Wildfires across Triassic–Jurassic (T–J) boundary have been reported from various parts of the world including Turkey (Korkmaz and Gülbay 2007), Poland (Marynowski and Simoneit 2009), USA (Jones et al. 2002), and Australia (Jiang et al. 1998). This paper, is the first report of paleo-wildfire events across the T–J boundary of the Tabas Basin (Central Iran). The stratigraphic properties and depositional environments of sedimentary units around the T–J boundary have been previously studied in Central Iran (Seyed-Emami 2003; Seyed-Emami et al. 2004; Shadan and Hosseini-Barzi 2013; Wilmsen et al. 2009a). Based on these studies, the Central Iranian basin was detached from the Gondwana during the Late Permian—Early Triassic and moved northward to collide with Eurasia in the Late Triassic. This collision event had a major impact on sedimentary evolution of the T–J boundary in Central Iran (Seyed-Emami et al. 2004; Wilmsen et al. 2009b). The platform carbonated of Lower and Middle Triassic were followed by the thick post-collisional sediments during Upper Triassic—Lower Jurassic (i.e. the Shemshak Group) (Seyed-Emami 2003; Wilmsen et al. 2009a). During the early phases of the orogenic movements, the Upper Triassic Nayband Formation was deposited under marine conditions, which were gradually replaced by the non-marine Ab-e-Haji Formation (Wilmsen et al. 2009a) (Fig. 1). The organic geochemistry and paleo-depositional environments of these sediments are recently addressed in the literature (Alizadeh et al. 2010, 2011; Zamansani et al. 2019).

Generalized stratigraphic column of the Central Iran basin during the Triassic–Jurassic boundary.

A thick sedimentary package, consisting of the Nayband and Ab-e-Haji formations (approximately 1600 m), is available at Kamarmacheh Kuh section located about 50 km SW of the Tabas city (Fig. 2). Unlike many other places in Iran, sedimentation across the T–J boundary is continuous at this location. The fine-grained marine siliciclastic and carbonate sediments of the Nayband Formation contain abundant fossils and pass into the overlying fluvial siliciclastic sediments of the Ab-e-Haji Formation conformably. These sediments are systematically sampled in this study and were subjected to detailed organic geochemical and petrographical analyses. Our results provided evidence for widespread wildfire events across T–J boundary in the studied sediments and helped better understand their paleo-depositional conditions.

The Mesozoic stratigraphy of Central Iran has largely been controlled by its tectonic history (Wilmsen et al. 2009b). During most of the Paleozoic the Central Iranian micro-continent was part of the Gondwana (Berberian and King 1981; Stöcklin 1974). However, it became detached from Gondwana during the Permian and collided with Eurasia during the Late Triassic (Stöcklin 1974). This collision resulted in the Eo-Cimmerian event (Wilmsen et al. 2009b) (Figs. 2, 9a). Due to this event, the Middle Triassic platform carbonates (i.e. the Shotori Formation) were uplifted, eroded, and unconformably overlain by a large siliciclastic sequence (i.e. the Norian-Bajocian Shemshak Group) (Fürsich et al. 2009; Stöcklin et al. 1965). Consequently, the lower boundary of the Shemshak Group in Central Iran is marked by the Eo-Cimmerian unconformity (Fig. 2).

Generalized geological map of the studied area indicating the location of the Kamarmacheh Kuh section.

Another important event related to the main-uplift phase of the Cimmerian Orogeny occurred at the T–J boundary (Fig. 2). This event (i.e. the Main Cimmerian event) signifies the ending of marine sedimentation (i.e. Nayband Formation) and establishment of non-marine/fluvial depositional regimes (i.e. Ab-e-Haji Formation) (Wilmsen et al. 2009a). Although the exact reason for this unconformity is not clear yet, some authors have related it to the slab break-off of the Paleo-Tethys oceanic crust (Wilmsen et al. 2009b) (Fig. 9b). Nevertheless, the subduction initiation of the Neo-Tethyan oceanic floor during the latest Triassic-Early Jurassic time (Hassanzadeh and Wernicke 2016) may also have played some roles during the Main Cimmerian event (Fig. 9b).

The Mid-Cimmerian unconformity defines the upper boundary of the Shemshak Group in Central Iran (Fig. 2). This event represents a brief pulse of uplift during the mid-Bajocian and has been ascribed to the break-up of South Caspian Basin (Wilmsen et al. 2009b).

Accordingly, the Mesozoic stratigraphy of the Central Iran is characterized by subduction processes and extensional tectonic regimes over much of the area (Seyed-Emami 2003). This is particularly the case with the Lower Jurassic sediments which are characterized by widespread presence of basic volcanic and volcano-clastic units (Fürsich et al. 2005b; Seyed-Emami 2003).

