1. Introduction
The Rhaetian (205.7 ± 0.4–201.4 ± 0.2 Ma; Gradstein et al. Reference Gradstein, Ogg, Schmitz and Ogg2020) is the final stage of the Triassic, during which a continental-scale marine transgression occurred over much of Europe (Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018; Lovegrove et al. Reference Lovegrove, Newell, Whiteside and Benton2021). This caused dramatic changes in the resulting deposits, since the depositional environments evolved from terrestrial to shallow marine environments (Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018; Lovegrove et al. Reference Lovegrove, Newell, Whiteside and Benton2021). In the UK, the long-term continental red-bed deposits of the Mercia Mudstone Group transitioned upward into the partially marine deposits of the Blue Anchor Formation, and then the fully marine units of the succeeding Penarth Group (Lovegrove et al. Reference Lovegrove, Newell, Whiteside and Benton2021). Faunas from the Rhaetian are dominated by marine taxa that occupied the epicontinental seas, with terrestrial reptiles and synapsids limited to the various islands remaining above sea level (Whiteside et al. Reference Whiteside, Duffin, Gill, Marshall and Benton2016; Lovegrove et al. Reference Lovegrove, Newell, Whiteside and Benton2021).
These marine Rhaetian faunas (Duffin Reference Duffin, Swif and Martill1999; Storrs Reference Storrs, Swift and Martill1999) include chondrichthyan fishes (hybodonts and neoselachians), Osteichthyan fishes (actinopterygians, including teleosts, and sarcopterygians, such as lungfishes and coelacanths) and marine reptiles (ichthyosaurs, plesiosaurs, placodonts and thalattosaurs). These faunas are mainly preserved in bone beds, and these are common throughout the British marine Rhaetian (Suan et al. Reference Suan, Föllmi, Adatte, Bomou, Spangenberg and Schootbrugge2012). These Upper Triassic deposits are mainly found in localities in the SW of England, around Bristol (Agassiz 1835; Foffa et al. Reference Foffa, Whiteside, Viegas and Benton2014; Allard et al. Reference Allard, Carpenter, Duffin and Benton2015; Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018), in the Mendips (Nordén et al. Reference Nordén, Duffin and Benton2015; Moreau et al. Reference Moreau, Duffin, Hildebrandt, Hutchinson, Parker, Carpenter and Benton2021; Ronan et al. Reference Ronan, Duffin, Hildebrandt, Parker, Hutchinson, Copp and Benton2020), in north Somerset (Richardson Reference Richardson1911; Tayler et al. Reference Tayler, Duffin, Hildebrandt, Parker and Benton2023), Devon (Korneisel et al. Reference Korneisel, Gallois, Duffin and Benton2015) and south Wales (Suan et al. Reference Suan, Föllmi, Adatte, Bomou, Spangenberg and Schootbrugge2012; Williams et al. Reference Williams, Duffin, Hildebrandt, Parker, Hutchinson and Benton2022).
In Somerset, these marine Rhaetian deposits are particularly well exposed along the north coast, on the shore near Watchet, in a section from Blue Anchor Point to Lilstock (Sykes Reference Sykes1977; Warrington & Whittaker Reference Warrington and Whittaker1984). Blue Anchor Point is thus at the western extremity of the exposure of these marine deposits (Figure 1). This is also the type locality of the Blue Anchor Formation, corresponding to the uppermost part of the Mercia Mudstone Group (Warrington et al. Reference Warrington, Audley-Charles, Elliott, Evans, Ivimey-Cook, Kent, Robinson, Shotton and Taylor1980; Warrington & Whittaker Reference Warrington and Whittaker1984).
Figure 1. Geological map of Blue Anchor Bay. The red dot indicates the location of the bone beds sampled. © Crown Copyright and Database Right 2023 Ordnance Survey (Digimap Licence).
Here, we describe the microvertebrate remains found in the two bone beds at Blue Anchor Bay, the Basal Bone-Bed and an upper bone bed mentioned by Richardson (Reference Richardson1911). These are significant as the succession here marks the type section of the Blue Anchor Formation, and was part of the supporting geological sections used to make the case that the St Audrie’s Bay section nearby should be the Global Stratigraphic Section and Point (GSSP) for the Triassic–Jurassic boundary (Warrington et al. Reference Warrington, Cope and Ivimey-Cook1994).
