New insights on the Permian mixed siliciclastic and carbonate deposits of southern Tunisia: Facies, ichnofacies and depositional environments

New insights on the Permian mixed siliciclastic and carbonate deposits of southern Tunisia: Facies, ichnofacies and depositional environments | Research Square window.SnipcartSettings = { analytics: { enabled: false } }; (function() { var accessVector = localStorage.getItem('access_vector') || ''; window.dataLayer = window.dataLayer || []; if (accessVector) { window.dataLayer.push({ user: { profile: { profileInfo: { snid: accessVector } } } }); } })(); (function(w,d,s,l,i){w[l]=w[l]||[];w[l].push({'gtm.start':new Date().getTime(),event:'gtm.js'});var f=d.getElementsByTagName(s)[0],j=d.createElement(s),dl=l!='dataLayer'?'&l='+l:'';j.async=true;j.src='https://www.googletagmanager.com/gtm.js?id='+i+dl;f.parentNode.insertBefore(j,f);})(window,document,'script','dataLayer','GTM-K279D39R'); Browse Preprints In Review Journals COVID-19 Preprints AJE Video Bytes Research Tools Research Promotion AJE Professional Editing AJE Rubriq About Preprint Platform In Review Editorial Policies Our Team Advisory Board Help Center Sign In Submit a Preprint Cite Share Download PDF Research Article New insights on the Permian mixed siliciclastic and carbonate deposits of southern Tunisia: Facies, ichnofacies and depositional environments Ali Khachira, Mohamed Soussi, Alfred Uchman This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-5706272/v1 This work is licensed under a CC BY 4.0 License Status: Published Journal Publication published 27 Jun, 2025 Read the published version in Facies → Version 1 posted 5 You are reading this latest preprint version Abstract The present study investigates the Permian mixed siliciclastic-carbonate system of southern Tunisia and describes the trace fossils recorded within the siliciclastic intervals. The carbonate facies represent a spectrum of depositional environments ranging from the outer shelf (CF1), through the shelf margin (CF2), to the middle to inner shelf (CF3 to CF6) settings, while CF7 corresponds to conglomeratic facies resulting from reef destruction. The siliciclastic facies (SF1 to SF9) developed on a ramp profile, while the latest Permian facies (SF10 to SF14) belong to a dominantly meandering fluvial system with flood plain red-beds. This work provides the first comprehensive review of trace fossils in this region. Seventeen ichnogenera produced by bivalves, trilobites, crustaceans, and vermiform organisms have been identified. In addition to being very common, facies-crossing ichnogenera, such as Planolites or Palaeophycus , Psammichnites , Protovirgularia , Parataenidium , Thalassinoides , and Taenidium appear to be more specific components of the Permian Cruziana ichnofacies. The combination of facies analysis and ichnofacies distribution demonstrates that the sedimentary evolution encompasses the alternation of two dominant depositional regimes represented by mixed siliciclastic-carbonate ramp sedimentation and rimmed carbonate platforms dominated by reefal development. The vertical transition from ramp to rimmed carbonate platform and vice versa reflects periodic variations in carbonate sedimentation rates, primarily controlled by sea-level fluctuations, subsidence, and resulting accommodation space, and climatic and palaeoecological conditions. Surface-to-subsurface stratigraphic correlation indicates that the subsidence played an important role in shaping the basin configuration comprising a shelf margin domain (Tebaga outcrops) separating a wide middle to inner shelf to the south from a rapidly subsiding depocenter to the north. The latter interpreted as a foredeep setting, accumulated over 4000 m of sediment, including thin turbiditic sandstones, carbonate breccias, and conglomerates derived from the adjacent rimmed platform. Facies Ichnofacies Carbonate platform Permian Southern Tunisia Gondwana Figures Figure 1 Figure 2 Figure 3 Figure 4 Figure 5 Figure 6 Figure 7 Figure 8 Figure 9 Figure 10 Figure 11 Figure 12 Figure 13 Figure 14 Figure 15 Figure 16 Figure 17 Figure 18 Figure 19 Figure 20 Figure 21 Figure 22 Figure 23 Figure 24 Figure 25 Figure 26 Figure 27 Figure 28 Figure 29 Figure 30 Introduction and objectives The Permian was a period of significant tectonic, eustatic, and climatic changes as reflected in the sedimentary record of the Gondwana realm (Ross and Ross 1987 ; Fielding et al. 2006 ; Fielding et al. 2008 ; Rygel et al. 2008 ; Haq and Schutter 2008 ; Gradstein et al. 2012 ; Chen et al. 2013 ; Scotese and Schettino 2017 ; Henderson et al. 2020 ). These changes record the transition from the Carboniferous-early Permian icehouse to the middle and late Permian greenhouse. The middle Permian (Guadalupian) greenhouse climate created optimal conditions for widespread reef development, particularly during the Wordian and Capitanian stages. This time interval represents the acme of Permian reef growth (Weidlich 2002 ), as evidenced by the global proliferation of shallow marine carbonate platforms with associated reef systems. Guadalupian reefs have been reported from both tropical and cool temperate zones, such as the Capitan Reef of Texas (Toomey and Babcock 1983 ; Fagerstrom and Weidlich 1999 ), Japan (Shen and Kawamura 2001 ), Arabian Platform (Weidlich 2007 ), Thailand (Dawson et al. 1993 ), Slovenia (Flügel et al. 1984 ), and China (Liu et al. 2016 ; Zhu et al. 2018; Tian et al. 2024 ). Most of these reef systems have been interpreted as being deposited in a shelf-margin context. The demise of reef ecosystems and the progressive decline of carbonate production (including the disappearance of tropical biota and the collapse of the carbonate factory) occurred globally near the end of the Capitanian (ca. 260 Ma) across various parts of Pangea. This crisis coincided with a major eustatic sea-level fall (Haq and Schutter 2008 ), global cooling and a decrease in seawater temperature (Isozaki et al. 2011 ; Kani et al. 2018 ) and glacial conditions in eastern Australia and Mongolia (Fielding et al. 2008 ; Fujimoto et al. 2012 ). During the late Permian, the prevalence of the greenhouse climate resulted in widespread aridity in northern Pangea, mainly characterized by the occurrence of playa and sabkha red beds, aeolianites, and evaporites (Schneider et al. 2006 ). During the Permian, large parts of the African Gondwana lacked marine Permian deposits. Except for the extreme southern part of the Karoo Basin in the southern part of Africa (Smith et al. 1995; Johnson et al. 1997 ; Catuneanu et al. 2005 ), and in southern Tunisia (Tebaga outcrops) (Fig. 1a, b, c). In Tunisia, well-bedded middle Permian marine fossiliferous and biohermal carbonates grade upwards into continental late Permian red-beds facies (Fig. 1d) (Douvillé et al. 1933 ; Berkaloff 1933 ; Mathieu 1949 ; Baird 1967 ; Skinner and Wilde 1967 ; Newell et al. 1976 ; Lethiers et al. 1989 ; Razgallah et al. 1989 ; Toomey 1991 ; Vachard and Razghallah 1993). Cyclic sedimentation, marked by alternating siliciclastic and carbonate strata, represents a defining characteristic of the Permian sequence in the Jebel Tebaga of Medenine (Toomey 1991 ). The siliciclastic deposits have not previously been the subject of a detailed investigation in terms of depositional environments when compared to carbonate deposits (Khessibi 1985 ; Chaouachi 1988 ; Toomey 1991 ). In addition, their associated invertebrate fossils, reported from various stratigraphic levels (Termier and Termier 1955 , 1977 ; Driggs 1977 ; Termier et al. 1977 ; Boyd and Newell 1979 ; Senowbari-Daryan and Rigby 1988 ; Angiolini et al. 2008 ; Verna et al. 2010 ; Ghazzay et al. 2015), are poorly documented and have never been thoroughly examined. This study provides a comprehensive analysis bringing together for the first time new sedimentological and ichnology data of the middle-to-upper Permian siliciclastic intervals and carbonates facies. It aims to: (1) refine the stratigraphic framework of the Tunisian Permian pattern based on an updated detailed mapping of both carbonate and siliciclastic main units in the E-W orientated Jebel Tebaga of Medenine; (2) characterize, based on lithology, sedimentary structures, faunal composition, the vertical and lateral facies, and thickness variations; (3) provide a detailed assessment, for the first time, of trace fossils from the siliciclastic intervals with a special focus on the trace fossil Cruziana , believed to be related to the unique trilobite specimen discovered in the Jebel Tebaga of Medenine; (4) interpret the depositional environment evolution over space and time, based on the combination of data collected from both carbonates and siliciclastic facies with their associated trace fossil assemblages; (5) integrate the surface to subsurface data to reconstruct the sedimentary evolution in relation to the global tectonic setting and sea level changes within the context of the northern Gondwana margin. Finally, a comparison of the southern Tunisia Permian sedimentary record with other age-equivalent strata from the USA and Arabia is attempted. Materials and methods Lithofacies mapping by integrating field observations, Google Earth imagery, and aerial photographs has been undertaken in order to emphasize the stratigraphic relationships and the interplay between siliciclastic and carbonate deposits. Panoramic views and close-up photographs have been taken to highlight the complex internal architecture of biohermal complexes and the surface boundaries between the different lithological units, especially the siliciclastic packages containing trace fossils. The well-exposed and representative sections have been logged to evaluate both the vertical and lateral facies changes as well as the distribution of trace fossils. Three cross-sections (Dar Njana-Halq Jmel (1), Baten Beni Zid-Merbah El Oussif (2) and Es Souinia-Saikha (3) sections) synthetizing the vertical stacking pattern of the Permian succession of Tebaga outcrops were constructed (Fig. 3). Furthermore, a synthetic cross-section encompassing the main stratigraphic units and associated trace fossil assemblages has been produced (base: N33°25′11.24″, E10°9′57.87″; top: N33°24′3.23″, E10°10′18.29″). Facies analysis of siliciclastic rocks was conducted based on Allen ( 1982 ), Scholle and Spearing ( 1982 ), Walker and James ( 1992 ), Dalrymple et al. ( 1992 ), Miall ( 1996 ), and Nichols ( 2007 , 2009 ) works. For the sedimentological interpretation of carbonate rocks, Dunham ( 1962 ), Tucker and Wright (1990), and Flügel ( 2004 ) were employed. Physical sedimentary structures and trace fossils were photographically illustrated, and their vertical distribution was precisely documented. The sandstone bed-bearing tetrapod tracks, initially described by Newell et al. ( 1976 ) (33°24'3.46"N; 10°10'15.53"E), and the holotype of the trilobite Pseudophillipsia azzouzi Termier and Termier ( 1974 ) housed in the Tunisian Geological Survey (ONM) have been reexamined and photographed. Geographic and geological settings Palaeogeographically, Tebaga outcrops constitute the remnant of the westernmost extension of the Peri-gondwanan shelves of the tropical Tethyan embayment. During the Permian, Tunisia occupied a critical palaeogeographic position at northern margin of Gondwana, marking the western tip of the Tethyan seaway (Fig. 1a) (Scotese and Schettino 2017 ). Geographically, the Permian outcrops are located in southern Tunisia, specifically in Jebel Tebaga of Medenine, situated near the Dkhilet Toujane village, approximately 25 km NW of Medenine, and 10 km SE of the Berber town of Toujane (Fig. 1b). They lie within the Dahar Plateau (Fig. 1c) and extend along a belt of E–W trending hills (3 km wide and 13 km long), bounded by the E-W Tebaga Fault (Bouaziz et al. 2002 ). The Permian strata of southern Tunisia form a monoclinal structure dipping southeastward (Fig. 1b, c). To the north of this monocline, the Permian rocks are unconformably overlain by the Jurassic (Callovian) deposits in the Es Souinia-Saikha area or by the Lower Cretaceous (Albian) Radhouane Member of the Zebbag Formation at Dar Njana-Halq Jmel area (Fig. 2). The buried Permian successions have been penetrated by more than thirty petroleum wells. In this study, only TB-1 and BMT-1 wells (Fig. 1b) have been utilised, as they offer the possibility to evaluate the vertical and lateral facies and thickness variations from north to south, thereby adding to the interpretation of depositional environments and palaeogeographic reconstructions. Results Updated surface lithostratigraphic framework Previous works have extensively studied the stratigraphic framework of Tebaga outcrops (Mathieu 1949 ; Newell et al. 1976 ; Khessibi 1985 ; Angiolini et al. 2008 ; Ghazzay et al. 2015). The field lithofacies mapping carried out during this work (Fig. 2) serves to enhance and refine those achieved by Mathieu ( 1949 ), Newell et al. ( 1976 ), Zouari et al. ( 1987 ), and Toomey ( 1991 ). This has enabled the identification and better characterization of key surfaces (e.g., transgressive, exposure, and karstification surfaces) that delineate the lithostratigraphic units. Three stratigraphic cross-sections representing three domains of Tebaga outcrops have been logged to characterize and document the E-W lateral facies and thickness variations affecting the different Permian lithostratigraphic units (Fig. 3) outcropping in the Dar Njana-Halq Jmel (Fig. 4), Baten Beni Zid-Merbah El Oussif (Fig. 5), and Es Souinia-Saikha (Fig. 6) sectors. The updated Permian lithostratigraphic framework, which comprises, from the base to the top, the Tebaga and Cheguimi formations, clarifies not only the vertical stacking pattern but also the key surfaces marking the major changes in sedimentation. The Tebaga Formation Oum El Afia Unit (OAU). This unit corresponds to r1 of Mathieu ( 1949 ), known as Oum El Afia isolated red shales outcrops, exposed along the road linking Dkhilet Toujane to the Berber town of Toujane (Fig. 1c). Its structural and stratigraphic relationships to the main Permian belt of Tebaga are still subject of controversy (Newell et al. 1976 ). In this study, only the trace fossils identified within this unit, comprising red shales and fine to medium-grained sandstones, are described. Dar Njana-Baten Beni Zid Unit (DNBBZU). This unit corresponds to r2 of Mathieu ( 1949 ). It outcrops both in Dar Njana (Fig. 4a, b) and in the Baten Beni Zid areas, where it underlies the first Biohermal Complex 1 (BC1) (Fig. 5a, b, c). This dominantly siliciclastic unit is composed of green to red shales alternating with white to iron-stained sandstones, well-bedded bioclastic/fusulinids limestones, and dolomites (Fig. 3). In the Dar Njana section, the DNBBZU is topped by a well-defined siliciclastic interval, grading upward into the BC1 or being unconformably overlain by the Albian-Turonian carbonates of the Zebbag Formation (Fig. 2). In the Baten Beni Zid area, the transition from the DNBBZU to the overlying BC1 is represented by fossiliferous shales (sponge-bearing) interlayered with fusulinid-rich limestones and cross-bedded sandstones (Figs. 2, 3, 4b, 5b, c). The revision of the fusulinid association, in addition to the investigation of associated smaller foraminifers, allowed Ghazzay et al. (2015) to assign an early to late Capitanian age to this unit. Biohermal Complex 1 (BC1). This unit consists of 60–100 m-thick, massive biohermal carbonates mainly built of encrusting algae Archaeolithoporella hidensis Endo, 1959, and Tubiphytes obscurus Maslov, 1956 (Newell et al. 1977; Chaouachi 1988 ). The bioherms interfere with shales, well-bedded bioclastic limestones, and locally cross-bedded iron-stained sandstones. The latter abut against the mounds, onlapping their flanks or completely covering them (Fig. 5b, c). In the western Dar Njana sector, lenticular sandstone bodies increase in both frequency and thickness (Figs. 2, 3) within the BC1. Herein, biohermal carbonates show partial to complete dolomitization and are unconformably overlain by Albian strata (Fig. 2). The BC1 is capped by conglomeratic facies in the Dar Njana area and by 2–3 m-thick iron-stained sandstones of considerable lateral extent in Merbah El Oussif area (Figs. 2, 3). Here, Khessibi ( 1985 ) identified an emersion surface at the top of BC1 and desiccation cracks at the top of the siliciclastic beds. In Baten Beni Zid-Merbah El Oussif, this unit thins significantly, with an increase in clay content between the bioherm masses. Merbah El Oussif Unit (MOU). This unit (140–280 m) occupies a broad area, separating BC 1 from the Biohermal Complex 2 (BC2). The MOU comprises stacked repetitive sequences (Fig. 5e) exhibiting a consistent vertical organization. The latter is made from base to top of fossiliferous olive-green to red shales alternating with fine-grained sandstone tempestites, sponge/algal patch reefs, and well-bedded bioclastic limestones. The unit shows notable lateral thickness variations and represents the most fossiliferous succession in the Tebaga outcrops (Fig. 3) (Newell et al. 1976 ; Toomey 1991 ). Cephalopods are rarely encountered within this unit in the Merbah El Oussif locality but are particularly abundant in the Es Souinia-Saikha area (Fig. 6a, b). Chusenella , Codonofusiella , Dunbarula , Neoschwagerina , Reichelina , and Yabeina fusulinids, found in the limestone beds, indicate a late Capitanian age for this unit (Ghazzay et al. 2015). Biohermal Complex 2 (BC2). This unit constitutes the second cliff of Jebel Tebaga and is exposed from the Es Souinia-Saikha to the Dar Njana-Halq Jmel (Figs. 2, 3, 4, 5, 6). It is composed of thick and vertically stacked massive biohermal dolomitic limestones laterally intercalated with shales, bedded bioclastic limestones, and a few lenticular iron-stained sandstones. These bioherms are primarily built by Archaeolithoporella hidensis and Tubiphytes obscurus encrusting algae, with notable increases in sponge and phylloid algae ( Ivanovia ) content in the Es Souinia sector (Chaouachi 1988 ; Razgallah et al. 1989 ). In the Denguir area (Figs. 1c, 2, 3), the uppermost part of this unit exhibits marked karstification, indicated by a distinct red dolomitic bed with algal lamination (Figs. 2, 3). Bellerophon Limestone Unit (BLU). Mathieu ( 1949 ) described this unit in the western (Halq Jmel) (Fig. 4c) and eastern (Es Souinia) (Fig. 6c) ends of J. Tebaga. It consists of well-bedded fossiliferous limestones (with Bellerophon ) interbedded with fossiliferous clay and small sponge patch reefs. Angiolini et al. ( 2008 ), based on the occurrence of fusulinids and conodonts ( Sweetognathus iranicus hanzhongensis Wang, 1978), the occurrence of Chusenella rabatei Skinner and Wilde, 1967 , smaller foraminifera, and brachiopods, assigned this unit in the Capitanian. The Cheguimi Formation Lower Cheguimi Unit (LCHU). This unit is dominantly composed of fossiliferous silty shales, bioclastic/oncolithic limestones, and small patch reefs at the base, grading upward into well-laminated to rippled sandstones, particularly rich in trace fossils. The LCH Unit is dated to the late Capitanian (Vachard and Razghallah 1993; Angiolini et al. 2008 ). The Last Permian Carbonate Interval (LPCI) of Permian Tebaga succession is located at the top of this unit (bed 31, section B of Newell et al. 1976 ) (Fig. 3). The LPCI yields the fusulinid Dunbarula mathieui , marking the late Capitanian stage (Ghazzay et al. 2015). Further east, in the Es Souinia area, this unit includes multiple patch reefs interfingering with bioclastic limestones and relatively few coastal marine sandstone beds (Figs. 2, 3, 6c, 7a). In the carbonates of this locality, a unique Tunisian trilobite specimen was discovered (Memmi and David 1965 ) (Fig. 7b). Upper Cheguimi Unit (UCHU). It represents the topmost unit of Tebaga outcrops and is only exposed at the western end of the outcrop belt (Halq Jmel) (Figs. 3, 4c). It is composed of red shales and ferruginous sandstones with scarce trace fossils. Newell et al. ( 1976 ) documented in this unit the first reptilian footprints that were re-examined by Contessi et al. ( 2017 ), who assigned them to the late Capitanian to Wuchiapingian age. Above this unit lies a large, flat area offering the opportunity to observe continental red beds with sandstone at Argoub El Oussif hill. These facies, entirely mapped within the Matmata geological sheet as the Triassic (Zouari et al. 1987 ), are still considered part of the Cheguimi sandstones (Capitanian–Lopingian) according to Bibonne ( 2014 ). In summary, according to the biostratigraphic chart by Angiolini et al. ( 2008 ), the mixed siliciclastic-carbonate of the Tebaga Formation, comprising the DNBBZU, BC1, MOU, BC2, and the BLU, spans approximately 7 Myr (268–ca. 261 Ma, zones from A. rowinsae to D. Mathieu ). Most of the units are estimated to last ~ 1.5 Myr each (Fig. 9). However, the duration of the LCHU time is approximately 1 Myr. The top of BC1 (~ 264.5 Ma) is capped by iron-stained siliciclastic beds in Merbah El Oussif (Fig. 8d) and by conglomerates in the Dar Njana area (Fig. 8c). Meanwhile, the top of BC2 (~ 261.5 Ma) is capped at Denguir Hill by karstification filled with red dolomites (Fig. 8a, b). Siliciclastic deposits are notably abundant in the western sections and become progressively scarcer towards the east (Figs. 3, 9). Facies analysis Carbonate facies and depositional environments The detailed description of the carbonate facies, their distribution, and interpretations of depositional environment are presented in Table 1. Sponge-algal patch-reefs (CF1) This facies consists of metric boundstone patch-reefs (Fig. 11a), dominated by diverse sponges (Fig. 11b, c, d), encrusting algae (Fig. 11d), with a subordinate contribution of fusulinids, crinoids and corals (Fig. 11e). The encrusting algae ( Archaeolithoporella hidensis and Tubiphytes obscurus ) contribute to the construction of the CF1 reef bodies, which display internal sediments (peloidal/bioclastic) and early submarine cement that greatly enhances their rigidity (Chaouachi 1988 ; Toomey 1991 ). The geometry and the composition of these reef bodies, especially their association with highly fossiliferous shales (SF1), indicate a deposition within a relatively open marine and low energy palaeoenvironment (outer-shelf setting). Newell et al. ( 1976 ) based on the examination of these bioherms, suggested that they grew and developed in a normal marine environment, most likely below the storm wave base, in water depths less than 50 m with relatively low turbulence (Toomey 1991 ). Encrusting algae massive bioherms (CF2) This facies consists of massive buildups, frequently dolomitized in the western end of the Tebaga outcrops. These reef bodies are plano-convex, with either symmetric or asymmetric geometry (Fig. 11f). They form part of the BC1 and BC2 units and show a boundstone framework with encrusting algae such as Archaeolithoporella hidensis and Tubiphytes obscurus (Figs. 11h, i, 13a, b, c) with minor contribution of calcisponges (Fig. 11h, i), corals (Fig. 11g) (Chaouachi 1988 ; Toomey 1991 ). In the Es Souinia area, this facies contains Parachaetetes lamellatus Koniski and the phylloid algae Ivanovia tebagaensis Vachard and Razgallah, 1989. The CF2 facies is both vertically and laterally associated with conglomerates, thin-bedded limestones, shales, and lenticular iron-stained sandstones (Fig. 5b, c). The boundstone texture, the planoconvex morphology, and the general absence of adjacent talus, in addition to the prevalent mud matrix and fine internal sediments (Fig. 11h, i), suggest a relatively low-energy depositional environment ranging from mid to shelf-margin settings (Toomey 1991 ). Gastropods ( Bellerophon )-rich limestones (CF3) This facies is primarily composed of packstones to grainstones, with Bellerophon gastropods. In the Halq Jmel area, it is particularly abundant in bioclast debris, bivalves, and miliolids (Figs. 12a, b, 13d), while to the east (Es Souinia area), it is rich in fusulinids and crinoids (Fig. 12b). The predominance of sessile benthos within this facies indicates deposition in inner to middle carbonate shelf settings under variable hydrodynamic conditions. Fossiliferous well-bedded limestones (CF4) Fusulinids-bioclastic packstone-grainstone (CF4.1) This subfacies consists of packstone to grainstone with fusulinids, bioclasts, algal debris (Figs. 12c, d, 13e, f), and rare oolites. Planar and low-angle cross-bedding, along with ripple marks, are observed within this facies. The presence of shallow marine fossils, ripple marks, and planar/oblique bedding indicates a high-energy shallow marine depositional environment. The association of the CF4.1 facies with foreshore to shoreface sandstones (SF5, Table 1) supports its interpretation as an inner to middle shelf setting influenced by wave action (cf. Tucker and Wright 1990). Oncoid packstone/“ Ottonosia ” (CF4.2) This facies consists of thin-bedded or massive beds where grains are algally coated and float within a lime mud to a bioclastic matrix. In thin section, the encrusted skeletal grains are composed of algae and sponge fragments (Figs. 12h, 13g). In the Hal Jmel area, particular oncoid facies of spherical shape (over 3 cm in diameter) named “Ottonosia” grains sensu Termier et al. ( 1977 ) (Fig. 12i), characterizes the LCHU. This facies has been interpreted as intertidal biopisoids by Ghazzay et al. (2015). They accumulated in the open-marine inner shelf, where fluctuating energy levels allowed repeated turnover and sufficient water movement, enabling the oncoliths to grow spherically and develop concentric laminae (Flügel 2004 ). Bioclastic limestones (CF4.3) This facies is composed of well-bedded, poorly sorted bioclastic limestones (wackestone to packstone), occasionally with fusulinids, encrusting algae, crinoids, lamellibranchs, ostracods, and oncoids (Figs. 12e, 13h). CF4.3 displays parallel to low-angle cross-stratifications. It is abundant in the BC1 unit, but particularly prevalent in the BC2 as an intermounds facies. In the Es Souinia area, CF4.3 exceptionally contains abundant straight nautiloid cephalopods ( Pseudorthoceras ) (Toomey 1991 ) (Fig. 12f, g) The poorly sorted character of CF4.3 and the abundance of bioclastic debris suggest a relatively high-energy depositional environment (Tucker and Wright 1990). CF4.3 has been interpreted as shell debris banks accumulating on a shelf setting by Toomey ( 1991 ). Patch-reefs with sponges and algae (CF5) This facies consists of patch reefs 1 to 1.5 m high and a few metres in width. They have a nodular appearance, especially in the Halk Jmel area, and are rich in sponges, oncoliths, corals, and locally, phylloid algae (Fig. 11j, k). The association of CF5 with the siliciclastic shoreface to foreshore facies (SF5, SF6) (Table 1), as well as CF4 indicates deposition within a coastal marine environment (cf. Tucker and Wright 1990). Dolomitized patch reefs and bioclastic limestones (CF6) This facies forms part of the “Barre dolomitique inférieure de Dar Njana” of Khessibi ( 1985 ) and consists of massive or well-bedded dolomites resulting from the secondary dolomitization of CF5 and CF4, such as in the upper part of the DNBBZ Unit, where it contains abundant ghosts of crinoids and bivalves (Fig. 12j). The dolomitic nature of this facies, the ripple marks, the neritic fauna, and its association with small patch reefs (CF5, see Table 1) indicate that CF6 most likely formed in an inner shelf setting. Conglomeratic facies CF7 This facies is only identified at the top of BC1 in the Dar Njana–Merbah El Oussif area. It corresponds to a conglomerate/breccia composed of angular to sub-rounded, poorly sorted debris, originating from the disaggregation of reefs. Sandstone elements reaching cobble size can also be present within this facies (Fig. 8c). This facies, recorded in the Dar Njana locality, reflects the exposure of the topmost part of BC 1, probably during a major sea-level fall. Siliciclastic facies and depositional environments Facies 1 (SF1): Lower offshore It corresponds to highly fossiliferous calcareous shales/marls that are relatively rich in brachiopods, sponges, algae, corals, crinoids, bryozoans, and fusulinids, and include thin-bedded tempestite sandstones (Fig. 18c, d) and trace fossils, such as Archaeonassa , ? Nereites , Planolites , Protovirgularia , Psammichnites , and Taenidium. The depositional environment of this facies is interpreted as a lower offshore setting occasionally affected by storms (Nichols 2009 ). The light colouration and high diversity of body and trace fossils may indicate a well-oxygenated marine environment. Facies 2 (SF2): Upper offshore It consists of shales that grade upward into increasingly silty deposits with thin-bedded siltstone intercalations. SF2 occurs in the lower strata of the DNBBZ Unit (Fig. 14). Sedimentary structures are generally absent in the siltstone beds, except for some planar lamination (Fig. 15g, h). The upward coarsening nature of SF2 and its transition into the heterolithic facies of SF3 (see Table 1) suggests a gradual evolution from deeper to shallower conditions during storm-weather periods in mud-dominated offshore environments (Walker and James 1992 ). Facies 3 (SF3): Offshore transition SF3 is found within the lower strata of the DNBBZ Unit in the Dar Njana area (Fig. 14). It consists of heterolithic facies composed of fine-grained rippled sandstones and tempestite beds, interbedded with green silty shales, arranged into coarsening- and thickening-upward cycles (10 and 40 cm thick) (Fig. 15c, e). The sandstones display rippled surfaces (oscillatory ripple marks) and planar parallel lamination (Fig. 15e, f). An interval containing seismite structures is also observed (Fig. 15d). Upwards, SF3 is capped by a sandstone package featuring hummocky and swaley cross-stratification (HCS/SCS), which is overlain by fine horizontally laminated siltstones (Fig. 15a, b). Trace fossils are mainly observed in the rippled sandstones and include Archaeonassa , Palaeophycus , Parataenidium , and Siphonichnus . The wave-rippled sandstones, with symmetrical crests, demonstrate the influence of oscillatory wave action. The formation and preservation of hummocky–swaley cross-stratification, followed by horizontally laminated fine siltstones as the strength of the oscillation decreases, suggest deposition in the offshore transition zone situated between the fair-weather wave base (FWWB) and storm wave base (SWB) (Nichols 2009 ). During fair-weather conditions, this zone experienced relatively calm conditions, with continuous mud deposition via suspension. Periods of intense storm activity led to an abrupt increase in wave energy and the deposition of HCS, planar-laminated, and wave-rippled sand beds in a muddy environment. Facies 4 (SF4): Lower shoreface SF4 comprises very fine to fine-grained sandstone beds forming a unit more than 4 m thick (Fig. 16g). The sandstones exhibit planar-lamination and a small-scale hummock approximately 1 m long (Fig. 16h). The transition from SF3 to SF4 is abrupt, shifting from heterolithic sediments below to homogeneous sandstones above. Trace fossils include ? Diplocraterion and Parataenidium , especially in the upper part of the section. The sandstones of SF4 indicate deposition in the lower shoreface setting above the mean fair-weather wave base, where the sediments were frequently reworked by storm and fair-weather waves (Walker and James 1992 ; Nichols 2009 ). Siliciclastic facies 5 (SF5): Upper-middle shoreface This facies is composed of fine-to-medium-grained tabular and thin-bedded sandstone showing planar bedding, oblique tabular bedding, hummocky cross-stratifications (HCS), trough cross-stratifications, and symmetrical ripple marks (Figs. 16c, d, e, 17f, g, h). Thin, rippled fusulinid limestone beds (Figs. 16f, 17e) are occasionally interbedded with the sandstone sequences. Some flame structures have been observed in the Halq Jmel area (Fig. 19a, b). Trace fossils include ? Ancorichnus , Cruziana , Halopoa , ? Helminthopsis , Palaeophycus , Parataenidium (Fig. 16a, b), Planolites , Psammichnites , and Siphonichnus. SF5 occurs within the DNBBZ Unit and the LCH Unit in the Halq Jmel area. The stratigraphic position of this facies between the lower shoreface SF4 facies and foreshore/upper shoreface trough cross-stratified SF6 sandstones (Table 1), along with the coarsening-up trend and the sedimentary structures, suggests a high-energy environment typical of an upper to middle shoreface setting (Walker and James 1992 ). Additionally, the presence of the flame structures may indicate wave-induced liquefaction during intense storm activity in the shoreface to foreshore settings (Howard and Frey 1984 ; Pemberton et al. 2012 ). Siliciclastic facies 6 (SF6): Upper shoreface to foreshore It comprises structureless thin-to-medium-bedded, medium-to coarse-grained white or ferruginous sandstones arranged in coarsening and thickening packages (Figs. 14, 17g, h). Sedimentary structures include wavy bedding (Fig. 17 a), ripple marks on the upper surface of beds (Figs. 17b, 19d), HCS and trough, horizontal/low-angle lamination (Fig. 19c), water escape (Figs. 19a, b, f), flute casts (Fig. 19e), convolute bedding (Fig. 19f), mud drapes (Fig. 19g) and flaser bedding (Fig. 19h). The tops of the beds are usually iron-stained and particularly rich in centimetre-sized (10–50 cm) wood fragments (Fig. 17c). Trace fossil diversity and abundance are low, with only Parataenidium , Planolites , and Thalassinoides observed. The alternation of parallel planar and small cross-ripple lamination demonstrates the importance of the tidal regime during the formation of SF6. The planar-parallel bedding commonly reflects deposition in the foreshore under high-energy conditions (Walker and James 1992 ). It is well established that the swash and backwash processes can produce low-angle seaward-dipping planar-parallel laminations, typically in well-sorted, medium to coarse-grained sandstones (Reineck and Singh 1980 ). Additionally, common symmetrical ripple and flaser bedding feature wave- and tidal-generated signatures. Siliciclastic facies 7 (SF7): Tidal channel This facies consists of iron-stained, fine-to-medium-grained sandstones featuring an erosive base and lenticular morphology (5 to 40 m of lateral extension) (Figs. 3, 5b, c, 18a, b). Low-angle to horizontal bedding with