- Original Article
- Open Access
Repeated occurrence of palaeo-wildfires during deposition of the Bahariya Formation (early Cenomanian) of Egypt
Journal of Palaeogeographyvolume 8, Article number: 28 (2019)
The Upper Cretaceous (early Cenomanian) Bahariya Formation of Egypt has an outstanding reputation for its wealth of vertebrate remains, including a variety of iconic dinosaurs, like the carnivorous Spinosaurus and Carcharodontosaurus, as well as the herbivorous Aegyptosaurus and Paralititan. Besides these dinosaur fossils, the Bahariya Formation yielded also a wealth of invertebrate and plant remains, but even today many aspects concerning the continental palaeoenvironments reflected in these deposits (including the occurrence of palaeo-wildfires) have not been studied in detail. So far six distinct macro-charcoal bearing levels could be identified within the type section of the Bahariya Formation at Gabal El Dist profile, one of the most prolific outcrops of this formation in terms of fossil occurrence located in the north of the Bahariya Oasis, Western Desert, Egypt. Most of the charcoal investigated by means of SEM originates from ferns, pointing to a considerable proportion of this plant group within the palaeo-ecosystems that experienced fires. Gymnosperms and (putative) angiosperms have less frequently been identified. The collected data present evidence that the landscapes at the northern shores of Gondwana repeatedly experienced palaeo-wildfires, adding extra proof to previous statements that the Late Cretaceous was a fiery world on a global scale.
For almost a century different proxies, such as charcoal, coal macerals like fusinite and semifusinite, as well as pyrogenic polyaromatic hydrocarbons have widely been used to reconstruct the history of palaeo-wildfires throughout the Earth’s deep time history (e.g. Potonié 1929; Harris 1958; Alvin 1974; Scott 2000, 2010; Scott et al. 2014). Numerous studies have demonstrated that wildfires were integral agents of disturbance in many continental ecosystems ever since the Silurian (e.g. Scott 2000, 2010; Scott et al. 2014; Jasper et al. 2017; Pole et al. 2018; and citations therein). Nevertheless there are still large stratigraphic and geographic gaps in the knowledge about pre-Quaternary wildfires (e.g. Abu Hamad et al. 2012; Brown et al. 2012).
The Cretaceous is widely regarded as a “high-fire” period in Earth’s history (e.g. Brown et al. 2012; Scott et al. 2014) and recently it has been argued that the frequent and intense fires occurring during large parts of the Cretaceous may have played an important role in the evolution of angiosperms and angiosperm dominated vegetation (e.g. Bond and Scott 2010; Brown et al. 2012; Belcher and Hudspith 2017). However, as summarized by Brown et al. (2012), the majority of published records for Cretaceous fires comes from the northern continents (i.e. North America, Europe, Asia) while there are large geographic and stratigraphic gaps on the southern continents, formerly parts of Gondwana.
In the last few years, a number of studies (e.g. Manfroi et al. 2015; Muir et al. 2015; Abu Hamad et al. 2016a, 2016b; Carpenter et al. 2016; dos Santos et al. 2016; El Atfy et al. 2016; Martill et al. 2012; Lima et al. 2019) have already demonstrated that the Cretaceous wildfires were more frequent on the southern continents than previously reported in the literature (e.g. Brown et al. 2012). However, compared to records from the northern continents still considerably less is known about the Cretaceous fires from the southern continents, including the entirety of Africa.
The occurrence of macro-charcoal in sediments of the Bahariya Formation at the Bahariya Oasis, Egypt has previously been mentioned by a number of authors (e.g. Dominik 1985; Nothdurft et al. 2002), unfortunately without providing any conclusive evidence (sensu Scott 2000, 2010) that the material really represents charcoal, and therefore it is not clear whether these reports can be used as evidence for the occurrence of wildfires or not. Here we present such evidence for the repeated occurrence of palaeo-wildfires during deposition of the Bahariya Formation in the form of macro-charcoal originating from six distinct levels at the Gabal El Dist profile at the Bahariya Oasis. This evidence confirms the previous claims about the occurrence of charcoal in the Bahariya Formation, and adds reliable information on the so far only known occurrence of Cenomanian palaeo-wildfires all over Africa.
