disconformity near Haftad Gholleh, central IranFigure 4. Stratigraphic column of the section being studied near Haftad GhollehBiozone age was Artin-skian, based on the standard Kozur biozoning (1977), proposed as being equal to the Neostreptognathodus pequopensis biozone.4.2. Merrillina divergens acrozoneThe base of this biozone started with Merrillina divergens and termi-nated with M. divergens. Conodont elements contained in this biozone were identified as follows: Merrillina divergens, Hindeodella triassic, Hideo-dus excavates.This biozone’s age, according to conodonts, was Guadalupian. Ac-cording to standard Kozur biozonation (1977) this zone was the biozone equivalent of Merrillina divergens.4.3. Lonchodina nevadensis - Ellisonia triassica assemblage zoneThe base of this biozone index was the presence of Lonchodina ne-vadensis and Ellisonia triassica and the top of the biozone consisted of Pachycladina oblique and Hadrontina anceps. Conodonts from elements contained in the biozone were assigned to the following: Prioniodella prio-niodellides, Hindeodella multihamat, Hindeodella nevadensis, Lonchodina nevadensis, Hindeodella triassica, Ligonodina triassica, Diplodella lautissima, Pachycladina oblique, Hadrodontina anceps, Ellisonia triassica, Hibardella subsymmertica, Parachirognathus geiseri, Prioniodella decrescens, Enantiog-nathus bitortus, Chirognathus sp. and Xaniognathus sp.According to conodonts, this biozone’s age was Scythian. Based on Kozur’s standard biozones (1997), this biozone was the equivalent of the Isarcicella isarcica biozone.4.4. Hindeodella multihamata - Prioniodella Prioniodellides as-semblage zoneThis biozone included conodonts such as Diplodella lautissima, Prio-niodella decrescens, Hindeodella multihamata, Prioniodella Prioniodellides, Hindeodella triassica and  Xaniognathus sp.The identified conodonts indicated that it was Anisian (Fig. 5).ConclusionsThe Permian-Triassic boundary located near Haftad Gholleh is an erosional unconformity or disconformity, as in other parts of Iran, where Figure 5. Conodont elements in the studied areaMostafa Yousefirad, Somayeh Ghanbari and Mahnaz Parvanehnejad ShiraziFigure 6. Distribution and biozonation of conodonts from the Permian-Triassic boundary of the area being studiedPermian sequences contain dolomitic limestone, shale and sandstone situa-ted below the Triassic sequence at a disconformity.Based on emergence, decline and expansion of index conodonts, one assemblage zone and one acrozone (Permian) and two assemblage zones (Triassic) were recognised as follows:- Neostreptognathodus pequopensis-Hindeodus minutes assemblage zone (Artinskian);- Merrillina divergens acrozone (Guadalupian); - Lonchodina nevadensis and Ellisonia triassica assemblage zone (early Triassic); and- Hindeodella multihamata, Prioniodella prioniodellides assemblage zone) Anisian).The age of the uppermost Permian sequence thus belonged to the Guadalupian era. The Triassic sequence consisted of vermiculate limestone layers with coloured shale inter-beds that belonging to the Scythian era.The conodont fauna indicated that the Permian-Triassic sequence from the studied area was deposited in a warm shallow sea having normal salinity. Most conodonts in the studied area were euryhaline (i.e. able to tolerate a wide range of salinity). Red clastic sediments at the base of the lower Trias-sic indicated that an erosion period started after sedimentation in the mid-Permian and has been dominant on land in the region. Disconformity thus occurred at the Permian-Triassic boundary in the studied area.AcknowledgementsThis research was supported by Arak Payame Noor University. I would like to thank Dr Hadi Ghaffari and Dr Mohammad Hashem Rezai for support and Dr Babazadeh for reviewing the manuscript and providing pertinent comments.ReferencesAghanabati, S.A. (2004). Geology of Iran, Geological Survey of Iran Publisher, Tehran, Iran, 183 pp.Erwin, D.H. 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The taxonomic structure of periodic extinction, In: Global Catastrophes in Earth History, SharptonV.L., Ward P.D., (Eds.), Geological Society of America Special Paper, 247, 33–44.Using conodont elements to distinguish Permian Triassic boundary disconformity near Haftad Gholleh, central Iran

Using conodont elements to distinguish Permian-Triassic boundary disconformity near Haftad Gholleh, central Iran

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