sigmoid tidal bundles are observed (Fig. 18b). The trace fossils Planolites , Phycodes , Parataenidium , Protovirgularia , and ? Gyrophyllites are present. Lens-shaped sand body geometry, finning-upward sequence, cross-stratification, and erosive basal surfaces suggest deposition in a shallow marine context via tidal channels. In the Biohermal complexes 1 and 2, SF7 cuts through biohermal carbonates and significantly disrupted their development. Siliciclastic facies 8 (SF8): Tidal sand bar It comprises of thickening-up white, yellow, to red, fine- to medium-grained, and moderately to well-sorted cross-stratified sandstones. The internal architecture is characterized by planar-parallel to low-angle cross-bedding with some reactivation surfaces (Fig. 20c). The mud drapes are not preserved. In the upper part, horizontal lamination and locally, ripple marks are present. The coarsening upward pattern and the sedimentary structures observed in this facies, and its association with the tidal flats facies (SF9, see Table 1) support the interpretation of SF8 as a tidal sand bar deposited within a tide-dominated estuary (sensu Dalrymple et al. 1992 ). Siliciclastic facies 9 (SF9): Mixed mud-sand flat This facies comprises red silty shales, locally green, intercalated with fine to medium-grained lenticular sandstone interbeds (Fig. 20d, e). The latter display liquefaction structures (convolute bedding), cross-stratification, climbing ripples (Fig. 20e), and planar lamination at the top. Roots may be observed locally. The thickness of the sandstone interbeds ranges from 10 cm to 1.5 m. The red muddy deposits indicate deposition in a low-energy environment. The interbedded sandstone bodies are interpreted as tidal creek deposits, accumulated through suspension settling in calmer environments on the margins of the estuary (cf. Dalrymple et al. 1992 ). Siliciclastic facies 10 (SF10): Shale of flood plain This facies consists of plurimetric clayey-silty intervals (Fig. 21a, d) incised by channelized lenticular sand bodies (SF12 and SF3, see Table 1) with varying thicknesses and extents. The fine grain size suggests deposition through suspension settling of the suspended clay and silt particles under very low-energy conditions, most likely on a floodplain (cf. Allen 1982 ; Scholle and Spearing 1982 ; Miall 1996 ). Siliciclastic facies 11 (SF11): Silt of flood plain It consists of thin-bedded (< 20 cm), horizontally laminated grey silt beds of metric-scale extent, showing fine parallel lamination (Fig. 21a, d). Based on sedimentological features and its interbedding within the SF10 facies, this facies is interpreted as deposits as deposited in calm, protected depositional setting within a floodplain, probably in interdistributary areas (cf. Allen 1982 ; Scholle and Spearing 1982 ; Miall 1996 ). Siliciclastic facies 12 (SF12): Non-amalgamated fluvial channels This facies is dominated by red sandstones with a lenticular geometry and an erosive base outlined by a lag deposit composed of shale clasts and wood fragments (Fig. 21f). In some areas, small ripple marks, convolute bedding, and planar/cross-stratifications are present (Fig. 21e). Root structures are observed at the top of some sand bodies. The trace fossil Planolites is present. The abundance and extensive nature of the floodplain deposits of SF10, along with the non-amalgamation and isolation of SF12, suggest that low-sinuosity, straight channels occupied the floodplain (cf. Miall 1996 ; Bridge 2003 ). Siliciclastic facies 13 (SF13): Crevasse splay sheet sands SF13 comprises red or white, fine- to medium-grained, sand sheet-like bodies, decimetres thick and metres in lateral extent. This facies is laterally discontinuous and encased within the silty shale of the facies SF10 (Fig. 21a). The surface of a sandstone bed of SF13 preserves tetrapod footprints (Fig. 21a, b, c). Plane and oblique cross-stratification, climbing ripples (Fig. 21g), ripple marks, root structures (Fig. 21h), and trace fossil Planolites are recognized. SF13 is likely interpreted as crevasse splay deposits formed by the rupture of a principal fluvial channel’s margins. The root traces suggest dense vegetation in the inter-channel zone, which also encroached on abandoned and pedogenized crevasse splays (cf. Walker and James 1992 ). Siliciclastic facies 14 (SF14): Palaeosol It comprises to highly bioturbated and slightly consolidated sand bodies, up to 2 m thick. The sand is fine- to medium-grained, nodular, and displays abundant root structures (Fig. 21i). Once the infilling stage of the channel was complete and the channel subsequently abandoned, the surfaces of the lithosomes of facies SF12 and SF13 became exposed and were colonized by vegetation. Progressive pedogenesis, including root action, caused significant mixing of the sediment. Therefore, SF14 is interpreted as an intensively vegetated palaeosol developed in the interfluve zone of a fluvio-deltaic system (cf. Walker and James 1992 ). Mixed siliciclastic-carbonate record The mixed siliciclastic-carbonate deposits are most prominently developed within the Tebaga Formation (DNBBZ, BC1, and MOU) (Figs. 2, 3). Sandstone rocks either are interbedded with shales or are laterally equivalent to carbonates (Fig. 22a, d). Within BC1, the sandstone beds are erosively based and show cross-stratification. Their dimensions vary according to their position relative to the reefs. They generally thin when overlying the reefs, and form massive, plurimetric lenses (averaging 4 m in thickness) with limited lateral extent (averaging 10 m) in the depressions between biohermal bodies. Three types of relationships between the reef mounds and sandstone lenses can be identified. Sandstone bodies may underlie reef framework and serve as a substrate for reef development, or may partially or completely encase the reef mounds (Fig. 22b). The sandstone lenses abut against the bio-constructed mounds and lap onto their flanks (Fig. 22c). Comparable internal architectures and relationships between reef and non-reef facies have been documented in the Late Eocene mixed carbonate–siliciclastic system in the southern Pyrenees, Spain, where coral buildups alternate with bedded limestones and sandstones (Morsilli et al. 2011). The sandstone-bioherm association is less commonly observed within the BC2, where bioherms are mostly associated with well-bedded bioclastic limestones (Fig. 22e, f). Ichnofossils assemblages As mentioned in the introduction, trace fossils from the Permian of Tunisia have not been extensively described and documented aside from a few references, most of which involve misidentification. This work presents the first comprehensive review of trace fossils, a novel contribution to the study of the investigated deposits. In addition, the trace fossils of the Tebaga outcrops are abundant and relatively diverse, and some of them are well preserved, contributing to a better interpretation of palaeoenvironmental conditions. Seventeen ichnogenera from the middle-late Permian siliciclastic deposits have been identified throughout the studied stratigraphic units (Fig. 10, Table 2), attributed to the activity of bivalves, trilobites, crustaceans, and vermiform organisms. They are highly abundant in DNBBZ and MO units. In the white to iron-stained sandstones of the basal DNBBZ Unit (SF3 to SF6), intense burrowing is observed, displaying vertical and sub-vertical dwelling structures of inferred suspension-feeding organisms and horizontal structures attributed to deposit feeders. They include ? Ancorichnus (Fig. 23a), Archaeonassa (Fig. 23b), Cruziana (Fig. 23d), ? Diplocraterion (Fig. 23e), ? Helminthopsis (Fig. 24b), Palaeophycus (Fig. 24d), Parataenidium (Figs. 23b, 24e, f), and Siphonichnus (Fig. 26a). Higher in the section, the tempestite sandstones (SF1) of the MO Unit contain abundant burrows, including Archaeonassa (Fig. 23c), Planolites (Fig. 25b), Protovirgularia (Fig. 25c), and Psammichnites (Fig. 25f). This suite of trace fossils reflects the activity of organisms mainly in an offshore setting. The inter-reef tidal sandstones (SF7) within the BC2 contain Phycodes (Fig. 25a), Planolites (Fig. 25b), Protovirgularia ( Fig. 25d), ? Gyrophyllites (Fig. 23f), and Taenidium (Fig. 26b). Towards the top of the succession, the foreshore to shoreface siliciclastic deposits of the LCHU (SF5-SF6) contain Halopa (Fig. 24a), Psammichnites (Fig. 25e), Parataenidium , Planolites , and ? Thalassinoides (Fig. 26c), while the fluvial deposits of the UCHU are characterized by a rare occurrence of trace fossils and contain only Planolites . All the aforementioned traces (Table 2) belong to the Cruziana ichnofacies. Trilobite and Cruziana in the Tebaga outcrops In the Es Souinia-Saikha outcrop, a single specimen of the trilobite Pseudophillipsia azzouzi Termier and Termier ( 1974 ) (Fig. 7b) has been found by Memmi and David ( 1965 ) at the eastern end of Jebel Tebaga (33°25'25.37"N; 10°16'30.70"E). Termier and Termier ( 1974 ) ascribed the trilobite to the Pseudophillipsia sumatrensis (Roemer) group, emphasizing its incomplete preservation and large size. P. sumatrensis is the Guadalupian – lower Lopingian taxon (Fig. 7c). A second specimen (Fig. 7e) was recently found in an isolated hill in the western part of the Permian belt (N33.408799°, E10.193526°) within the LCHU, close to the Halq Jmel area. The new mapping indicates that this interval is a stratigraphic equivalent to the interval where the only Tunisian trilobite has been collected (Figs. 7a, 8). As Cruziana could have been left by organisms other than trilobites, the identification of the producing organism is uncertain. Cruziana was mostly produced by trilobites, but it may also have been produced by bilaterally symmetrical organisms, including non-trilobite arthropods and arthropod-like organisms, even in the Palaeozoic era (e.g., Boucot 1990 ; Donovan 2010 ). Nevertheless, Permian Cruziana is relatively rare. So far, it has been reported from the USA (Minter et al. 2007; Minter and Lucas 2009 ), Brazil (Lima and Netto 2012 ), Australia (Feng et al. 2021 ), and Egypt (ElRefaiy et al. 2023). Discussion Depositional environments evolution The sedimentary evolution of the middle-late Permian records the multiple superpositions of ramp and shelf margin carbonate platform depositional settings. Phase 1: First ramp profile The sedimentary succession of the DNBBZ Unit corresponds to a ramp depositional profile characterized by the interplay of siliciclastic and carbonate sediments (Fig. 27). The basal part broadly reflects a transgressive offshore shale/dolomite, overlain by regressive shales and siltstone beds of upper offshore setting (SF2). The succession grades upward to heterolithic facies reflecting storm-dominated conditions of an offshore transition setting. The upper part, consisting of mixed siliciclastic/carbonate deposits (SF4, SF5, SF6, and CF4), reflects a deposition fluctuating between the lower shoreface to the foreshore, while the topmost iron-stained sandstones interval (Fig. 27) indicates shoreface to foreshore settings. This phase corresponds to a major transgressive-regressive sequence made of several stacked high-order sequences (4th order) (Fig. 14). Siliciclastic facies of this phase are rich in trace fossils, such as ? Ancorichnus in SF5, Archaeonassa in SF3, Cruziana in SF5, ? Diplocraterion in SF4, ? Helminthopsis in SF5, Parataenidiumin SF4, SF5 and SF6, Palaeophycus in SF4 and SF5, Psammichnites in SF5, Siphonichnus in SF3 and SF4, and ? Thalassinoides in SF6. Well-preserved Parataenidium predominantly occupies the most regressive parts of the coarsening upward cycles. The trace fossil assemblage is typical of the Cruziana ichnofacies, especially its archetypal variety, typical of the upper offshore and the offshore-shoreface transition zones. The occurrence of Diplocraterion in the middle part of this phase (Fig. 10) may indicate the proximal Cruziana ichnofacies (Fig. 28), which is typical of the lower shoreface (Pemberton et al. 2001 ; MacEachern et al. 2012 ). The presence of the proximal above the archetypal Cruziana ichnofacies corroborates the overall shallowing upward trend. Phase 2: “Rimmed” shelf carbonate platform This phase encompasses the BC1 deposits. It marks the shift from a mixed siliciclastic-carbonate ramp (phase 1) to a thick carbonate platform system still recording minor siliciclastic influence. Indeed, following the renewed deepening of the depositional environment, siliciclastic influx greatly decreased, reef communities flourished, and massive reef-like bodies developed (facies CF2). The absence or limited extent of an adjacent reef talus and the presence of mudstones deposited between reefs suggest quiet, calm conditions within the photic zone (Toomey 1991 ). Reef development could be interrupted by the input of coastal terrigenous material derived from the west (Figs. 3, 5b, c, 27). The internal architecture of BC1, characterized by successive vertically and laterally stacked reef bodies, can be explained by the 'build-and-fill' model (McKirahan et al. 2003 ), highlighting the interplay between sea-level fluctuations, sedimentation rate, and accommodation space creation. This build-and-fill pattern is developed during periods of high-frequency, high-amplitude sea-level changes (Oborny et al. 2017 ), where each cycle may represent either a single depositional event or multiple stacked cycles. In the Tebaga outcrops, BC1 is composed of three distinct bioherm intervals separated by terrigenous shaly and sandstone sediments and well-bedded bioclastic limestones, documenting successive build-and-fill phases (Fig. 22d). During transgressive phases, reef growth produced massive carbonate bodies up to 20 m thick, which were subsequently killed by detrital influx during short regressive phases potentially amplified by increased humidity. The BC1, with an estimated duration of ~ 1.5 Ma (Angiolini et al. 2008 ) and thickness of 60–100 m, likely represents a 3rd-order depositional sequence containing multiple higher-order cycles (Haq and Schutter 2008 ). The abrupt contact between the massive reefal bodies (CF2) and overlying sandstones (SF6) and the presence of an exposed surface or thick conglomeratic horizon at the top BC1 indicate the termination of Phase 2 following the retreat of the sea during a probable sea-level drop. Similar patterns where siliciclastic influx during sea-level lowstands terminated mound development are documented from Pennsylvanian carbonate mounds of the Cantabrian Mountains (Spain) (Corrochano et al. 2012 ; Samankassou et al. 2013). Phase 3: Second ramp profile The lithological composition of the MOU unit essentially represented by highly fossiliferous shales (SF1) encasing metric-boundstone calcisponge/algal patch reefs (facies CF1) (Fig. 27) and the abundant nautiloids in the Es-Sounia-saikha indicate the establishement of a second ramp depositional system. In this system, the patch reefs have been deposited in a normal marine environment at less than 50 m depth, with relatively low turbulence (Toomey 1991 ). The upper part of this unit, composed of relatively thick patch reefs, frequent well-bedded limestones, and sandstone tempestite bodies, testifies to a shallowing upward trend. The trace fossil assemblage encountered within the sandstones ( Archaeonassa , ? Nereites , Planolites , Protovirgularia , Psammichnites , and Taenidium ; Fig. 28), dominated by horizontal feeding and locomotion traces are which is consistent with the archetypal Cruziana ichnofacies of upper offshore to transitional offshore-shoreface environments. The sporadic occurrence of ? Nereites may indicate intermittent development of distal Cruziana ichnofacies, typical of lower offshore settings (cf. Pemberton et al. 2001 ; MacEachern et al. 2012 ). In sum, the sedimentary record of the MOU broadly recorded a high amplitude sea level rise followed by a progressive shallowing-upward trend. The greater thickness and E-W facies variation compared to BC1 reflect high sedimentation rates and substantial accommodation space, probably driven by the combination of subsidence and sea level rise. Phase 4: Rimmed shelf to ramp The filling of the created accommodation space marking the upper part of the MOU, enabled the reinitiation of a new carbonate production (Fig. 27). This recovery allowed the construction of extensive (up to 20 m thick) massive bioherm bodies under optimal palaeoecological conditions within the photic zone (e.g., sunlight, low turbidity). These bioherms are mainly constructed by encrusting algae ( Archaeolithoporella hidensis , Tubiphytes obscurus ) in the western and central parts of Tebaga outcrops, while in the eastern areas, they are predominantly composed of the blue algae ‘ Parachaetetes lamellatus’ and the green phylloid algae ‘Ivanovia tebagaensis’ (Chaouachi et al. 1988 ; Chaouachi 1988 ; Razgallah et al. 1989 ). This phase marks the transition from a distally ramp system (Phase 3) to a rimmed shelf depositional environment (BC2), likely developed during late highstand conditions, associated with a net decrease in accommodation space. The regressive nature of this phase is evidenced by the eastward (seaward) progradation of biohermal carbonate bodies. Furthermore, the uppermost BC2 interval exhibiting karstification features confirms the regression trend that culminated in subaerial exposure of the carbonate platform. The overlying package, composed at the base of well-bedded carbonates with fusulinids (CF4.1), conodonts, and Bellerophon gastropods (CF3), and the top by highly fossiliferous shale (crinoids, brachiopods), indicates the establishement of open marine conditions probable of ramp system during a short deepening phase before the installation of a broadly regressive siliciclastic system (Fig. 27). Phase 5: Esturian to fluvial system These basal Cheguimi sandstone deposits, containing ripple marks, wood, and trace fossils, indicate a significant shallowing in the depositional environment. Sedimentary structures, including symmetrical ripple marks, mud drapes, and flaser bedding, collectively suggest a depositional setting dominated by tidal influences. Further up-section, these sandstones become dominant with a diverse trace fossil assemblage comprising Parataenidium , Psammichnites , Siphonichnus , and ? Thalassinoides . This trace fossil assemblage represents the archetypal Cruziana ichnofacies (Fig. 28), characteristic of the offshore to shoreface transition (Pemberton et al. 2001 ; MacEachern et al. 2012 ). However, the Upper Cheguimi Unit, mainly represented by silty shale floodplain facies (facies SF10), siltstones (facies SF11), sandstones (facies SF12 and SF13), and palaeosols (facies SF14), reflects deposition in very marginal marine to continental environments. Carbonate platform evolution The vertical transition from ramp to rimmed shelf systems has been extensively documented in the literature (e.g., Read 1985 ; Burchette and Wright 1992 ; Pomar 2001 ). These repeated changes in platform geometry reflect the dynamic interaction between accommodation space (controlled by rates of subsidence and sea-level fluctuations), sediment supply, and carbonate production regimes (governed by ecological factors). The DNBBZ Unit accumulated on a mixed siliciclastic-carbonate ramp system where organic communities were unable to form reefs. In contrast, BC1 deposition occurred during a period of increased accommodation space, which facilitated the formation of a platform-margin barrier (Figs. 27, 28). This transition may also be linked to biological control (a shift in the biotic system), leading to a high carbonate production by organisms able to build reef bodies (Pomar 2001 ). This shift in depositional style illustrates how the interaction between physical accommodation and biotic evolution can fundamentally control carbonate platform architecture. Following the demise of the rimmed shelf (BC1), a subsequent transgression allowed the development of a new carbonate ramp system during Phase 3, which in turn evolved into a second rimmed shelf (BC2) during late highstand conditions. The overlying BC2, formed within optimal photic zone conditions, supported renewed carbonate production and reef-building biota along a shallow shelf margin. This repeated ramp-to-rim transition is also evident in the Guadalupian strata of the Guadalupe Mountains, where the ramp of the San Andres Formation evolves into the reef-rimmed margin of the Capitan Formation (Kerans et al. 2013 ). Significance of the Tunisian Permian sedimentary record Sedimentological aspect The correlation presented in Fig. 29 has been developed to enhance our understanding of the N S evolution of the Tunisian Permian sedimentary system, prior to its comparison with analogous examples worldwide. The TB-1 well, located approximately 4 km north of Jebel Tebaga, penetrates a thick dominated shales succession (~ 4000 m) (Fig. 29). Notably, the correlation identifies the distinctive Bellerophon -bearing interval from the Halq Jmel section within the 144–620 m depth interval of the TB-1 well. This chronostratigraphic tie-point allows for a confident correlation between surface and subsurface data. The dominant shale unit, interbedded either with sandy to silty turbidites or breccia and conglomerates composed of reef limestone debris (Glintzboeckel and Rabaté 1964 ), is interpreted in this study as talus and gravity flow deposits. These probable fore-reefs to slope sediments likely originated from the collapse of a platform-margin to the south. The silty to sandy “turbiditic” sediments embedded within the thick shale succession may represent equivalents of the coastal marine siliciclastic intervals observed in the proximal Jebel Tebaga area. These findings support the hypothesis that the TB-1 well records, along with those of the MAR-1, MA-1, and KGF-1 wells (Fig. 1b), which are also made of shale-dominated, correspond to a large-scale foredeep subsiding basin. This basin extends southward into a mixed carbonate-siliciclastic system developed along ramp or rimmed carbonate profiles, and is supplied from the south by siliciclastic input (Fig. 29). In the BMT-1 well, located 88 km SE of Tebaga outcrops (Fig. 1b), the Permian succession comprises: (1) the lower Permian carbonates of the Zoumit Formation (2913–3009 m), (2) a dominantly siliciclastic interval (middle Permian?), (3) a middle Permian dominantly carbonate succession, and (4) a middle to late Permian dominantly siliciclastic deposits assignable to the Cheguimi Formation. The NW-SE correlation (Fig. 29) demonstartes that the two major siliciclastic intervals (DNBBZ Unit and the Cheguimi Formation) documented in outcrop are also present in the subsurface. Despite variations in thickness, the dominant carbonate interval (2285–2791 m), characterized by the presence of Globivalvulina sp., Glomomidiella sp., and Nodosaria sp. (Ghazzay et al. 2015), along with associated shales and evaporates, can be confidently correlated with the carbonate-dominated succession of the Tebaga Formation, including the BC1, the MOU, and the overlying BC2 and BLU intervals in outcrops. Palaeogeographically, this correlation strongly suggests that Tebaga outcrops represent the northern edge of a wide shelf-margin barrier reef system, well-documented in the subsurface near the Medenine area (ongoing work). This reef trend, which extends between the Tebaga outcrops and the MED-1 well (Fig. 29), delineated two distinct depositional domains: (1) a broad, shallow inner shelf to the south, characterized by bedded carbonates interbedded with shales, sands, and evaporites (e.g., BMT-1 well), and (2) a deeper, subsiding basinal domain dominated by shaly facies to the north (Fig. 29). Paleocurrent data recorded in the siliciclastic intervals provide insight into the sediment source and transport direction. Measurements from the DNBBZ Unit indicate a dominant sediment transport from south to north, with the source system likely located south-west of the Tebaga region (Chaouachi 1988 ). This source region may correspond to the Talemzane Arch, interpreted as a paleohigh during the Permian (Memmi et al. 1986 ). In contrast, paleocurrent indicators observed within tidal deposits of the LCHU (facies SF7 and SF8) and continental facies of the UCHU (facies SF12 and SF13) in the Halq Jmel and Argoub El Oussif areas reveal a predominantly southward flow direction (Bibonne 2014 ). This southeast directed paleoflow supports the emergence of an uplifted area northwest of the Tebaga outcrops since the Capitanian (late middle Permian). This interpretation is corroborated by the well-documented unconformities observed at the surface and in the subsurface, particularly in the TB-1 and MA-1 wells (Fig. 29), where Jurassic and Upper Cretaceous strata unconformably above the Permian succession. This uplifted area, corresponding to the Matmata Paleo-high, interpreted in this study as a major source terrain subjected to substantial erosion, likely acting as a sediment feeder region that experienced significant denudation since the Late Permian-Triassic (Fig. 29). The mechanisms driniving the pronounced facies and thickness variations between the shallow southern shelf and the rapidly subsiding northern foredeep basin, as well as the evolving geometry of the Permian basin in southern Tunisia, are currently being explored through intergrated well and seismic data (Dixon et al., Khachira et al., ongoing works). The vertical regressive trend is consistent with the progressive retreat of the Permian Sea to the east, leaving Tunisia during the late Permian period. This retreat is thought to have resulted from the interplay between the major late Permian glaciation (Rosa and Isbell 2020 ), in combination with the Variscan orogeny, which separated the Palaeozoic Gondwana cycle from the overlying Tethyan cycle in Tunisia (Boote et al. 1998 ; Guiraud et al. 2005 ; Galeazzi et al. 2010 ). Our analysis of the outcrop and subsurface data reveals a consistent shallowing-upward trend throughout the Permian succession. This trend reflecting the broader second-order middle Permian regression (Haq and Schutter 2008 ) (Fig. 30) is comparable to the Permian succession of west Texas, which also displays a regressive trend and a clear shift in the sedimentation regime from middle Permian carbonate shelf margin deposits (Capitan Reef Fm) and its lateral inner shelf deposits to evaporites/red beds. This large-scale regression led to a widespread emergence of marine shelves throughout Pangea and, consequently, the demise of many carbonate platforms (Ross and Ross 1995 ). Ross and Ross ( 1987 ) stated that the sea level dropped gradually from the late Early Permian and reached its lowest point (more than − 50 m below present level) for the entire Palaeozoic just before or at the middle-late Permian boundary. Ichnological aspect The trace fossil assemblage recorded in the Tebaga outcrops of Tunisia represents the archetypal Cruziana ichnofacies, with some indications of the proximal (DNBBZ Unit) and distal (MO Unit) variants. A brief review of the well-documented Cruziana ichnofacies in the Permian deposits in Gondwana and beyond (Table 3) shows that the diversity of the ichnogenera within this ichnofacies is highest (17 ichnogenera) in the Tunisian deposits. The composition of ichnotaxa varies from place to place and from formation to formation. Nevertheless, one-third to half of the ichnogenera are recurrent. Besides being very common, facies-crossing ichnogenera, such as Planolites or Palaeophycus , Psammichnites , Protovirgularia , Parataenidium , Thalassinoides , and Taenidium , appear to be more characteristic components of the Permian Cruziana ichnofacies. To some extent, similar trace fossil assemblages occur in the Carboniferous (e.g., Baucon et al. 2008; Alonso-Muruaga et al. 2013 ; Muszer 2020 ). Conclusions The novelty of this work lies in the integration of multiple approaches, which have enabled a better understanding of the internal architecture of the middle-Late Permian sedimentary succession of southern Tunisia and facilated the discussion of the main controlling factors of their depositional environments. The carbonate facies (CF1 to CF7) that dominate the Permian succession are representative of depositional settings ranging from ramp to rimmed carbonate platforms. The sponge-algal patch-reefs (CF1) embedded with fossiliferous shales, formed in an outer shelf/ramp setting (c.a 50 m depth). In contrast, the massive bioherms formed by encrusting algae with minor contributions from calcisponges and corals (CF2), which form prominent cliff exposures (BC1 and BC2), are representative of shelf margin contexts. The well-bedded limestones (CF3 and CF4) made of fusulinids, brachiopods, gastropods ( Bellerophon ), oncoliths, and bioclasts were deposited across inner to middle shelf settings. Facies CF5 and CF6 developed in coastal marine environments. The siliciclastic intervals, mainly identified within the DNBBZ, MO, and LCH units, comprise nine distinct facies (SF1 to SF9) deposited in offshore, shoreface, foreshore, and tide-dominated estuary settings. These intervals yielded a variety of well-preserved trace fossils, comprising 17 ichnotaxa belonging to the Cruziana ichnofacies. The trace fossil Cruziana is reported here for the first time from the Tebaga outcrops, particularly within LCHU sandstones, where the only Tunisian trilobite specimen has been collected. However, the overlying UCHU siliciclastic facies (SF10-SF14) reflect a significant regressive shift, transitioning from marginal marine to fully continental fluvial environments. The vertical transition between ramp and rimmed carbonate platform configurations could result from the changes in the carbonate sedimentation rate, primarily controlled by sea level changes, available accommodation space, and climatic conditions that strongly influenced faunal associations. Tectonic subsidence also played a major role in shaping the basin architecture, with maximum facies and thickness variations occurring north of the carbonate platform margin along the E-W trending Tebaga fault. The subsiding depocentre (TB-1 well) recording at least 4000 m of sedimentary fill is interpreted in this study as a foredeep basin. Within this setting, breccias and conglomerates composed of shallow-marine carbonate clasts derived from the adjacent platform occur as redeposited gravity flows. The latest Permian records the complete continentalisation in Tunisia, which is thought to be caused by the interplay between the major late Permian glaciation and the Variscan orogeny. In southern Tunisia, this coincides with the development of the Matmata-Mednine paleaohigh, which most likely acted as a local sediment source for the latest Permian-Early to Middle Triassic continental fluvial-deltaic settings. Declarations Acknowledgments The results presented in this paper are part of Ali Khachira's ongoing PhD thesis, being carried out within the research laboratory LR18ES07 (Sedimentary Basins and Petroleum Geology) at the Faculty of Sciences (FST), Tunis El Manar University (UTM). The authors would like to express their gratitude to the Tunisian Ministry of Higher Education and Scientific Research for financial support. The contribution of A.U. was supported by a grant from the Faculty of Geography and Geology under the Strategic Programme Excellence Initiative at Jagiellonian University.We are grateful to the Editor-in-Chief, Wolfgang Kiessling, and to Jean-Yves Reynaud and Francisco J. Rodríguez-Tovar for their invaluable and helpful comments and constructive reviews, which significantly improved the original manuscript. Special thanks are extended to my collegue Rami Sliti for his great help in the last moment of the preparation of the paper. We thank Mr Jihed Dridi for granting access to the Geological Patrimony Museum of ONM, which enabled consultation of the Tunisian trilobite holotype. Our thanks are also extended to Mr Sami Riahi, Mr Kamel Boukhalfa, Mr Moncef Saidi, and Mrs. Rahma Znazen for their support and Rabii for his help. 