Geology, palaeontology and stratigraphy
The Bahariya Oasis is situated in a morphological depression of an Eocene Limestone Plateau, where Cretaceous sediments are exposed. It is located about 340 km southwest of Cairo in the Western Desert of Egypt (Fig. 1). Within the area of the Bahariya Oasis, the oldest sediments exposed at the surface belong to the clastic unit of the Bahariya Formation, which is unconformably overlain by the late Campanian Hefuf Formation (Werner, 1990). The Bahariya Formation was defined by Said (1962) and El Akkad and Issawi (1963). According to Klitzsch and Hermina (1989), the Bahariya Formation at its type locality (and near our studied area) is lithologically composed of fluviatile sandstone and siltstone in the lower part, grading upwards into alternating beds of estuarine sandstone and shale, especially in the Abu Roash area.
Lithostratigraphically, the Bahariya Formation has been subdivided into two members: the lower Gebel Ghorabi Member (fluviatile sandstone); and, the upper Gebel Dist Member, which is strongly affected by tides with some intercalations of lagoonal origin, made up of intercalations of partly glauconitic sandstone, siltstone and claystones (Dominik 1985). Some authors (e.g. Dominik 1985) also include the overlying El Heiz Formation as a third member, which is composed of calcareous or siliceous sandstones and claystones that represent gradual regression and which is of lagoonal and supratidal origin. However, in the current study we treat this rock unit as El Heiz Formation, following El Akkad and Issawi (1963) and others, as this nomenclature is widely accepted.
The fossil content of the Bahariya Formation is well known for its outstanding record of vertebrate remains, including a variety of iconic dinosaurs, like the carnivorous Spinosaurus and Carcharodontosaurus, as well as the herbivorous Aegyptosaurus and Paralititan (e.g. Stromer 1915, 1931, 1932; Smith et al. 2001; Nothdurft et al. 2002). However, besides dinosaurs and other vertebrates as well as invertebrates (e.g. Stromer 1936; Nothdurft et al. 2002; Schweitzer et al. 2003), the Bahariya Formation provided also a wealth of fossil plants in different preservational states (e.g, Kräusel 1924, 1939; Hirmer 1925; Lejal-Nicol 1987, 1990; Lejal-Nicol and Dominik 1990; El-Saadawi et al. 2016).
The presence of vertebrate and plant remains, especially in the upper part of the Gebel Dist Member (Dominik 1985), points to a Cenomanian age for the formation (Schaal 1984; Dominik 1985; Lejal-Nicol 1987). The fossil content includes terrestrial vertebrates like aquatic lungfishes, turtles, crocodiles, dinosaurs, marine vertebrates like sharks, plesiosaurs and the sea serpent Symoliophis sp., as well as ammonites, lamellibranchiates and mangrove-dwelling crabs (e.g. Schaal 1984; Dominik 1985; Werner 1989; Smith et al. 2001; Schweitzer et al. 2003). Plant remains include Paradoxopteris stromeri, Weichselia reticulata, Nelumbites, Cornaephyllum, Dipterocarpophyllum, Magnoliaephyllum, Ficophyllum, Laurophyllum, Araliaephyllum, Salix and Rogersia (e.g. Kräusel 1924, 1939; Hirmer 1925; Lejal-Nicol 1987, 1990; Lejal-Nicol and Dominik 1990; El-Saadawi et al. 2016). All these findings represented a unique source of information about the Late Cretaceous North African continental palaeoecosystems, although there are still many aspects of these ecosystems which have so far not been studied in sufficient detail.
Material and methods
During field work in 2016, a total of 50 samples (labelled D1–D50) were taken from the Gabal El Dist profile for further analysis (Fig. 2). All samples were checked for the presence of macroscopically recognizable charcoal and if present, charcoal samples were extracted mechanically from the sediment with the aid of preparation needles and tweezers under a binocular microscope in the laboratory.