2. Geological setting
The Penarth Group is well exposed on the foreshore at low tide and in the cliffs at Blue Anchor Point (ST 04048 43773), north Somerset (Figures 1 and 2). The succession spans the upper part of the Mercia Mudstone Group and most of the Penarth Group, terminating in the lower part of the Hettangian, thus encompassing the Triassic–Jurassic boundary (Richardson Reference Richardson1911). All these Mesozoic deposits are disrupted by a series of normal faults, forming part of the classic view (Figure 2A) of Blue Anchor Point. Among these faults, the westernmost is the main fault (Glen et al. Reference Glen, Hancock and Whittaker2005, figure 9c), and west of this main fault, the cliff comprises the red beds of the Mercia Mudstone Group. The Blue Anchor Formation and Penarth Group beds to the east of the main fault are slightly folded (Richardson Reference Richardson1911), with the anticlinal axis pointing towards the foreshore, confirming that the deposits of the cliff and the foreshore were once contiguous, forming a single deposit (Figure 2A).
Figure 2. Field photographs at Blue Anchor Point. (A) Overview of the cliffs showing the faults. (B) Field photograph of a fallen rock showing pink gypsum veins. (C) Field photograph of the basal bone bed on the foreshore. (D) Field photograph of the upper bone bed and Pleurophorus bed on the foreshore. Abbreviations: BBB: basal bone bed; PB: Pleurophorus bed; RC: rip-up clast; SB: Sully bed; UBB: upper bone bed. Limits of beds are indicated by the black segments.
The first geological account of the Blue Anchor location was by Horner (Reference Horner1816, pp. 366–372), who reported high cliffs up to 100 feet (30 m) high on the coast between Minehead and the River Parrett, and reported alternations of the red siltstones (Mercia Mudstone Formation) and the ‘lyas’ (Rhaetian plus Early Jurassic), but he divined correctly that this appearance had been generated by faults (‘dislocations’, as he calls them). He walked from the River Parrett in the east, and encountered the Lias on the shore at Lilstock, and walked past Watchet to Blue Anchor Bay, which marks the western extent of these units. He noted the way in which the bedding of the Rhaetian and Lias shows up as great sweeping ridges of rock across the rocky shore, and he reported ammonites and other typical Lower Jurassic fossils. He reports black shales, some with bituminous contents, but it is not clear that he encountered the Rhaetian bone bed.
Eight years later, a more professional study was published by Buckland and Conybeare (Reference Buckland and Conybeare1824). There they presented a map and categorized the stratigraphy. They reported the Triassic and Jurassic of the north Somerset coastline (Buckland & Conybeare Reference Buckland and Conybeare1824, pp. 298–301), and identified black-coloured shales beneath the regular Lias, presumably what we call now the Westbury Formation. They matched these black shales, and especially their bone beds to similar occurrences they had seen at Aust and Westbury Garden Cliff (see also Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018; Williams et al. Reference Williams, Duffin, Hildebrandt, Parker, Hutchinson and Benton2022). In a lengthy footnote, they note that the bone bed had been identified first by Robert Anstice ‘near Watchet’, (see Duffin Reference Duffin2009, p. 107) but they do not specify exactly where, whether to the east (Doniford, Lilstock) or west (Blue Anchor Bay) of the town, but more probably to the east, and we describe further historical detail in our account of Doniford Bay (Tayler et al. Reference Tayler, Duffin, Hildebrandt, Parker and Benton2023).
The locality was then studied by De la Beche (Reference De la Beche1839, pp. 196, 232) who reported the Mercia Mudstones and Lias along the coast and inland, from St Decumans past Watchet to Blue Anchor Bay. He noted the gypsum in the red beds portions of the Mercia Mudstones Group, and the overlying ‘variegated marls’ (Blue Anchor Formation), and the Lias above that, but did not refer to the black shales (Westbury Beds) or the bonebed at the base.
Some 20 years later, the Rhaetian was widely recognized as a distinct temporal unit but termed the ‘Zone of Avicula contorta’ by Wright (Reference Wright1860) in his detailed review of many of the classic sections around Bristol and south Wales. This succession included all the mudstones and marls between the red Keuper marls (Mercia Mudstone Group) and the White Lias, and Wright did assign these to the uppermost Triassic. Wright (Reference Wright1860, p. 336) drew attention to the bone bed at Watchet but did not comment on Blue Anchor Bay in particular. Boyd Dawkins (Reference Boyd Dawkins1864) extended that work with evidence from his visits to the sections around Watchet, including to the west of that town, even though he did not refer to Blue Anchor Bay. He equated the ‘Zone of Avicula contorta’ with the Rhaetic of Germany, and reported his fossil finds. In particular, he reported a bone bed in the Williton Member (Sully Beds), below the base of the Westbury Formation, and a fossil he found ten feet under this basal bone bed, comprising common Rhaetian fish taxa and a mammal tooth on which he based the mammal species Hypsiprymnopsis rhaeticus. However, the tooth has been lost, and it remains a tantalizingly early mammal record that has not been replicated since either here or elsewhere.