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Middle shelf to shelf margin BC1 and BC2 A Figures 11f-i, 13a-c CF3 Well bedded, grey packstone to grainstone limestones rich in Bellerophon gastropods, fusulinids, brachiopods, conodonts and algae, interbedded with fossiliferous green shales. Middle shelf BLU A Figures 12a, b, 13d CF4 CF4.1 Well bedded, grey to brown limestones, decimetric to metric, pack-grainstone, rich in fusulinids, algae and bioclastic debris and rare oolites. Inner to middle shelf All units (except UCHU) Figures 12c, d, 13e, f CF4.2 Yellow massive to thin bedded (50 cm) wackstone limestone with oncoliths. In Halq Jmel area, this facies is composed of spherical shape oncoid (over 3 cm in diameter) known as “ Ottonosia ” grains sensu Termier et al. ( 1977 ). Figures 12h, i, 13g CF4.3 Grey to brown, yellow metric (up to 1m) to decametric bioclastic limestone (packstone) with parallel to low angle cross-stratifications. In microfacies, the matrix is mainly composed of rich-skeletal brown sediments. Figures 12 e-g, 13h CF5 Grey to yellow small (1 m to 1.2 m thick) isolated sponge-algal patch reefs. CF6 is rich in sponge and locally with phylloid alga, especially in the Es Souinia area. Coastal marine DNBBZU, LCHU Figure 11 j, k CF6 Yellow massive dolomite, rich in crinoids, lamellibranches, oncoliths and algae debris. Algae patch reefs interfere with CF6. Symmetrical ripple marks could be locally observed. Inner shelf DNBBZU Figure 12j CF7 Conglomerate/breccia facies composed of a mixture of angular to sub-rounded elements, poorly sorted debris derived from reef bodies and sandstone small blocs (up to cobble size). - Top BC1 A Figure 8c Table 1 (continued) Siliciclastic Facies and associated trace fossils Facies Description: color, texture, and sedimentary structures Trace fossils Depositional environment Occurrence (Units) Age Photos SF1 Tempestite sandstones with trace fossils interbedded with fossiliferous shales, bioclastic limestones and patch reefs. Archaeonassa , ?Nereites Planolites , Protovirgularia Psammichnites , Taenidium Lower offshore MOU Middle Permian A Figure 18c, d SF2 Green shale with thin bedded bioturbated siltstones with parallel lamination. - Upper offshore DNBBZU A Figure 15g, h SF3 Heterolithic facies made up of green silty shale interbedded with fine-grained rippled sandstones with tempestite beds with HCS/SCS and Seismite structures. Archaeonassa, Palaeophycus Parataenidium Siphonichnus Offshore transition DNBBZU Figure 15a-f SF4 Structureless to laminated fine-grained sandstones with planar stratification and HCS. ?Diplocraterion Parataenidium Lower shoreface DNBBZU A Figure 16g, h SF5 30 to 150 cm thick very fine to medium and poorly to well sorted tabular sandstones organized in coarsening-upward sequences. Planar, low angle bedding, and symmetrical ripple marks characterize SF5. ?Ancorichnus , Cruziana Thalassinoides , Halopoa ?Helminthopsis Palaeophycus Parataenidium Psammichnites Planolites, Siphonichnus Upper-middle shoreface DNBBZU, LCHU A A Figures 16a-f, 17g, h, 19a-d SF6 Ferruginous, medium to coarse-grained, moderate to well indurated sandstones, up to 9 m thick. Moderate to well-sorted grained, reverse graded, locally bioturbated and with mud drapes. Sedimentary structures: plan and through cross-stratifications, ripple marks, HCS structures, and flaser bedding. Parataenidium Planolites ?Thalassinoides Upper shoreface to foreshore DNBBZU, LCHU Figures 17, 19e SF7 Ferruginous medium to coarse-grained lenticular sandstones with low angle cross bedding and soft-sediment deformation structures. Normal grading organization with irregular and erosive bases marked by lags, coarse particles. Planolites Phycodes Parataenidium Protovirgularia ?Gyrophyllites Tidal channel DNBBZU, BC1, 2, LCHU A Figure 22a, b SF8 Coarsening, thickening-upward white to yellow fine to medium grained and moderately to well-sorted sandstones. Sedimentary structures: Flat, trough and low angle bedding and reactivation surfaces. In the upper part, horizontal lamination and ripple marks are present. - Tidal sand bar LCHU A Figure 20c SF9 Red silty-shale interbedded with thick/ thin (10 cm to 2 m) lenticular sandstones. - Mixed mud-sand flat LCHU Figure 20a, d, e SF10 Red silty shale interbedded with both thick and thin lenticular sandstones, silt and thin yellow dolomite intercalations. - Shale of flood plain UCHU Late Permian A Figure 21d SF11 Grey thin bedded, horizontally laminated siltstone beds (< 20cm). - Silt of flood plain Figure 21d SF12 Thick bedded, fine to medium grained normal grading lenticular sandstones (up to 8 m) with shale clast at the base, plan and through cross stratifications, convolute structures and flute casts. Planolites Non-amalgamated fluvial channels Figure 21e, f SF13 Red to white thin lenticular fine to medium grained, well sorted sandstone beds (20–70 cm) with small, climbing ripples and root traces. Planolites Crevasse splay, sheet sands Figure 21g, h SF14 Massive to locally consolidate nodular and coarse bioturbated red sandstone beds (30–120 cm) with root traces. - Flood plain Figure 21i Table 2 Trace fossils from the Permian of southern Tunisia Ichnotaxon, occurrence Description Remarks Figure ? Ancorichnus isp. Upper surface of a fine- to medium-grained sandstone bed, facies SF5, Dar DNBBZ Unit. Horizontal, winding, meniscate burrow with a distinct moat on both sides of its course. The meniscate part is 5–6 mm wide, and the moat is up to 3 mm wide. The moat probably resulted from the weathering of a less resistant material that surrounded the meniscate part, which can be interpreted as a mantle, forming an integral part of the trace. This is a diagnostic feature of Ancorichnus Heinberg, 1974 , a locomotion and feeding burrow primarily known from Mesozoic shelf deposits (Keighley and Pickerill 1994 ). A Figure 23a Archaeonassa isp. DNBBZU and MOU. A Horizontal, winding, wide, and shallow, V-shaped (Fig. 14b) or U-shaped (Fig. 14c) gutter bounded by discontinuous, narrow levees. The gutter is 10–12 mm wide in the V-shaped forms, and 9–25 mm wide in the U-shaped forms. Archaeonassa Fenton and Fenton, 1937 , is a grazing trail mainly produced by gastropods (Fenton and Fenton 1937 ; Buckman 1994 ; Stanley and Feldmann 1998 ) or arthropods (Yochelson and Fedonkin 1997). Figure 23b, c Cruziana isp. Top of a sandstone bed in SF5 of DNBBZU. Single, short segment of horizontal bilobate burrow, 60–65 mm wide, with oblique, regular ribs converging in the midline at an angle of 90°–100° Cruzian a ďOrbigny, 1842 is a locomotion and feeding burrow primarily produced by trilobites in the Paleozoic and by some other arthropods in younger deposits (e.g., Seilacher 1970 , 2007 ; Zonneveld et al. 2002 ). Paleozoic Cruziana occurs mostly in shoreface and offshore siliciclastic deposits (e.g., Seilacher 1985 ). Figure 23d ? Diplocraterion isp. DNBBZU. Pairs of circular knobs on the bedding plain, 6–10 mm in diameter and 10–14 mm apart, connected by a bridge-like bar. This morphology suggests a vertical U-shaped burrow with spreiten, typical of Diplocraterion Torell, 1870 , which is a domichnion of suspension feeders (e.g., Fürsich 1974 ). Its type ichnospecies, D. parallelum Torell, 1870 , is common in very shallow marine Paleozoic and Mesozoic deposits (e.g., Fürsich 1981 ; Bromley and Hanken 1991 ; Jensen 1997 ; Bromley and Uchman 2003 ; Stachacz 2016 ). Figure 23e ? Gyrophyllites isp. A single sandstone slab in BC2. Two epichnial, neighbouring, shallow depressions, lobate in outline, rimmed by a collar. The depressions are 50–55 mm wide. The collar is 3 mm wide. The morphology suggests a rosette trace fossil of the Gyrophyllites group. Gyrophyllites Glocker, 1841 , is a fodinichnion (e.g., Fürsich and Kennedy1975; Fu 1991 ) of a polychaete or echiuran worm (Strzeboński and Uchman 2015 ). Figure 23f Halopoa isp. LCHU Hypichnial, gently curved or straight cylindrical burrow, 5–7 mm, rarely up to 10 mm wide, covered with irregular, discontinuous, longitudinal wrinkles. Halopoa Torell, 1870 , which is a locomotion and feeding burrow known from shallow-marine Paleozoic and deep-sea Mesozoic and Cenozoic deposits (Uchman 1998 ). A Figure 24a ? Helminthopsis isp. DNBBZU. Hypichnial, unornamented ridges, 10–12 mm wide, running subparallel, 24–40 mm apart. The extent of the ridges is unknown due to the incompleteness of the slab bearing them, but the curvature of the ridges suggests Helminthopsis Wetzel and Bromley, 1996 , a repichnion likely produced by polychaetes or priapulids (Fillion and Pickerill 1990 ) in various, mostly marine environments since the Cambrian (Crimes 1987 ). Figure 24b ? Nereites isp. On the top of a fine-grained sandstone bed in the isolated escarpment of the OA Unit. A short fragment of a horizontal, winding, tape-like structure that is 20–22 mm wide. It shows a low median ridge, which is 3 mm wide, and oblique, dense lateral lobes. The levees are interpreted as reworked zones bounding faecal strings (cf. Uchman 1995 ). Nereites MacLeay, 1839 , is a pascichnion (Mángano et al. 2000 ), but is also considered a fodinichnion (Knaust 2017 ). Nereites is a typical deep-sea ichnogenus, although it may also occur on slopes (Callow et al., 2013 ; Demircan and Uchman 2016 ), shelves (Knaust 2017 ), and exceptionally in sandy estuarine deposits and tidal flats (Martin and Rindsberg 2007 ; Neto de Carvalho and Baucon 2010 ). Figure 24c Palaeophycus isp. DNBBZU. A horizontal, straight to gently curved, cylindrical burrow, 10–15 mm wide, showing a distinct lining. Palaeophycus Hall, 1847 is an open locomotion and feeding burrow produced by several deposit-feeding or predaceous organisms in many environments (e.g., Pemberton and Frey 1982 ). Figure 24d Parataenidium isp. The top of a fine-grained sandstone bed (facies SF6, DNBBZU) A horizontal winding structure that is 6–16 mm wide. Its basal part is semicylindrical and lined. The upper part shows regular knobs, which protrude up from the basal part. They are inclined in the same direction along the course of the trace. The centres of the knobs are 8–15 mm apart. Boyd and McIlroy ( 2018 ) excluded P. moniliformis (Tate 1859 ) from Parataenidium Buckman, 2001 , and reassigned it to the newly introduced ichnogenus Neoeione . However, it appears that the differences between P. mullaghmorensis Buckman, 2001 , the type ichnospecies of Parataenidium , and P. moniliformis are insufficient to justify their separation at the ichnogenus level (Riahi and Uchman 2022 ). Parataenidium is a pascichnion attributed to an unknown vermiform organism (Buckman 2001 ; Boyd and McIlroy 2018 ). In the studied Permian deposits, it was identified as Arenicolites solignaci Mathieu, 1949 (also illustrated by Khessibi 1985 ), but Arenicolites Salter, 1857 is a U-shaped burrow (e.g., Hanken et al. 2016 ), and the assignment of this trace fossil was incorrect. Nevertheless, the ichnospecies name remains available. However, this issue warrants further study. Figures 23b, 24e, f Phycodes isp. BC2. Horizontal or subhorizontal cylindrical burrows, 10–12 mm wide and diverging from a common stem. Seilacher ( 2007 ) restricted Phycodes to tightly spaced bundles. Phycodes Richter, 1850 , is considered a feeding structure of unknown organisms. In the Paleozoic, it is primarily found in shallow marine sediments (Osgood 1970 ; Fillion and Pickerill 1990 ; Han and Pickerill 1994 ; Seilacher 2000 ). A Figure 25a Planolites isp. MOU and BC2. Horizontal, straight or winding, simple, cylindrical, unlined burrow. It shows diverse size and sinuosity, e.g., some nearly straight burrows are 8 mm wide, and some winding burrows are 4–5 mm wide. Planolites Nicholson, 1873 , is a locomotion-and-feeding, actively filled trace (pascichnion) probably produced by several different organisms occurring in a wide range of environments (e.g., Pemberton and Frey 1982 ; Fillion and Pickerill 1990 ; Keighley and Pickerill 1995 , and references therein). Figure 25a, b Protovirgularia isp. MOU and BC2. A hypichnial, horizontal, curved structure, 10–15 mm wide, showing a median string, which is 2 mm wide, and oblique, lateral ribs, which are 4–6 mm apart (2 or 3 ribs/cm). The ribs are elevated along the median string and slope towards the structure margins. Protovirgularia McCoy, 1850, is a molluscan (mostly bivalve) locomotion trace in which the chevron ridges are imprints of the cleft foot (Seilacher and Seilacher, 1994 ). The ichnospecies of Protovirgularia are highly variable and occur in various marine environments at different depths (Uchman 1998 ; Mángano et al. 2002 ). It is likely that the newly identified trace fossil Tabagacolites lautieri , distinguished by Mathieu ( 1949 ) from the studied Permian deposits and also illustrated by Khessibi ( 1985 ), represents the same trace fossil. Figure 25c, d Psammichnites isp. MOU and LCHU. A horizontal, winding, three-lobate structure showing three basic morphotypes: (1) a smooth furrow, 10–15 mm wide, with a 1–2 mm wide median ridge; (2) a furrow with chevron dense menisci in the median part (five menisci per 1 cm); or (3) a ridge, 10–20 mm wide, with a 1–2 mm wide median crest. Psammichnites Torell, 1870 , is a locomotion and feeding burrow known from the Paleozoic shallow-marine deposits (Mángano et al. 2022 ). Figures 25e, f Siphonichnus isp. Mainly in facies SF4 in the lower strata of DNBBZU. A horizontal subcircular section of a vertical cylindrical burrow, which is 20–25 mm wide, and shows a thick wall or a mantle, which is 4–5 mm wide. The mantle surrounds a central core. Siphonichnus Stanistreet et al., 1980 , is a dwelling trace of suspension-feeding bivalves (Stanistreet et al. 1980 ; Gingras et al. 2008 ; Dashtgard 2011 ) or a pascichnion of bivalves such as tellinids (Knaust 2015 ). It is commonly found in shallow-marine and marginal-marine deposits (Pollard 1988 ), often associated with salinity fluctuations and freshwater influx (Knaust 2015 ). It is infrequently reported from deep-sea deposits (Krobicki et al. 2006 ). A A Figure 26a Taenidium isp. Upper bedding plane of tempestite sandstone beds in in MOU. Horizontal, subcylindrical (?), winding, meniscate burrow, which is 6–7 mm wide. There are eight menisci per cm. At the termination, there is an oval, sand-filled body of the corresponding width. Taenidium Heer, 1877 is interpreted as a locomotion and deposit-feeding trace produced by marine vermiform organisms from shallow-to-deep-sea environments (Gevers et al. 1971 ; Keighley and Pickerill 1994 ; Smith et al. 2008 ; Smith and Hasiotis 2008 ; Jackson et al. 2016 ) from the Ediacaran to the recent (e.g., Crimes 1992 ; Jenkins 1995 ; Uchman 1998 ; Jackson et al. 2016 ). Figure 26b ? Thalassinoides isp. Sandstone beds, facies SF6 of facies SF6 of LCHU Horizontal, endichnial, branched burrow, 10–20 mm wide, in which fragments are visible on a parting surface due to weathering. The branches are Y-shaped. Thalassinoides Ehrenberg, 1944 , is a semi-permanent domichnion-fodinichnion produced primarily by scavenging and deposit-feeding crustaceans (Frey et al. 1978 , 1984 ; Schlirf 2000 ; Neto de Carvalho et al. 2007 ; Yanin and Baraboshkin 2013 ). However, cerianthid sea anemones, trilobites, or enteropneust acorn worms have also been suggested as potential producers of some Paleozoic Thalassinoides (Myrow 1995 ; Ekdale and Bromley 2003 ). It is possible that its trace makers fed on microbes growing within the burrows (Bromley 1996 ; Ekdale and Bromley 2003 ). Thalassinoides occurs in deposits of various, presumably shallow marine environments (Frey et al. 1984 ; Pemberton et al. 2001 ). Figure 26c Table 3 Examples of the Cruziana ichnofacies in the lower–middle Permian deposits, mostly from Gondwana. * – interpretation of the ichnofacies in this paper. In bold – ichnogenera which occur in southern Tunisia and in other section Location, formation; age; publication Facies Trace fossils Ichnofacies; no igen./no igen. found in S Tunisia Pebbley Beach Fm, Sydney Basin, Australia; Lower Permian (Sakmarian–Artinskian); Bann et al. ( 2004 ) Thoroughly bioturbated siltstone: siltstone and silty mudstone with few if any preserved sedimentary structures; rare thin (< 1 cm), sharp-based, very fine- to fine-grained sandstone beds. Phycosiphon , Planolites , Rosselia socialis, R. rotates , Taenidium , Zoophycos, Chondrites, Teichichnus , Palaeophycus tubularis, P. heberti, Helminthopsis, Asterosoma , Diplocraterion habichi, Skolithos , fugichnia distal Cruziana , some Skolithos ichnofacies elements in storms sand beds; 12/4 Thoroughly bioturbated sandy siltstone and sandy siltstone with rare but upwardly increasing numbers of discrete, thin (0.5–2 cm), very fine- to fine-grained sandstone beds. Rare synaeresis cracks, are rare, dispersed outsized clasts Rosselia socialis, Zoophycos, Phycosiphon , Planolites , Palaeophycus tubularis, P. heberti, Teichichnus, Rhizocorallium irregulare , Diplocraterion habichi , Taenidium , Rosselia rotatus, Skolithos, Bergaueria , fugichnia archetypal Cruziana , Skolithos ichnofacies in tempestites; 11/4 Sparsely to moderately bioturbated interbedded bioturbated sandy siltstone and fine-grained laminated sandstone; dark mudstone beds. Rosselia socialis, R. rotatus, Teichichnus , Palaeophycus tubularis, P. heberti, Phycosiphon , Planolites , Chondrites, Zoophycos, Rhizocorallium irregulare , Diplocraterion habichi, D. parallelum , Taenidium , Conichnus , Helminthopsis , Skolithos, Cylindrichnus , Psammichnites , Macaronichnus , fugichnia archetypal Cruziana , ichnofacies, Skolithos in sandstone beds (mixed Skolithos - Cruziana ichnofacies); 16/6 Thoroughly bioturbated muddy sandstones; some beds laminated Rosselia socialis, Phycosiphon , Planolites , Diplocraterion habichi, Rhizocorallium irregulare, Teichichnus, Macaronichnus , Palaeophycus tubularis, P. heberti , Taenidium , ? Zoophycos , Skolithos , fugichnia, Psammichnites , Chondrites proximal Cruziana; 13/5 Aheimer Fm, Gulf of Suez, Egypt; Lower Permian; El Refaiy et al. (2023) Rippled and HCS laminated sandstones with shale intercalations Planolites , Palaeophycus , Zoophycos , Skolithos , Thalassinoides , Helminthopsis proximal Cruziana; 6/3 Heterolithic cross bedded sandstones and mudstones, fossiliferous dolomitic sandstones, siltstones, and sandy dolomites, HCS laminated sandstones and siltstones Planolites , Palaeophycus , Zoophycos , Skolithos , Thalassinoides , Helminthopsis , Cruziana , Rusophycus , Phycodes , Rhizocorallium, Gordia, Circulichnis , Protovirgularia , Schaubcylindrichnus archetypal Cruziana; 14/7 Twin Bores, section, Mungadan Sandstone Fm, Carnarvon Basin, W Australia; Middle Permian: Guadalupian; Feng et al. ( 2021 ) Intensely bioturbated or cross-stratified sandstones, or planar laminated siltstones Chondrites , Cruziana , Curvolithus , Palaeophycus , Paleodictyon , Parataenidium , Phycodes , Planolites , Psammichnites , Rosselia, Rusophycus, Skolithos , Taenidium , Thalassinoides , Zoophycos Cruziana; 15/8 Teresina Fm, Rio Grande do Sul State,S Brazi; Upper Permian; Lima and Netto ( 2012 ) Mudstones, fine-grained heterolithic deposits, sandstone with climbing ripple lamination, sandstone with trough cross-stratification, and sandstone with HCS and SCS lamination Bergaueria, Cochlichnus cf. anguineus , Cruziana problematica , cf. Diplocraterion , Diplopodichnus biformis , Helminthopsis , Lockeia siliquaria, Multina arcuata, Oldhamia , Palaeophycus striatus, P. tubularis, Phymatoderma burkei , Planolites beverleyensis, P. montanus, Teichichnus , Thalassinoides Cruziana; 14/6 Broughton Fm, Sydney Basin, SE Australia; Middle Permian (uppermost Wordian–lower Capitanian; Luo et al. ( 2017 ) Fine to medium-grained sandstone alternated with siltstone Macaronichnus, Palaeophycus , Psammichnites , Protovirgularia , Rosselia, Teichichnus Cruziana*; 6/2 Kapp Starostin Fm, central Spitsbergen; Svalbard; Permian: Artinskian–?Changhsingian; Uchman et al. ( 2016 ) chert/cherty shale and spiculites with rare intercalations of glauconitic sandstone, limestones in the lower part Arenicolites, Chondrites , cf. Cylindrichnus , Helminthopsis , Macaronichnus segregatis , Nereites missouriensis , Palaeophycus , cf. Phycosiphon incertum , Planolites , Teichichnus , Thalassinoides , Zoophycos Cruziana; 12/5 Tebaga of Medenine, S Tunisia; middle–upper Permian; this paper Sandstones, shales, marls between carbonate buildups ? Ancorichnus, Archaeonassa, Cruziana , ? Diplocraterion , ? Gyrophyllites, Halopoa , ? Helminthopsis , ? Nereites, Palaeophycus, Parataenidium, Phycodes, Planolites, Protovirgularia, Psammichnites, Siphonichnus, Taenidium , ? Thalassinoides Cruziana , with transition to its proximal or distal variants*; 17/17 Cite Share Download PDF Status: Published Journal Publication published 27 Jun, 2025 Read the published version in Facies → Version 1 posted Reviewers agreed at journal 22 Apr, 2025 Reviewers invited by journal 22 Apr, 2025 Editor assigned by journal 18 Apr, 2025 First submitted to journal 17 Apr, 2025 Editorial decision: Minor Revision 23 Jan, 2025 You are reading this latest preprint version Research Square lets you share your work early, gain feedback from the community, and start making changes to your manuscript prior to peer review in a journal. As a division of Research Square Company, we’re committed to making research communication faster, fairer, and more useful. We do this by developing innovative software and high quality services for the global research community. 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Also discoverable on Platform About Our Team In Review Editorial Policies Advisory Board Help Center Resources Author Services Accessibility API Access RSS feed Manage Cookie Preferences © Research Square 2026 | ISSN 2693-5015 (online) Privacy Policy Terms of Service Do Not Sell My Personal Information {"props":{"pageProps":{"initialData":{"identity":"rs-5706272","acceptedTermsAndConditions":true,"allowDirectSubmit":false,"archivedVersions":[],"articleType":"Research Article","associatedPublications":[],"authors":[{"id":446274522,"identity":"9e856ce3-754b-47d5-9319-d330047fded9","order_by":0,"name":"Ali Khachira","email":"","orcid":"","institution":"University of Tunis El Manar: Universite de Tunis El Manar","correspondingAuthor":false,"prefix":"","firstName":"Ali","middleName":"","lastName":"Khachira","suffix":""},{"id":446274523,"identity":"ad86bd39-744f-4b7f-9d28-72a389382cf9","order_by":1,"name":"Mohamed Soussi","email":"data:image/png;base64,iVBORw0KGgoAAAANSUhEUgAAAZAAAAAyAQMAAABI0h/eAAAABlBMVEX///8AAABVwtN+AAAACXBIWXMAAA7EAAAOxAGVKw4bAAAA90lEQVRIiWNgGAWjYFACHhDBDOUY2PCTrCVNsoENSB9gYJAgUgvDYcJadNt7D366UWHNIN/eY/zxR8F5Cfn5DWzSH3MY6sxxaDE7cy5ZOudMOoPBmTNm0jwGtyUMjjGwSRzcxiBh2YBDy40cA+nctsMMBhI5ZswMBrfrDNigWgwO4NRi/Dv332EG+Rk5QIcZnJOQbyOsxUw6t+EwAwPQOgkegwMSDMcIaQF6wTrnWDqPwZljZUC/JAP9kthscXabhOQGXFqO9xjfzqmxlpNvb9788ccfOwn55sMHb1Rus+HHZQsM8CCxGRsY8MbkKBgFo2AUjAKCAACckFXlzKn/iQAAAABJRU5ErkJggg==","orcid":"https://orcid.org/0000-0001-7819-2231","institution":"Tunis El Manar University: Universite de Tunis El Manar","correspondingAuthor":true,"prefix":"","firstName":"Mohamed","middleName":"","lastName":"Soussi","suffix":""},{"id":446274524,"identity":"07c67e44-0cf7-41a6-b29d-2a5856e7f1d8","order_by":2,"name":"Alfred Uchman","email":"","orcid":"","institution":"Jagiellonian University: Uniwersytet Jagiellonski w Krakowie","correspondingAuthor":false,"prefix":"","firstName":"Alfred","middleName":"","lastName":"Uchman","suffix":""}],"badges":[],"createdAt":"2024-12-24 12:42:00","currentVersionCode":1,"declarations":"","doi":"10.21203/rs.3.rs-5706272/v1","doiUrl":"https://doi.org/10.21203/rs.3.rs-5706272/v1","draftVersion":[],"editorialEvents":[{"content":"https://doi.org/10.1007/s10347-025-00704-6","type":"published","date":"2025-06-27T15:57:43+00:00"}],"editorialNote":"","failedWorkflow":false,"files":[{"id":81189844,"identity":"cd423f90-48a9-45df-b132-3ad1fa2a97db","added_by":"auto","created_at":"2025-04-23 09:06:22","extension":"jpg","order_by":1,"title":"Figure 1","display":"","copyAsset":false,"role":"figure","size":3802355,"visible":true,"origin":"","legend":"\u003cp\u003eLocation and stratigraphy of the Permian deposits in southern Tunisia. \u003cstrong\u003ea\u003c/strong\u003e Global middle to late Permian Paleogeography (after \u003ca href=\"https://www.researchgate.net/profile/Christopher-Scotese?_sg%5B0%5D=mrNJDBpqqBV8fzNWf__bxulwrYKmHQLQo_EraMKcqldgI9la_TQuq4ekFQQjvTx3LUS0br4.D-v3XNpOQZlsyN2nqojGoXPW1Mzo8BNltqWufyHwXz95ZQN6WAA7-8ymcS07aeiabNmHqcMX6eIQGH7PMhvzIQ\u0026amp;_sg%5B1%5D=lrkESnfy6qxqDcLDWFPJ-VuddQ-GqYVv4xVBjbzD0QYDQiVNfwJJeEqJbMYaVGHP1gAjY-0.jw0X-BUI8EiEiW50ogfG8vBJCN_mCiAMmwIhJSE8i_Iplg6K-vT_WVqm0hWUJbPpz8JO33dLMjz2pwZeRoTrqw\u0026amp;_tp=eyJjb250ZXh0Ijp7ImZpcnN0UGFnZSI6InB1YmxpY2F0aW9uIiwicGFnZSI6InB1YmxpY2F0aW9uIiwicG9zaXRpb24iOiJwYWdlSGVhZGVyIn19\"\u003eScotese\u003c/a\u003e 2014) with location of the study area. \u003cstrong\u003eb\u003c/strong\u003e Google Earth image of southern Tunisia with highlights of the main structural domains, simplified geology of the region, and the location of the Permian outcrops of Tebaga of Medenine and petroleum wells crossing the Permian sequence. \u003cstrong\u003ec \u003c/strong\u003ePortion of the 1/100 000 geological map of Matmata with the location of the studied synthetic lithostratigraphic cross-section (after Zouari et al. 1987). \u003cstrong\u003ed \u003c/strong\u003eClassical lithostratigraphic subdivision of Tebaga successions (slightly modified from Vachard and Razgallah 1993)\u003c/p\u003e","description":"","filename":"Fig1.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/5a79a9332c46cf00304a9fd0.jpg"},{"id":81189825,"identity":"4c5171ba-e178-4eed-8fd1-f98a022c0f33","added_by":"auto","created_at":"2025-04-23 09:06:22","extension":"jpg","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":3935971,"visible":true,"origin":"","legend":"\u003cp\u003eLithofacies map of the Tebaga outcrops showing distribution of the Permian siliciclastic-carbonate rocks with indication of areas rich in trace fossils. The amount of siliciclastic deposits greatly decreases from west to east, probably in relation to the deepening of the depositional environment towards this direction, where siliciclastic influx is minor\u003c/p\u003e","description":"","filename":"Fig2.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/e58b12b24dd3cf05ef12edba.jpg"},{"id":81191076,"identity":"28eeab92-380c-47b2-aaa1-7ec554414357","added_by":"auto","created_at":"2025-04-23 09:14:21","extension":"jpg","order_by":3,"title":"Figure 3","display":"","copyAsset":false,"role":"figure","size":3374025,"visible":true,"origin":"","legend":"\u003cp\u003eE–W correlation of lithostratigraphic units of the Permian succession between three lithostratigraphic cross-sections, showing lateral facies changes and thickness variations\u003c/p\u003e","description":"","filename":"Fig3.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/5b2c19db368996082240c6d2.jpg"},{"id":81189818,"identity":"999c969f-c111-46cb-b886-c73692e25ff0","added_by":"auto","created_at":"2025-04-23 09:06:21","extension":"jpg","order_by":4,"title":"Figure 4","display":"","copyAsset":false,"role":"figure","size":4607714,"visible":true,"origin":"","legend":"\u003cp\u003eGeology of the Permian in the Google Earth images and panoramic views. \u003cstrong\u003ea\u003c/strong\u003e Google Earth image of the western part of Tebaga outcrops (Dar Njana- Halq Jmel) with location of the lithostratigraphic cross-section (1). \u003cstrong\u003eb \u003c/strong\u003eWestward panoramic view along the Dar Njana area. Horizontal Albian rocks rest with marked angularity upon the gently dipping (SE) Permian strata of the DNBBZU. Cliffs in the foreground are the Cenomanian and Turonian of Kef En Nsoura. \u003cstrong\u003ec\u003c/strong\u003ePanoramic view showing the upper part of the Tebaga succession in the Halq Jmel area. Herein, it appears the famous angular unconformity between the SE inclined Permian strata of the LCHU and the sub-horizontal Albian rocks\u003c/p\u003e","description":"","filename":"Fig4.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/dfa9d1d33388c47f964b355f.jpg"},{"id":81189826,"identity":"c0c38425-e780-48c3-b2d3-f22e548a4ead","added_by":"auto","created_at":"2025-04-23 09:06:22","extension":"jpg","order_by":5,"title":"Figure 5","display":"","copyAsset":false,"role":"figure","size":4954140,"visible":true,"origin":"","legend":"\u003cp\u003eGeology of the Permian in the Google Earth images and panoramic views.\u003cstrong\u003e a\u003c/strong\u003e Google Earth image of the central part of Tebaga outcrops (BBZ-MO) with the location of the lithostratigraphic cross-section (2). \u003cstrong\u003eb\u003c/strong\u003e Panoramic view of the DNBBZU and BC1 in the central part of J. Tebaga, Sh: Shale, C: Carbonate, S: Sandstone, Tz: Transitional zone, BC1: Biohermal Complex1. \u003cstrong\u003ec\u003c/strong\u003eDetail of b. Herein, the upper part of the mixed siliciclastic (yellow)/carbonate (blue) of the DNBBZU is represented by a fossiliferous shale interval interbedded with cross-bedded sandstones (Tz) just below the BC1. The latter exhibits a complex internal architecture represented by the interference with bioherms (B), well-bedded carbonate and lenticular sandstone bodies (lsb). \u003cstrong\u003ed \u003c/strong\u003eView eastward, from the top of the BC1, of the MOU and the BC2 (Denguir area).\u003cstrong\u003e e \u003c/strong\u003eView southward of the MOU, mainly composed of repetitive sequences made of shale at the base and patch reefs (PR) at the top\u003c/p\u003e","description":"","filename":"Fig5.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/4a203d2e2205e9bb3d7afc9a.jpg"},{"id":81189810,"identity":"d38073c3-bd50-4a44-831c-ff8b76adc592","added_by":"auto","created_at":"2025-04-23 09:06:20","extension":"jpg","order_by":6,"title":"Figure 6","display":"","copyAsset":false,"role":"figure","size":4151979,"visible":true,"origin":"","legend":"\u003cp\u003eGeology of the Permian in the Google Earth images and panoramic views. \u003cstrong\u003ea \u003c/strong\u003eGoogle Earth image of the eastern part of Tebaga outcrops with the location of the lithostratigraphic cross-section (3). \u003cstrong\u003eb\u003c/strong\u003e Panoramic view of the dominant-shaly MOU topped by the BC2. \u003cstrong\u003ec \u003c/strong\u003ePanoramic view of the BLU and LCHU at the Es Souinia area\u003c/p\u003e","description":"","filename":"Fig6.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/b5ad04c407067e0c67403a55.jpg"},{"id":81189820,"identity":"ad074a86-cbe4-4914-b61a-d25027537fbe","added_by":"auto","created_at":"2025-04-23 09:06:21","extension":"jpg","order_by":7,"title":"Figure 7","display":"","copyAsset":false,"role":"figure","size":5440818,"visible":true,"origin":"","legend":"\u003cp\u003eGeology of the Permian in panoramic views.\u003cstrong\u003e a\u003c/strong\u003e Panoramic view of the strata lying above the BC2 at Es Souinia-Saikha area with highlighting the position of the trilobite identified by Memmi and David (1965). The succession is made up of the BLU, followed by a package composed of an alternance of marine sandstones, fossiliferous shale, and bioclastic limestones with the intercalation of small patch reefs. \u003cstrong\u003eb\u003c/strong\u003e The holotype of the only Tunisian trilobite \u003cem\u003ePseudophillipsia azzouzi \u003c/em\u003eTermier and Termier, 1974, photographed at the geological museum of the Tunisian Geological Survey (ONM). \u003cstrong\u003ec\u003c/strong\u003eReconstitution and line drawing of \u003cem\u003ePseudophillipsia azzouzi \u003c/em\u003efrom Termier and Termier (1974). \u003cstrong\u003ed\u003c/strong\u003e Close-up view of a ferruginous sandstone bed of shoreface to foreshore setting of an isolated outcrop (lateral equivalent of the LCHU). In this interval, where the \u003cem\u003eCruziana\u003c/em\u003e trace has been found. \u003cstrong\u003ee\u003c/strong\u003e \u003cem\u003eCruziana\u003c/em\u003e isp., LCHU near the Halq Jmel area\u003c/p\u003e","description":"","filename":"Fig7.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/0dccbdc15a184ed0d830aa45.jpg"},{"id":81189851,"identity":"15f1ac85-c94c-49bb-aafa-450902e30e52","added_by":"auto","created_at":"2025-04-23 09:06:22","extension":"jpg","order_by":8,"title":"Figure 8","display":"","copyAsset":false,"role":"figure","size":3674546,"visible":true,"origin":"","legend":"\u003cp\u003eKey sedimentary features in outcrops of the Permian in southern Tunisia.\u003cstrong\u003e a\u003c/strong\u003e and \u003cstrong\u003eb\u003c/strong\u003e Filled karsts and red laminated dolomite at the top of the BC2. \u003cstrong\u003ec \u003c/strong\u003eA conglomeratic body (CF7 facies) surmounting the BC1 at Dar Njana area. \u003cstrong\u003ed \u003c/strong\u003eWell bedded ferruginous sandstone (SF6) directly overlying the biohermal carbonate (CF2) of the BC1\u003c/p\u003e","description":"","filename":"Fig8.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/e07c7bc2992d83859b9998fc.jpg"},{"id":81189813,"identity":"361b7e9c-46ba-4959-8abf-8b7f941a69a7","added_by":"auto","created_at":"2025-04-23 09:06:21","extension":"jpg","order_by":9,"title":"Figure 9","display":"","copyAsset":false,"role":"figure","size":1220938,"visible":true,"origin":"","legend":"\u003cp\u003eSynthetic\u003cstrong\u003e \u003c/strong\u003elithostratigraphic chart of the middle to upper Permian units in Jebel Tebaga.\u003c/p\u003e","description":"","filename":"Fig9.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/c97863a75d708050d9123c8b.jpg"},{"id":81191077,"identity":"10e2ee7f-af28-4507-8efd-5e27133ebaff","added_by":"auto","created_at":"2025-04-23 09:14:21","extension":"jpg","order_by":10,"title":"Figure 10","display":"","copyAsset":false,"role":"figure","size":1850518,"visible":true,"origin":"","legend":"\u003cp\u003eLithostratigraphic log with vertical distribution of trace fossils across Permian units of the Tebaga outcrops. See Fig. 1c for the log’s location\u003c/p\u003e","description":"","filename":"Fig10.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/74df2bdbd9218b2855ce13fe.jpg"},{"id":81189836,"identity":"94e7a796-2bd4-4213-83a7-dc2066f37a3d","added_by":"auto","created_at":"2025-04-23 09:06:22","extension":"jpg","order_by":11,"title":"Figure 11","display":"","copyAsset":false,"role":"figure","size":6287402,"visible":true,"origin":"","legend":"\u003cp\u003eField photographs of biohermal carbonate facies. \u003cstrong\u003ea\u003c/strong\u003e Small patch reef (CF1) exposed near the Merbah El Oussif road connecting Dkhilet Toujane and the Halq Jmel village. \u003cstrong\u003eb \u003c/strong\u003eand \u003cstrong\u003ec \u003c/strong\u003eSponge-dominated patch-reefs of CF1. \u003cstrong\u003ed\u003c/strong\u003e Boundstone texture of CF1 mainly composed of sponge (Sp) and encrusting algae (Al). \u003cstrong\u003ee\u003c/strong\u003e Close-up view of CF1 with coral. \u003cstrong\u003ef\u003c/strong\u003e Panoramic view of the CB1, composed herein by three biohermal events vertically related by shales. \u003cstrong\u003eg\u003c/strong\u003e Close-up view of CF2 facies with coral and a radial fibrous early marine cement. \u003cstrong\u003eh\u003c/strong\u003e and \u003cstrong\u003ei\u003c/strong\u003eField photographs of the facies CF2 mainly made up of the encrusting algae \u003cem\u003eArchaeolithoporella\u003c/em\u003e \u003cem\u003ehidensis\u003c/em\u003e and subordinatley by sponges. Al: Algae, Sp: Sponge, IS: Internal sediment, V: Void.\u003cstrong\u003e j\u003c/strong\u003e View east toward a patch reef (CF5) and associated strata of the LCHU exposed in the Es Souinia area. \u003cstrong\u003ek\u003c/strong\u003e Close-up view of CF5 facies with phylloid algae\u003c/p\u003e","description":"","filename":"Fig11.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/b9eafedb918ce4837fcf4df9.jpg"},{"id":81189848,"identity":"26997da5-c6d4-4aa3-a784-9acabea0adb9","added_by":"auto","created_at":"2025-04-23 09:06:22","extension":"jpg","order_by":12,"title":"Figure 12","display":"","copyAsset":false,"role":"figure","size":7455957,"visible":true,"origin":"","legend":"\u003cp\u003eField photographs of non-biohermal carbonate facies. \u003cstrong\u003ea\u003c/strong\u003e Close-up view of a yellow limestone bed of CF3 showing abundant brachiopods and \u003cem\u003eBellerophon \u003c/em\u003egastropods (BLU) at the Halq Jmel area. \u003cstrong\u003eb\u003c/strong\u003e Close-up view of CF3 showing abundance in fusulinids with \u003cem\u003eBellerophon \u003c/em\u003egastropods. \u003cstrong\u003ec\u003c/strong\u003e Fusulinid/bioclastic calcarenite metric bed (CF4.1), BLU, Halq Jmel area. \u003cstrong\u003ed\u003c/strong\u003e Close-up view of CF4.1 facies showing fusulinid accumulations with a shell fragment. \u003cstrong\u003ee\u003c/strong\u003eCoarsening-upward bioclastic limestone bed of CF4.3 facies. \u003cstrong\u003ef\u003c/strong\u003e and \u003cstrong\u003eg \u003c/strong\u003eField photographs of CF4.3 facies rich in nautiloid cephalopods at Es Souinia area. \u003cstrong\u003eh \u003c/strong\u003eand \u003cstrong\u003ei\u003c/strong\u003e Field photographs of CF5.2 facies in DNBBZU and LCHU, respectively. \u003cstrong\u003ei\u003c/strong\u003e Close-up view of CF6 facies containing algae (Al) and crinoid fragments (Cr)\u003c/p\u003e","description":"","filename":"Fig12.