Due to the very fragile nature of the charcoal specimens, they could not be cleaned further with acids to remove adhering mineral remains, as even very careful treatment has led to the total fragmentation of comparable material into even smaller fragments. The samples collected at Gabal El Dist profile are stored in the collection of the Department of Geology, Mansoura University (Egypt). Samples prepared for SEM are stored in the collection of the Senckenberg Forschungsinstitut und Naturmuseum Frankfurt (Germany).
Samples were mounted on standard stubs with LeitC (Plano, Münster, Germany), and subsequently examined with the aid of a JEOL JSM 6490 LV Scanning Electron Microscope (SEM; accelerator current 20 kV) at the Senckenberg Forschungsinstitut und Naturmuseum Frankfurt (Germany).
Macro-charcoal was recovered from 6 levels of the studied profile, labelled here in ascending order as “Charcoal level” (Chl) 1 to 6. In Chl 1 (sample D2), charcoal fragments occur in grey, massive, gypsiferous, slope forming clay. This level corresponds to the so called “dinosaur bed”, from which numerous vertebrate remains have been recovered during the last century (Dominik 1985). Charcoal fragments are between 2 × 3 mm and 10 × 10 mm large, with rounded edges. A total of 3 pieces of charcoal has been analysed by SEM.
In Chl 2 (sample D4), charcoal fragments occur in a grey, fissile, gypsiferous, moderately hard shale, which forms slopes. They are between 1 × 1 mm and 4 × 4 mm large, with slightly rounded edges. A single piece of charcoal could be analysed by means of SEM. The charcoal from this level is heavily crushed due to sediment compaction and no taxonomically meaningful anatomical details can be observed, which would be necessary for any further interpretation.
In Chl 3 (sample D15), charcoal fragments occur in varicoloured green and yellow, slightly hard to friable, glauconitic sandstone, which forms cliffs. They range from tiny fragments (smaller than 1 × 1 mm) up to 10 × 15 mm large fragments, with rounded edges in large fragments. Charcoal is rather abundant in this level, as compared to the other levels, and only slightly compressed. A total of 15 pieces of charcoal has been analysed by means of SEM.
In Chl 4 (sample D39), charcoal fragments occur in a grey, moderately hard, gypsiferous sandstone, which forms cliffs. They are between 2 × 2 mm and 10 × 10 mm large, with slightly rounded edges. A single piece of charcoal has been analysed by means of SEM.
In Chl 5 (sample D47), charcoal fragments occur in a dark grey to black, fissile, gypsiferous shale, containing plant remains, which forms slopes. They are between 2 × 2 mm and 5 × 10 mm large, with sharp edges. A total of 2 pieces of charcoal have been analysed by means of SEM.
In Chl 6 (sample D50), charcoal fragments occur in dark grey, fissile, gypsiferous shale units, topped by ferruginous, slope forming sandstone. They are between 1 × 1 mm and 5 × 15 mm large, with rounded edges. A single piece of charcoal was analysed by means of SEM.
The specimens from all six levels investigated for this study exhibit black streak, silky lustre, as well as three-dimensionally and well preserved anatomical details (Figs. 3, 4, 5, 6) and homogenized cell walls under the SEM (e.g. Fig. 4a). These features are considered as diagnostic for charcoal (e.g. Jones and Chaloner 1991; Scott 2000, 2010) and thus represent direct evidence for the repeated occurrence of palaeo-wildfires during deposition of the Cenomanian Bahariya Formation at Gabal El Dist profile, Western Desert, Egypt.
Charcoal from Chl 2 has heavily been compacted and shattered, showing limited anatomical details, which would be necessary for further interpretations of the taxonomic affiliation of charred source plants and thus the potential source vegetation. In some specimens from Chls 1, 3 and 6, fungal hyphae occur on tracheid walls (Fig. 4b, c), occasionally growing through pit apertures (Fig. 4c). One specimen from Chl 1 exhibits large cavities in the center of the cell walls, which can be interpreted as the result of microbial decay by so far unidentified microorganisms prior to charring (Fig. 4c-f) (cf. El Atfy et al. 2017). These cavities also include putative fungal remains (Fig. 4e), and numerous three-dimensionally preserved, filamentous structures of unknown origin (Fig. 4f).