The first detailed stratigraphic description at Blue Anchor Bay was by Richardson (Reference Richardson1911), who identified on the shore four bone beds from the Westbury Formation and named three of them (Figure 3A). He also reported the vertebrate remains from the Blue Anchor Formation mentioned by Boyd Dawkins. Despite the description of these bone beds, only sporadic studies of the assemblages have been made since then. Thus, Sykes (Reference Sykes1974) found two teeth of the shark Pseudodalatias barnstonensis (Sykes Reference Sykes1971) at Blue Anchor Point. Hamilton and Whittaker (Reference Hamilton, Whittaker and Savage1977) also reported common Rhaetian fish assemblages, together with plesiosaur vertebrae. Further, a number of sarcopterygian remains have been found on the shore, including the gular plate of an indeterminate coelacanth in a bone bed from the Westbury Formation (Hauser & Martill Reference Hauser and Martill2013), and a partially articulated skeleton of the dipnoan ?Ceratodus sp. also from the Westbury Formation (Duffin Reference Duffin, Swif and Martill1999). An important reptile discovery from the basal Westbury Formation bone bed is the thalattosaur Pachystropheus rhaeticus based on vertebrae and limb bones from here and from Westbury Garden Cliff in Gloucestershire (E. von Huene Reference Huene1935; Storrs Reference Storrs1993; Storrs & Gower Reference Storrs and Gower1993; Storrs et al. Reference Storrs, Gower and Large1996).
Figure 3. Stratigraphic logs of the section on the foreshore at Blue Anchor Point. (A) Section described by Richardson (Reference Richardson1911). (B) Section described by C. Duffin in his unpublished PhD thesis in 1980.
Since the cliff is difficult to access (Richardson Reference Richardson1911) and the Rhaetian horizons are often covered by banked beach shingle, the Penarth Group of Blue Anchor Point has mainly been studied from exposures on the foreshore. Nonetheless, the cliff is the location of the type section of the Blue Anchor Formation, the uppermost part of the Mercia Mudstone Group (Warrington et al. Reference Warrington, Audley-Charles, Elliott, Evans, Ivimey-Cook, Kent, Robinson, Shotton and Taylor1980; Warrington & Whittaker Reference Warrington and Whittaker1984). On the shore, the uppermost part of the Blue Anchor Formation and the basal part of the Penarth Group, the Westbury Formation, are represented by a series of limestone beds separated by black shales beds of various thickness. Richardson (Reference Richardson1911, pp. 15–20) made the first detailed stratigraphic log (Figure 3A), reproduced by Edwards (Reference Edwards1999, figure 26, 27). Our stratigraphic log (Figure 3B) was made by C. Duffin in his unpublished PhD thesis in 1980, supplemented with our field observations in 2023.
The differences between the two logs (Figure 3A, B) can be explained by the fact that the beds are not continuous, and that the logs were made in slightly different locations, also including Richardson’s (1911) observations from the cliff, and with 69 years of erosion separating the two observations. This erosion is important at Blue Anchor Point, since storms regularly occur, pulling off parts of the cliff. This was reported by Edwards (Reference Edwards1999), who specified that rocks fell from the cliff in a storm in 1996 after he took the photographs he presented. Such fallen rocks, of various sizes, sometimes more than 1 m across, cover some parts of the shore under the cliffs, and some of them contain vertebrate remains in bone beds (Figure 2B). These remains can measure dozens of centimetres, but the fact that their stratigraphic origin is uncertain lowers their scientific interest.
Among the beds found on the foreshore, two bone beds with millimetre-size vertebrate remains can easily be found low in the Westbury Formation, although Richardson (Reference Richardson1911) mentioned four such bone beds. We identify his basal Westbury Formation bone bed, and a second bone bed 5 m higher, but could not identify the other two bone beds, including that named ‘The Clough’ (Richardson Reference Richardson1911, bed 27), which Sykes (Reference Sykes1977) also failed to find.
The lower bone bed is the Basal Bone-Bed (bed 33 in Richardson Reference Richardson1911) at the base of the Westbury Formation. It lies on the upper surface of the Blue Anchor Formation, which is eroded and bioturbated by Thalassinoides burrows (Figure 2C). These burrows are filled with deposits of the Basal Bone-Bed, as depicted by Korneisel et al. (Reference Korneisel, Gallois, Duffin and Benton2015, figure 8) from Charton Bay, Devon. The bone bed also contains rip-up cream-coloured pebbles from the Sully Bed, the uppermost unit of the Blue Anchor Formation, suggesting deposition during storm events (Figure 2C).
The upper bone bed is Richardson’s (Reference Richardson1911) bed 15, ‘The Bone-Bed’, situated just under the Pleurophorus bed (bed 13 in Richardson Reference Richardson1911), whose Pleurophorus shell remains make it easy to recognize. This upper bone bed (Figure 2D) comprises layers of hard, grey, calcareous sandstones (Richardson Reference Richardson1911) that are finer grained and more clay-rich at the base and coarsen upwards. Quartz grains from the base show solution pits whereas those from higher parts of the bone bed show euhedral quartz overgrowths that formed after deposition in the more porous conditions there (Antia & Sykes Reference Antia and Sykes1979). Apart from the microfossils, we identified marcasite crystals in the bone bed, indicating euxinic deposition conditions.