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/ad8168bff06802c760b4f48a.jpg"},{"id":81189816,"identity":"69a99489-ff98-4f55-91e4-8ec49c0117ff","added_by":"auto","created_at":"2025-04-23 09:06:21","extension":"jpg","order_by":13,"title":"Figure 13","display":"","copyAsset":false,"role":"figure","size":6454793,"visible":true,"origin":"","legend":"\u003cp\u003eMicrofacies of some carbonate facies encountered in Tebaga outcrops. \u003cstrong\u003ea\u003c/strong\u003e, \u003cstrong\u003eb\u003c/strong\u003e, and \u003cstrong\u003ec\u003c/strong\u003e Photomicrographs of CF2 facies mainly composed of \u003cem\u003eArchaeolithoporella\u003c/em\u003e \u003cem\u003ehidensis\u003c/em\u003e (Ar) and \u003cem\u003eTubiphytes\u003c/em\u003e \u003cem\u003eobscurus \u003c/em\u003e(T). In a and b, the matrix consists of fine brown sediments highly enriched in quartz particles (Qz). \u003cstrong\u003ed\u003c/strong\u003e Poorly sorted fusulinids/bioclastic grainstone of CF3 facies. Herein, most of the skeletal grains have micrite envelopes, and the inter-granular space is occupied by calcite cement. Bellerophon Limestone Unit, Halq Jmel area. Al (Algae), G (Gastropods), F (Fusulinids), M (Miliolids), L (Lamellibranches). \u003cstrong\u003ee\u003c/strong\u003e Fusulinids wackstone to packstone within a micritic/pelloidal matrix of CF4.1 facies. Bellerophon Limestone Unit, Halq Jmel area. \u003cstrong\u003ef\u003c/strong\u003e Algal (A) grainstone passing to fusulinids (F) grainstone in CF4.1 facies, DNBBZ Unit. \u003cstrong\u003eg \u003c/strong\u003eOncoid packstones composed of algally coated-grains (grains up to 2 cm in diameter) in a peloidal/bioclastic matrix, CF4.2 facies. \u003cstrong\u003eh\u003c/strong\u003e Bioclastic packstone of CF4.3 facies. Herein, skeletal elements encompass bryozoans (Br) and lamellibranch fragments (L)\u003c/p\u003e","description":"","filename":"Fig13.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/993d25c1f61d56c85edc91b6.jpg"},{"id":81192736,"identity":"d636129f-9f4b-45e9-b1c1-cad70bb0ce50","added_by":"auto","created_at":"2025-04-23 09:30:21","extension":"jpg","order_by":14,"title":"Figure 14","display":"","copyAsset":false,"role":"figure","size":4549392,"visible":true,"origin":"","legend":"\u003cp\u003ePanoramic view of the lower part of the DNBBZ Unit in the Dar Njana area. It consists of set of coarsening and shallowing-upward carbonate-siliciclastic sequences. Pink stars indicate the position of trace fossils, mainly burrowing the upper surfaces of sandstone beds\u003c/p\u003e","description":"","filename":"Fig14.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/dcb6e3a0bb4582dfb9c12dd3.jpg"},{"id":81189812,"identity":"1f9f3bee-091b-46c3-9077-12630f9d0744","added_by":"auto","created_at":"2025-04-23 09:06:21","extension":"jpg","order_by":15,"title":"Figure 15","display":"","copyAsset":false,"role":"figure","size":7891214,"visible":true,"origin":"","legend":"\u003cp\u003eField photographs of siliciclastic facies within DNBBZ Unit in the Dar Njana area. \u003cstrong\u003ea \u003c/strong\u003eTempestite lenticular sand body in hummock (H) and swale (S) configuration, resting on a bioturbated muddy interval and overlain by silty/very bioturbated sandstones with planar lamination (PL). This sand body is interpreted as storm deposits typical of an offshore transition setting (SF3) in the basal strata of the DNBBZ Unit. \u003cstrong\u003eb\u003c/strong\u003e Close-up view of a. Herein, the tempestite body has an irregular base and shows internal cross-stratification. \u003cstrong\u003ec\u003c/strong\u003e Heterolithic deposits of SF3 deposits materialized by interbedding of rippled sandstones with trace fossils, seismite structures (SS), and yellow to green silty shales. \u003cstrong\u003ed\u003c/strong\u003e Zoom in on a seismite structure within SF3.\u003cstrong\u003e e \u003c/strong\u003eCoarsening-upward cycles consisting of sandstones with low-angle (LAS) to planar stratification (PS), rippled surface (RS) alternating with thin shale intercalations (SF3 facies). \u003cstrong\u003ef \u003c/strong\u003ePhotograph of the upper surface of a rippled sandstone with trace fossils.\u003cstrong\u003e g\u003c/strong\u003ePhotograph of the transition from upper offshore (green-yellow shale) to offshore transition settings. \u003cstrong\u003eh\u003c/strong\u003e Thin grey siltstone intercalations in the upper part of the dominated mudstone facies of SF2. Pencil and hammer for scale are 14 cm and 35 cm, respectively\u003c/p\u003e","description":"","filename":"Fig15.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/c1172f7d4afad7a65bbf5b0f.jpg"},{"id":81191093,"identity":"9fd27089-27f5-403f-87f9-c3b8de28ae41","added_by":"auto","created_at":"2025-04-23 09:14:23","extension":"jpg","order_by":16,"title":"Figure 16","display":"","copyAsset":false,"role":"figure","size":6818162,"visible":true,"origin":"","legend":"\u003cp\u003eField photographs of siliciclastic facies of Tebaga outcrops. \u003cstrong\u003ea \u003c/strong\u003eand\u003cstrong\u003e b \u003c/strong\u003eClose-up view of the upper surfaces of SF5 sandstones with large scale and well-preserved \u003cem\u003eParataenidium\u003c/em\u003e. \u003cstrong\u003ec \u003c/strong\u003eCoarsening and thickening-upward cycles of SF5 facies, sandstones are thin to medium bedded at the base, passing upward into massif ferruginous bodies. \u003cstrong\u003ed\u003c/strong\u003e HCS and SCS structures observed within SF5 facies. \u003cstrong\u003ee\u003c/strong\u003e Zoom in on HCS sandstone beds. \u003cstrong\u003ef\u003c/strong\u003e Fusulinid-rich limestones (CF4.1) bed intercalated in the dominantly siliciclastic deposits of SF5. \u003cstrong\u003eg \u003c/strong\u003eand \u003cstrong\u003eh\u003c/strong\u003e photographs of the massive well laminated sandstones with decametric HCS bedding of SF4 facies. F: fracture. Pencil and hammer for scale are 14 cm and 35 cm, respectively\u003c/p\u003e","description":"","filename":"Fig16.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/b1251bb1c262801acf3ce7d2.jpg"},{"id":81189829,"identity":"2628c22e-c570-4fb8-b1a9-056791b8e3df","added_by":"auto","created_at":"2025-04-23 09:06:22","extension":"jpg","order_by":17,"title":"Figure 17","display":"","copyAsset":false,"role":"figure","size":7655288,"visible":true,"origin":"","legend":"\u003cp\u003eField photographs of siliciclastic facies within the DNBBZ Unit in the Dar Njana area. \u003cstrong\u003ea\u003c/strong\u003e Wavy bedding structure in a sandstone bed of SF6 facies. \u003cstrong\u003eb \u003c/strong\u003eThin-bedded medium to coarse-grained hematized sandstones with ripple marks. \u003cstrong\u003ec \u003c/strong\u003eand\u003cstrong\u003e d \u003c/strong\u003eHighly oxidized upper surface of SF6 facies with wood fragments.\u003cstrong\u003e e \u003c/strong\u003eA bioclastic thin limestone bed intercalating with a dominantly siliciclastic sequence (SF5 facies). f White fine to medium-grained sandstones (SF5) with trough cross-stratification.\u003cstrong\u003eg\u003c/strong\u003e The vertical stacking pattern of the lower strata of the DNBBZ Unit. Herein, thin-bedded white sandstone beds (with \u003cem\u003eParataenidium\u003c/em\u003e) are surmounted by a decametric ferruginous sandstone bed interpreted as the maximum regression of a coarsening-upward cycle. Upward, the next cycle starts with a fossiliferous shaly interval and ends with a massive metric sandstone bed with wood fragments on its top. \u003cstrong\u003eh\u003c/strong\u003e Details of g\u003c/p\u003e","description":"","filename":"Fig17.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/ca692df8c1a83358088c2cf5.jpg"},{"id":81191085,"identity":"82a041b1-a8d5-4c28-af2e-fb33c4f55414","added_by":"auto","created_at":"2025-04-23 09:14:22","extension":"jpg","order_by":18,"title":"Figure 18","display":"","copyAsset":false,"role":"figure","size":2810403,"visible":true,"origin":"","legend":"\u003cp\u003eSedimentary features of siliciclastic facies within the MOU and the BC2. \u003cstrong\u003ea\u003c/strong\u003e Sandstone interval (SF7) intercalated within the BC2. \u003cstrong\u003eb \u003c/strong\u003eClose-up view of the sandstone interval in a, showing sigmoidal cross bedding indicating tidal activities. \u003cstrong\u003ec\u003c/strong\u003e Brown to grey thin bedded bioturbated fine-grained tempestite sandstones with trace fossil intercalated within a calcareous shale mass (SF1) of the MOU. \u003cstrong\u003ed\u003c/strong\u003e Close-up view of a storm sandstone bed\u003c/p\u003e","description":"","filename":"Fig18.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/21b7eaa0a384cb67287f19d8.jpg"},{"id":81189831,"identity":"554a924f-ac1e-4913-8b9a-a512194381e0","added_by":"auto","created_at":"2025-04-23 09:06:22","extension":"jpg","order_by":19,"title":"Figure 19","display":"","copyAsset":false,"role":"figure","size":6607323,"visible":true,"origin":"","legend":"\u003cp\u003eSedimentological characteristics of the siliciclastic facies of LCH Unit. \u003cstrong\u003ea\u003c/strong\u003e Mixed siliciclastic/carbonate aspect of the strata of LCHU in Halq Jmel area, herein a regressive cross-stratified sandstone bed (SF5) is surmounted by a transgressive yellow to green highly fossiliferous limestones (CF3). \u003cstrong\u003eb\u003c/strong\u003e Close-up of the erosive contact (transgressive surface (TS)) between CF3 and SF5 facies. The latter is marked by low-angle cross-stratifications (LACS) and flame structures (FS). \u003cstrong\u003ec\u003c/strong\u003e. Alternation of small ripples (SR) and parallel stratifications (PS) in facies SF6. \u003cstrong\u003ed\u003c/strong\u003eSymmetrical ripple marks at the top of a fine-grained shoreface to foreshore sandstones (LCH Unit). \u003cstrong\u003ee\u003c/strong\u003e Flute casts in SF6 facies. \u003cstrong\u003ef\u003c/strong\u003e Convolute bedding (CB) and flame structures (FS) in SF6 in the Es Souinia area, LCHU. \u003cstrong\u003eg\u003c/strong\u003eFine to medium-grained shoreface to foreshore sandstones (SF6) with mud drapes where finer sediments typically accumulate during periods of low hydrodynamic regime. Oncoliths limestones (CF4.2) occurring at the top announce the beginning of the subsequent cycle. CS: Cross-Stratifications, RS: Rippled surface. \u003cstrong\u003eh \u003c/strong\u003eFlaser bedding in SF6 facies (LCHU). Pencil and hammer for scale are 14 cm and 35 cm, respectively\u003c/p\u003e","description":"","filename":"Fig19.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/cffe10add49660b5546017eb.jpg"},{"id":81189822,"identity":"9f497f1f-4e3e-47ce-84a4-409978b04485","added_by":"auto","created_at":"2025-04-23 09:06:21","extension":"jpg","order_by":20,"title":"Figure 20","display":"","copyAsset":false,"role":"figure","size":6346914,"visible":true,"origin":"","legend":"\u003cp\u003eCharacterisation of the siliciclastic facies at the top of LCH Unit.\u003cstrong\u003e a\u003c/strong\u003e Panoramic view of the upper part of the Permian strata in the Halq Jmel area showing the transition from tidal/estuarine (LCH Unit) to continental (UCH Unit) contexts.\u003cstrong\u003e b\u003c/strong\u003e Tidal channel deposits (SF7) cut into the top of a fine-grained white sandstone bed of foreshore to shoreface setting (SF6) in the Halq Jmel area (LCHU). \u003cstrong\u003ec\u003c/strong\u003e Close-up view on SF8 facies showing thickening and coarsening-upward cross-bedded sandstones. \u003cstrong\u003ed \u003c/strong\u003eRed silty shales interbedded with tidal creeks, fine-grained sandstones with climbing ripples. \u003cstrong\u003ee\u003c/strong\u003e Detail of d\u003c/p\u003e","description":"","filename":"Fig20.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/46b8eb218244a91c6f451ad5.jpg"},{"id":81191094,"identity":"06962f4a-c50e-458e-b4da-a5be8da86f46","added_by":"auto","created_at":"2025-04-23 09:14:23","extension":"jpg","order_by":21,"title":"Figure 21","display":"","copyAsset":false,"role":"figure","size":7437109,"visible":true,"origin":"","legend":"\u003cp\u003eField photographs of lithological facies of the UCH Unit. \u003cstrong\u003ea \u003c/strong\u003eVertical stacking pattern of the fluvial strata of the UCH Unit. \u003cstrong\u003eb\u003c/strong\u003e Tetrapod footprints on the upper surface of a sandstone bed collected from the topmost Permian strata of the Tebaga outcrops by Newell et al. (1976), scale equal 9 cm.\u003cstrong\u003e c\u003c/strong\u003e Close-up view on two different kinds of tetrapod tracks (circles), after Contessi et al. (2017). \u003cstrong\u003ed\u003c/strong\u003eRed silty shales (SF10) interbedded with red thin-bedded siltstones (SF11). \u003cstrong\u003ee\u003c/strong\u003eMassive ferruginous sandstone body (SF12) with large-scale cross-bedding, shale clasts, and wood fragments at its base. \u003cstrong\u003ef\u003c/strong\u003e Shale clasts and wood debris at the base of the SF12 facies. \u003cstrong\u003eg \u003c/strong\u003eA sandstone bed of crevasse splay deposits (SF13) with climbing ripples. \u003cstrong\u003eh\u003c/strong\u003e A crevasse splays sandstone bed densely occupied by roots. \u003cstrong\u003ei\u003c/strong\u003e Massive palaeosol (SF14) with root trace, hammer for scale is 35 cm\u003c/p\u003e","description":"","filename":"Fig21.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/dc802997138f28142d4a9ddc.jpg"},{"id":81191084,"identity":"dbef3ee5-1c39-4754-b21d-957ecde826c5","added_by":"auto","created_at":"2025-04-23 09:14:22","extension":"jpg","order_by":22,"title":"Figure 22","display":"","copyAsset":false,"role":"figure","size":3521336,"visible":true,"origin":"","legend":"\u003cp\u003eInternal architecture of BC1 and BC2. \u003cstrong\u003ea, b, \u003c/strong\u003eand \u003cstrong\u003ec \u003c/strong\u003eRelationships between sand-bodies and the bioconstructed buildups.\u003cstrong\u003e \u003c/strong\u003eHS: Hematized sandstones, PR: Patch reef. \u003cstrong\u003ed\u003c/strong\u003e Proposed architecture of the BC1 and its evolution laterally and vertically. \u003cstrong\u003ee\u003c/strong\u003e Field photograph of the concomitance between bedded bioclastic limestones and biohermal bodies in the BC2, Es Souinia area. \u003cstrong\u003ee \u003c/strong\u003eProposed architecture of the BC2 and facies relationships\u003c/p\u003e","description":"","filename":"Fig22.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/8c3c21b72c71aa93f1d6789e.jpg"},{"id":81191809,"identity":"8f4ca24e-d0f8-45a8-ab5b-9fe01ad90e4b","added_by":"auto","created_at":"2025-04-23 09:22:22","extension":"jpg","order_by":23,"title":"Figure 23","display":"","copyAsset":false,"role":"figure","size":6068800,"visible":true,"origin":"","legend":"\u003cp\u003eField photographs of trace fossils. \u003cstrong\u003ea\u003c/strong\u003e ?\u003cem\u003eAncorichnus\u003c/em\u003e isp. developed on the upper bedding surface of SF4. \u003cstrong\u003eb\u003c/strong\u003e \u003cem\u003eArchaeonassa\u003c/em\u003eisp. co-occurring with \u003cem\u003eParataenidium\u003c/em\u003eisp. in a fine-grained sandstone sediment of offshore-transition setting (DNBBZ Unit). \u003cstrong\u003ec\u003c/strong\u003e \u003cem\u003eArchaeonassa\u003c/em\u003e isp. on the top of a sandy limestone bed within the MO Unit. \u003cstrong\u003ed\u003c/strong\u003e \u003cem\u003eCruziana\u003c/em\u003e isp. (DNBBZ Unit). \u003cstrong\u003ee \u003c/strong\u003e?\u003cem\u003eDiplocraterion\u003c/em\u003e isp. (DNBBZ Unit). \u003cstrong\u003ef \u003c/strong\u003e?\u003cem\u003eGyrophyllites\u003c/em\u003e isp. (BC2)\u003c/p\u003e","description":"","filename":"Fig23.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/0b97146e170f4d8cd1eae91f.jpg"},{"id":81189846,"identity":"b83b65ad-e6af-4055-8c08-10bd26593d59","added_by":"auto","created_at":"2025-04-23 09:06:22","extension":"jpg","order_by":24,"title":"Figure 24","display":"","copyAsset":false,"role":"figure","size":7986419,"visible":true,"origin":"","legend":"\u003cp\u003eField photographs of other trace fossils.\u003cstrong\u003e a \u003c/strong\u003eUpper surface of a sandstone bed densely\u003cstrong\u003e \u003c/strong\u003ecolonized by\u003cstrong\u003e \u003c/strong\u003e\u003cem\u003eHalopoa\u003c/em\u003e isp. (Lower Cheguimi Unit) \u003cstrong\u003eb \u003c/strong\u003e?\u003cem\u003eHelminthopsis\u003c/em\u003e isp. (DNBBZ Unit) \u003cstrong\u003ec\u003c/strong\u003e?\u003cem\u003eNereites\u003c/em\u003e isp. occurring on a fine-grained sandstone bed at the Oum El Afia isolated escarpment (OA Unit). \u003cstrong\u003ed\u003c/strong\u003e \u003cem\u003ePalaeophycus\u003c/em\u003e isp. (DNBBZ Unit) \u003cstrong\u003ee\u003c/strong\u003e, \u003cstrong\u003ef \u003c/strong\u003e\u003cem\u003eParataenidium\u003c/em\u003e isp. (DNBBZ Unit)\u003c/p\u003e","description":"","filename":"Fig24.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/4044f0c21a913b4739b1039b.jpg"},{"id":81191805,"identity":"95fa2255-01c2-4150-b329-c1f3d9468fd9","added_by":"auto","created_at":"2025-04-23 09:22:21","extension":"jpg","order_by":25,"title":"Figure 25","display":"","copyAsset":false,"role":"figure","size":7528033,"visible":true,"origin":"","legend":"\u003cp\u003eField photographs of more trace fossils. \u003cstrong\u003ea\u003c/strong\u003e \u003cem\u003ePhycodes\u003c/em\u003e isp. and \u003cem\u003ePlanolites\u003c/em\u003e isp. (BC2). \u003cstrong\u003eb\u003c/strong\u003e \u003cem\u003ePlanolites\u003c/em\u003eisp. (BC2). \u003cstrong\u003ec, d \u003c/strong\u003e\u003cem\u003eProtovirgularia\u003c/em\u003eisp. developed on the upper bedding surface of a tempestite sand body (MO Unit).\u003cstrong\u003e e\u003c/strong\u003e, \u003cstrong\u003ef\u003c/strong\u003e \u003cem\u003ePsammichnites\u003c/em\u003eisp. (MO, LCH units)\u003c/p\u003e","description":"","filename":"Fig25.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/6270bdd267822aa2125176fd.jpg"},{"id":81189853,"identity":"4760c794-071c-4a56-aacb-e13f5a45c037","added_by":"auto","created_at":"2025-04-23 09:06:23","extension":"jpg","order_by":26,"title":"Figure 26","display":"","copyAsset":false,"role":"figure","size":3431692,"visible":true,"origin":"","legend":"\u003cp\u003eField photographs of trace fossils. \u003cstrong\u003ea\u003c/strong\u003e \u003cem\u003eSiphonichnus\u003c/em\u003e isp. (Dar Njana-Baten Beni Zid Unit) \u003cstrong\u003eb\u003c/strong\u003e \u003cem\u003eTaenidium\u003c/em\u003e isp. (MO Unit). \u003cstrong\u003ec\u003c/strong\u003e ?\u003cem\u003eThalassinoides\u003c/em\u003e isp. (LCH Unit)\u003c/p\u003e","description":"","filename":"Fig26.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/ee089927feabde66eb2bf714.jpg"},{"id":81189815,"identity":"ddbe6cd4-3228-42f0-85db-059f6f123329","added_by":"auto","created_at":"2025-04-23 09:06:21","extension":"jpg","order_by":27,"title":"Figure 27","display":"","copyAsset":false,"role":"figure","size":2203289,"visible":true,"origin":"","legend":"\u003cp\u003eDepositional models of the main units of Tebaga outcrops. During deposition of the DNBBZ Unit, the environment was predominantly siliciclastic and fluctuated between offshore and coastal marine settings, while during deposition of the units BC1 and BC2, the sedimentation took place mainly in the middle shelf to shelf margin with reefs. Later, the coastal marine conditions (BLU, LCHU) prevailed and progressively evolved into the continental environment (UCHU) in relation to the global eustatic sea level fall\u003c/p\u003e","description":"","filename":"Fig27.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/9b06e9208b50d4769ce68cb8.jpg"},{"id":81189841,"identity":"83757247-7a9a-4322-8679-efa1789b3b33","added_by":"auto","created_at":"2025-04-23 09:06:22","extension":"jpg","order_by":28,"title":"Figure 28","display":"","copyAsset":false,"role":"figure","size":1914113,"visible":true,"origin":"","legend":"\u003cp\u003eDepositional models of siliciclastic (\u003cstrong\u003ea\u003c/strong\u003e) and carbonate facies (\u003cstrong\u003eb\u003c/strong\u003e) of Tebaga outcrops and the distribution of trace fossils. The latter belong to the \u003cem\u003eCruziana \u003c/em\u003eichnofacies, indicating a wide spectrum of depositional environments ranging from outer shelf to continental settings. During the carbonate platform development, maximum carbonate production favoured reef development in the shelf margin (b), while siliciclastic deposits formed a ramp system with minor carbonate intervals (a)\u003c/p\u003e","description":"","filename":"Fig28.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/70ac71e3baca8f6c10281504.jpg"},{"id":81191087,"identity":"aa201656-724c-4c1b-b309-ff208db5e7cc","added_by":"auto","created_at":"2025-04-23 09:14:22","extension":"jpg","order_by":29,"title":"Figure 29","display":"","copyAsset":false,"role":"figure","size":5198037,"visible":true,"origin":"","legend":"\u003cp\u003eNW-SE\u003cstrong\u003e \u003c/strong\u003esurface-subsurface correlation between the BMT-1 well (Jeffara Basin), Tebaga outcrops, and the TB-1 well, showing basin architecture and temporal-spatial evolution\u003c/p\u003e","description":"","filename":"Fig29.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/d707f5f2fde8000d9721639a.jpg"},{"id":81191808,"identity":"22196830-eca7-4248-95ce-554eeeea7ab6","added_by":"auto","created_at":"2025-04-23 09:22:22","extension":"jpg","order_by":30,"title":"Figure 30","display":"","copyAsset":false,"role":"figure","size":1348371,"visible":true,"origin":"","legend":"\u003cp\u003ePermian sedimentary evolution of Tunisia correlated with the global sea level curve by Haq and Schutter (2008)\u003c/p\u003e","description":"","filename":"Fig30.jpg","url":"https://assets-eu.researchsquare.com/files/rs-5706272/v1/91c449b983eb005eaa357a99.jpg"}],"financialInterests":"","formattedTitle":"New insights on the Permian mixed siliciclastic and carbonate deposits of southern Tunisia: Facies, ichnofacies and depositional environments","fulltext":[{"header":"Introduction and objectives","content":"\u003cp\u003eThe Permian was a period of significant tectonic, eustatic, and climatic changes as reflected in the sedimentary record of the Gondwana realm (Ross and Ross \u003cspan citationid=\"CR139\" class=\"CitationRef\"\u003e1987\u003c/span\u003e; Fielding et al. \u003cspan citationid=\"CR53\" class=\"CitationRef\"\u003e2006\u003c/span\u003e; Fielding et al. \u003cspan citationid=\"CR52\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Rygel et al. \u003cspan citationid=\"CR143\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Haq and Schutter \u003cspan citationid=\"CR79\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Gradstein et al. \u003cspan citationid=\"CR74\" class=\"CitationRef\"\u003e2012\u003c/span\u003e; Chen et al. \u003cspan citationid=\"CR28\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Scotese and Schettino \u003cspan citationid=\"CR149\" class=\"CitationRef\"\u003e2017\u003c/span\u003e; Henderson et al. \u003cspan citationid=\"CR82\" class=\"CitationRef\"\u003e2020\u003c/span\u003e). These changes record the transition from the Carboniferous-early Permian icehouse to the middle and late Permian greenhouse. The middle Permian (Guadalupian) greenhouse climate created optimal conditions for widespread reef development, particularly during the Wordian and Capitanian stages. This time interval represents the acme of Permian reef growth (Weidlich \u003cspan citationid=\"CR189\" class=\"CitationRef\"\u003e2002\u003c/span\u003e), as evidenced by the global proliferation of shallow marine carbonate platforms with associated reef systems.\u003c/p\u003e \u003cp\u003eGuadalupian reefs have been reported from both tropical and cool temperate zones, such as the Capitan Reef of Texas (Toomey and Babcock \u003cspan citationid=\"CR176\" class=\"CitationRef\"\u003e1983\u003c/span\u003e; Fagerstrom and Weidlich \u003cspan citationid=\"CR49\" class=\"CitationRef\"\u003e1999\u003c/span\u003e), Japan (Shen and Kawamura \u003cspan citationid=\"CR157\" class=\"CitationRef\"\u003e2001\u003c/span\u003e), Arabian Platform (Weidlich \u003cspan citationid=\"CR191\" class=\"CitationRef\"\u003e2007\u003c/span\u003e), Thailand (Dawson et al. \u003cspan citationid=\"CR36\" class=\"CitationRef\"\u003e1993\u003c/span\u003e), Slovenia (Fl\u0026uuml;gel et al. \u003cspan citationid=\"CR57\" class=\"CitationRef\"\u003e1984\u003c/span\u003e), and China (Liu et al. \u003cspan citationid=\"CR100\" class=\"CitationRef\"\u003e2016\u003c/span\u003e; Zhu et al. 2018; Tian et al. \u003cspan citationid=\"CR173\" class=\"CitationRef\"\u003e2024\u003c/span\u003e). Most of these reef systems have been interpreted as being deposited in a shelf-margin context.\u003c/p\u003e \u003cp\u003eThe demise of reef ecosystems and the progressive decline of carbonate production (including the disappearance of tropical biota and the collapse of the carbonate factory) occurred globally near the end of the Capitanian (ca. 260 Ma) across various parts of Pangea. This crisis coincided with a major eustatic sea-level fall (Haq and Schutter \u003cspan citationid=\"CR79\" class=\"CitationRef\"\u003e2008\u003c/span\u003e), global cooling and a decrease in seawater temperature (Isozaki et al. \u003cspan citationid=\"CR84\" class=\"CitationRef\"\u003e2011\u003c/span\u003e; Kani et al. \u003cspan citationid=\"CR89\" class=\"CitationRef\"\u003e2018\u003c/span\u003e) and glacial conditions in eastern Australia and Mongolia (Fielding et al. \u003cspan citationid=\"CR52\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Fujimoto et al. \u003cspan citationid=\"CR62\" class=\"CitationRef\"\u003e2012\u003c/span\u003e). During the late Permian, the prevalence of the greenhouse climate resulted in widespread aridity in northern Pangea, mainly characterized by the occurrence of playa and sabkha red beds, aeolianites, and evaporites (Schneider et al. \u003cspan citationid=\"CR150\" class=\"CitationRef\"\u003e2006\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eDuring the Permian, large parts of the African Gondwana lacked marine Permian deposits. Except for the extreme southern part of the Karoo Basin in the southern part of Africa (Smith et al. 1995; Johnson et al. \u003cspan citationid=\"CR88\" class=\"CitationRef\"\u003e1997\u003c/span\u003e; Catuneanu et al. \u003cspan citationid=\"CR25\" class=\"CitationRef\"\u003e2005\u003c/span\u003e), and in southern Tunisia (Tebaga outcrops) (Fig.\u0026nbsp;1a, b, c). In Tunisia, well-bedded middle Permian marine fossiliferous and biohermal carbonates grade upwards into continental late Permian red-beds facies (Fig.\u0026nbsp;1d) (Douvill\u0026eacute; et al. \u003cspan citationid=\"CR42\" class=\"CitationRef\"\u003e1933\u003c/span\u003e; Berkaloff \u003cspan citationid=\"CR8\" class=\"CitationRef\"\u003e1933\u003c/span\u003e; Mathieu \u003cspan citationid=\"CR109\" class=\"CitationRef\"\u003e1949\u003c/span\u003e; Baird \u003cspan citationid=\"CR4\" class=\"CitationRef\"\u003e1967\u003c/span\u003e; Skinner and Wilde \u003cspan citationid=\"CR159\" class=\"CitationRef\"\u003e1967\u003c/span\u003e; Newell et al. \u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e1976\u003c/span\u003e; Lethiers et al. \u003cspan citationid=\"CR98\" class=\"CitationRef\"\u003e1989\u003c/span\u003e; Razgallah et al. \u003cspan citationid=\"CR132\" class=\"CitationRef\"\u003e1989\u003c/span\u003e; Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e; Vachard and Razghallah 1993).\u003c/p\u003e \u003cp\u003eCyclic sedimentation, marked by alternating siliciclastic and carbonate strata, represents a defining characteristic of the Permian sequence in the Jebel Tebaga of Medenine (Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e). The siliciclastic deposits have not previously been the subject of a detailed investigation in terms of depositional environments when compared to carbonate deposits (Khessibi \u003cspan citationid=\"CR93\" class=\"CitationRef\"\u003e1985\u003c/span\u003e; Chaouachi \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e1988\u003c/span\u003e; Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e). In addition, their associated invertebrate fossils, reported from various stratigraphic levels (Termier and Termier \u003cspan citationid=\"CR169\" class=\"CitationRef\"\u003e1955\u003c/span\u003e, \u003cspan citationid=\"CR171\" class=\"CitationRef\"\u003e1977\u003c/span\u003e; Driggs \u003cspan citationid=\"CR43\" class=\"CitationRef\"\u003e1977\u003c/span\u003e; Termier et al. \u003cspan citationid=\"CR172\" class=\"CitationRef\"\u003e1977\u003c/span\u003e; Boyd and Newell \u003cspan citationid=\"CR14\" class=\"CitationRef\"\u003e1979\u003c/span\u003e; Senowbari-Daryan and Rigby \u003cspan citationid=\"CR156\" class=\"CitationRef\"\u003e1988\u003c/span\u003e; Angiolini et al. \u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Verna et al. \u003cspan citationid=\"CR186\" class=\"CitationRef\"\u003e2010\u003c/span\u003e; Ghazzay et al. 2015), are poorly documented and have never been thoroughly examined.\u003c/p\u003e \u003cp\u003eThis study provides a comprehensive analysis bringing together for the first time new sedimentological and ichnology data of the middle-to-upper Permian siliciclastic intervals and carbonates facies.\u003c/p\u003e \u003cp\u003eIt aims to:\u003c/p\u003e \u003cp\u003e(1) refine the stratigraphic framework of the Tunisian Permian pattern based on an updated detailed mapping of both carbonate and siliciclastic main units in the E-W orientated Jebel Tebaga of Medenine;\u003c/p\u003e \u003cp\u003e(2) characterize, based on lithology, sedimentary structures, faunal composition, the vertical and lateral facies, and thickness variations;\u003c/p\u003e \u003cp\u003e(3) provide a detailed assessment, for the first time, of trace fossils from the siliciclastic intervals with a special focus on the trace fossil \u003cem\u003eCruziana\u003c/em\u003e, believed to be related to the unique trilobite specimen discovered in the Jebel Tebaga of Medenine;\u003c/p\u003e \u003cp\u003e(4) interpret the depositional environment evolution over space and time, based on the combination of data collected from both carbonates and siliciclastic facies with their associated trace fossil assemblages;\u003c/p\u003e \u003cp\u003e(5) integrate the surface to subsurface data to reconstruct the sedimentary evolution in relation to the global tectonic setting and sea level changes within the context of the northern Gondwana margin.\u003c/p\u003e \u003cp\u003eFinally, a comparison of the southern Tunisia Permian sedimentary record with other age-equivalent strata from the USA and Arabia is attempted.\u003c/p\u003e"},{"header":"Materials and methods","content":"\u003cp\u003eLithofacies mapping by integrating field observations, Google Earth imagery, and aerial photographs has been undertaken in order to emphasize the stratigraphic relationships and the interplay between siliciclastic and carbonate deposits. Panoramic views and close-up photographs have been taken to highlight the complex internal architecture of biohermal complexes and the surface boundaries between the different lithological units, especially the siliciclastic packages containing trace fossils.\u003c/p\u003e \u003cp\u003eThe well-exposed and representative sections have been logged to evaluate both the vertical and lateral facies changes as well as the distribution of trace fossils. Three cross-sections (Dar Njana-Halq Jmel (1), Baten Beni Zid-Merbah El Oussif (2) and Es Souinia-Saikha (3) sections) synthetizing the vertical stacking pattern of the Permian succession of Tebaga outcrops were constructed (Fig.\u0026nbsp;3). Furthermore, a synthetic cross-section encompassing the main stratigraphic units and associated trace fossil assemblages has been produced (base: N33\u0026deg;25\u0026prime;11.24\u0026Prime;, E10\u0026deg;9\u0026prime;57.87\u0026Prime;; top: N33\u0026deg;24\u0026prime;3.23\u0026Prime;, E10\u0026deg;10\u0026prime;18.29\u0026Prime;).\u003c/p\u003e \u003cp\u003eFacies analysis of siliciclastic rocks was conducted based on Allen (\u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e1982\u003c/span\u003e), Scholle and Spearing (\u003cspan citationid=\"CR147\" class=\"CitationRef\"\u003e1982\u003c/span\u003e), Walker and James (\u003cspan citationid=\"CR188\" class=\"CitationRef\"\u003e1992\u003c/span\u003e), Dalrymple et al. (\u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e1992\u003c/span\u003e), Miall (\u003cspan citationid=\"CR114\" class=\"CitationRef\"\u003e1996\u003c/span\u003e), and Nichols (\u003cspan citationid=\"CR122\" class=\"CitationRef\"\u003e2007\u003c/span\u003e, \u003cspan citationid=\"CR123\" class=\"CitationRef\"\u003e2009\u003c/span\u003e) works. For the sedimentological interpretation of carbonate rocks, Dunham (\u003cspan citationid=\"CR44\" class=\"CitationRef\"\u003e1962\u003c/span\u003e), Tucker and Wright (1990), and Fl\u0026uuml;gel (\u003cspan citationid=\"CR56\" class=\"CitationRef\"\u003e2004\u003c/span\u003e) were employed.\u003c/p\u003e \u003cp\u003ePhysical sedimentary structures and trace fossils were photographically illustrated, and their vertical distribution was precisely documented. The sandstone bed-bearing tetrapod tracks, initially described by Newell et al. (\u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e1976\u003c/span\u003e) (33\u0026deg;24'3.46\"N; 10\u0026deg;10'15.53\"E), and the holotype of the trilobite \u003cem\u003ePseudophillipsia azzouzi\u003c/em\u003e Termier and Termier (\u003cspan citationid=\"CR170\" class=\"CitationRef\"\u003e1974\u003c/span\u003e) housed in the Tunisian Geological Survey (ONM) have been reexamined and photographed.\u003c/p\u003e \u003cdiv id=\"Sec3\" class=\"Section2\"\u003e \u003ch2\u003eGeographic and geological settings\u003c/h2\u003e \u003cp\u003ePalaeogeographically, Tebaga outcrops constitute the remnant of the westernmost extension of the Peri-gondwanan shelves of the tropical Tethyan embayment. During the Permian, Tunisia occupied a critical palaeogeographic position at northern margin of Gondwana, marking the western tip of the Tethyan seaway (Fig.