A total of 41 samples were collected from a surface outcrop of the Nayband and Ab-e-Haji formations in the Kamarmacheh Kuh section (Fig. 1 and Table 1). Special care was taken in collecting samples as to pick them from non-weathered fresh parts of the rocks.

These samples were first analyzed by Rock–Eval pyrolysis instrument for geochemical evaluation. Prior to analysis, the samples were grounded in the laboratory and stored in the oven for 24 h under a constant temperature of 40 °C to eliminate moisture. Approximately 70 mg aliquots were loaded into crucibles and analyzed following the standard guidelines (Espitalié et al. 1977).

Representative samples were selected from each of the studied formations for petrographic evaluations. For this, crushed aliquots of the samples were mounted in epoxy resin, ground and polished for microscopic studies. A computerized Zeiss Axioplan (II) photomicroscope equipped with a J&M photomultiplier calibrated with standards of known reflectance (0.431% to 5.35%) was used for organic petrographic analyses. Observations were made using standard guidelines (Stach et al. 1982; Taylor et al. 1998) under reflected light using a 100X oil immersed objective.

4.1 Rock–Eval pyrolysis

Rock–Eval parameters obtained from pyrolysis of Nayband and Ab-e-Haji samples (Table 1) indicate minor potential for generation of hydrocarbons from the associated organic matter (Fig. 3). This is consistent with previous findings about the quality of organic matter preserved in the studied formations (Alizadeh et al. 2011; Yousefi and Behbahani 2017; Zamansani et al. 2019).

Plots of HI versus OI a and generation potential (S₁ + S₂) versus TOC b for the studied samples from the Kamarmacheh Kuh section

According to the obtained geochemical results, the organic matter contained within the Nayband formation is of terrestrial origin and has low hydrogen contents (e.g., HI values mostly below 70 mg HC/g TOC) (Fig. 3). This indicates that the organic matter suffered major oxidation during transport and/or sedimentation. Similarly, samples from the Ab-e-Haji Formation are consistent with predominantly hydrogen-poor terrestrial organic matter that was deposited under oxic conditions (Figs. 3, 4). The very low HI values (mostly below 100 mg HC/g TOC) along with very low S₂ readings (mostly below 1 mg HC/g rock) indicate that a major fraction of the associated TOC in both formations is inert and will not participate in the process of hydrocarbon generation (Table 1). Therefore, it can be concluded that the majority of the studied samples from Nayband and Ab-e-Haji formations are characterized as poor to fair source rocks with minor potential for hydrocarbon generation (Figs. 3, 4).

Geochemical log based on Rock–Eval pyrolysis data for the studied formations at Kamarmacheh Kuh Section. Samples selected for organic petrographic analyses are highlighted in boldface (see Table 2)

In terms of thermal maturity, the obtained T_max values should be used with caution. Owing to very low S₂ readings for our samples, T_max values cannot provide an accurate measure of maturity. This is supported by the wide ranges of variation observed for the T_max readings (Fig. 4). Therefore, we rely upon vitrinite reflectance measurements for maturity evaluation of the studied formations.

4.2 Organic petrography

Representative samples were selected from Nayband and Ab-e-Haji formations for detailed organic petrographic inspections and for vitrinite reflectance measurements (Table 2). Our criteria for selecting these samples were based on (i) visual examination of their colors in the hand specimen, and (ii) geochemical screening based on TOC readings from Rock–Eval pyrolysis (Table 1 and Fig. 4). Generally, samples with higher TOC and darker colors were preferentially selected for petrographic analyses (Table 2).

In line with previous studies (Yousefi and Behbahani 2017), vitrinite reflectance readings obtained from organic petrography indicate that the studied formations are thermally mature (Table 2). In addition, organic petrographic inspections provided more robust assessment of the maceral constitution of studied samples. This technique was used in combination with bulk-rock pyrolysis data to better understand the variations of organic matter type among the studied formations. Our results indicate that the samples from lower parts of the Nayband Formation (i.e. samples N-4 and N-7) are rich in vitrinite and inertinite macerals (Fig. 5). In addition, vitrinite macerals in these samples are mostly characterized with micro-fractures and dark oxidation rims. These observations are strong indications for the natural oxidation during transport and/or sedimentation of the organic matter (Lo and Cardott 1995). These interpretations are further supported by the Rock–Eval pyrolysis results mentioned above.