The underlying Blue Anchor Formation at and east of Blue Anchor Bay was described in detail by Mayall (Reference Mayall1981). In particular, he wrote about the Sully Beds of north Somerset and Penarth in South Wales, renamed by him the Williton Member, a unit varying in thickness from 0 to 3 m. Although it is named after the village Williton, near St Audries Bay, Mayall (Reference Mayall1981, pl. 1) illustrated some key features from Blue Anchor Bay, including the base of the unit, marked by Diplocraterion burrows, as well as trace fossils throughout, bivalves, and some horizons with mud cracks. All evidence shows that, as long suspected, the Williton Member was deposited in a fully marine environment.
More recently, when St Audrie’s Bay was a candidate GSSP for the Triassic–Jurassic boundary, highly detailed studies of the stratigraphy of the Penarth and Lias groups along the whole north Somerset section, including Blue Anchor Bay, were completed, providing a thorough basis for comparison of the succession to the international standard stratigraphic scale, according to biostratigraphy (dinoflagellates, ammonites), stable isotopes and magnetostratigraphy (e.g. Hesselbo et al. Reference Hesselbo, Robinson and Surlyk2004; Hounslow et al. Reference Hounslow, Posen and Warrington2004; Korte et al. Reference Korte, Hesselbo, Jenkyns, Rickaby and Spötl2009; Bonis et al. Reference Bonis, Ruhl and Kürschner2010).
3. Materials and methods
The microfossils studied here come from both bone beds. We studied three rock samples, two from the basal Westbury Formation bone bed, and one from the upper bone bed, the first collected in 2019 and the other two in 2023. In the lower bone bed, millimetre-sized fish remains can be seen with the naked eye in the sediment, which comprises greyish gritty calcareous sandstones with cream-coloured mudstone lenses. The upper bone bed sample is also a calcareous sandstone but appears more massive and with more concentrated microvertebrate remains.
The samples were processed according to standard methods as in other studies (e.g. Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018). They were put in a 2 L acid bath made of acetic acid (5% volume concentration in water) with sodium carbonate (7.5 g.L−1) and tri-calcium di-orthophosphate (2 g.L−1) acting as a buffer to protect the fossils from acid digestion. After immersion for 48 hours, the resulting fragments were washed with water through a series of sieves with meshes of 2 mm, 500 μm and 180 μm to separate them from the finer clay fraction which is washed away. The 500 μm and 180 μm fragments where then gathered and dried separately and the 2 mm portion was processed a second time following the same protocol, and this was repeated until all the matrix of the rock samples was fragmented into pieces smaller than 2 mm.
The microfossils were then picked from the 500 μm and 180 μm samples under a Nikon SMZ445 C-LEDS stereomicroscope. When possible, fossil specimens were identified and sorted by species and type (tooth, scale, bone), and the best-preserved specimens were photographed. Identified specimens were also counted in the same way as in other studies (e.g. Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018). Thus, Rhomphaiodon minor teeth were counted when there was at least the central cusp with a part of the root. For Lissodus minimus teeth, they were counted when the central cusp was present with the labial node. All Parascylloides turnerae teeth were counted, given the fact they all had an intact central cusp. Synechodus rhaeticus and Pseudodalatias barnstonensis teeth were too fragmentary to be counted. For osteichthyan teeth, Gyrolepis albertii, Birgeria acuminata and Saurichthys longidens teeth were counted when the apical cap was present with at least a portion of the shaft. For Lepidotes sp. and Sargodon tomicus, teeth were counted when they had their cap unbroken with shaft. For other remains, all identified specimens were counted. All specimen photographs were taken with a Leica M205C microscope using multifocus photography methods provided by the Leica Application Suite v4.12. These images were then processed with GIMP v2.10.34 software to remove the background and adjust the colour balance.
4. Systematic palaeontology
4.a. Chondrichthyes
4.a.1. Lissodus minimus (Agassiz, Reference Agassiz1839)
A total of 86 specimens were found (Figure 4A–D), 66 from the upper bone bed and 20 from the basal bone bed. Only crowns of teeth have been found, most of them incomplete. These narrow crowns consist of a small flattened central cusp, sometimes flanked by a pair of lateral cusplets. The crown is ornamented with ridges that are generally perpendicular to the cutting edge, running from this edge to the base of the crown. A labial node is also present at the base of the central cusp.