\u0026nbsp;1a) (Scotese and Schettino \u003cspan citationid=\"CR149\" class=\"CitationRef\"\u003e2017\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eGeographically, the Permian outcrops are located in southern Tunisia, specifically in Jebel Tebaga of Medenine, situated near the Dkhilet Toujane village, approximately 25 km NW of Medenine, and 10 km SE of the Berber town of Toujane (Fig.\u0026nbsp;1b). They lie within the Dahar Plateau (Fig.\u0026nbsp;1c) and extend along a belt of E\u0026ndash;W trending hills (3 km wide and 13 km long), bounded by the E-W Tebaga Fault (Bouaziz et al. \u003cspan citationid=\"CR12\" class=\"CitationRef\"\u003e2002\u003c/span\u003e). The Permian strata of southern Tunisia form a monoclinal structure dipping southeastward (Fig.\u0026nbsp;1b, c). To the north of this monocline, the Permian rocks are unconformably overlain by the Jurassic (Callovian) deposits in the Es Souinia-Saikha area or by the Lower Cretaceous (Albian) Radhouane Member of the Zebbag Formation at Dar Njana-Halq Jmel area (Fig.\u0026nbsp;2).\u003c/p\u003e \u003cp\u003eThe buried Permian successions have been penetrated by more than thirty petroleum wells. In this study, only TB-1 and BMT-1 wells (Fig.\u0026nbsp;1b) have been utilised, as they offer the possibility to evaluate the vertical and lateral facies and thickness variations from north to south, thereby adding to the interpretation of depositional environments and palaeogeographic reconstructions.\u003c/p\u003e \u003c/div\u003e"},{"header":"Results","content":"\u003cdiv id=\"Sec5\" class=\"Section2\"\u003e \u003ch2\u003eUpdated surface lithostratigraphic framework\u003c/h2\u003e \u003cp\u003ePrevious works have extensively studied the stratigraphic framework of Tebaga outcrops (Mathieu \u003cspan citationid=\"CR109\" class=\"CitationRef\"\u003e1949\u003c/span\u003e; Newell et al. \u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e1976\u003c/span\u003e; Khessibi \u003cspan citationid=\"CR93\" class=\"CitationRef\"\u003e1985\u003c/span\u003e; Angiolini et al. \u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e2008\u003c/span\u003e; Ghazzay et al. 2015).\u003c/p\u003e \u003cp\u003eThe field lithofacies mapping carried out during this work (Fig.\u0026nbsp;2) serves to enhance and refine those achieved by Mathieu (\u003cspan citationid=\"CR109\" class=\"CitationRef\"\u003e1949\u003c/span\u003e), Newell et al. (\u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e1976\u003c/span\u003e), Zouari et al. (\u003cspan citationid=\"CR198\" class=\"CitationRef\"\u003e1987\u003c/span\u003e), and Toomey (\u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e). This has enabled the identification and better characterization of key surfaces (e.g., transgressive, exposure, and karstification surfaces) that delineate the lithostratigraphic units. Three stratigraphic cross-sections representing three domains of Tebaga outcrops have been logged to characterize and document the E-W lateral facies and thickness variations affecting the different Permian lithostratigraphic units (Fig.\u0026nbsp;3) outcropping in the Dar Njana-Halq Jmel (Fig.\u0026nbsp;4), Baten Beni Zid-Merbah El Oussif (Fig.\u0026nbsp;5), and Es Souinia-Saikha (Fig.\u0026nbsp;6) sectors. The updated Permian lithostratigraphic framework, which comprises, from the base to the top, the Tebaga and Cheguimi formations, clarifies not only the vertical stacking pattern but also the key surfaces marking the major changes in sedimentation.\u003c/p\u003e \u003c/div\u003e\n\u003ch3\u003eThe Tebaga Formation\u003c/h3\u003e\n\u003cp\u003e \u003cb\u003eOum El Afia Unit (OAU).\u003c/b\u003e This unit corresponds to r1 of Mathieu (\u003cspan citationid=\"CR109\" class=\"CitationRef\"\u003e1949\u003c/span\u003e), known as Oum El Afia isolated red shales outcrops, exposed along the road linking Dkhilet Toujane to the Berber town of Toujane (Fig.\u0026nbsp;1c). Its structural and stratigraphic relationships to the main Permian belt of Tebaga are still subject of controversy (Newell et al. \u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e1976\u003c/span\u003e). In this study, only the trace fossils identified within this unit, comprising red shales and fine to medium-grained sandstones, are described.\u003c/p\u003e \u003cp\u003e \u003cb\u003eDar Njana-Baten Beni Zid Unit (DNBBZU).\u003c/b\u003e This unit corresponds to r2 of Mathieu (\u003cspan citationid=\"CR109\" class=\"CitationRef\"\u003e1949\u003c/span\u003e). It outcrops both in Dar Njana (Fig.\u0026nbsp;4a, b) and in the Baten Beni Zid areas, where it underlies the first Biohermal Complex 1 (BC1) (Fig.\u0026nbsp;5a, b, c). This dominantly siliciclastic unit is composed of green to red shales alternating with white to iron-stained sandstones, well-bedded bioclastic/fusulinids limestones, and dolomites (Fig.\u0026nbsp;3).\u003c/p\u003e \u003cp\u003eIn the Dar Njana section, the DNBBZU is topped by a well-defined siliciclastic interval, grading upward into the BC1 or being unconformably overlain by the Albian-Turonian carbonates of the Zebbag Formation (Fig.\u0026nbsp;2). In the Baten Beni Zid area, the transition from the DNBBZU to the overlying BC1 is represented by fossiliferous shales (sponge-bearing) interlayered with fusulinid-rich limestones and cross-bedded sandstones (Figs.\u0026nbsp;2, 3, 4b, 5b, c). The revision of the fusulinid association, in addition to the investigation of associated smaller foraminifers, allowed Ghazzay et al. (2015) to assign an early to late Capitanian age to this unit.\u003c/p\u003e \u003cp\u003e \u003cb\u003eBiohermal Complex 1 (BC1).\u003c/b\u003e This unit consists of 60\u0026ndash;100 m-thick, massive biohermal carbonates mainly built of encrusting algae \u003cem\u003eArchaeolithoporella hidensis\u003c/em\u003e Endo, 1959, and \u003cem\u003eTubiphytes obscurus\u003c/em\u003e Maslov, 1956 (Newell et al. 1977; Chaouachi \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e1988\u003c/span\u003e). The bioherms interfere with shales, well-bedded bioclastic limestones, and locally cross-bedded iron-stained sandstones. The latter abut against the mounds, onlapping their flanks or completely covering them (Fig.\u0026nbsp;5b, c).\u003c/p\u003e \u003cp\u003eIn the western Dar Njana sector, lenticular sandstone bodies increase in both frequency and thickness (Figs.\u0026nbsp;2, 3) within the BC1. Herein, biohermal carbonates show partial to complete dolomitization and are unconformably overlain by Albian strata (Fig.\u0026nbsp;2). The BC1 is capped by conglomeratic facies in the Dar Njana area and by 2\u0026ndash;3 m-thick iron-stained sandstones of considerable lateral extent in Merbah El Oussif area (Figs.\u0026nbsp;2, 3). Here, Khessibi (\u003cspan citationid=\"CR93\" class=\"CitationRef\"\u003e1985\u003c/span\u003e) identified an emersion surface at the top of BC1 and desiccation cracks at the top of the siliciclastic beds. In Baten Beni Zid-Merbah El Oussif, this unit thins significantly, with an increase in clay content between the bioherm masses.\u003c/p\u003e \u003cp\u003e \u003cb\u003eMerbah El Oussif Unit (MOU).\u003c/b\u003e This unit (140\u0026ndash;280 m) occupies a broad area, separating BC 1 from the Biohermal Complex 2 (BC2). The MOU comprises stacked repetitive sequences (Fig.\u0026nbsp;5e) exhibiting a consistent vertical organization. The latter is made from base to top of fossiliferous olive-green to red shales alternating with fine-grained sandstone tempestites, sponge/algal patch reefs, and well-bedded bioclastic limestones. The unit shows notable lateral thickness variations and represents the most fossiliferous succession in the Tebaga outcrops (Fig.\u0026nbsp;3) (Newell et al. \u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e1976\u003c/span\u003e; Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e). Cephalopods are rarely encountered within this unit in the Merbah El Oussif locality but are particularly abundant in the Es Souinia-Saikha area (Fig.\u0026nbsp;6a, b).\u003c/p\u003e \u003cp\u003e \u003cem\u003eChusenella\u003c/em\u003e, \u003cem\u003eCodonofusiella\u003c/em\u003e, \u003cem\u003eDunbarula\u003c/em\u003e, \u003cem\u003eNeoschwagerina\u003c/em\u003e, \u003cem\u003eReichelina\u003c/em\u003e, and \u003cem\u003eYabeina\u003c/em\u003e fusulinids, found in the limestone beds, indicate a late Capitanian age for this unit (Ghazzay et al. 2015).\u003c/p\u003e \u003cp\u003e \u003cb\u003eBiohermal Complex 2 (BC2).\u003c/b\u003e This unit constitutes the second cliff of Jebel Tebaga and is exposed from the Es Souinia-Saikha to the Dar Njana-Halq Jmel (Figs.\u0026nbsp;2, 3, 4, 5, 6). It is composed of thick and vertically stacked massive biohermal dolomitic limestones laterally intercalated with shales, bedded bioclastic limestones, and a few lenticular iron-stained sandstones. These bioherms are primarily built by \u003cem\u003eArchaeolithoporella hidensis\u003c/em\u003e and \u003cem\u003eTubiphytes obscurus\u003c/em\u003e encrusting algae, with notable increases in sponge and phylloid algae (\u003cem\u003eIvanovia\u003c/em\u003e) content in the Es Souinia sector (Chaouachi \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e1988\u003c/span\u003e; Razgallah et al. \u003cspan citationid=\"CR132\" class=\"CitationRef\"\u003e1989\u003c/span\u003e). In the Denguir area (Figs.\u0026nbsp;1c, 2, 3), the uppermost part of this unit exhibits marked karstification, indicated by a distinct red dolomitic bed with algal lamination (Figs.\u0026nbsp;2, 3).\u003c/p\u003e \u003cp\u003e \u003cb\u003eBellerophon Limestone Unit (BLU).\u003c/b\u003e Mathieu (\u003cspan citationid=\"CR109\" class=\"CitationRef\"\u003e1949\u003c/span\u003e) described this unit in the western (Halq Jmel) (Fig.\u0026nbsp;4c) and eastern (Es Souinia) (Fig.\u0026nbsp;6c) ends of J. Tebaga. It consists of well-bedded fossiliferous limestones (with \u003cem\u003eBellerophon\u003c/em\u003e) interbedded with fossiliferous clay and small sponge patch reefs. Angiolini et al. (\u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e2008\u003c/span\u003e), based on the occurrence of fusulinids and conodonts (\u003cem\u003eSweetognathus iranicus hanzhongensis\u003c/em\u003e Wang, 1978), the occurrence of \u003cem\u003eChusenella rabatei\u003c/em\u003e Skinner and Wilde, \u003cspan citationid=\"CR159\" class=\"CitationRef\"\u003e1967\u003c/span\u003e, smaller foraminifera, and brachiopods, assigned this unit in the Capitanian.\u003c/p\u003e\n\u003ch3\u003eThe Cheguimi Formation\u003c/h3\u003e\n\u003cp\u003e \u003cb\u003eLower Cheguimi Unit (LCHU).\u003c/b\u003e This unit is dominantly composed of fossiliferous silty shales, bioclastic/oncolithic limestones, and small patch reefs at the base, grading upward into well-laminated to rippled sandstones, particularly rich in trace fossils. The LCH Unit is dated to the late Capitanian (Vachard and Razghallah 1993; Angiolini et al. \u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e2008\u003c/span\u003e). The Last Permian Carbonate Interval (LPCI) of Permian Tebaga succession is located at the top of this unit (bed 31, section B of Newell et al. \u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e1976\u003c/span\u003e) (Fig.\u0026nbsp;3). The LPCI yields the fusulinid \u003cem\u003eDunbarula mathieui\u003c/em\u003e, marking the late Capitanian stage (Ghazzay et al. 2015). Further east, in the Es Souinia area, this unit includes multiple patch reefs interfingering with bioclastic limestones and relatively few coastal marine sandstone beds (Figs.\u0026nbsp;2, 3, 6c, 7a). In the carbonates of this locality, a unique Tunisian trilobite specimen was discovered (Memmi and David \u003cspan citationid=\"CR112\" class=\"CitationRef\"\u003e1965\u003c/span\u003e) (Fig.\u0026nbsp;7b).\u003c/p\u003e \u003cp\u003e \u003cb\u003eUpper Cheguimi Unit (UCHU).\u003c/b\u003e It represents the topmost unit of Tebaga outcrops and is only exposed at the western end of the outcrop belt (Halq Jmel) (Figs.\u0026nbsp;3, 4c). It is composed of red shales and ferruginous sandstones with scarce trace fossils. Newell et al. (\u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e1976\u003c/span\u003e) documented in this unit the first reptilian footprints that were re-examined by Contessi et al. (\u003cspan citationid=\"CR29\" class=\"CitationRef\"\u003e2017\u003c/span\u003e), who assigned them to the late Capitanian to Wuchiapingian age.\u003c/p\u003e \u003cp\u003eAbove this unit lies a large, flat area offering the opportunity to observe continental red beds with sandstone at Argoub El Oussif hill. These facies, entirely mapped within the Matmata geological sheet as the Triassic (Zouari et al. \u003cspan citationid=\"CR198\" class=\"CitationRef\"\u003e1987\u003c/span\u003e), are still considered part of the Cheguimi sandstones (Capitanian\u0026ndash;Lopingian) according to Bibonne (\u003cspan citationid=\"CR9\" class=\"CitationRef\"\u003e2014\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eIn summary, according to the biostratigraphic chart by Angiolini et al. (\u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e2008\u003c/span\u003e), the mixed siliciclastic-carbonate of the Tebaga Formation, comprising the DNBBZU, BC1, MOU, BC2, and the BLU, spans approximately 7 Myr (268\u0026ndash;ca. 261 Ma, zones from \u003cem\u003eA. rowinsae\u003c/em\u003e to \u003cem\u003eD. Mathieu\u003c/em\u003e). Most of the units are estimated to last\u0026thinsp;~\u0026thinsp;1.5 Myr each (Fig.\u0026nbsp;9). However, the duration of the LCHU time is approximately 1 Myr.\u003c/p\u003e \u003cp\u003eThe top of BC1 (~\u0026thinsp;264.5 Ma) is capped by iron-stained siliciclastic beds in Merbah El Oussif (Fig.\u0026nbsp;8d) and by conglomerates in the Dar Njana area (Fig.\u0026nbsp;8c). Meanwhile, the top of BC2 (~\u0026thinsp;261.5 Ma) is capped at Denguir Hill by karstification filled with red dolomites (Fig.\u0026nbsp;8a, b). Siliciclastic deposits are notably abundant in the western sections and become progressively scarcer towards the east (Figs.\u0026nbsp;3, 9).\u003c/p\u003e \u003cdiv id=\"Sec8\" class=\"Section2\"\u003e \u003ch2\u003eFacies analysis\u003c/h2\u003e \u003cdiv id=\"Sec9\" class=\"Section3\"\u003e \u003ch2\u003eCarbonate facies and depositional environments\u003c/h2\u003e \u003cp\u003eThe detailed description of the carbonate facies, their distribution, and interpretations of depositional environment are presented in Table\u0026nbsp;1.\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e\n\u003ch3\u003eSponge-algal patch-reefs (CF1)\u003c/h3\u003e\n\u003cp\u003eThis facies consists of metric boundstone patch-reefs (Fig.\u0026nbsp;11a), dominated by diverse sponges (Fig.\u0026nbsp;11b, c, d), encrusting algae (Fig.\u0026nbsp;11d), with a subordinate contribution of fusulinids, crinoids and corals (Fig.\u0026nbsp;11e). The encrusting algae (\u003cem\u003eArchaeolithoporella hidensis\u003c/em\u003e and \u003cem\u003eTubiphytes obscurus\u003c/em\u003e) contribute to the construction of the CF1 reef bodies, which display internal sediments (peloidal/bioclastic) and early submarine cement that greatly enhances their rigidity (Chaouachi \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e1988\u003c/span\u003e; Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe geometry and the composition of these reef bodies, especially their association with highly fossiliferous shales (SF1), indicate a deposition within a relatively open marine and low energy palaeoenvironment (outer-shelf setting). Newell et al. (\u003cspan citationid=\"CR121\" class=\"CitationRef\"\u003e1976\u003c/span\u003e) based on the examination of these bioherms, suggested that they grew and developed in a normal marine environment, most likely below the storm wave base, in water depths less than 50 m with relatively low turbulence (Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e).\u003c/p\u003e \u003cdiv id=\"Sec11\" class=\"Section2\"\u003e \u003ch2\u003eEncrusting algae massive bioherms (CF2)\u003c/h2\u003e \u003cp\u003eThis facies consists of massive buildups, frequently dolomitized in the western end of the Tebaga outcrops. These reef bodies are plano-convex, with either symmetric or asymmetric geometry (Fig.\u0026nbsp;11f). They form part of the BC1 and BC2 units and show a boundstone framework with encrusting algae such as \u003cem\u003eArchaeolithoporella hidensis\u003c/em\u003e and \u003cem\u003eTubiphytes obscurus\u003c/em\u003e (Figs.\u0026nbsp;11h, i, 13a, b, c) with minor contribution of calcisponges (Fig.\u0026nbsp;11h, i), corals (Fig.\u0026nbsp;11g) (Chaouachi \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e1988\u003c/span\u003e; Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e). In the Es Souinia area, this facies contains Parachaetetes \u003cem\u003elamellatus\u003c/em\u003e Koniski and the phylloid algae \u003cem\u003eIvanovia tebagaensis\u003c/em\u003e Vachard and Razgallah, 1989. The CF2 facies is both vertically and laterally associated with conglomerates, thin-bedded limestones, shales, and lenticular iron-stained sandstones (Fig.\u0026nbsp;5b, c).\u003c/p\u003e \u003cp\u003eThe boundstone texture, the planoconvex morphology, and the general absence of adjacent talus, in addition to the prevalent mud matrix and fine internal sediments (Fig.\u0026nbsp;11h, i), suggest a relatively low-energy depositional environment ranging from mid to shelf-margin settings (Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e).\u003c/p\u003e \u003cp\u003e \u003cb\u003eGastropods (\u003c/b\u003e \u003cb\u003eBellerophon\u003c/b\u003e \u003cb\u003e)-rich limestones (CF3)\u003c/b\u003e \u003c/p\u003e \u003cp\u003eThis facies is primarily composed of packstones to grainstones, with \u003cem\u003eBellerophon\u003c/em\u003e gastropods. In the Halq Jmel area, it is particularly abundant in bioclast debris, bivalves, and miliolids (Figs.\u0026nbsp;12a, b, 13d), while to the east (Es Souinia area), it is rich in fusulinids and crinoids (Fig.\u0026nbsp;12b).\u003c/p\u003e \u003cp\u003eThe predominance of sessile benthos within this facies indicates deposition in inner to middle carbonate shelf settings under variable hydrodynamic conditions.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec12\" class=\"Section2\"\u003e \u003ch2\u003eFossiliferous well-bedded limestones (CF4)\u003c/h2\u003e \u003cdiv id=\"Sec13\" class=\"Section3\"\u003e \u003ch2\u003eFusulinids-bioclastic packstone-grainstone (CF4.1)\u003c/h2\u003e \u003cp\u003eThis subfacies consists of packstone to grainstone with fusulinids, bioclasts, algal debris (Figs.\u0026nbsp;12c, d, 13e, f), and rare oolites. Planar and low-angle cross-bedding, along with ripple marks, are observed within this facies.\u003c/p\u003e \u003cp\u003eThe presence of shallow marine fossils, ripple marks, and planar/oblique bedding indicates a high-energy shallow marine depositional environment. The association of the CF4.1 facies with foreshore to shoreface sandstones (SF5, Table\u0026nbsp;1) supports its interpretation as an inner to middle shelf setting influenced by wave action (cf. Tucker and Wright 1990).\u003c/p\u003e \u003cp\u003e \u003cb\u003eOncoid packstone/\u0026ldquo;\u003c/b\u003e \u003cb\u003eOttonosia\u003c/b\u003e \u003cb\u003e\u0026rdquo; (CF4.2)\u003c/b\u003e \u003c/p\u003e \u003cp\u003eThis facies consists of thin-bedded or massive beds where grains are algally coated and float within a lime mud to a bioclastic matrix. In thin section, the encrusted skeletal grains are composed of algae and sponge fragments (Figs.\u0026nbsp;12h, 13g). In the Hal Jmel area, particular oncoid facies of spherical shape (over 3 cm in diameter) named \u0026ldquo;Ottonosia\u0026rdquo; grains \u003cem\u003esensu\u003c/em\u003e Termier et al. (\u003cspan citationid=\"CR172\" class=\"CitationRef\"\u003e1977\u003c/span\u003e) (Fig.\u0026nbsp;12i), characterizes the LCHU.\u003c/p\u003e \u003cp\u003eThis facies has been interpreted as intertidal biopisoids by Ghazzay et al. (2015). They accumulated in the open-marine inner shelf, where fluctuating energy levels allowed repeated turnover and sufficient water movement, enabling the oncoliths to grow spherically and develop concentric laminae (Fl\u0026uuml;gel \u003cspan citationid=\"CR56\" class=\"CitationRef\"\u003e2004\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv id=\"Sec14\" class=\"Section2\"\u003e \u003ch2\u003eBioclastic limestones (CF4.3)\u003c/h2\u003e \u003cp\u003eThis facies is composed of well-bedded, poorly sorted bioclastic limestones (wackestone to packstone), occasionally with fusulinids, encrusting algae, crinoids, lamellibranchs, ostracods, and oncoids (Figs.\u0026nbsp;12e, 13h). CF4.3 displays parallel to low-angle cross-stratifications. It is abundant in the BC1 unit, but particularly prevalent in the BC2 as an intermounds facies. In the Es Souinia area, CF4.3 exceptionally contains abundant straight nautiloid cephalopods (\u003cem\u003ePseudorthoceras\u003c/em\u003e) (Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e) (Fig.\u0026nbsp;12f, g)\u003c/p\u003e \u003cp\u003eThe poorly sorted character of CF4.3 and the abundance of bioclastic debris suggest a relatively high-energy depositional environment (Tucker and Wright 1990). CF4.3 has been interpreted as shell debris banks accumulating on a shelf setting by Toomey (\u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec15\" class=\"Section2\"\u003e \u003ch2\u003ePatch-reefs with sponges and algae (CF5)\u003c/h2\u003e \u003cp\u003eThis facies consists of patch reefs 1 to 1.5 m high and a few metres in width. They have a nodular appearance, especially in the Halk Jmel area, and are rich in sponges, oncoliths, corals, and locally, phylloid algae (Fig.\u0026nbsp;11j, k).\u003c/p\u003e \u003cp\u003eThe association of CF5 with the siliciclastic shoreface to foreshore facies (SF5, SF6) (Table\u0026nbsp;1), as well as CF4 indicates deposition within a coastal marine environment (cf. Tucker and Wright 1990).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec16\" class=\"Section2\"\u003e \u003ch2\u003eDolomitized patch reefs and bioclastic limestones (CF6)\u003c/h2\u003e \u003cp\u003eThis facies forms part of the \u0026ldquo;Barre dolomitique inf\u0026eacute;rieure de Dar Njana\u0026rdquo; of Khessibi (\u003cspan citationid=\"CR93\" class=\"CitationRef\"\u003e1985\u003c/span\u003e) and consists of massive or well-bedded dolomites resulting from the secondary dolomitization of CF5 and CF4, such as in the upper part of the DNBBZ Unit, where it contains abundant ghosts of crinoids and bivalves (Fig.\u0026nbsp;12j).\u003c/p\u003e \u003cp\u003eThe dolomitic nature of this facies, the ripple marks, the neritic fauna, and its association with small patch reefs (CF5, see Table\u0026nbsp;1) indicate that CF6 most likely formed in an inner shelf setting.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec17\" class=\"Section2\"\u003e \u003ch2\u003eConglomeratic facies CF7\u003c/h2\u003e \u003cp\u003eThis facies is only identified at the top of BC1 in the Dar Njana\u0026ndash;Merbah El Oussif area. It corresponds to a conglomerate/breccia composed of angular to sub-rounded, poorly sorted debris, originating from the disaggregation of reefs. Sandstone elements reaching cobble size can also be present within this facies (Fig.\u0026nbsp;8c). This facies, recorded in the Dar Njana locality, reflects the exposure of the topmost part of BC 1, probably during a major sea-level fall.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec18\" class=\"Section2\"\u003e \u003ch2\u003eSiliciclastic facies and depositional environments\u003c/h2\u003e \u003cdiv id=\"Sec19\" class=\"Section3\"\u003e \u003ch2\u003eFacies 1 (SF1): Lower offshore\u003c/h2\u003e \u003cp\u003eIt corresponds to highly fossiliferous calcareous shales/marls that are relatively rich in brachiopods, sponges, algae, corals, crinoids, bryozoans, and fusulinids, and include thin-bedded tempestite sandstones (Fig.\u0026nbsp;18c, d) and trace fossils, such as \u003cem\u003eArchaeonassa\u003c/em\u003e, ?\u003cem\u003eNereites\u003c/em\u003e, \u003cem\u003ePlanolites\u003c/em\u003e, \u003cem\u003eProtovirgularia\u003c/em\u003e, \u003cem\u003ePsammichnites\u003c/em\u003e, and \u003cem\u003eTaenidium.\u003c/em\u003e\u003c/p\u003e \u003cp\u003eThe depositional environment of this facies is interpreted as a lower offshore setting occasionally affected by storms (Nichols \u003cspan citationid=\"CR123\" class=\"CitationRef\"\u003e2009\u003c/span\u003e). The light colouration and high diversity of body and trace fossils may indicate a well-oxygenated marine environment.\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv id=\"Sec20\" class=\"Section2\"\u003e \u003ch2\u003eFacies 2 (SF2): Upper offshore\u003c/h2\u003e \u003cp\u003eIt consists of shales that grade upward into increasingly silty deposits with thin-bedded siltstone intercalations. SF2 occurs in the lower strata of the DNBBZ Unit (Fig.\u0026nbsp;14). Sedimentary structures are generally absent in the siltstone beds, except for some planar lamination (Fig.\u0026nbsp;15g, h).\u003c/p\u003e \u003cp\u003eThe upward coarsening nature of SF2 and its transition into the heterolithic facies of SF3 (see Table\u0026nbsp;1) suggests a gradual evolution from deeper to shallower conditions during storm-weather periods in mud-dominated offshore environments (Walker and James \u003cspan citationid=\"CR188\" class=\"CitationRef\"\u003e1992\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec21\" class=\"Section2\"\u003e \u003ch2\u003eFacies 3 (SF3): Offshore transition\u003c/h2\u003e \u003cp\u003eSF3 is found within the lower strata of the DNBBZ Unit in the Dar Njana area (Fig.\u0026nbsp;14). It consists of heterolithic facies composed of fine-grained rippled sandstones and tempestite beds, interbedded with green silty shales, arranged into coarsening- and thickening-upward cycles (10 and 40 cm thick) (Fig.\u0026nbsp;15c, e). The sandstones display rippled surfaces (oscillatory ripple marks) and planar parallel lamination (Fig.\u0026nbsp;15e, f). An interval containing seismite structures is also observed (Fig.\u0026nbsp;15d). Upwards, SF3 is capped by a sandstone package featuring hummocky and swaley cross-stratification (HCS/SCS), which is overlain by fine horizontally laminated siltstones (Fig.\u0026nbsp;15a, b). Trace fossils are mainly observed in the rippled sandstones and include \u003cem\u003eArchaeonassa\u003c/em\u003e, \u003cem\u003ePalaeophycus\u003c/em\u003e, \u003cem\u003eParataenidium\u003c/em\u003e, and \u003cem\u003eSiphonichnus\u003c/em\u003e.\u003c/p\u003e \u003cp\u003eThe wave-rippled sandstones, with symmetrical crests, demonstrate the influence of oscillatory wave action. The formation and preservation of hummocky\u0026ndash;swaley cross-stratification, followed by horizontally laminated fine siltstones as the strength of the oscillation decreases, suggest deposition in the offshore transition zone situated between the fair-weather wave base (FWWB) and storm wave base (SWB) (Nichols \u003cspan citationid=\"CR123\" class=\"CitationRef\"\u003e2009\u003c/span\u003e). During fair-weather conditions, this zone experienced relatively calm conditions, with continuous mud deposition via suspension. Periods of intense storm activity led to an abrupt increase in wave energy and the deposition of HCS, planar-laminated, and wave-rippled sand beds in a muddy environment.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec22\" class=\"Section2\"\u003e \u003ch2\u003eFacies 4 (SF4): Lower shoreface\u003c/h2\u003e \u003cp\u003eSF4 comprises very fine to fine-grained sandstone beds forming a unit more than 4 m thick (Fig.\u0026nbsp;16g). The sandstones exhibit planar-lamination and a small-scale hummock approximately 1 m long (Fig.\u0026nbsp;16h). The transition from SF3 to SF4 is abrupt, shifting from heterolithic sediments below to homogeneous sandstones above. Trace fossils include ?\u003cem\u003eDiplocraterion\u003c/em\u003e and \u003cem\u003eParataenidium\u003c/em\u003e, especially in the upper part of the section.\u003c/p\u003e \u003cp\u003eThe sandstones of SF4 indicate deposition in the lower shoreface setting above the mean fair-weather wave base, where the sediments were frequently reworked by storm and fair-weather waves (Walker and James \u003cspan citationid=\"CR188\" class=\"CitationRef\"\u003e1992\u003c/span\u003e; Nichols \u003cspan citationid=\"CR123\" class=\"CitationRef\"\u003e2009\u003c/span\u003e).\u003c/p\u003e \u003cdiv id=\"Sec23\" class=\"Section3\"\u003e \u003ch2\u003e\u003cb\u003eSiliciclastic facies 5 (SF5): Upper-middle shoreface\u003c/b\u003e\u003c/h2\u003e \u003cp\u003eThis facies is composed of fine-to-medium-grained tabular and thin-bedded sandstone showing planar bedding, oblique tabular bedding, hummocky cross-stratifications (HCS), trough cross-stratifications, and symmetrical ripple marks (Figs.\u0026nbsp;16c, d, e, 17f, g, h). Thin, rippled fusulinid limestone beds (Figs.\u0026nbsp;16f, 17e) are occasionally interbedded with the sandstone sequences. Some flame structures have been observed in the Halq Jmel area (Fig.\u0026nbsp;19a, b). Trace fossils include ?\u003cem\u003eAncorichnus\u003c/em\u003e, \u003cem\u003eCruziana\u003c/em\u003e, \u003cem\u003eHalopoa\u003c/em\u003e, ?\u003cem\u003eHelminthopsis\u003c/em\u003e, \u003cem\u003ePalaeophycus\u003c/em\u003e, \u003cem\u003eParataenidium\u003c/em\u003e (Fig.\u0026nbsp;16a, b), \u003cem\u003ePlanolites\u003c/em\u003e, \u003cem\u003ePsammichnites\u003c/em\u003e, and \u003cem\u003eSiphonichnus.\u003c/em\u003e SF5 occurs within the DNBBZ Unit and the LCH Unit in the Halq Jmel area.\u003c/p\u003e \u003cp\u003eThe stratigraphic position of this facies between the lower shoreface SF4 facies and foreshore/upper shoreface trough cross-stratified SF6 sandstones (Table\u0026nbsp;1), along with the coarsening-up trend and the sedimentary structures, suggests a high-energy environment typical of an upper to middle shoreface setting (Walker and James \u003cspan citationid=\"CR188\" class=\"CitationRef\"\u003e1992\u003c/span\u003e). Additionally, the presence of the flame structures may indicate wave-induced liquefaction during intense storm activity in the shoreface to foreshore settings (Howard and Frey \u003cspan citationid=\"CR83\" class=\"CitationRef\"\u003e1984\u003c/span\u003e; Pemberton et al. \u003cspan citationid=\"CR129\" class=\"CitationRef\"\u003e2012\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv id=\"Sec24\" class=\"Section2\"\u003e \u003ch2\u003eSiliciclastic facies 6 (SF6): Upper shoreface to foreshore\u003c/h2\u003e \u003cp\u003eIt comprises structureless thin-to-medium-bedded, medium-to coarse-grained white or ferruginous sandstones arranged in coarsening and thickening packages (Figs.\u0026nbsp;14, 17g, h). Sedimentary structures include wavy bedding (Fig.\u0026nbsp;17 a), ripple marks on the upper surface of beds (Figs.\u0026nbsp;17b, 19d), HCS and trough, horizontal/low-angle lamination (Fig.\u0026nbsp;19c), water escape (Figs.\u0026nbsp;19a, b, f), flute casts (Fig.\u0026nbsp;19e), convolute bedding (Fig.\u0026nbsp;19f), mud drapes (Fig.\u0026nbsp;19g) and flaser bedding (Fig.\u0026nbsp;19h). The tops of the beds are usually iron-stained and particularly rich in centimetre-sized (10\u0026ndash;50 cm) wood fragments (Fig.\u0026nbsp;17c). Trace fossil diversity and abundance are low, with only \u003cem\u003eParataenidium\u003c/em\u003e, \u003cem\u003ePlanolites\u003c/em\u003e, and \u003cem\u003eThalassinoides\u003c/em\u003e observed.\u003c/p\u003e \u003cp\u003eThe alternation of parallel planar and small cross-ripple lamination demonstrates the importance of the tidal regime during the formation of SF6. The planar-parallel bedding commonly reflects deposition in the foreshore under high-energy conditions (Walker and James \u003cspan citationid=\"CR188\" class=\"CitationRef\"\u003e1992\u003c/span\u003e). It is well established that the swash and backwash processes can produce low-angle seaward-dipping planar-parallel laminations, typically in well-sorted, medium to coarse-grained sandstones (Reineck and Singh \u003cspan citationid=\"CR134\" class=\"CitationRef\"\u003e1980\u003c/span\u003e). Additionally, common symmetrical ripple and flaser bedding feature wave- and tidal-generated signatures.\u003c/p\u003e \u003cdiv id=\"Sec25\" class=\"Section3\"\u003e \u003ch2\u003eSiliciclastic facies 7 (SF7): Tidal channel\u003c/h2\u003e \u003cp\u003eThis facies consists of iron-stained, fine-to-medium-grained sandstones featuring an erosive base and lenticular morphology (5 to 40 m of lateral extension) (Figs.\u0026nbsp;3, 5b, c, 18a, b). Low-angle to horizontal bedding with sigmoid tidal bundles are observed (Fig.\u0026nbsp;18b). The trace fossils \u003cem\u003ePlanolites\u003c/em\u003e, \u003cem\u003ePhycodes\u003c/em\u003e, \u003cem\u003eParataenidium\u003c/em\u003e, \u003cem\u003eProtovirgularia\u003c/em\u003e, and ?\u003cem\u003eGyrophyllites\u003c/em\u003e are present.\u003c/p\u003e \u003cp\u003eLens-shaped sand body geometry, finning-upward sequence, cross-stratification, and erosive basal surfaces suggest deposition in a shallow marine context via tidal channels. In the Biohermal complexes 1 and 2, SF7 cuts through biohermal carbonates and significantly disrupted their development.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec26\" class=\"Section3\"\u003e \u003ch2\u003eSiliciclastic facies 8 (SF8): Tidal sand bar\u003c/h2\u003e \u003cp\u003eIt comprises of thickening-up white, yellow, to red, fine- to medium-grained, and moderately to well-sorted cross-stratified sandstones. The internal architecture is characterized by planar-parallel to low-angle cross-bedding with some reactivation surfaces (Fig.\u0026nbsp;20c). The mud drapes are not preserved. In the upper part, horizontal lamination and locally, ripple marks are present.\u003c/p\u003e \u003cp\u003eThe coarsening upward pattern and the sedimentary structures observed in this facies, and its association with the tidal flats facies (SF9, see Table\u0026nbsp;1) support the interpretation of SF8 as a tidal sand bar deposited within a tide-dominated estuary (sensu Dalrymple et al. \u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e1992\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec27\" class=\"Section3\"\u003e \u003ch2\u003eSiliciclastic facies 9 (SF9): Mixed mud-sand flat\u003c/h2\u003e \u003cp\u003eThis facies comprises red silty shales, locally green, intercalated with fine to medium-grained lenticular sandstone interbeds (Fig.