Anatomy and taxonomy
In most charcoal levels, charcoal fragments are either too small or heavily compressed and thus no anatomical details of any taxonomic value can be obtained from these specimens. However, some specimens from Chl 5 and Chl 6, as well as all specimens from Chl 3 show enough anatomical details to enable at least some general taxonomic interpretation. So far, these charcoal specimens can be assigned to ferns, a gymnosperm and a (putative) angiosperm.
Charcoal fragments assignable to ferns have so far only been identified within Chl 3, but here they are abundant. Charcoal specimens consist of sclerenchymatic fibres (Fig. 5a, b), tracheids (30–70 μm wide) with scalariform pitting (Fig. 5d, f) and parenchymatic cells (Fig. 5c).
The observed anatomical details in these specimens are in agreement with the anatomy of Paradoxopteris stromeri Hirmer (cf. Hirmer 1925, 1927; Edwards 1933; Koeniguer 1966), which has previously been described from the Bahariya Formation at the Bahariya Oasis (e.g. Hirmer 1925, 1927; Kräusel 1939; El-Saadawi et al. 2016). Silicified remains belonging to this taxon occur frequently in the basal most horizons at Gabal El Dist (Stromer 1914; Hirmer 1925). This taxon represents the rachis of the mattoniaceous fern Weichselia reticulata (e.g. Schuster 1930; Edwards 1933), which also occurs in the Bahariya Formation at Bahariya Oasis (e.g. Hirmer 1925; Kräusel 1939; El-Saadawi et al. 2016). However, due to the fragmentary nature of the charcoal specimens, a definitive assignment to either of these taxa is not possible, although it seems very likely that at least some of the charcoal specimens belong to the same source plant as these taxa. A comparable co-occurrence of anatomically comparable, charred fern rachis-fragments and Weichselia reticulata fronds has previously been described from other Cretaceous localities (e.g. Abu Hamad et al. 2016a).
Ferns were abundant and diverse in the Cenomanian habitats on the northern shore of Gondwana, as indicated by palynological studies. Based on spores, a number of fern families, i.e. Cyatheaceae/Dicksoniaceae, Osmundaceae, Matoniaceae/Dipteridaceae, Gleicheniaceae and Schizaeaceae, were known from the Bahariya Formation (e.g. Abdel-Kireem et al. 1996; Ibrahim 2002; El Atfy 2011).
Only a single specimen of charcoal from Chl 6 can unequivocally be assigned to the gymnosperms. It consists of pycnoxylic wood (Fig. 6a) with abundant rays (Fig. 6b). Rays are either 2 (Fig. 6d) or 4–8 cells (Fig. 6f) high, with one (or rarely two) pits on cross-fields (Fig. 6e, f). Tracheids are ~ 8–18 μm wide (Fig. 6d). Pits on radial tracheid walls are uni-seriate and touching, with relatively large apertures. The same can be seen in cross-field-pits which resemble taxodioid or cupressoid pits. As the form of pit-apertures is easily altered during charring (Gerards et al. 2007), it is not clear whether this observation represents the primary state of the apertures or a charring artefact. Due to these alterations and the fragmentary nature of the specimen, it is not possible to provide a more specific taxonomic affiliation.
Kräusel (1939) compared silicified gymnosperm wood from the Bahariya Formation at Bahariya Oasis with Dadoxylon aegyptiacum Unger. Otherwise gymnosperm remains seem to be rather rare in the macroflora of the Bahariya Formation. In contrast pollen assignable to a number of different gymnosperm groups, including conifers, cycads and Gnetales, are abundant and diverse in the sediments of the Bahariya Formation (e.g. Abdel-Kireem et al. 1996; Ibrahim 2002; El Atfy 2011).