Figure 4. Chondrichthyan teeth from the upper and basal bone beds at Blue Anchor Point. (A, B) Lissodus minimus anterolateral teeth: (A) BRSUG 29974-26 in occlusal view; (B) BRSUG 29974-23 in labial view. (C) Lissodus minimus anterior tooth BRSUG 29974-25 in labial view. (D) Lissodus minimus lateral tooth BRSUG 29974-66 in occlusal view. (E–I) Rhomphaiodon minor teeth: (E, F) BRSUG 29974-28 in lingual (E), and occlusal (F) views; (G) BRSUG 29974-31 in labial view; (H) BRSUG 29974-27 in lingual view; (I) BRSUG 29974-29 in occlusal view. (J, K) Parascylloides turnerae teeth: (J) BRSUG 29974-39 in labial view; (K) BRSUG 29974-40 in occlusal view. (L) Synechodus rhaeticus tooth BRSUG 29974-32 in labial view. (M) Pseudodalatias barnstonensis lower tooth fragment BRSUG 29974-43 in labial or lingual view. (N, O) ?Pseudocetorhinus pickfordi lateral teeth: (N) BRSUG 29974-182 in lateral view; (O) BRSUG 29974-190 in lateral view. Scale bar: 1 mm, except for K, N and O: 500 µm.
There are variable tooth types present in the heterodont dentition, and we have identified complete anterior, anterolateral and lateral teeth, but only incomplete posterolateral and posterior teeth. The most common teeth are anterolateral teeth, often lacking both lateral extremities.
4.a.2. Rhomphaiodon minor (Agassiz, 1837)
This species (Figure 4E–I) has been found in both the upper (41 teeth) and basal bone beds (12 teeth). Complete teeth are symmetrical, and their crowns consist of a row of an odd number of cusps, with the cusps being taller towards the centre. The central cusp is generally significantly larger than the lateral cusplets. The cusps are conical, slightly flattened labio-lingually, and their apices are generally slightly curved lingually. The cusps are also ornamented on both faces with strong, widely spaced ridges from the base of the cusps almost to the tip. The crown is supported by a root that expands lingually and presents a number of foramina on both lingual and labial faces.
Four more teeth (with one from the basal bone bed) could also belong to R. minor or perhaps to ‘Hybodus’ cloacinus Quenstedt, Reference Quenstedt1858. There is a debate about this last species, sometimes referred to as Polyacrodus cloacinus, the generic allocation remaining uncertain (Skinner et al. Reference Skinner, Whiteside and Benton2020).
4.a.3. Parascylloides turnerae Thies et al., Reference Thies, Vespermann and Solcher2014
Five teeth of this species have been found (Figure 4J, K), with only one from the basal bone bed. The teeth consist of an elongate, massive and symmetrical central cusp, flanked by two small lateral cusplets whose bases are fused with the main cusp base. The central cusp is curved lingually, and both its labial and lingual faces have widely spaced ridges originating at the base and extending almost up to the tip. The root of the tooth extends lingually, giving it a laterally flattened ovoid shape in basal view. A few foramina are present on the labial and lingual faces of the root.
The species was first described from teeth from a railway cutting near Barnstone, Nottinghamshire (England) and three localities in the Federal State of Lower Saxony (Germany), all of Rhaetian age (Thies et al. Reference Thies, Vespermann and Solcher2014). The species has since been recorded in two other localities of the Rhaetian of England, at Aust Cliff, Gloucestershire (Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018) and Saltford, Somerset (Moreau et al. Reference Moreau, Duffin, Hildebrandt, Hutchinson, Parker, Carpenter and Benton2021). Whiteside and Duffin (Reference Whiteside and Duffin2021) also mentioned its occurrence at a new locality near the ‘Microlestes’ Quarry of Holwell, Somerset. Our discovery of Parascylloides turnerae in the basal bone bed at Blue Anchor Point is thus the fifth confirmed occurrence of the taxon in the UK.
4.a.4. Synechodus rhaeticus (Duffin, Reference Duffin1982)
Only one tooth of this species has been found in the upper bone bed (Figure 4L). It consists of the lateral portion of a tooth, presenting a crown with three thick, pointed and flattened cusplets in a row, supported by a root of similar size. The cusplets are ornamented by a few thick ridges that extend from the apex to the middle of the crown, where a row of labial nodes is located, each node being located beneath a cusplet.
4.a.5. Pseudodalatias barnstonensis Sykes, Reference Sykes1971
Only a portion of a lower tooth of this species has been found, from the upper bone bed (Figure 4M). This specimen corresponds to the upper part of the crown. Complete teeth of this species have a triangular shape, with a thin serrated cutting edge, but only one side of the cutting edge with one serration is present in our specimen.