\u0026nbsp;20d, e). The latter display liquefaction structures (convolute bedding), cross-stratification, climbing ripples (Fig.\u0026nbsp;20e), and planar lamination at the top. Roots may be observed locally. The thickness of the sandstone interbeds ranges from 10 cm to 1.5 m.\u003c/p\u003e \u003cp\u003eThe red muddy deposits indicate deposition in a low-energy environment. The interbedded sandstone bodies are interpreted as tidal creek deposits, accumulated through suspension settling in calmer environments on the margins of the estuary (cf. Dalrymple et al. \u003cspan citationid=\"CR33\" class=\"CitationRef\"\u003e1992\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv id=\"Sec28\" class=\"Section2\"\u003e \u003ch2\u003eSiliciclastic facies 10 (SF10): Shale of flood plain\u003c/h2\u003e \u003cp\u003eThis facies consists of plurimetric clayey-silty intervals (Fig.\u0026nbsp;21a, d) incised by channelized lenticular sand bodies (SF12 and SF3, see Table\u0026nbsp;1) with varying thicknesses and extents.\u003c/p\u003e \u003cp\u003eThe fine grain size suggests deposition through suspension settling of the suspended clay and silt particles under very low-energy conditions, most likely on a floodplain (cf. Allen \u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Scholle and Spearing \u003cspan citationid=\"CR147\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Miall \u003cspan citationid=\"CR114\" class=\"CitationRef\"\u003e1996\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec29\" class=\"Section2\"\u003e \u003ch2\u003eSiliciclastic facies 11 (SF11): Silt of flood plain\u003c/h2\u003e \u003cp\u003eIt consists of thin-bedded (\u0026lt;\u0026thinsp;20 cm), horizontally laminated grey silt beds of metric-scale extent, showing fine parallel lamination (Fig.\u0026nbsp;21a, d).\u003c/p\u003e \u003cp\u003eBased on sedimentological features and its interbedding within the SF10 facies, this facies is interpreted as deposits as deposited in calm, protected depositional setting within a floodplain, probably in interdistributary areas (cf. Allen \u003cspan citationid=\"CR1\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Scholle and Spearing \u003cspan citationid=\"CR147\" class=\"CitationRef\"\u003e1982\u003c/span\u003e; Miall \u003cspan citationid=\"CR114\" class=\"CitationRef\"\u003e1996\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e\n\u003ch3\u003eSiliciclastic facies 12 (SF12): Non-amalgamated fluvial channels\u003c/h3\u003e\n\u003cp\u003eThis facies is dominated by red sandstones with a lenticular geometry and an erosive base outlined by a lag deposit composed of shale clasts and wood fragments (Fig.\u0026nbsp;21f). In some areas, small ripple marks, convolute bedding, and planar/cross-stratifications are present (Fig.\u0026nbsp;21e). Root structures are observed at the top of some sand bodies. The trace fossil \u003cem\u003ePlanolites\u003c/em\u003e is present.\u003c/p\u003e \u003cp\u003eThe abundance and extensive nature of the floodplain deposits of SF10, along with the non-amalgamation and isolation of SF12, suggest that low-sinuosity, straight channels occupied the floodplain (cf. Miall \u003cspan citationid=\"CR114\" class=\"CitationRef\"\u003e1996\u003c/span\u003e; Bridge \u003cspan citationid=\"CR17\" class=\"CitationRef\"\u003e2003\u003c/span\u003e).\u003c/p\u003e \u003cdiv id=\"Sec31\" class=\"Section2\"\u003e \u003ch2\u003eSiliciclastic facies 13 (SF13): Crevasse splay sheet sands\u003c/h2\u003e \u003cp\u003eSF13 comprises red or white, fine- to medium-grained, sand sheet-like bodies, decimetres thick and metres in lateral extent. This facies is laterally discontinuous and encased within the silty shale of the facies SF10 (Fig.\u0026nbsp;21a). The surface of a sandstone bed of SF13 preserves tetrapod footprints (Fig.\u0026nbsp;21a, b, c). Plane and oblique cross-stratification, climbing ripples (Fig.\u0026nbsp;21g), ripple marks, root structures (Fig.\u0026nbsp;21h), and trace fossil \u003cem\u003ePlanolites\u003c/em\u003e are recognized.\u003c/p\u003e \u003cp\u003eSF13 is likely interpreted as crevasse splay deposits formed by the rupture of a principal fluvial channel\u0026rsquo;s margins. The root traces suggest dense vegetation in the inter-channel zone, which also encroached on abandoned and pedogenized crevasse splays (cf. Walker and James \u003cspan citationid=\"CR188\" class=\"CitationRef\"\u003e1992\u003c/span\u003e).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec32\" class=\"Section2\"\u003e \u003ch2\u003eSiliciclastic facies 14 (SF14): Palaeosol\u003c/h2\u003e \u003cp\u003eIt comprises to highly bioturbated and slightly consolidated sand bodies, up to 2 m thick. The sand is fine- to medium-grained, nodular, and displays abundant root structures (Fig.\u0026nbsp;21i).\u003c/p\u003e \u003cp\u003eOnce the infilling stage of the channel was complete and the channel subsequently abandoned, the surfaces of the lithosomes of facies SF12 and SF13 became exposed and were colonized by vegetation. Progressive pedogenesis, including root action, caused significant mixing of the sediment. Therefore, SF14 is interpreted as an intensively vegetated palaeosol developed in the interfluve zone of a fluvio-deltaic system (cf. Walker and James \u003cspan citationid=\"CR188\" class=\"CitationRef\"\u003e1992\u003c/span\u003e).\u003c/p\u003e \u003cdiv id=\"Sec33\" class=\"Section3\"\u003e \u003ch2\u003eMixed siliciclastic-carbonate record\u003c/h2\u003e \u003cp\u003eThe mixed siliciclastic-carbonate deposits are most prominently developed within the Tebaga Formation (DNBBZ, BC1, and MOU) (Figs.\u0026nbsp;2, 3). Sandstone rocks either are interbedded with shales or are laterally equivalent to carbonates (Fig.\u0026nbsp;22a, d). Within BC1, the sandstone beds are erosively based and show cross-stratification. Their dimensions vary according to their position relative to the reefs. They generally thin when overlying the reefs, and form massive, plurimetric lenses (averaging 4 m in thickness) with limited lateral extent (averaging 10 m) in the depressions between biohermal bodies. Three types of relationships between the reef mounds and sandstone lenses can be identified. Sandstone bodies may underlie reef framework and serve as a substrate for reef development, or may partially or completely encase the reef mounds (Fig.\u0026nbsp;22b). The sandstone lenses abut against the bio-constructed mounds and lap onto their flanks (Fig.\u0026nbsp;22c). Comparable internal architectures and relationships between reef and non-reef facies have been documented in the Late Eocene mixed carbonate\u0026ndash;siliciclastic system in the southern Pyrenees, Spain, where coral buildups alternate with bedded limestones and sandstones (Morsilli et al. 2011). The sandstone-bioherm association is less commonly observed within the BC2, where bioherms are mostly associated with well-bedded bioclastic limestones (Fig.\u0026nbsp;22e, f).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec34\" class=\"Section3\"\u003e \u003ch2\u003eIchnofossils assemblages\u003c/h2\u003e \u003cp\u003eAs mentioned in the introduction, trace fossils from the Permian of Tunisia have not been extensively described and documented aside from a few references, most of which involve misidentification. This work presents the first comprehensive review of trace fossils, a novel contribution to the study of the investigated deposits. In addition, the trace fossils of the Tebaga outcrops are abundant and relatively diverse, and some of them are well preserved, contributing to a better interpretation of palaeoenvironmental conditions.\u003c/p\u003e \u003cp\u003eSeventeen ichnogenera from the middle-late Permian siliciclastic deposits have been identified throughout the studied stratigraphic units (Fig.\u0026nbsp;10, Table\u0026nbsp;2), attributed to the activity of bivalves, trilobites, crustaceans, and vermiform organisms. They are highly abundant in DNBBZ and MO units.\u003c/p\u003e \u003cp\u003eIn the white to iron-stained sandstones of the basal DNBBZ Unit (SF3 to SF6), intense burrowing is observed, displaying vertical and sub-vertical dwelling structures of inferred suspension-feeding organisms and horizontal structures attributed to deposit feeders. They include ?\u003cem\u003eAncorichnus\u003c/em\u003e (Fig.\u0026nbsp;23a), \u003cem\u003eArchaeonassa\u003c/em\u003e (Fig.\u0026nbsp;23b), \u003cem\u003eCruziana\u003c/em\u003e (Fig.\u0026nbsp;23d), ?\u003cem\u003eDiplocraterion\u003c/em\u003e (Fig.\u0026nbsp;23e), ?\u003cem\u003eHelminthopsis\u003c/em\u003e (Fig.\u0026nbsp;24b), \u003cem\u003ePalaeophycus\u003c/em\u003e (Fig.\u0026nbsp;24d), \u003cem\u003eParataenidium\u003c/em\u003e (Figs.\u0026nbsp;23b, 24e, f), and \u003cem\u003eSiphonichnus\u003c/em\u003e (Fig.\u0026nbsp;26a).\u003c/p\u003e \u003cp\u003eHigher in the section, the tempestite sandstones (SF1) of the MO Unit contain abundant burrows, including \u003cem\u003eArchaeonassa\u003c/em\u003e (Fig.\u0026nbsp;23c), \u003cem\u003ePlanolites\u003c/em\u003e (Fig.\u0026nbsp;25b), \u003cem\u003eProtovirgularia\u003c/em\u003e (Fig.\u0026nbsp;25c), and \u003cem\u003ePsammichnites\u003c/em\u003e (Fig.\u0026nbsp;25f). This suite of trace fossils reflects the activity of organisms mainly in an offshore setting. The inter-reef tidal sandstones (SF7) within the BC2 contain \u003cem\u003ePhycodes\u003c/em\u003e (Fig.\u0026nbsp;25a), \u003cem\u003ePlanolites\u003c/em\u003e (Fig.\u0026nbsp;25b), \u003cem\u003eProtovirgularia (\u003c/em\u003eFig.\u0026nbsp;25d), ?\u003cem\u003eGyrophyllites\u003c/em\u003e (Fig.\u0026nbsp;23f), and \u003cem\u003eTaenidium\u003c/em\u003e (Fig.\u0026nbsp;26b).\u003c/p\u003e \u003cp\u003eTowards the top of the succession, the foreshore to shoreface siliciclastic deposits of the LCHU (SF5-SF6) contain \u003cem\u003eHalopa\u003c/em\u003e (Fig.\u0026nbsp;24a), \u003cem\u003ePsammichnites\u003c/em\u003e (Fig.\u0026nbsp;25e), \u003cem\u003eParataenidium\u003c/em\u003e, \u003cem\u003ePlanolites\u003c/em\u003e, and ?\u003cem\u003eThalassinoides\u003c/em\u003e (Fig.\u0026nbsp;26c), while the fluvial deposits of the UCHU are characterized by a rare occurrence of trace fossils and contain only \u003cem\u003ePlanolites\u003c/em\u003e. All the aforementioned traces (Table\u0026nbsp;2) belong to the \u003cem\u003eCruziana\u003c/em\u003e ichnofacies.\u003c/p\u003e \u003cp\u003e \u003cb\u003eTrilobite and\u003c/b\u003e \u003cb\u003eCruziana\u003c/b\u003e \u003cb\u003ein the Tebaga outcrops\u003c/b\u003e\u003c/p\u003e \u003cp\u003eIn the Es Souinia-Saikha outcrop, a single specimen of the trilobite \u003cem\u003ePseudophillipsia azzouzi\u003c/em\u003e Termier and Termier (\u003cspan citationid=\"CR170\" class=\"CitationRef\"\u003e1974\u003c/span\u003e) (Fig.\u0026nbsp;7b) has been found by Memmi and David (\u003cspan citationid=\"CR112\" class=\"CitationRef\"\u003e1965\u003c/span\u003e) at the eastern end of Jebel Tebaga (33\u0026deg;25'25.37\"N; 10\u0026deg;16'30.70\"E). Termier and Termier (\u003cspan citationid=\"CR170\" class=\"CitationRef\"\u003e1974\u003c/span\u003e) ascribed the trilobite to the \u003cem\u003ePseudophillipsia sumatrensis\u003c/em\u003e (Roemer) group, emphasizing its incomplete preservation and large size. \u003cem\u003eP. sumatrensis\u003c/em\u003e is the Guadalupian \u0026ndash; lower Lopingian taxon (Fig.\u0026nbsp;7c).\u003c/p\u003e \u003cp\u003eA second specimen (Fig.\u0026nbsp;7e) was recently found in an isolated hill in the western part of the Permian belt (N33.408799\u0026deg;, E10.193526\u0026deg;) within the LCHU, close to the Halq Jmel area. The new mapping indicates that this interval is a stratigraphic equivalent to the interval where the only Tunisian trilobite has been collected (Figs.\u0026nbsp;7a, 8).\u003c/p\u003e \u003cp\u003eAs \u003cem\u003eCruziana\u003c/em\u003e could have been left by organisms other than trilobites, the identification of the producing organism is uncertain. \u003cem\u003eCruziana\u003c/em\u003e was mostly produced by trilobites, but it may also have been produced by bilaterally symmetrical organisms, including non-trilobite arthropods and arthropod-like organisms, even in the Palaeozoic era (e.g., Boucot \u003cspan citationid=\"CR13\" class=\"CitationRef\"\u003e1990\u003c/span\u003e; Donovan \u003cspan citationid=\"CR40\" class=\"CitationRef\"\u003e2010\u003c/span\u003e). Nevertheless, Permian \u003cem\u003eCruziana\u003c/em\u003e is relatively rare. So far, it has been reported from the USA (Minter et al. 2007; Minter and Lucas \u003cspan citationid=\"CR116\" class=\"CitationRef\"\u003e2009\u003c/span\u003e), Brazil (Lima and Netto \u003cspan citationid=\"CR99\" class=\"CitationRef\"\u003e2012\u003c/span\u003e), Australia (Feng et al. \u003cspan citationid=\"CR50\" class=\"CitationRef\"\u003e2021\u003c/span\u003e), and Egypt (ElRefaiy et al. 2023).\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e"},{"header":"Discussion","content":"\u003cdiv id=\"Sec36\" class=\"Section2\"\u003e \u003ch2\u003eDepositional environments evolution\u003c/h2\u003e \u003cp\u003eThe sedimentary evolution of the middle-late Permian records the multiple superpositions of ramp and shelf margin carbonate platform depositional settings.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec37\" class=\"Section2\"\u003e \u003ch2\u003ePhase 1: First ramp profile\u003c/h2\u003e \u003cp\u003eThe sedimentary succession of the DNBBZ Unit corresponds to a ramp depositional profile characterized by the interplay of siliciclastic and carbonate sediments (Fig.\u0026nbsp;27). The basal part broadly reflects a transgressive offshore shale/dolomite, overlain by regressive shales and siltstone beds of upper offshore setting (SF2). The succession grades upward to heterolithic facies reflecting storm-dominated conditions of an offshore transition setting. The upper part, consisting of mixed siliciclastic/carbonate deposits (SF4, SF5, SF6, and CF4), reflects a deposition fluctuating between the lower shoreface to the foreshore, while the topmost iron-stained sandstones interval (Fig.\u0026nbsp;27) indicates shoreface to foreshore settings. This phase corresponds to a major transgressive-regressive sequence made of several stacked high-order sequences (4th order) (Fig.\u0026nbsp;14).\u003c/p\u003e \u003cp\u003eSiliciclastic facies of this phase are rich in trace fossils, such as ?\u003cem\u003eAncorichnus\u003c/em\u003e in SF5, \u003cem\u003eArchaeonassa\u003c/em\u003e in SF3, \u003cem\u003eCruziana\u003c/em\u003e in SF5, ?\u003cem\u003eDiplocraterion\u003c/em\u003e in SF4, ?\u003cem\u003eHelminthopsis\u003c/em\u003e in SF5, \u003cem\u003eParataenidiumin\u003c/em\u003e SF4, SF5 and SF6, \u003cem\u003ePalaeophycus\u003c/em\u003e in SF4 and SF5, \u003cem\u003ePsammichnites\u003c/em\u003e in SF5, \u003cem\u003eSiphonichnus\u003c/em\u003e in SF3 and SF4, and ?\u003cem\u003eThalassinoides\u003c/em\u003e in SF6. Well-preserved \u003cem\u003eParataenidium\u003c/em\u003e predominantly occupies the most regressive parts of the coarsening upward cycles. The trace fossil assemblage is typical of the \u003cem\u003eCruziana\u003c/em\u003e ichnofacies, especially its archetypal variety, typical of the upper offshore and the offshore-shoreface transition zones. The occurrence of \u003cem\u003eDiplocraterion\u003c/em\u003e in the middle part of this phase (Fig.\u0026nbsp;10) may indicate the proximal \u003cem\u003eCruziana\u003c/em\u003e ichnofacies (Fig.\u0026nbsp;28), which is typical of the lower shoreface (Pemberton et al. \u003cspan citationid=\"CR128\" class=\"CitationRef\"\u003e2001\u003c/span\u003e; MacEachern et al. \u003cspan citationid=\"CR102\" class=\"CitationRef\"\u003e2012\u003c/span\u003e). The presence of the proximal above the archetypal \u003cem\u003eCruziana\u003c/em\u003e ichnofacies corroborates the overall shallowing upward trend.\u003c/p\u003e \u003cdiv id=\"Sec38\" class=\"Section3\"\u003e \u003ch2\u003ePhase 2: \u0026ldquo;Rimmed\u0026rdquo; shelf carbonate platform\u003c/h2\u003e \u003cp\u003eThis phase encompasses the BC1 deposits. It marks the shift from a mixed siliciclastic-carbonate ramp (phase 1) to a thick carbonate platform system still recording minor siliciclastic influence. Indeed, following the renewed deepening of the depositional environment, siliciclastic influx greatly decreased, reef communities flourished, and massive reef-like bodies developed (facies CF2). The absence or limited extent of an adjacent reef talus and the presence of mudstones deposited between reefs suggest quiet, calm conditions within the photic zone (Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eReef development could be interrupted by the input of coastal terrigenous material derived from the west (Figs.\u0026nbsp;3, 5b, c, 27). The internal architecture of BC1, characterized by successive vertically and laterally stacked reef bodies, can be explained by the 'build-and-fill' model (McKirahan et al. \u003cspan citationid=\"CR111\" class=\"CitationRef\"\u003e2003\u003c/span\u003e), highlighting the interplay between sea-level fluctuations, sedimentation rate, and accommodation space creation. This build-and-fill pattern is developed during periods of high-frequency, high-amplitude sea-level changes (Oborny et al. \u003cspan citationid=\"CR125\" class=\"CitationRef\"\u003e2017\u003c/span\u003e), where each cycle may represent either a single depositional event or multiple stacked cycles.\u003c/p\u003e \u003cp\u003eIn the Tebaga outcrops, BC1 is composed of three distinct bioherm intervals separated by terrigenous shaly and sandstone sediments and well-bedded bioclastic limestones, documenting successive build-and-fill phases (Fig.\u0026nbsp;22d). During transgressive phases, reef growth produced massive carbonate bodies up to 20 m thick, which were subsequently killed by detrital influx during short regressive phases potentially amplified by increased humidity. The BC1, with an estimated duration of ~\u0026thinsp;1.5 Ma (Angiolini et al. \u003cspan citationid=\"CR3\" class=\"CitationRef\"\u003e2008\u003c/span\u003e) and thickness of 60\u0026ndash;100 m, likely represents a 3rd-order depositional sequence containing multiple higher-order cycles (Haq and Schutter \u003cspan citationid=\"CR79\" class=\"CitationRef\"\u003e2008\u003c/span\u003e). The abrupt contact between the massive reefal bodies (CF2) and overlying sandstones (SF6) and the presence of an exposed surface or thick conglomeratic horizon at the top BC1 indicate the termination of Phase 2 following the retreat of the sea during a probable sea-level drop. Similar patterns where siliciclastic influx during sea-level lowstands terminated mound development are documented from Pennsylvanian carbonate mounds of the Cantabrian Mountains (Spain) (Corrochano et al. \u003cspan citationid=\"CR30\" class=\"CitationRef\"\u003e2012\u003c/span\u003e; Samankassou et al. 2013).\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e \u003cdiv id=\"Sec39\" class=\"Section2\"\u003e \u003ch2\u003ePhase 3: Second ramp profile\u003c/h2\u003e \u003cp\u003eThe lithological composition of the MOU unit essentially represented by highly fossiliferous shales (SF1) encasing metric-boundstone calcisponge/algal patch reefs (facies CF1) (Fig.\u0026nbsp;27) and the abundant nautiloids in the Es-Sounia-saikha indicate the establishement of a second ramp depositional system. In this system, the patch reefs have been deposited in a normal marine environment at less than 50 m depth, with relatively low turbulence (Toomey \u003cspan citationid=\"CR175\" class=\"CitationRef\"\u003e1991\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThe upper part of this unit, composed of relatively thick patch reefs, frequent well-bedded limestones, and sandstone tempestite bodies, testifies to a shallowing upward trend. The trace fossil assemblage encountered within the sandstones (\u003cem\u003eArchaeonassa\u003c/em\u003e, ?\u003cem\u003eNereites\u003c/em\u003e, \u003cem\u003ePlanolites\u003c/em\u003e, \u003cem\u003eProtovirgularia\u003c/em\u003e, \u003cem\u003ePsammichnites\u003c/em\u003e, and \u003cem\u003eTaenidium\u003c/em\u003e; Fig.\u0026nbsp;28), dominated by horizontal feeding and locomotion traces are which is consistent with the archetypal \u003cem\u003eCruziana\u003c/em\u003e ichnofacies of upper offshore to transitional offshore-shoreface environments. The sporadic occurrence of ?\u003cem\u003eNereites\u003c/em\u003e may indicate intermittent development of distal \u003cem\u003eCruziana\u003c/em\u003e ichnofacies, typical of lower offshore settings (cf. Pemberton et al. \u003cspan citationid=\"CR128\" class=\"CitationRef\"\u003e2001\u003c/span\u003e; MacEachern et al. \u003cspan citationid=\"CR102\" class=\"CitationRef\"\u003e2012\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eIn sum, the sedimentary record of the MOU broadly recorded a high amplitude sea level rise followed by a progressive shallowing-upward trend. The greater thickness and E-W facies variation compared to BC1 reflect high sedimentation rates and substantial accommodation space, probably driven by the combination of subsidence and sea level rise.\u003c/p\u003e \u003cdiv id=\"Sec40\" class=\"Section3\"\u003e \u003ch2\u003ePhase 4: Rimmed shelf to ramp\u003c/h2\u003e \u003cp\u003eThe filling of the created accommodation space marking the upper part of the MOU, enabled the reinitiation of a new carbonate production (Fig.\u0026nbsp;27). This recovery allowed the construction of extensive (up to 20 m thick) massive bioherm bodies under optimal palaeoecological conditions within the photic zone (e.g., sunlight, low turbidity). These bioherms are mainly constructed by encrusting algae (\u003cem\u003eArchaeolithoporella hidensis\u003c/em\u003e, \u003cem\u003eTubiphytes obscurus\u003c/em\u003e) in the western and central parts of Tebaga outcrops, while in the eastern areas, they are predominantly composed of the blue algae \u0026lsquo;\u003cem\u003eParachaetetes lamellatus\u0026rsquo;\u003c/em\u003e and the green phylloid algae \u003cem\u003e\u0026lsquo;Ivanovia tebagaensis\u0026rsquo;\u003c/em\u003e (Chaouachi et al. \u003cspan citationid=\"CR27\" class=\"CitationRef\"\u003e1988\u003c/span\u003e; Chaouachi \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e1988\u003c/span\u003e; Razgallah et al. \u003cspan citationid=\"CR132\" class=\"CitationRef\"\u003e1989\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThis phase marks the transition from a distally ramp system (Phase 3) to a rimmed shelf depositional environment (BC2), likely developed during late highstand conditions, associated with a net decrease in accommodation space. The regressive nature of this phase is evidenced by the eastward (seaward) progradation of biohermal carbonate bodies. Furthermore, the uppermost BC2 interval exhibiting karstification features confirms the regression trend that culminated in subaerial exposure of the carbonate platform.\u003c/p\u003e \u003cp\u003eThe overlying package, composed at the base of well-bedded carbonates with fusulinids (CF4.1), conodonts, and \u003cem\u003eBellerophon\u003c/em\u003e gastropods (CF3), and the top by highly fossiliferous shale (crinoids, brachiopods), indicates the establishement of open marine conditions probable of ramp system during a short deepening phase before the installation of a broadly regressive siliciclastic system (Fig.\u0026nbsp;27).\u003c/p\u003e \u003c/div\u003e \u003c/div\u003e\n\u003ch3\u003ePhase 5: Esturian to fluvial system\u003c/h3\u003e\n\u003cp\u003eThese basal Cheguimi sandstone deposits, containing ripple marks, wood, and trace fossils, indicate a significant shallowing in the depositional environment. Sedimentary structures, including symmetrical ripple marks, mud drapes, and flaser bedding, collectively suggest a depositional setting dominated by tidal influences. Further up-section, these sandstones become dominant with a diverse trace fossil assemblage comprising \u003cem\u003eParataenidium\u003c/em\u003e, \u003cem\u003ePsammichnites\u003c/em\u003e, \u003cem\u003eSiphonichnus\u003c/em\u003e, and ?\u003cem\u003eThalassinoides\u003c/em\u003e. This trace fossil assemblage represents the archetypal \u003cem\u003eCruziana\u003c/em\u003e ichnofacies (Fig.\u0026nbsp;28), characteristic of the offshore to shoreface transition (Pemberton et al. \u003cspan citationid=\"CR128\" class=\"CitationRef\"\u003e2001\u003c/span\u003e; MacEachern et al. \u003cspan citationid=\"CR102\" class=\"CitationRef\"\u003e2012\u003c/span\u003e). However, the Upper Cheguimi Unit, mainly represented by silty shale floodplain facies (facies SF10), siltstones (facies SF11), sandstones (facies SF12 and SF13), and palaeosols (facies SF14), reflects deposition in very marginal marine to continental environments.\u003c/p\u003e\n\u003ch3\u003eCarbonate platform evolution\u003c/h3\u003e\n\u003cp\u003eThe vertical transition from ramp to rimmed shelf systems has been extensively documented in the literature (e.g., Read \u003cspan citationid=\"CR133\" class=\"CitationRef\"\u003e1985\u003c/span\u003e; Burchette and Wright \u003cspan citationid=\"CR23\" class=\"CitationRef\"\u003e1992\u003c/span\u003e; Pomar \u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2001\u003c/span\u003e). These repeated changes in platform geometry reflect the dynamic interaction between accommodation space (controlled by rates of subsidence and sea-level fluctuations), sediment supply, and carbonate production regimes (governed by ecological factors).\u003c/p\u003e \u003cp\u003eThe DNBBZ Unit accumulated on a mixed siliciclastic-carbonate ramp system where organic communities were unable to form reefs. In contrast, BC1 deposition occurred during a period of increased accommodation space, which facilitated the formation of a platform-margin barrier (Figs.\u0026nbsp;27, 28). This transition may also be linked to biological control (a shift in the biotic system), leading to a high carbonate production by organisms able to build reef bodies (Pomar \u003cspan citationid=\"CR131\" class=\"CitationRef\"\u003e2001\u003c/span\u003e). This shift in depositional style illustrates how the interaction between physical accommodation and biotic evolution can fundamentally control carbonate platform architecture.\u003c/p\u003e \u003cp\u003eFollowing the demise of the rimmed shelf (BC1), a subsequent transgression allowed the development of a new carbonate ramp system during Phase 3, which in turn evolved into a second rimmed shelf (BC2) during late highstand conditions. The overlying BC2, formed within optimal photic zone conditions, supported renewed carbonate production and reef-building biota along a shallow shelf margin. This repeated ramp-to-rim transition is also evident in the Guadalupian strata of the Guadalupe Mountains, where the ramp of the San Andres Formation evolves into the reef-rimmed margin of the Capitan Formation (Kerans et al. \u003cspan citationid=\"CR92\" class=\"CitationRef\"\u003e2013\u003c/span\u003e).\u003c/p\u003e\n\u003ch3\u003eSignificance of the Tunisian Permian sedimentary record\u003c/h3\u003e\n\u003cp\u003e \u003cb\u003eSedimentological aspect\u003c/b\u003e \u003c/p\u003e \u003cp\u003eThe correlation presented in Fig.\u0026nbsp;29 has been developed to enhance our understanding of the N S evolution of the Tunisian Permian sedimentary system, prior to its comparison with analogous examples worldwide.\u003c/p\u003e \u003cp\u003eThe TB-1 well, located approximately 4 km north of Jebel Tebaga, penetrates a thick dominated shales succession (~\u0026thinsp;4000 m) (Fig.\u0026nbsp;29). Notably, the correlation identifies the distinctive \u003cem\u003eBellerophon\u003c/em\u003e-bearing interval from the Halq Jmel section within the 144\u0026ndash;620 m depth interval of the TB-1 well. This chronostratigraphic tie-point allows for a confident correlation between surface and subsurface data. The dominant shale unit, interbedded either with sandy to silty turbidites or breccia and conglomerates composed of reef limestone debris (Glintzboeckel and Rabat\u0026eacute; \u003cspan citationid=\"CR72\" class=\"CitationRef\"\u003e1964\u003c/span\u003e), is interpreted in this study as talus and gravity flow deposits. These probable fore-reefs to slope sediments likely originated from the collapse of a platform-margin to the south. The silty to sandy \u0026ldquo;turbiditic\u0026rdquo; sediments embedded within the thick shale succession may represent equivalents of the coastal marine siliciclastic intervals observed in the proximal Jebel Tebaga area. These findings support the hypothesis that the TB-1 well records, along with those of the MAR-1, MA-1, and KGF-1 wells (Fig.\u0026nbsp;1b), which are also made of shale-dominated, correspond to a large-scale foredeep subsiding basin. This basin extends southward into a mixed carbonate-siliciclastic system developed along ramp or rimmed carbonate profiles, and is supplied from the south by siliciclastic input (Fig.\u0026nbsp;29).\u003c/p\u003e \u003cp\u003eIn the BMT-1 well, located 88 km SE of Tebaga outcrops (Fig.\u0026nbsp;1b), the Permian succession comprises: (1) the lower Permian carbonates of the Zoumit Formation (2913\u0026ndash;3009 m), (2) a dominantly siliciclastic interval (middle Permian?), (3) a middle Permian dominantly carbonate succession, and (4) a middle to late Permian dominantly siliciclastic deposits assignable to the Cheguimi Formation. The NW-SE correlation (Fig.\u0026nbsp;29) demonstartes that the two major siliciclastic intervals (DNBBZ Unit and the Cheguimi Formation) documented in outcrop are also present in the subsurface. Despite variations in thickness, the dominant carbonate interval (2285\u0026ndash;2791 m), characterized by the presence of \u003cem\u003eGlobivalvulina\u003c/em\u003e sp., \u003cem\u003eGlomomidiella\u003c/em\u003e sp., and \u003cem\u003eNodosaria\u003c/em\u003e sp. (Ghazzay et al. 2015), along with associated shales and evaporates, can be confidently correlated with the carbonate-dominated succession of the Tebaga Formation, including the BC1, the MOU, and the overlying BC2 and BLU intervals in outcrops.\u003c/p\u003e \u003cp\u003ePalaeogeographically, this correlation strongly suggests that Tebaga outcrops represent the northern edge of a wide shelf-margin barrier reef system, well-documented in the subsurface near the Medenine area (ongoing work). This reef trend, which extends between the Tebaga outcrops and the MED-1 well (Fig.\u0026nbsp;29), delineated two distinct depositional domains: (1) a broad, shallow inner shelf to the south, characterized by bedded carbonates interbedded with shales, sands, and evaporites (e.g., BMT-1 well), and (2) a deeper, subsiding basinal domain dominated by shaly facies to the north (Fig.\u0026nbsp;29).\u003c/p\u003e \u003cp\u003ePaleocurrent data recorded in the siliciclastic intervals provide insight into the sediment source and transport direction. Measurements from the DNBBZ Unit indicate a dominant sediment transport from south to north, with the source system likely located south-west of the Tebaga region (Chaouachi \u003cspan citationid=\"CR26\" class=\"CitationRef\"\u003e1988\u003c/span\u003e). This source region may correspond to the Talemzane Arch, interpreted as a paleohigh during the Permian (Memmi et al. \u003cspan citationid=\"CR113\" class=\"CitationRef\"\u003e1986\u003c/span\u003e). In contrast, paleocurrent indicators observed within tidal deposits of the LCHU (facies SF7 and SF8) and continental facies of the UCHU (facies SF12 and SF13) in the Halq Jmel and Argoub El Oussif areas reveal a predominantly southward flow direction (Bibonne \u003cspan citationid=\"CR9\" class=\"CitationRef\"\u003e2014\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eThis southeast directed paleoflow supports the emergence of an uplifted area northwest of the Tebaga outcrops since the Capitanian (late middle Permian). This interpretation is corroborated by the well-documented unconformities observed at the surface and in the subsurface, particularly in the TB-1 and MA-1 wells (Fig.\u0026nbsp;29), where Jurassic and Upper Cretaceous strata unconformably above the Permian succession. This uplifted area, corresponding to the Matmata Paleo-high, interpreted in this study as a major source terrain subjected to substantial erosion, likely acting as a sediment feeder region that experienced significant denudation since the Late Permian-Triassic (Fig.\u0026nbsp;29). The mechanisms driniving the pronounced facies and thickness variations between the shallow southern shelf and the rapidly subsiding northern foredeep basin, as well as the evolving geometry of the Permian basin in southern Tunisia, are currently being explored through intergrated well and seismic data (Dixon et al., Khachira et al., ongoing works).\u003c/p\u003e \u003cp\u003eThe vertical regressive trend is consistent with the progressive retreat of the Permian Sea to the east, leaving Tunisia during the late Permian period. This retreat is thought to have resulted from the interplay between the major late Permian glaciation (Rosa and Isbell \u003cspan citationid=\"CR141\" class=\"CitationRef\"\u003e2020\u003c/span\u003e), in combination with the Variscan orogeny, which separated the Palaeozoic Gondwana cycle from the overlying Tethyan cycle in Tunisia (Boote et al. \u003cspan citationid=\"CR10\" class=\"CitationRef\"\u003e1998\u003c/span\u003e; Guiraud et al. \u003cspan citationid=\"CR75\" class=\"CitationRef\"\u003e2005\u003c/span\u003e; Galeazzi et al. \u003cspan citationid=\"CR67\" class=\"CitationRef\"\u003e2010\u003c/span\u003e).\u003c/p\u003e \u003cp\u003eOur analysis of the outcrop and subsurface data reveals a consistent shallowing-upward trend throughout the Permian succession. This trend reflecting the broader second-order middle Permian regression (Haq and Schutter \u003cspan citationid=\"CR79\" class=\"CitationRef\"\u003e2008\u003c/span\u003e) (Fig.\u0026nbsp;30) is comparable to the Permian succession of west Texas, which also displays a regressive trend and a clear shift in the sedimentation regime from middle Permian carbonate shelf margin deposits (Capitan Reef Fm) and its lateral inner shelf deposits to evaporites/red beds. This large-scale regression led to a widespread emergence of marine shelves throughout Pangea and, consequently, the demise of many carbonate platforms (Ross and Ross \u003cspan citationid=\"CR140\" class=\"CitationRef\"\u003e1995\u003c/span\u003e). Ross and Ross (\u003cspan citationid=\"CR139\" class=\"CitationRef\"\u003e1987\u003c/span\u003e) stated that the sea level dropped gradually from the late Early Permian and reached its lowest point (more than \u0026minus;\u0026thinsp;50 m below present level) for the entire Palaeozoic just before or at the middle-late Permian boundary.