In some charcoal levels (Chls 1, 4 and 5), a few charcoal fragments occur, which might be related to angiosperms. However, in most levels these fragments are too small to allow for an unequivocal decision whether they really belong to angiosperms or not. Only specimens from Chl 5 show enough anatomical details allowing for at least some anatomical description.
The matrix of the wood consists of rather small fibres and/or tracheids and parenchymatic cells (Fig. 7a-e). Vessels (?) are around 50 μm wide, with scalariform perforation plates (Fig. 7a-c). Intervessel pits on vessel walls are scalariform (Fig. 7a-c). Vessels are surrounded by vasicentric tracheids (Fig. 7d-f). Due to the fragmentary nature of all specimens, it is not possible to provide a more specific taxonomic affiliation than to state that these remains probably represent angiosperms.
According to Kräusel (1939), silicified wood of Evodioxylon intermedium Kräusel, a putative Rutaceae, occurs in the Bahariya Formation at Bahariya Oasis. Additionally a number of angiosperm taxa based on leaf remains have been cited in the literature (e.g. Kräusel 1924, 1939; Lejal-Nicol 1987, 1990; Lejal-Nicol and Dominik 1990), but these remains are in urgent need of a modern taxonomic revision. A number of pollen taxa assignable to angiosperms have also been reported from the Bahariya Formation (e.g. Abdel-Kireem et al. 1996; Ibrahim 2002; El Atfy 2011).
The occurrence of putative charcoal, in form of black and opaque phytoclasts, has repeatedly been mentioned by palynological studies of sediments attributed to the Bahariya Formation from different subsurface wells within the North Western Desert (e.g. Tahoun and Mohamed 2013), but none of this material has so far been figured and thus it is not clear whether it really represents charcoal or not. Additionally, Dominik (1985) and Nothdurft et al. (2002) mentioned the occurrence of macroscopic plant fragments, which might represent charcoal within sediments of the Bahariya Formation at the Bahariya Oasis. However, also these authors conducted no in depth analysis of these remains, to provide proof for a pyrogenic origin of the material mentioned by them. The charcoal presented here (including the material studied by El Afty et al. 2017, for taphonomic purposes), represents unequivocal proof for the (previously only assumed) occurrence of palaeo-wildfires during deposition of the sediments of the early Cenomanian Bahariya Formation in Egypt.
Additionally our results provide further evidence for the globally widespread occurrence of wildfires during large parts of the Cretaceous (cf. Brown et al. 2012 and citations therein). It represents only the fourth Cenomanian report for the entirety of Gondwana (Table 1; Fig. 8) and constitutes the first description of evidence for repeated palaeo-wildfires in a single profile for that palaeo-continent. This demonstrates that such fire-events repeatedly affected the landscapes at the northern shore of Africa during this age and that they were important factors in palaeoenvironments in which iconic dinosaurs, like the carnivorous Spinosaurus and Carcharodontosaurus, roamed. However, at the moment it is not clear, how these dinosaurs were affected by these recurrent wildfires, but it seems at least reasonable to assume that fires may have influenced the animals living in the habitats experiencing the wildfires, either through the direct negative effects of fire and heat or indirectly through destruction of the vegetation as primary source of food, shelter etc.
The occurrence of charred fern remains as well as gymnosperm and (putative) angiosperm charcoal in different levels (but so far not together in the same level) suggests that maybe different vegetation types were affected by fires during deposition of the Bahariya Formation. Of particular interest is the abundant charcoal from Chl 3, as this material seems to consist only of charcoal derived from ferns comparable to Paradoxopteris/Weichselia reticulata. Similar accumulations of charred fern remains attributed to Paradoxopteris/Weichselia reticulata, are known from other Cretaceous deposits (e.g. Harris 1958, 1981; Alvin 1974; Brown et al. 2012; Sender et al. 2015; Abu Hamad et al. 2016a), and experimental work on different potential sources of fuel for Cretaceous fires showed that many ferns are highly flammable and may support rapidly spreading fires (e.g. Harris 1981; Belcher and Hudspith 2017). Under the high-oxygen atmosphere of the Late Cretaceous, not only the potential to be ignited would even be higher than today (e.g. Belcher and McElwain 2008; Belcher et al. 2010) but also the intensity of such fern fuelled fires (Belcher and Hudspith 2017). This higher flammability of Cretaceous vegetation is also reflected in the relatively high concentrations of pyrogenic inertinites in numerous coals from this period (e.g. Diessel 2010; Glasspool and Scott 2010).