Photomicrographs of samples from the lower parts of the Nayband Formation. Samples N-4 a and N-7 b contain vitrinite particles with microfractures and dark reaction rims (see Fig. 4 for stratigrpahic locations of these samples)

Moving up within the Nayband Formation (i.e. samples N-12 and N-13), the relative abundance of semifusinite macerals increases (Fig. 6a, b). In addition, a similar increase in the relative abundance of combustion chars is conspicuous towards the top of the Nayband Formation (Fig. 6c, d).

Photomicrographs of Nayband Formation samples N-12 (a, b) and N-13 (c, d) (see Fig. 4 for stratigrpahic locations of these samples)

In a similar fashion, semifusinite and combustion chars are predominant in the lowermost samples of the Ab-e-Haji Formation (i.e. samples A-17 and A-18, Fig. 7).

Photomicrographs of the Ab-e-Haji Formation samples A-17 a, b and A-18 c, d, showing the predominance of semifusinite macerals and combustion chars (see Fig. 4 for stratigrpahic locations of these samples)

However, the relative abundance of semifusinite and combustion chars decreases rapidly towards the top of the Ab-e-Haji Formation (i.e. samples A-25 and A-39). Vitrinites with marked weathering characteristics Once again become the dominant maceral type in the upper parts of the Ab-e-Haji Formation (Fig. 8). It is noteworthy that weathering features are relatively stronger in the Ab-e-Haji samples compared to those observed in the basal parts of the Nayband Formation (Fig. 8).

Photomicrographs of samples from the Ab-e-Haji Formation showing reworked fusinite particles in sample A-25 a and reworked vitrinite particles in sample A-39 b (see Fig. 4 for stratigrpahic locations of these samples)

Several lines of evidence corroborate the occurrence of wildfire events at the T–J boundary of Central Iran. In the aftermath of Eo-Cimmerian event, a large retrograding sedimentary sequence started across most of the Central Iranian Micro-continent (Fig. 9a, b). The originally marine conditions during deposition of the Nayband Formation gradually transformed into fluvial/continental environments during deposition of the Ab-e-Haji Formation. Organic petrographic results obtained in this study are consistent with an increase in the concentration of semifusinite and combustion chars around the T–J boundary (Figs. 6, 7). Similar observations have been interpreted by other researchers as evidence for wildfire events in various sedimentary basins around the world (Collinson et al. 2007; Hudspith et al. 2012). Therefore, we suggest that widespread wildfire events could have occurred during the T–J boundary in the Central Iranian basin (Fig. 9b).

Paleo-geographic settings of Central Iran during the Eo-Cimmerian event a and during the Main Cimmerian Event b (with modifications from Wilmsen et al. 2009b)

It is well known that wildfire events can remove the vegetation cover and increase the surface water run-off, which in turn, would affect sedimentation in the adjacent depositional environments (Nichols and Jones 1992). The Late Triassic sediments of the Nayband Formation are composed of highly fossiliferous marine carbonates and shallow-marine siliciclastic sediments containing coal inter-layers (Fürsich et al. 2005a). In contrast, the Lower Jurassic Ab-e-Haji Formation consists of recycled fluvio-deltaic sediments deposited under humid conditions with short transport distances (Salehi et al. 2014; Shadan and Hosseini-Barzi 2013). Provenance studies on sandstones of the Ab-e-Haji Formation have indicated that these sediments were formed by recycling of older sedimentary rocks (Salehi et al. 2014; Shadan and Hosseini-Barzi 2013). Such conditions could have been met following a major wildfire event, which could potentially remove the vegetation cover and expose older sedimentary units (including the Nayband Formation) (Fig. 9b). Additionally, the enhanced erosion and increased sediment supply into nearby depocenters would explain the exceptionally large thickness of sediments accumulated in the Jurassic system (e.g., Fürsich et al. 2005b). This model can also explain petrographic observations including the predominance of reworked organic matter in the Ab-e-Haji Formation. These organic constituents have likely experienced multiple cycles of transportation under oxic conditions. These factors could have resulted in considerable loss of hydrocarbon generation potential for the studied sediments, which is also supported by the Rock–Eval pyrolysis results (Fig. 3).

Results from organic geochemical and petrographical analyses of a suit of samples from an Upper Triassic–Lower Jurassic sedimentary succession from Central Iran provides evidence for wildfire events at T–J boundary. The removal of vegetation cover exposed the older sedimentary units for enhanced erosion. Subsequently, a large thickness of recycled sediments were accumulated in the nearby depocenters. The organic matter contained in these sediments underwent intensive oxidation and therefore has negligible hydrocarbon generation potential. Additional evidence for widespread wildfire events could come from detailed PAH analysis of the extractable organic material and plant fossil studies across the T–J boundary.