\u003c/p\u003e\n\u003ch3\u003eIchnological aspect\u003c/h3\u003e\n\u003cp\u003eThe trace fossil assemblage recorded in the Tebaga outcrops of Tunisia represents the archetypal \u003cem\u003eCruziana\u003c/em\u003e ichnofacies, with some indications of the proximal (DNBBZ Unit) and distal (MO Unit) variants.\u003c/p\u003e \u003cp\u003eA brief review of the well-documented \u003cem\u003eCruziana\u003c/em\u003e ichnofacies in the Permian deposits in Gondwana and beyond (Table\u0026nbsp;3) shows that the diversity of the ichnogenera within this ichnofacies is highest (17 ichnogenera) in the Tunisian deposits. The composition of ichnotaxa varies from place to place and from formation to formation. Nevertheless, one-third to half of the ichnogenera are recurrent. Besides being very common, facies-crossing ichnogenera, such as \u003cem\u003ePlanolites\u003c/em\u003e or \u003cem\u003ePalaeophycus\u003c/em\u003e, \u003cem\u003ePsammichnites\u003c/em\u003e, \u003cem\u003eProtovirgularia\u003c/em\u003e, \u003cem\u003eParataenidium\u003c/em\u003e, \u003cem\u003eThalassinoides\u003c/em\u003e, and \u003cem\u003eTaenidium\u003c/em\u003e, appear to be more characteristic components of the Permian \u003cem\u003eCruziana\u003c/em\u003e ichnofacies. To some extent, similar trace fossil assemblages occur in the Carboniferous (e.g., Baucon et al. 2008; Alonso-Muruaga et al. \u003cspan citationid=\"CR2\" class=\"CitationRef\"\u003e2013\u003c/span\u003e; Muszer \u003cspan citationid=\"CR117\" class=\"CitationRef\"\u003e2020\u003c/span\u003e).\u003c/p\u003e"},{"header":"Conclusions","content":"\u003cp\u003eThe novelty of this work lies in the integration of multiple approaches, which have enabled a better understanding of the internal architecture of the middle-Late Permian sedimentary succession of southern Tunisia and facilated the discussion of the main controlling factors of their depositional environments.\u003c/p\u003e \u003cp\u003eThe carbonate facies (CF1 to CF7) that dominate the Permian succession are representative of depositional settings ranging from ramp to rimmed carbonate platforms. The sponge-algal patch-reefs (CF1) embedded with fossiliferous shales, formed in an outer shelf/ramp setting (c.a 50 m depth). In contrast, the massive bioherms formed by encrusting algae with minor contributions from calcisponges and corals (CF2), which form prominent cliff exposures (BC1 and BC2), are representative of shelf margin contexts. The well-bedded limestones (CF3 and CF4) made of fusulinids, brachiopods, gastropods (\u003cem\u003eBellerophon\u003c/em\u003e), oncoliths, and bioclasts were deposited across inner to middle shelf settings. Facies CF5 and CF6 developed in coastal marine environments.\u003c/p\u003e \u003cp\u003eThe siliciclastic intervals, mainly identified within the DNBBZ, MO, and LCH units, comprise nine distinct facies (SF1 to SF9) deposited in offshore, shoreface, foreshore, and tide-dominated estuary settings. These intervals yielded a variety of well-preserved trace fossils, comprising 17 ichnotaxa belonging to the \u003cem\u003eCruziana\u003c/em\u003e ichnofacies. The trace fossil \u003cem\u003eCruziana\u003c/em\u003e is reported here for the first time from the Tebaga outcrops, particularly within LCHU sandstones, where the only Tunisian trilobite specimen has been collected. However, the overlying UCHU siliciclastic facies (SF10-SF14) reflect a significant regressive shift, transitioning from marginal marine to fully continental fluvial environments.\u003c/p\u003e \u003cp\u003eThe vertical transition between ramp and rimmed carbonate platform configurations could result from the changes in the carbonate sedimentation rate, primarily controlled by sea level changes, available accommodation space, and climatic conditions that strongly influenced faunal associations. Tectonic subsidence also played a major role in shaping the basin architecture, with maximum facies and thickness variations occurring north of the carbonate platform margin along the E-W trending Tebaga fault. The subsiding depocentre (TB-1 well) recording at least 4000 m of sedimentary fill is interpreted in this study as a foredeep basin. Within this setting, breccias and conglomerates composed of shallow-marine carbonate clasts derived from the adjacent platform occur as redeposited gravity flows.\u003c/p\u003e \u003cp\u003eThe latest Permian records the complete continentalisation in Tunisia, which is thought to be caused by the interplay between the major late Permian glaciation and the Variscan orogeny. In southern Tunisia, this coincides with the development of the Matmata-Mednine paleaohigh, which most likely acted as a local sediment source for the latest Permian-Early to Middle Triassic continental fluvial-deltaic settings.\u003c/p\u003e"},{"header":"Declarations","content":"\u003ch2\u003eAcknowledgments\u003c/h2\u003e \u003cp\u003eThe results presented in this paper are part of Ali Khachira's ongoing PhD thesis, being carried out within the research laboratory LR18ES07 (Sedimentary Basins and Petroleum Geology) at the Faculty of Sciences (FST), Tunis El Manar University (UTM). The authors would like to express their gratitude to the Tunisian Ministry of Higher Education and Scientific Research for financial support. The contribution of A.U. was supported by a grant from the Faculty of Geography and Geology under the Strategic Programme Excellence Initiative at Jagiellonian University.We are grateful to the Editor-in-Chief, Wolfgang Kiessling, and to Jean-Yves Reynaud and Francisco J. Rodr\u0026iacute;guez-Tovar for their invaluable and helpful comments and constructive reviews, which significantly improved the original manuscript. Special thanks are extended to my collegue Rami Sliti for his great help in the last moment of the preparation of the paper. We thank Mr Jihed Dridi for granting access to the Geological Patrimony Museum of ONM, which enabled consultation of the Tunisian trilobite holotype. Our thanks are also extended to Mr Sami Riahi, Mr Kamel Boukhalfa, Mr Moncef Saidi, and Mrs. Rahma Znazen for their support and Rabii for his help. Special thanks also go to Mr Atef Bel Kahla for his trace trilobite field photo and Mr Ahmed Nasri for insightful discussions about the Permian. Finally, we express our gratitude to the NARG team, with whom we are collaborating on other studies related to Permian Tunisia. Particular thanks go to Dr. Richard Dixon (NARG) for his continuous support and fruitful discussions.\u003c/p\u003e"},{"header":"References","content":"\u003col\u003e\u003cli\u003e\u003cspan\u003eAllen JRL (1982) Sedimentary structures: their character and physical basis, Volume I. Developments in Sedimentology, 30B. Elsevier Science, Amsterdam, p 663\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eAlonso-Muruaga PJ, Buatois LA, Limarino CO (2013) Ichnology of the Late Carboniferous Hoyada Verde Formation of western Argentina: exploring postglacial shallow-marine ecosystems of Gondwana. 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(ONM), Tunis, feuille no. 91\u003c/span\u003e\u003c/li\u003e\u003c/ol\u003e"},{"header":"Tables","content":"\u003cp\u003e\u003cstrong\u003eTable\u0026nbsp;1\u003c/strong\u003e Facies type, depositional environment, and associated ichnotaxa contribution from the different units of the Tebaga outcrops\u0026nbsp;\u003c/p\u003e\n\u003cdiv class=\"gridtable\"\u003e\n \u003ctable id=\"Taba\" border=\"1\"\u003e\n \u003cthead\u003e\n \u003ctr\u003e\n \u003cth colspan=\"2\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFacies\u003c/div\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDescription: color, texture, and sedimentary structures\u003c/div\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDepositional environment\u003c/div\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eOccurrence\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e(Units)\u003c/div\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u003c/div\u003e\n \u003c/th\u003e\n \u003c/tr\u003e\n \u003c/thead\u003e\n \u003ctbody\u003e\n \u003ctr\u003e\n \u003ctd colspan=\"2\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCF1\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSponge/algal patch-reefs (up to 2 m wide, 6 m high, and 20 m of lateral extension) embedded within fossiliferous shales. Dominated by sponges and varied skeletal components (algae, coral, bryozoan, fusulinids)\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eOuter shelf\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eMOU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"43\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;11a-e\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd colspan=\"2\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCF2\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eHighly cemented massive boundstone algae buildups (5\u0026ndash;15 m thick and occasionally up to 50 m wide), vertically and laterally separated by shales. Reefs interfere with lenticular sandstones and bedded bioclastic limestones.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eMiddle shelf to shelf margin\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eBC1 and BC2\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"44\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigures\u0026nbsp;11f-i, 13a-c\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd colspan=\"2\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCF3\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eWell bedded, grey packstone to grainstone limestones rich in \u003cspan class=\"Italic\"\u003eBellerophon\u003c/span\u003e gastropods, fusulinids, brachiopods, conodonts and algae, interbedded with fossiliferous green shales.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eMiddle shelf\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eBLU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"45\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigures\u0026nbsp;12a, b, 13d\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd rowspan=\"3\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCF4\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCF4.1\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eWell bedded, grey to brown limestones, decimetric to metric, pack-grainstone, rich in fusulinids, algae and bioclastic debris and rare oolites.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd rowspan=\"3\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eInner to middle shelf\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd rowspan=\"3\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eAll units (except UCHU)\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigures\u0026nbsp;12c, d, 13e, f\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCF4.2\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eYellow massive to thin bedded (50 cm) wackstone limestone with oncoliths.\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003eIn Halq Jmel area, this facies is composed of spherical shape oncoid (over 3 cm in diameter) known as \u0026ldquo;\u003cspan class=\"Italic\"\u003eOttonosia\u003c/span\u003e\u0026rdquo; grains \u003cspan class=\"Italic\"\u003esensu\u003c/span\u003e Termier et al. (\u003cspan class=\"CitationRef\"\u003e1977\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigures\u0026nbsp;12h, i, 13g\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCF4.3\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eGrey to brown, yellow metric (up to 1m) to decametric bioclastic limestone (packstone) with parallel to low angle cross-stratifications. In microfacies, the matrix is mainly composed of rich-skeletal brown sediments.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigures\u0026nbsp;12 e-g, 13h\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd colspan=\"2\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCF5\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eGrey to yellow small (1 m to 1.2 m thick) isolated sponge-algal patch reefs. CF6 is rich in sponge and locally with phylloid alga, especially in the Es Souinia area.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCoastal\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003emarine\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDNBBZU, LCHU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;11 j, k\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd colspan=\"2\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCF6\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eYellow massive dolomite, rich in crinoids, lamellibranches, oncoliths and algae debris. Algae patch reefs interfere with CF6. Symmetrical ripple marks could be locally observed.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eInner shelf\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDNBBZU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;12j\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd colspan=\"2\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCF7\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eConglomerate/breccia facies composed of a mixture of angular to sub-rounded elements, poorly sorted debris derived from reef bodies and sandstone small blocs (up to cobble size).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e-\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTop BC1\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"46\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;8c\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003c/tbody\u003e\n \u003c/table\u003e\u0026nbsp;\n\u003c/div\u003e\n\u003cdiv class=\"gridtable\"\u003e\n \u003cdiv class=\"colspec\" align=\"left\"\u003e\u0026nbsp;\u003c/div\u003e\n \u003ctable id=\"Tab1\" border=\"1\"\u003e\n \u003ccaption\u003e\n \u003cdiv class=\"CaptionNumber\"\u003eTable 1\u003c/div\u003e\n \u003cdiv class=\"CaptionContent\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e(continued)\u003c/div\u003e\n \u003c/div\u003e\n \u003c/caption\u003e\n \u003cthead\u003e\n \u003ctr\u003e\n \u003cth colspan=\"7\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSiliciclastic Facies and associated trace fossils\u003c/div\u003e\n \u003c/th\u003e\n \u003c/tr\u003e\n \u003c/thead\u003e\n \u003ctbody\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFacies\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDescription: color, texture, and sedimentary structures\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTrace fossils\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDepositional environment\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eOccurrence\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e(Units)\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eAge\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003ePhotos\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF1\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTempestite sandstones with trace fossils interbedded with fossiliferous shales, bioclastic limestones and patch reefs.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eArchaeonassa\u003c/span\u003e, \u003cspan class=\"Italic\"\u003e?Nereites\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePlanolites\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eProtovirgularia\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePsammichnites\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eTaenidium\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eLower offshore\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eMOU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd rowspan=\"9\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eMiddle Permian\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"47\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;18c, d\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF2\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eGreen shale with thin bedded bioturbated siltstones with parallel lamination.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e-\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eUpper\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003eoffshore\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDNBBZU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"48\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;15g, h\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF3\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eHeterolithic facies made up of green silty shale interbedded with fine-grained rippled sandstones with tempestite beds with HCS/SCS and Seismite structures.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eArchaeonassa, Palaeophycus Parataenidium\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eSiphonichnus\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eOffshore\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003etransition\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDNBBZU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;15a-f\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF4\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eStructureless to laminated fine-grained sandstones with planar stratification and HCS.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003e?Diplocraterion\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eParataenidium\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eLower shoreface\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDNBBZU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"49\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;16g, h\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF5\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e30 to 150 cm thick very fine to medium and poorly to well sorted tabular sandstones organized in coarsening-upward sequences. Planar, low angle bedding, and symmetrical ripple marks characterize SF5.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003e?Ancorichnus\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eCruziana\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eThalassinoides\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eHalopoa\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003e?Helminthopsis Palaeophycus Parataenidium\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePsammichnites\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePlanolites, Siphonichnus\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eUpper-middle shoreface\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDNBBZU, LCHU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"50\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003e\n \u003cdiv id=\"51\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigures\u0026nbsp;16a-f, 17g, h, 19a-d\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF6\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFerruginous, medium to coarse-grained, moderate to well indurated sandstones, up to 9 m thick. Moderate to well-sorted grained, reverse graded, locally bioturbated and with mud drapes.\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003eSedimentary structures: plan and through cross-stratifications, ripple marks, HCS structures, and flaser bedding.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eParataenidium\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePlanolites\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003e?Thalassinoides\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eUpper shoreface to foreshore\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDNBBZU, LCHU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigures\u0026nbsp;17, 19e\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF7\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFerruginous medium to coarse-grained lenticular sandstones with low angle cross bedding and soft-sediment deformation structures. Normal grading organization with irregular and erosive bases marked by lags, coarse particles.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePlanolites\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePhycodes\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eParataenidium\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eProtovirgularia\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003e?Gyrophyllites\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTidal channel\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDNBBZU, BC1, 2, LCHU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"52\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;22a, b\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF8\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCoarsening, thickening-upward white to yellow fine to medium grained and moderately to well-sorted sandstones. Sedimentary structures: Flat, trough and low angle bedding and reactivation surfaces. In the upper part, horizontal lamination and ripple marks are present.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e-\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTidal sand bar\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eLCHU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"53\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;20c\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF9\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eRed silty-shale interbedded with thick/ thin (10 cm to 2 m) lenticular sandstones.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e-\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eMixed mud-sand flat\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eLCHU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;20a, d, e\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF10\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eRed silty shale interbedded with both thick and thin lenticular sandstones, silt and thin yellow dolomite intercalations.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e-\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eShale of flood plain\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd rowspan=\"5\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eUCHU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd rowspan=\"5\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eLate Permian\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"54\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;21d\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF11\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eGrey thin bedded, horizontally laminated siltstone beds (\u0026lt;\u0026thinsp;20cm).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e-\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSilt of flood plain\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;21d\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF12\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eThick bedded, fine to medium grained normal grading lenticular sandstones (up to 8 m) with shale clast at the base, plan and through cross stratifications, convolute structures and flute casts.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePlanolites\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eNon-amalgamated fluvial channels\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;21e, f\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF13\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eRed to white thin lenticular fine to medium grained, well sorted sandstone beds (20\u0026ndash;70 cm) with small, climbing ripples and root traces.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePlanolites\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eCrevasse splay, sheet sands\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;21g, h\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSF14\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eMassive to locally consolidate nodular and coarse bioturbated red sandstone beds (30\u0026ndash;120 cm) with root traces.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e-\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFlood plain\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;21i\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003c/tbody\u003e\n \u003c/table\u003e\n\u003c/div\u003e\n\u003cp\u003e\u0026nbsp;\u003c/p\u003e\n\u003cdiv class=\"gridtable\"\u003e\n \u003ctable id=\"Tab2\" border=\"1\"\u003e\n \u003ccaption\u003e\n \u003cdiv class=\"CaptionNumber\"\u003eTable 2\u003c/div\u003e\n \u003cdiv class=\"CaptionContent\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTrace fossils from the Permian of southern Tunisia\u003c/div\u003e\n \u003c/div\u003e\n \u003c/caption\u003e\n \u003cthead\u003e\n \u003ctr\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eIchnotaxon, occurrence\u003c/div\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eDescription\u003c/div\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eRemarks\u003c/div\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u003c/div\u003e\n \u003c/th\u003e\n \u003c/tr\u003e\n \u003c/thead\u003e\n \u003ctbody\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e?\u003cspan class=\"Italic\"\u003eAncorichnus\u003c/span\u003e isp. Upper surface of a fine- to medium-grained sandstone bed, facies SF5, Dar DNBBZ Unit.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eHorizontal, winding, meniscate burrow with a distinct moat on both sides of its course. The meniscate part is 5\u0026ndash;6 mm wide, and the moat is up to 3 mm wide.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eThe moat probably resulted from the weathering of a less resistant material that surrounded the meniscate part, which can be interpreted as a mantle, forming an integral part of the trace. This is a diagnostic feature of \u003cspan class=\"Italic\"\u003eAncorichnus\u003c/span\u003e Heinberg, \u003cspan class=\"CitationRef\"\u003e1974\u003c/span\u003e, a locomotion and feeding burrow primarily known from Mesozoic shelf deposits (Keighley and Pickerill \u003cspan class=\"CitationRef\"\u003e1994\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"55\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;23a\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eArchaeonassa\u003c/span\u003e isp. DNBBZU and MOU.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"56\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eHorizontal, winding, wide, and shallow, V-shaped (Fig.\u0026nbsp;14b) or U-shaped (Fig.\u0026nbsp;14c) gutter bounded by discontinuous, narrow levees. The gutter is 10\u0026ndash;12 mm wide in the V-shaped forms, and 9\u0026ndash;25 mm wide in the U-shaped forms.\n \u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eArchaeonassa\u003c/span\u003e Fenton and Fenton, \u003cspan class=\"CitationRef\"\u003e1937\u003c/span\u003e, is a grazing trail mainly produced by gastropods (Fenton and Fenton \u003cspan class=\"CitationRef\"\u003e1937\u003c/span\u003e; Buckman \u003cspan class=\"CitationRef\"\u003e1994\u003c/span\u003e; Stanley and Feldmann \u003cspan class=\"CitationRef\"\u003e1998\u003c/span\u003e) or arthropods (Yochelson and Fedonkin 1997).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;23b, c\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eCruziana\u003c/span\u003e isp.\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003eTop of a sandstone bed in SF5 of DNBBZU.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSingle, short segment of horizontal bilobate burrow, 60\u0026ndash;65 mm wide, with oblique, regular ribs converging in the midline at an angle of 90\u0026deg;\u0026ndash;100\u0026deg;\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eCruzian\u003c/span\u003ea ďOrbigny, \u003cspan class=\"CitationRef\"\u003e1842\u003c/span\u003e is a locomotion and feeding burrow primarily produced by trilobites in the Paleozoic and by some other arthropods in younger deposits (e.g., Seilacher \u003cspan class=\"CitationRef\"\u003e1970\u003c/span\u003e, \u003cspan class=\"CitationRef\"\u003e2007\u003c/span\u003e; Zonneveld et al. \u003cspan class=\"CitationRef\"\u003e2002\u003c/span\u003e). Paleozoic \u003cspan class=\"Italic\"\u003eCruziana\u003c/span\u003e occurs mostly in shoreface and offshore siliciclastic deposits (e.g., Seilacher \u003cspan class=\"CitationRef\"\u003e1985\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;23d\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e?\u003cspan class=\"Italic\"\u003eDiplocraterion\u003c/span\u003e isp. DNBBZU.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003ePairs of circular knobs on the bedding plain, 6\u0026ndash;10 mm in diameter and 10\u0026ndash;14 mm apart, connected by a bridge-like bar.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eThis morphology suggests a vertical U-shaped burrow with spreiten, typical of \u003cspan class=\"Italic\"\u003eDiplocraterion\u003c/span\u003e Torell, \u003cspan class=\"CitationRef\"\u003e1870\u003c/span\u003e, which is a domichnion of suspension feeders (e.g., F\u0026uuml;rsich \u003cspan class=\"CitationRef\"\u003e1974\u003c/span\u003e). Its type ichnospecies, \u003cspan class=\"Italic\"\u003eD. parallelum\u003c/span\u003e Torell, \u003cspan class=\"CitationRef\"\u003e1870\u003c/span\u003e, is common in very shallow marine Paleozoic and Mesozoic deposits (e.g., F\u0026uuml;rsich \u003cspan class=\"CitationRef\"\u003e1981\u003c/span\u003e; Bromley and Hanken \u003cspan class=\"CitationRef\"\u003e1991\u003c/span\u003e; Jensen \u003cspan class=\"CitationRef\"\u003e1997\u003c/span\u003e; Bromley and Uchman \u003cspan class=\"CitationRef\"\u003e2003\u003c/span\u003e; Stachacz \u003cspan class=\"CitationRef\"\u003e2016\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;23e\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e?\u003cspan class=\"Italic\"\u003eGyrophyllites\u003c/span\u003e isp.\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003eA single sandstone slab in BC2.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTwo epichnial, neighbouring, shallow depressions, lobate in outline, rimmed by a collar. The depressions are 50\u0026ndash;55 mm wide. The collar is 3 mm wide.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eThe morphology suggests a rosette trace fossil of the \u003cspan class=\"Italic\"\u003eGyrophyllites\u003c/span\u003e group. \u003cspan class=\"Italic\"\u003eGyrophyllites\u003c/span\u003e Glocker, \u003cspan class=\"CitationRef\"\u003e1841\u003c/span\u003e, is a fodinichnion (e.g., F\u0026uuml;rsich and Kennedy1975; Fu \u003cspan class=\"CitationRef\"\u003e1991\u003c/span\u003e) of a polychaete or echiuran worm (Strzeboński and Uchman \u003cspan class=\"CitationRef\"\u003e2015\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;23f\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eHalopoa\u003c/span\u003e isp.\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003eLCHU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eHypichnial, gently curved or straight cylindrical burrow, 5\u0026ndash;7 mm, rarely up to 10 mm wide, covered with irregular, discontinuous, longitudinal wrinkles.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eHalopoa\u003c/span\u003e Torell, \u003cspan class=\"CitationRef\"\u003e1870\u003c/span\u003e, which is a locomotion and feeding burrow known from shallow-marine Paleozoic and deep-sea Mesozoic and Cenozoic deposits (Uchman \u003cspan class=\"CitationRef\"\u003e1998\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"57\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;24a\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e?\u003cspan class=\"Italic\"\u003eHelminthopsis\u003c/span\u003e isp. DNBBZU.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eHypichnial, unornamented ridges, 10\u0026ndash;12 mm wide, running subparallel, 24\u0026ndash;40 mm apart.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eThe extent of the ridges is unknown due to the incompleteness of the slab bearing them, but the curvature of the ridges suggests \u003cspan class=\"Italic\"\u003eHelminthopsis\u003c/span\u003e Wetzel and Bromley, \u003cspan class=\"CitationRef\"\u003e1996\u003c/span\u003e, a repichnion likely produced by polychaetes or priapulids (Fillion and Pickerill \u003cspan class=\"CitationRef\"\u003e1990\u003c/span\u003e) in various, mostly marine environments since the Cambrian (Crimes \u003cspan class=\"CitationRef\"\u003e1987\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;24b\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e?\u003cspan class=\"Italic\"\u003eNereites\u003c/span\u003e isp.\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003eOn the top of a fine-grained sandstone bed in the isolated escarpment of the OA Unit.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eA short fragment of a horizontal, winding, tape-like structure that is 20\u0026ndash;22 mm wide. It shows a low median ridge, which is 3 mm wide, and oblique, dense lateral lobes.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eThe levees are interpreted as reworked zones bounding faecal strings (cf. Uchman \u003cspan class=\"CitationRef\"\u003e1995\u003c/span\u003e). \u003cspan class=\"Italic\"\u003eNereites\u003c/span\u003e MacLeay, \u003cspan class=\"CitationRef\"\u003e1839\u003c/span\u003e, is a pascichnion (M\u0026aacute;ngano et al. \u003cspan class=\"CitationRef\"\u003e2000\u003c/span\u003e), but is also considered a fodinichnion (Knaust \u003cspan class=\"CitationRef\"\u003e2017\u003c/span\u003e). \u003cspan class=\"Italic\"\u003eNereites\u003c/span\u003e is a typical deep-sea ichnogenus, although it may also occur on slopes (Callow et al., \u003cspan class=\"CitationRef\"\u003e2013\u003c/span\u003e; Demircan and Uchman \u003cspan class=\"CitationRef\"\u003e2016\u003c/span\u003e), shelves (Knaust \u003cspan class=\"CitationRef\"\u003e2017\u003c/span\u003e), and exceptionally in sandy estuarine deposits and tidal flats (Martin and Rindsberg \u003cspan class=\"CitationRef\"\u003e2007\u003c/span\u003e; Neto de Carvalho and Baucon \u003cspan class=\"CitationRef\"\u003e2010\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;24c\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePalaeophycus\u003c/span\u003e isp. DNBBZU.