4.a.6. ?Pseudocetorhinus pickfordi Duffin, Reference Duffin1998a
Four sharks’ teeth with an atypical shape have been found in the basal bone bed. Three of them (Figure 4N) have a crown resembling morph 2 placoid scales (see below), with a sloping labial face with a drop-like shape ornamented with at least three bulging ridges running from the lower part of this face to its apex. Beneath this crown an elongate, cylindrical root is present, with no ornamentation. In a further specimen (Figure 4O), the root is similar, but the crown is pointed and much more elongated, bending lingually. Some ridges are also present, but they are less bulging and do not extend towards the apex, being confined to the labial base of the crown. Most of the crown is thus unornamented.
Because this last specimen has an elongate, pointed and unornamented crown, and resembles the three other specimens, but with a more developed crown, the four specimens are attributed with some trepidation to Pseudocetorhinus pickfordi. The four specimens would likely be lateral teeth.
4.a.7. Other chondrichthyan remains
Two neoselachian vertebrae have been found in the upper bone bed (Figure 5A, B). They have a cylindrical shape with a concave lateral face and are only slightly eroded.
Figure 5. Chondrichthyan denticles and vertebrae. (A, B) Neoselachian vertebra BRSUG 29974-10 in anterior or posterior (A) and lateral (B) views. (C) Miscellaneous denticle BRSUG 29974-77 in lateral view. (D, E) Morphotype 1 placoid denticles: (D) BRSUG 29974-178 in anterior view; (E) BRSUG 29974-76 in lateral view. (F) Morphotype 2 placoid denticle BRSUG 29974-180 in anterior view. (G) Morphotype 3 placoid denticle BRSUG 29974-183 in exterior view. (H) Morphotype 4 placoid denticle BRSUG 29974-185 in anterolateral view. (I–L) Hybodontid denticles: (I, J) BRSUG 29974-9 in exterior (I) and anterior or posterior (J) views; (K) BRSUG 29974-81 in exterior view; (L) BRSUG 29974-79 in exterior view. Scale bar: 1 mm, except A and B: 2 mm, and D-H: 500 µm.
4.a.8. Denticles
Seventy-two denticles have been found. Among them, three denticles from the basal bone bed possessing a thick, tall and rounded base and a flat and circular crown (Figure 5C) have not been assigned to a specific denticle type. The other denticles are sorted based on the classification proposed by Reif (Reference Reif1978), and each type is further described in the following subsections.
4.a.8.a. Placoid scales
A total of 66 placoid scales have been found, with only three from the upper bone bed. Two of them are fragmentary, one being a denticle base and the other an incomplete crown. This incompleteness made them impossible to classify more precisely. Among the other specimens, that comprise most of the crown when they are not complete, four morphotypes have been found.
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Morphotype 1 (Figure 5D, E) is the most abundant type with 48 specimens, three from the upper bone bed. They correspond to morphotype 1 in Cross et al. (Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018). They have a rounded base with a central depression, and a posteriorly curved paddle-like crown, with at least three thick vertical ridges on the anterior face that stand out on the edge of the crown.
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Morphotype 2 (Figure 5F) is less well represented, with only five specimens from the basal bone bed. They correspond to morphotype 2 in Cross et al. (Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018). They are similar to morphotype 1, but with a thick rounded neck and crown, and usually more ridges on the anterior face.
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One specimen of morphotype 3 placoid scales (Figure 5G) has been found in the basal bone bed. It has a high neck, and a small top with three eroded thick ridges. The occlusal view resembles that illustrated in Landon et al. (Reference Landon, Duffin, Hildebrandt, Davies, Simms and Benton2017, figure 5E).
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Eight morphotype 4 placoid scales (Figure 5H) have been found, confined to the basal bone bed. These denticles have a flattened crown that is bent anteriorly, and with vertical ridges on the anterior part of the crown edge. Morphotype 4 denticles resemble morphotype 2 denticles but they have a flatter and lower crown on which ridges are less visible.
4.a.8.2. Hybodontid scales
Three hybodontid scales have been found. The first (Figure 5I, J), from the upper bone bed, has a bulbous crown, supported by a thick neck, and is posteriorly flattened. Thick ridges arise from the base of the root to the top of the crown are also present all around the denticle. The last two specimens (Figure 5K, L) are from the lower bone bed, and they have a large, ovoid base and a quite flat but eroded ovoid top. These two denticles are eroded, making their classification uncertain.
4.b. Osteichthyes
4.b.1. Gyrolepis albertii Agassiz, 1835
There are 66 Gyrolepis teeth (Figure 6A), mainly from the basal bone bed (only two are from the upper bone bed). The teeth are elongate, conical, with a slight sinusoidal curvature towards the apex, which is covered with an unornamented, translucent, conical and sharp acrodin cap. The shaft is smooth, with fine wrinkles, and the base is slightly flared. However, around half of these teeth are incomplete, lacking either the base or the cap.