Based on plant macroremains (mainly impressions, root traces and permineralised remains), Lacovara et al. (2003) and El-Saadawi et al. (2016) interpreted the palaeoflora of the Bahariya Formation as mainly representing a mangrove, an interpretation supported by the occurrence of typical mangrove-dwelling crabs (Schweitzer et al. 2003). It is possible that the charred ferns from Chl 3 were growing in a comparable coastal (mangrove or mangrove-like) ecosystem, as it has been assumed for another deposit also containing abundant fern-charcoal probably related to Paradoxopteris from the Early Cretaceous (Barremian) of Jordan (Abu Hamad et al. 2016a). A number of authors (e.g. Retallack and Dilcher 1981; Shinaq and Bandel 1998; Lacovara et al. 2003) interpreted Weichselia/Paradoxopteris as a typical constituent of such a mangrove-like vegetation type, flourishing during the Early–early Late Cretaceous. However, as the charcoal from this sandstone level at Bahariya Oasis has to be regarded as allochthonous, an origin from mangrove-like vegetation must remain speculative at the moment.
The occurrence of charcoal as evidence of repeated wildfires is in good agreement with palaeoclimatic interpretations for the Bahariya Formation. Based on palynological studies, a number of authors reconstructed a tropical warm and semi-arid climate during deposition of this formation (e.g. Abdel-Kireem et al. 1996; Ibrahim 2002). Such climatic conditions, with a marked and prolonged dry season, can promote the ignition and spread of wildfires (e.g. Scott et al. 2014), especially when the atmospheric oxygen concentration is assumed higher than today (see above).
In short, our data suggest that these wildfires probably affected different vegetation types, maybe extending into the wet-endmember of coastal ecosystems, fern dominated mangroves (or mangrove-like vegetation), which were probably the habitat of Spinosaurus that has been reconstructed as a piscivorous and semiaquatic predator (e.g. Ibrahim et al. 2014).
Based on current data and interpretations, we can conclude that palaeo-wildfires repeatedly occurred during the deposition of the early Cenomanian Bahariya Formation at the Bahariya Oasis in Egypt, located at the northern shores of Gondwana during that time. Our analysis also indicates that different types of vegetation, including angiosperms, gymnosperms and ferns, were possibly affected by fires. In one charcoal bearing level (Chl 3), it seems that (mangrove-like) coastal vegetation, dominated by ferns comparable to Paradoxopteris/Weichselia reticulata, was subjected to such fires. Our data supplement the so far scarce record of Cenomanian wildfires on the southern continents, providing further evidence that during the early Late Cretaceous fires were a common type of disturbance on a global scale.
Availability of data and materials
All data are available from the authors. Material is available from the corresponding repositories, as stated in the material section.
Sample number of samples taken at locality Gabal El Dist
Scanning Electron Microscope
Collection acronym: Senckenberg Museum Botany
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The authors gratefully thank Claudia Franz (Senckenberg Forschungsinstitut und Naturmuseum Frankfurt) for technical assistance with SEM facilities, and Ahmed Gomaa (Mansoura University) for his help during the field work. H. El Atfy and T. Anan thank Department of Geology, Mansoura University for logistic support during field work at the Bahariya Oasis.
D. Uhl and A. Jasper acknowledge the financial support by Coordenadoria de Aperfeiçoamento de Pessoal de Nível Superior - CAPES (A072/2013 and 8107-14-9), Conselho Nacional de Desenvolvimento Científico e Tecnológico - CNPq (444330/2014–3, 305436/2015–5), Brazil and Alexander von Humboldt Foundation (3.4-8151/18 025), Germany.
The authors declare that they have no competing interests.
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