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eA horizontal, straight to gently curved, cylindrical burrow, 10\u0026ndash;15 mm wide, showing a distinct lining.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePalaeophycus\u003c/span\u003e Hall, \u003cspan class=\"CitationRef\"\u003e1847\u003c/span\u003e is an open locomotion and feeding burrow produced by several deposit-feeding or predaceous organisms in many environments (e.g., Pemberton and Frey \u003cspan class=\"CitationRef\"\u003e1982\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;24d\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eParataenidium\u003c/span\u003e isp. The top of a fine-grained sandstone bed (facies SF6, DNBBZU)\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eA horizontal winding structure that is 6\u0026ndash;16 mm wide. Its basal part is semicylindrical and lined. The upper part shows regular knobs, which protrude up from the basal part. They are inclined in the same direction along the course of the trace. The centres of the knobs are 8\u0026ndash;15 mm apart.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eBoyd and McIlroy (\u003cspan class=\"CitationRef\"\u003e2018\u003c/span\u003e) excluded \u003cspan class=\"Italic\"\u003eP. moniliformis\u003c/span\u003e (Tate \u003cspan class=\"CitationRef\"\u003e1859\u003c/span\u003e) from \u003cspan class=\"Italic\"\u003eParataenidium\u003c/span\u003e Buckman, \u003cspan class=\"CitationRef\"\u003e2001\u003c/span\u003e, and reassigned it to the newly introduced ichnogenus \u003cspan class=\"Italic\"\u003eNeoeione\u003c/span\u003e. However, it appears that the differences between \u003cspan class=\"Italic\"\u003eP. mullaghmorensis\u003c/span\u003e Buckman, \u003cspan class=\"CitationRef\"\u003e2001\u003c/span\u003e, the type ichnospecies of \u003cspan class=\"Italic\"\u003eParataenidium\u003c/span\u003e, and \u003cspan class=\"Italic\"\u003eP. moniliformis\u003c/span\u003e are insufficient to justify their separation at the ichnogenus level (Riahi and Uchman \u003cspan class=\"CitationRef\"\u003e2022\u003c/span\u003e). \u003cspan class=\"Italic\"\u003eParataenidium\u003c/span\u003e is a pascichnion attributed to an unknown vermiform organism (Buckman \u003cspan class=\"CitationRef\"\u003e2001\u003c/span\u003e; Boyd and McIlroy \u003cspan class=\"CitationRef\"\u003e2018\u003c/span\u003e). In the studied Permian deposits, it was identified as \u003cspan class=\"Italic\"\u003eArenicolites solignaci\u003c/span\u003e Mathieu, \u003cspan class=\"CitationRef\"\u003e1949\u003c/span\u003e (also illustrated by Khessibi \u003cspan class=\"CitationRef\"\u003e1985\u003c/span\u003e), but \u003cspan class=\"Italic\"\u003eArenicolites\u003c/span\u003e Salter, \u003cspan class=\"CitationRef\"\u003e1857\u003c/span\u003e is a U-shaped burrow (e.g., Hanken et al. \u003cspan class=\"CitationRef\"\u003e2016\u003c/span\u003e), and the assignment of this trace fossil was incorrect. Nevertheless, the ichnospecies name remains available. However, this issue warrants further study.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigures\u0026nbsp;23b, 24e, f\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePhycodes\u003c/span\u003e isp.\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003eBC2.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eHorizontal or subhorizontal cylindrical burrows, 10\u0026ndash;12 mm wide and diverging from a common stem.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSeilacher (\u003cspan class=\"CitationRef\"\u003e2007\u003c/span\u003e) restricted \u003cspan class=\"Italic\"\u003ePhycodes\u003c/span\u003e to tightly spaced bundles. \u003cspan class=\"Italic\"\u003ePhycodes\u003c/span\u003e Richter, \u003cspan class=\"CitationRef\"\u003e1850\u003c/span\u003e, is considered a feeding structure of unknown organisms. In the Paleozoic, it is primarily found in shallow marine sediments (Osgood \u003cspan class=\"CitationRef\"\u003e1970\u003c/span\u003e; Fillion and Pickerill \u003cspan class=\"CitationRef\"\u003e1990\u003c/span\u003e; Han and Pickerill \u003cspan class=\"CitationRef\"\u003e1994\u003c/span\u003e; Seilacher \u003cspan class=\"CitationRef\"\u003e2000\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"58\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;25a\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePlanolites\u003c/span\u003e isp. MOU and BC2.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eHorizontal, straight or winding, simple, cylindrical, unlined burrow. It shows diverse size and sinuosity, e.g., some nearly straight burrows are 8 mm wide, and some winding burrows are 4\u0026ndash;5 mm wide.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePlanolites\u003c/span\u003e Nicholson, \u003cspan class=\"CitationRef\"\u003e1873\u003c/span\u003e, is a locomotion-and-feeding, actively filled trace (pascichnion) probably produced by several different organisms occurring in a wide range of environments (e.g., Pemberton and Frey \u003cspan class=\"CitationRef\"\u003e1982\u003c/span\u003e; Fillion and Pickerill \u003cspan class=\"CitationRef\"\u003e1990\u003c/span\u003e; Keighley and Pickerill \u003cspan class=\"CitationRef\"\u003e1995\u003c/span\u003e, and references therein).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;25a, b\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eProtovirgularia\u003c/span\u003e isp. MOU and BC2.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eA hypichnial, horizontal, curved structure, 10\u0026ndash;15 mm wide, showing a median string, which is 2 mm wide, and oblique, lateral ribs, which are 4\u0026ndash;6 mm apart (2 or 3 ribs/cm). The ribs are elevated along the median string and slope towards the structure margins.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eProtovirgularia\u003c/span\u003e McCoy, 1850, is a molluscan (mostly bivalve) locomotion trace in which the chevron ridges are imprints of the cleft foot (Seilacher and Seilacher, \u003cspan class=\"CitationRef\"\u003e1994\u003c/span\u003e). The ichnospecies of \u003cspan class=\"Italic\"\u003eProtovirgularia\u003c/span\u003e are highly variable and occur in various marine environments at different depths (Uchman \u003cspan class=\"CitationRef\"\u003e1998\u003c/span\u003e; M\u0026aacute;ngano et al. \u003cspan class=\"CitationRef\"\u003e2002\u003c/span\u003e). It is likely that the newly identified trace fossil \u003cspan class=\"Italic\"\u003eTabagacolites lautieri\u003c/span\u003e, distinguished by Mathieu (\u003cspan class=\"CitationRef\"\u003e1949\u003c/span\u003e) from the studied Permian deposits and also illustrated by Khessibi (\u003cspan class=\"CitationRef\"\u003e1985\u003c/span\u003e), represents the same trace fossil.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;25c, d\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePsammichnites\u003c/span\u003e isp. MOU and LCHU.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eA horizontal, winding, three-lobate structure showing three basic morphotypes: (1) a smooth furrow, 10\u0026ndash;15 mm wide, with a 1\u0026ndash;2 mm wide median ridge; (2) a furrow with chevron dense menisci in the median part (five menisci per 1 cm); or (3) a ridge, 10\u0026ndash;20 mm wide, with a 1\u0026ndash;2 mm wide median crest.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePsammichnites\u003c/span\u003e Torell, \u003cspan class=\"CitationRef\"\u003e1870\u003c/span\u003e, is a locomotion and feeding burrow known from the Paleozoic shallow-marine deposits (M\u0026aacute;ngano et al. \u003cspan class=\"CitationRef\"\u003e2022\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigures\u0026nbsp;25e, f\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eSiphonichnus\u003c/span\u003e isp. Mainly in facies SF4 in the lower strata of DNBBZU.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eA horizontal subcircular section of a vertical cylindrical burrow, which is 20\u0026ndash;25 mm wide, and shows a thick wall or a mantle, which is 4\u0026ndash;5 mm wide. The mantle surrounds a central core.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eSiphonichnus\u003c/span\u003e Stanistreet et al., \u003cspan class=\"CitationRef\"\u003e1980\u003c/span\u003e, is a dwelling trace of suspension-feeding bivalves (Stanistreet et al. \u003cspan class=\"CitationRef\"\u003e1980\u003c/span\u003e; Gingras et al. \u003cspan class=\"CitationRef\"\u003e2008\u003c/span\u003e; Dashtgard \u003cspan class=\"CitationRef\"\u003e2011\u003c/span\u003e) or a pascichnion of bivalves such as tellinids (Knaust \u003cspan class=\"CitationRef\"\u003e2015\u003c/span\u003e). It is commonly found in shallow-marine and marginal-marine deposits (Pollard \u003cspan class=\"CitationRef\"\u003e1988\u003c/span\u003e), often associated with salinity fluctuations and freshwater influx (Knaust \u003cspan class=\"CitationRef\"\u003e2015\u003c/span\u003e). It is infrequently reported from deep-sea deposits (Krobicki et al. \u003cspan class=\"CitationRef\"\u003e2006\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\n \u003cdiv id=\"59\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003e\n \u003cdiv id=\"60\" class=\"btn-xs-small Annotation tooltipped\" data-position=\"top\" data-tooltip=\"\"\u003eA\u003c/div\u003eFigure\u0026nbsp;26a\n \u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eTaenidium\u003c/span\u003e isp.\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003eUpper bedding plane of tempestite sandstone beds in in MOU.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eHorizontal, subcylindrical (?), winding, meniscate burrow, which is 6\u0026ndash;7 mm wide. There are eight menisci per cm. At the termination, there is an oval, sand-filled body of the corresponding width.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eTaenidium\u003c/span\u003e Heer, \u003cspan class=\"CitationRef\"\u003e1877\u003c/span\u003e is interpreted as a locomotion and deposit-feeding trace produced by marine vermiform organisms from shallow-to-deep-sea environments (Gevers et al. \u003cspan class=\"CitationRef\"\u003e1971\u003c/span\u003e; Keighley and Pickerill \u003cspan class=\"CitationRef\"\u003e1994\u003c/span\u003e; Smith et al. \u003cspan class=\"CitationRef\"\u003e2008\u003c/span\u003e; Smith and Hasiotis \u003cspan class=\"CitationRef\"\u003e2008\u003c/span\u003e; Jackson et al. \u003cspan class=\"CitationRef\"\u003e2016\u003c/span\u003e) from the Ediacaran to the recent (e.g., Crimes \u003cspan class=\"CitationRef\"\u003e1992\u003c/span\u003e; Jenkins \u003cspan class=\"CitationRef\"\u003e1995\u003c/span\u003e; Uchman \u003cspan class=\"CitationRef\"\u003e1998\u003c/span\u003e; Jackson et al. \u003cspan class=\"CitationRef\"\u003e2016\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;26b\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e?\u003cspan class=\"Italic\"\u003eThalassinoides\u003c/span\u003e isp. Sandstone beds, facies SF6 of facies SF6 of LCHU\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eHorizontal, endichnial, branched burrow, 10\u0026ndash;20 mm wide, in which fragments are visible on a parting surface due to weathering. The branches are Y-shaped.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eThalassinoides\u003c/span\u003e Ehrenberg, \u003cspan class=\"CitationRef\"\u003e1944\u003c/span\u003e, is a semi-permanent domichnion-fodinichnion produced primarily by scavenging and deposit-feeding crustaceans (Frey et al. \u003cspan class=\"CitationRef\"\u003e1978\u003c/span\u003e, \u003cspan class=\"CitationRef\"\u003e1984\u003c/span\u003e; Schlirf \u003cspan class=\"CitationRef\"\u003e2000\u003c/span\u003e; Neto de Carvalho et al. \u003cspan class=\"CitationRef\"\u003e2007\u003c/span\u003e; Yanin and Baraboshkin \u003cspan class=\"CitationRef\"\u003e2013\u003c/span\u003e). However, cerianthid sea anemones, trilobites, or enteropneust acorn worms have also been suggested as potential producers of some Paleozoic \u003cspan class=\"Italic\"\u003eThalassinoides\u003c/span\u003e (Myrow \u003cspan class=\"CitationRef\"\u003e1995\u003c/span\u003e; Ekdale and Bromley \u003cspan class=\"CitationRef\"\u003e2003\u003c/span\u003e). It is possible that its trace makers fed on microbes growing within the burrows (Bromley \u003cspan class=\"CitationRef\"\u003e1996\u003c/span\u003e; Ekdale and Bromley \u003cspan class=\"CitationRef\"\u003e2003\u003c/span\u003e). \u003cspan class=\"Italic\"\u003eThalassinoides\u003c/span\u003e occurs in deposits of various, presumably shallow marine environments (Frey et al. \u003cspan class=\"CitationRef\"\u003e1984\u003c/span\u003e; Pemberton et al. \u003cspan class=\"CitationRef\"\u003e2001\u003c/span\u003e).\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFigure\u0026nbsp;26c\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003c/tbody\u003e\n \u003c/table\u003e\n\u003c/div\u003e\n\u003cp\u003e\u0026nbsp;\u003c/p\u003e\n\u003cdiv class=\"gridtable\"\u003e\n \u003ctable id=\"Tab3\" border=\"1\"\u003e\n \u003ccaption\u003e\n \u003cdiv class=\"CaptionNumber\"\u003eTable 3\u003c/div\u003e\n \u003cdiv class=\"CaptionContent\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eExamples of the \u003cspan class=\"Italic\"\u003eCruziana\u003c/span\u003e ichnofacies in the lower\u0026ndash;middle Permian deposits, mostly from Gondwana. * \u0026ndash; interpretation of the ichnofacies in this paper. In bold \u0026ndash; ichnogenera which occur in southern Tunisia and in other section\u003c/div\u003e\n \u003c/div\u003e\n \u003c/caption\u003e\n \u003cthead\u003e\n \u003ctr\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eLocation, formation; age; publication\u003c/div\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFacies\u003c/div\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTrace fossils\u003c/div\u003e\n \u003c/th\u003e\n \u003cth align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eIchnofacies; no igen./no igen. found in S Tunisia\u003c/div\u003e\n \u003c/th\u003e\n \u003c/tr\u003e\n \u003c/thead\u003e\n \u003ctbody\u003e\n \u003ctr\u003e\n \u003ctd rowspan=\"4\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003ePebbley Beach Fm, Sydney Basin, Australia; Lower Permian (Sakmarian\u0026ndash;Artinskian); Bann et al. (\u003cspan class=\"CitationRef\"\u003e2004\u003c/span\u003e)\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eThoroughly bioturbated siltstone: siltstone and silty mudstone with few if any preserved sedimentary structures; rare thin (\u0026lt;\u0026thinsp;1 cm), sharp-based, very fine- to fine-grained sandstone beds.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003ePhycosiphon\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePlanolites\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eRosselia socialis, R. rotates\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eTaenidium\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eZoophycos, Chondrites, Teichichnus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePalaeophycus\u003c/span\u003e \u003cspan class=\"Italic\"\u003etubularis, P. heberti, Helminthopsis, Asterosoma\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eDiplocraterion\u003c/span\u003e \u003cspan class=\"Italic\"\u003ehabichi, Skolithos\u003c/span\u003e, fugichnia\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003edistal \u003cspan class=\"Italic\"\u003eCruziana\u003c/span\u003e,\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003esome \u003cspan class=\"Italic\"\u003eSkolithos\u003c/span\u003e\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003eichnofacies elements in storms sand beds; 12/4\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eThoroughly bioturbated sandy siltstone and sandy siltstone with rare but upwardly increasing numbers of discrete, thin (0.5\u0026ndash;2 cm), very fine- to fine-grained sandstone beds. Rare synaeresis cracks, are rare, dispersed outsized clasts\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eRosselia socialis, Zoophycos, Phycosiphon\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePlanolites\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePalaeophycus\u003c/span\u003e \u003cspan class=\"Italic\"\u003etubularis, P. heberti, Teichichnus, Rhizocorallium irregulare\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eDiplocraterion\u003c/span\u003e \u003cspan class=\"Italic\"\u003ehabichi\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eTaenidium\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eRosselia rotatus, Skolithos, Bergaueria\u003c/span\u003e, fugichnia\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003earchetypal \u003cspan class=\"Italic\"\u003eCruziana\u003c/span\u003e,\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eSkolithos\u003c/span\u003e ichnofacies\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003ein tempestites; 11/4\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSparsely to moderately\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003ebioturbated interbedded bioturbated sandy siltstone and fine-grained laminated sandstone; dark mudstone beds.\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eRosselia socialis, R. rotatus, Teichichnus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePalaeophycus\u003c/span\u003e \u003cspan class=\"Italic\"\u003etubularis, P. heberti, Phycosiphon\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePlanolites\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eChondrites, Zoophycos, Rhizocorallium irregulare\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eDiplocraterion\u003c/span\u003e \u003cspan class=\"Italic\"\u003ehabichi, D. parallelum\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eTaenidium\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eConichnus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eHelminthopsis\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eSkolithos, Cylindrichnus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePsammichnites\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eMacaronichnus\u003c/span\u003e, fugichnia\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003earchetypal \u003cspan class=\"Italic\"\u003eCruziana\u003c/span\u003e, ichnofacies, \u003cspan class=\"Italic\"\u003eSkolithos\u003c/span\u003e in sandstone beds (mixed\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eSkolithos\u003c/span\u003e-\u003cspan class=\"Italic\"\u003eCruziana\u003c/span\u003e ichnofacies); 16/6\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eThoroughly bioturbated muddy sandstones; some beds laminated\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eRosselia socialis, Phycosiphon\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePlanolites\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eDiplocraterion\u003c/span\u003e \u003cspan class=\"Italic\"\u003ehabichi, Rhizocorallium irregulare, Teichichnus, Macaronichnus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePalaeophycus\u003c/span\u003e \u003cspan class=\"Italic\"\u003etubularis, P. heberti\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eTaenidium\u003c/span\u003e, ?\u003cspan class=\"Italic\"\u003eZoophycos\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eSkolithos\u003c/span\u003e, fugichnia, \u003cspan class=\"BoldItalic\"\u003ePsammichnites\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eChondrites\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eproximal \u003cspan class=\"Italic\"\u003eCruziana;\u003c/span\u003e 13/5\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd rowspan=\"2\" align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eAheimer Fm, Gulf of Suez, Egypt; Lower Permian; El Refaiy et al. (2023)\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eRippled and HCS laminated sandstones with shale intercalations\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"BoldItalic\"\u003ePlanolites\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePalaeophycus\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eZoophycos\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eSkolithos\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eThalassinoides\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eHelminthopsis\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eproximal \u003cspan class=\"Italic\"\u003eCruziana;\u003c/span\u003e 6/3\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eHeterolithic cross bedded sandstones and mudstones, fossiliferous dolomitic sandstones, siltstones, and sandy dolomites, HCS laminated sandstones and siltstones\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"BoldItalic\"\u003ePlanolites\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePalaeophycus\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eZoophycos\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eSkolithos\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eThalassinoides\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eHelminthopsis\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eCruziana\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eRusophycus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePhycodes\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eRhizocorallium, Gordia, Circulichnis\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eProtovirgularia\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eSchaubcylindrichnus\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003earchetypal \u003cspan class=\"Italic\"\u003eCruziana;\u003c/span\u003e 14/7\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTwin Bores, section, Mungadan Sandstone Fm, Carnarvon Basin, W Australia; Middle Permian: Guadalupian; Feng et al. (\u003cspan class=\"CitationRef\"\u003e2021\u003c/span\u003e)\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eIntensely bioturbated or cross-stratified sandstones, or planar laminated siltstones\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eChondrites\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eCruziana\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eCurvolithus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePalaeophycus\u003c/span\u003e, \u003cspan class=\"Italic\"\u003ePaleodictyon\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eParataenidium\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePhycodes\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePlanolites\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePsammichnites\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eRosselia, Rusophycus, Skolithos\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eTaenidium\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eThalassinoides\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eZoophycos\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eCruziana;\u003c/span\u003e 15/8\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTeresina Fm, Rio Grande do Sul State,S Brazi; Upper Permian; Lima and Netto (\u003cspan class=\"CitationRef\"\u003e2012\u003c/span\u003e)\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eMudstones, fine-grained heterolithic deposits, sandstone with climbing ripple lamination, sandstone with trough cross-stratification, and sandstone with HCS and SCS lamination\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eBergaueria, Cochlichnus\u003c/span\u003e cf. \u003cspan class=\"Italic\"\u003eanguineus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eCruziana\u003c/span\u003e \u003cspan class=\"Italic\"\u003eproblematica\u003c/span\u003e, cf. \u003cspan class=\"BoldItalic\"\u003eDiplocraterion\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eDiplopodichnus biformis\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eHelminthopsis\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eLockeia siliquaria, Multina arcuata, Oldhamia\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePalaeophycus\u003c/span\u003e \u003cspan class=\"Italic\"\u003estriatus, P. tubularis, Phymatoderma burkei\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePlanolites\u003c/span\u003e \u003cspan class=\"Italic\"\u003ebeverleyensis, P. montanus, Teichichnus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eThalassinoides\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eCruziana;\u003c/span\u003e 14/6\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eBroughton Fm, Sydney Basin, SE Australia; Middle Permian (uppermost Wordian\u0026ndash;lower Capitanian; Luo et al. (\u003cspan class=\"CitationRef\"\u003e2017\u003c/span\u003e)\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eFine to medium-grained sandstone alternated with\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003esiltstone\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eMacaronichnus, Palaeophycus\u003c/span\u003e,\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"BoldItalic\"\u003ePsammichnites\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eProtovirgularia\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eRosselia, Teichichnus\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eCruziana*;\u003c/span\u003e 6/2\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eKapp Starostin Fm, central Spitsbergen; Svalbard; Permian: Artinskian\u0026ndash;?Changhsingian; Uchman et al. (\u003cspan class=\"CitationRef\"\u003e2016\u003c/span\u003e)\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003echert/cherty shale and spiculites with rare intercalations of glauconitic sandstone, limestones in the lower part\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eArenicolites, Chondrites\u003c/span\u003e, cf. \u003cspan class=\"Italic\"\u003eCylindrichnus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eHelminthopsis\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eMacaronichnus segregatis\u003c/span\u003e,\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"BoldItalic\"\u003eNereites\u003c/span\u003e \u003cspan class=\"Italic\"\u003emissouriensis\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePalaeophycus\u003c/span\u003e, cf. \u003cspan class=\"Italic\"\u003ePhycosiphon incertum\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003ePlanolites\u003c/span\u003e,\u003c/div\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eTeichichnus\u003c/span\u003e, \u003cspan class=\"BoldItalic\"\u003eThalassinoides\u003c/span\u003e, \u003cspan class=\"Italic\"\u003eZoophycos\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eCruziana;\u003c/span\u003e12/5\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003ctr\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eTebaga of Medenine, S Tunisia; middle\u0026ndash;upper Permian; this paper\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003eSandstones, shales, marls between carbonate buildups\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Bold\"\u003e?\u003c/span\u003e\u003cspan class=\"BoldItalic\"\u003eAncorichnus, Archaeonassa, Cruziana\u003c/span\u003e, \u003cspan class=\"Bold\"\u003e?\u003c/span\u003e\u003cspan class=\"BoldItalic\"\u003eDiplocraterion\u003c/span\u003e, \u003cspan class=\"Bold\"\u003e?\u003c/span\u003e\u003cspan class=\"BoldItalic\"\u003eGyrophyllites, Halopoa\u003c/span\u003e, \u003cspan class=\"Bold\"\u003e?\u003c/span\u003e\u003cspan class=\"BoldItalic\"\u003eHelminthopsis\u003c/span\u003e, \u003cspan class=\"Bold\"\u003e?\u003c/span\u003e\u003cspan class=\"BoldItalic\"\u003eNereites, Palaeophycus, Parataenidium, Phycodes, Planolites, Protovirgularia, Psammichnites, Siphonichnus, Taenidium\u003c/span\u003e, \u003cspan class=\"Bold\"\u003e?\u003c/span\u003e\u003cspan class=\"BoldItalic\"\u003eThalassinoides\u003c/span\u003e\u003c/div\u003e\n \u003c/td\u003e\n \u003ctd align=\"left\"\u003e\n \u003cdiv class=\"SimplePara\"\u003e\u003cspan class=\"Italic\"\u003eCruziana\u003c/span\u003e, with transition to its proximal or distal variants*; 17/17\u003c/div\u003e\n \u003c/td\u003e\n \u003c/tr\u003e\n \u003c/tbody\u003e\n \u003c/table\u003e\n\u003c/div\u003e\n\u003cp\u003e\u0026nbsp;\u003c/p\u003e"}],"fulltextSource":"","fullText":"","funders":[],"hasAdminPriorityOnWorkflow":false,"hasManuscriptDocX":true,"hasOptedInToPreprint":true,"hasPassedJournalQc":"","hasAnyPriority":false,"hideJournal":false,"highlight":"","institution":"","isAcceptedByJournal":true,"isAuthorSuppliedPdf":false,"isDeskRejected":"","isHiddenFromSearch":false,"isInQc":false,"isInWorkflow":false,"isPdf":false,"isPdfUpToDate":false,"isWithdrawnOrRetracted":false,"journal":{"display":true,"email":"[email protected]","identity":"facies","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"faci","sideBox":"Learn more about [Facies](http://link.springer.com/journal/10347)","snPcode":"10347","submissionUrl":"https://www.editorialmanager.com/faci/default2.aspx","title":"Facies","twitterHandle":"","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"em","reportingPortfolio":"Springer Hybrid","inReviewEnabled":true,"inReviewRevisionsEnabled":false},"keywords":"Facies, Ichnofacies, Carbonate platform, Permian, Southern Tunisia, Gondwana","lastPublishedDoi":"10.21203/rs.3.rs-5706272/v1","lastPublishedDoiUrl":"https://doi.org/10.21203/rs.3.rs-5706272/v1","license":{"name":"CC BY 4.0","url":"https://creativecommons.org/licenses/by/4.0/"},"manuscriptAbstract":"\u003cp\u003eThe present study investigates the Permian mixed siliciclastic-carbonate system of southern Tunisia and describes the trace fossils recorded within the siliciclastic intervals. The carbonate facies represent a spectrum of depositional environments ranging from the outer shelf (CF1), through the shelf margin (CF2), to the middle to inner shelf (CF3 to CF6) settings, while CF7 corresponds to conglomeratic facies resulting from reef destruction. The siliciclastic facies (SF1 to SF9) developed on a ramp profile, while the latest Permian facies (SF10 to SF14) belong to a dominantly meandering fluvial system with flood plain red-beds.\u003c/p\u003e \u003cp\u003eThis work provides the first comprehensive review of trace fossils in this region. Seventeen ichnogenera produced by bivalves, trilobites, crustaceans, and vermiform organisms have been identified. In addition to being very common, facies-crossing ichnogenera, such as \u003cem\u003ePlanolites\u003c/em\u003e or \u003cem\u003ePalaeophycus\u003c/em\u003e, \u003cem\u003ePsammichnites\u003c/em\u003e, \u003cem\u003eProtovirgularia\u003c/em\u003e, \u003cem\u003eParataenidium\u003c/em\u003e, \u003cem\u003eThalassinoides\u003c/em\u003e, and \u003cem\u003eTaenidium\u003c/em\u003e appear to be more specific components of the Permian \u003cem\u003eCruziana\u003c/em\u003e ichnofacies.\u003c/p\u003e \u003cp\u003eThe combination of facies analysis and ichnofacies distribution demonstrates that the sedimentary evolution encompasses the alternation of two dominant depositional regimes represented by mixed siliciclastic-carbonate ramp sedimentation and rimmed carbonate platforms dominated by reefal development. The vertical transition from ramp to rimmed carbonate platform and vice versa reflects periodic variations in carbonate sedimentation rates, primarily controlled by sea-level fluctuations, subsidence, and resulting accommodation space, and climatic and palaeoecological conditions.\u003c/p\u003e \u003cp\u003eSurface-to-subsurface stratigraphic correlation indicates that the subsidence played an important role in shaping the basin configuration comprising a shelf margin domain (Tebaga outcrops) separating a wide middle to inner shelf to the south from a rapidly subsiding depocenter to the north. The latter interpreted as a foredeep setting, accumulated over 4000 m of sediment, including thin turbiditic sandstones, carbonate breccias, and conglomerates derived from the adjacent rimmed platform.\u003c/p\u003e","manuscriptTitle":"New insights on the Permian mixed siliciclastic and carbonate deposits of southern Tunisia: Facies, ichnofacies and depositional environments","msid":"","msnumber":"","nonDraftVersions":[{"code":1,"date":"2025-04-23 09:06:15","doi":"10.21203/rs.3.rs-5706272/v1","editorialEvents":[{"type":"communityComments","content":0},{"type":"reviewerAgreed","content":"","date":"2025-04-22T10:34:00+00:00","index":0,"fulltext":""},{"type":"reviewersInvited","content":"","date":"2025-04-22T10:29:46+00:00","index":"","fulltext":""},{"type":"editorAssigned","content":"","date":"2025-04-18T11:01:38+00:00","index":"","fulltext":""},{"type":"submitted","content":"Facies","date":"2025-04-17T17:44:31+00:00","index":"","fulltext":""},{"type":"decision","content":"Minor Revision","date":"2025-01-23T12:41:46+00:00","index":"","fulltext":""}],"status":"published","journal":{"display":true,"email":"[email protected]","identity":"facies","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":false,"externalIdentity":"faci","sideBox":"Learn more about [Facies](http://link.springer.com/journal/10347)","snPcode":"10347","submissionUrl":"https://www.editorialmanager.com/faci/default2.aspx","title":"Facies","twitterHandle":"","acdcEnabled":true,"dfaEnabled":true,"editorialSystem":"em","reportingPortfolio":"Springer Hybrid","inReviewEnabled":true,"inReviewRevisionsEnabled":false}}],"origin":"","ownerIdentity":"2c8efbe2-6263-424a-9f12-9a0e9f93f607","owner":[],"postedDate":"April 23rd, 2025","published":true,"recentEditorialEvents":[],"rejectedJournal":[],"revision":"","amendment":"","status":"published-in-journal","subjectAreas":[],"tags":[],"updatedAt":"2025-06-30T16:01:19+00:00","versionOfRecord":{"articleIdentity":"rs-5706272","link":"https://doi.org/10.1007/s10347-025-00704-6","journal":{"identity":"facies","isVorOnly":false,"title":"Facies"},"publishedOn":"2025-06-27 15:57:43","publishedOnDateReadable":"June 27th, 2025"},"versionCreatedAt":"2025-04-23 09:06:15","video":"","vorDoi":"10.1007/s10347-025-00704-6","vorDoiUrl":"https://doi.org/10.1007/s10347-025-00704-6","workflowStages":[]},"version":"v1","identity":"rs-5706272","journalConfig":"researchsquare"},"__N_SSP":true},"page":"/article/[identity]/[[...version]]","query":{"redirect":"/article/rs-5706272","identity":"rs-5706272","version":["v1"]},"buildId":"8U1c8b4HqxoKbykW_rLl7","isFallback":false,"isExperimentalCompile":false,"dynamicIds":[84888],"gssp":true,"scriptLoader":[]}