Figure 6. Osteichthyan teeth from the upper and basal bone beds at Blue Anchor Point. (A) Gyrolepis tooth BRSUG 29974-67 in lateral view. (B) Birgeria tooth BRSUG 29974-68 in lateral view. (C) Saurichthys tooth BRSUG 29974-176 in lateral view. (D, E) Sargodon teeth: (D) incisiform tooth BRSUG 29974-151 in occlusal view; (E) molariform tooth BRSUG 29974-63 in lateral view. (F) Lepidotes pharyngeal tooth BRSUG 29974-208 in lateral view. (G) Lepidotes tooth BRSUG 29974-141 in occlusal view. (H, I) ?Eomesodon tooth BRSUG 29974-64 in lateral (H) an occlusal (I) views. (J) Jaw fragment with tooth BRSUG 29974-106 in lateral view. (K) Jaw fragment with teeth BRSUG 29974-100 in occlusal view. (L) Jaw fragment with teeth BRSUG 29974-105 in occlusal view. (M) Gill raker BRSUG 29974-74 in lateral view. (N) Pharyngeal tooth BRSUG 29974-191 in lateral view. Scale bar: 1 mm, except F and N: 500 µm.
4.b.2. Birgeria acuminata (Agassiz, 1835)
There are 20 teeth (Figure 6B) from both the upper (four) and basal bone beds (16). The teeth generally lack the basal part of the shaft. These teeth are conical, elongate, rarely slightly curved towards the apex, and covered on the top with a translucent, conical and sharp acrodin cap. This cap possesses straight ridges going from its base to the tip. The shaft is finely ridged from the base to the boundary with the cap, which is generally very clearly defined.
In previous studies, this taxon was often combined with Saurichthys longidens into the taxon Severnichthys acuminatus, following Storrs (Reference Storrs1994) who synonymized the two taxa based on isolated teeth and jaw fragments. B. acuminata and S. longidens teeth were then considered morphotypes of S. acuminatus. Diependaal and Reumer (Reference Diependaal and Reumer2021) argued that this taxon is a nomen dubium, based on morphological differences between B. acuminata and S. longidens in terms of their taxonomic allocation to two distinct families, and their overall body shapes, as Tintori and Lombardo (Reference Tintori, Lombardo and Tanner2017) had already stated, and we treat them as distinct taxa here.
4.b.3. Saurichthys longidens Agassiz, 1835
This taxon (Figure 6C) is present in both the upper bone bed (four teeth) and the basal bone bed (five teeth). One specimen from the basal bone bed is a small tooth attached to a jaw fragment. The apical cap of these teeth is conical, translucent and unornamented, and the shaft has thick vertical ridges going from the base to the cap. For the complete tooth, the shaft is smoother, and the apex is slightly curved. One large, conical tooth with thick ridges on both shaft and cap has also been found and could be an abnormal S. longidens tooth.
4.b.4. Sargodon tomicus Plieninger, Reference Plieninger1847
This species has two types of teeth: incisiforms (Figure 6D) and molariforms (Figure 6E), both of which have been found at Blue Anchor Point. Molariform teeth occur in both bone beds (two from the basal and one from the upper bone bed). They are cylindrical, laterally flattened, giving them an ovoid shape in occlusal view. The top of these teeth is covered by an ovoid translucent cap. Bunches of dentine tubules can be seen in occlusal view, but they lie underneath the translucent cap whose top is flat. The specimens have no preserved root.
Only one incisiform tooth was found, from the basal bone bed. The specimen is incomplete, lacking a great part of the root and the right posterolateral extremity. The tooth crown is eroded, the cutting edge being blunt. The narrower centre that usually slightly divides the crown into two lateral parts is still visible in occlusal view despite the abrasion.
4.b.5. Lepidotes sp. (Agassiz, Reference Agassiz1832)
Twelve pharyngeal teeth (Figure 6F) were found in the basal bone bed, and they generally have broken tips. These teeth are cylindrical and flattened laterally, with a bulbous apex on the top of which a conical, translucent cap is laterally attached, sometimes giving to the tooth apex a hooked shape in lateral view.
These pharyngeal teeth were doubtfully allocated to Sargodon tomicus by Duffin and Gazdzicki (Reference Duffin and Gazdzicki1977). However, more recent studies (Korneisel et al. Reference Korneisel, Gallois, Duffin and Benton2015; Cavicchini et al. Reference Cavicchini, Heyworth, Duffin, Hildebrandt and Benton2018) suggest that they belong to Lepidotes, based on their resemblance to branchial toothplates of Lepidotes gloriae Thies, Reference Thies1989 (see Thies Reference Thies1989, figure 10) from the Late Jurassic of Cuba.
Fifty-nine teeth, each with a cylindrical shaft and an apical translucent cap with a dome shape were also found and are tentatively attributed to Lepidotes (Figure 6G). Three of them are from the upper bone bed. This is also the case for 30 isolated caps that have been found in the basal bone bed, 27 of which have a reversed-bowl shape, with three of them having a more-or-less central tubercle on top of the cap. These caps are eroded, making it impossible to be sure whether the tubercle is in a central position or not, and whether the smoothness of the caps is the result of abrasion. Therefore, these three teeth could also belong to Colobodus (Sykes Reference Sykes1979).
This taxon has been used for these types of dome-shaped isolated teeth that do not correspond to any other taxon from the Triassic and Jurassic (López-Arbarello Reference López-Arbarello2012; Nordén et al. Reference Nordén, Duffin and Benton2015; Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018). In agreement with these studies, we refer these different teeth to Lepidotes despite the uncertainty.
4.b.6. ?Eomesodon sp. (Woodward, Reference Woodward1918)
One unexpected and distinctive tooth was identified in the basal bone bed (Figure 6H, I). It is a dome-shaped crown, with a crown of three dot-like cusps surrounding a central depression on the occlusal face of the tooth.
If correctly identified, this represents an important new record. This tooth resembles Eomesodon liassicus (Egerton Reference Egerton1854), from the middle Hettangian (Delsate et al. Reference Delsate, Duffin and Weis2002, figure 29a, b). However, Triassic specimens of this genus are only known from the Norian Zorzino fauna of Italy (Tintori Reference Tintori2003; Tintori & Lombardo Reference Tintori, Lombardo and Tanner2017), and the Norian and Rhaetian of Austria (Poyato-Arizona & Martín-Abad Reference Poyato-Arizona and Martín-Abad2013; Schultz & Piller Reference Schultz and Piller2013; Hornung et al. Reference Hornung, Kogan, Moosleitner, Wolf and Wielen2019), although the corresponding species, Eomesodon hoeferi (Gorjanović-Kramberger Reference Gorjanović-Kramberger1905), could even belong to a new genus according to Ebert (Reference Ebert2020). Pycnodontiformes, the order to which E. liassicus belongs, have not been found before in the Triassic of the UK, and are only present in the previously mentioned regions and the Germanic basin during the Late Triassic (Delsate & Kriwet Reference Delsate and Kriwet2004).
4.b.7. Other Osteichthyan remains
4.b.7.a. Unassigned Osteichthyan teeth
Twenty-eight elongate, conical teeth with a sharp acrodin cap and a broken shaft were found in the basal bone bed. They are too abraded to determine whether they belong to G. albertii, B. acuminata, or S. longidens.
4.b.7.b. Unassigned teeth with jaw fragments
Four unassigned teeth with jaw fragments have been found. One is from the upper bone bed, and is very abraded, with no tooth really protruding from the jaw fragment. One of the other specimens from the basal bone bed is a single small tooth with a jaw fragment (Figure 6J). The tooth has an acrodin cap with a flat top but does not present any particular feature to help identify it. The last two, from the basal bone bed, are protruding teeth that all have broken crowns, making a more precise identification uncertain (Figure 6K, L).
4.b.7.c. Gill rakers
Five gill rakers have been found in the basal bone bed. The biggest specimen is 2 mm long (Figure 6M). The specimens have a slender, elongate, slightly curved and laterally flattened shaft. They all have a broken apex, and thus no cap is present, contrary to better preserved specimens found at other localities (e.g. Landon et al. Reference Landon, Duffin, Hildebrandt, Davies, Simms and Benton2017, figure 6H, I).
This type of specimen was previously identified by Duffin (Reference Duffin1998a, Reference Duffin, Swif and Martill1999) as a gill raker of Pseudocetorhinus pickfordi, interpreted as a filter-feeding shark. However, this interpretation was questioned by Shimada et al. (Reference Shimada, Popov, Siversson, Welton and Long2015) and these gill rakers are now thought to belong to an unknown Osteichthyan fish (Landon et al. Reference Landon, Duffin, Hildebrandt, Davies, Simms and Benton2017).
4.b.7.d. Pharyngeal tooth
One tooth with a hook-like shape has been found in the basal bone bed (Figure 6N). It could be an Osteichthyan pharyngeal tooth.
4.b.7.e. Scales
A total of 334 scale fragments were found, of which 89 come from the upper bone bed. Unfortunately, they are too eroded to determine whether they are Gyrolepis albertii scales, although 203 of them have a ganoine layer with a similar ridge pattern (Figure 7A) (see also Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018, Figure 4a, b). Nine scale fragments show the rectangular concentric pattern found under the ganoin layer as in Landon et al. (Reference Landon, Duffin, Hildebrandt, Davies, Simms and Benton2017, figure 6L) and Cross et al. (Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018, figure 11c).
Figure 7. Other remains. (A) Gyrolepis scale BRSUG 29974-153 in exterior view. (B) Vertebra BRSUG 29974-73 in anterior or posterior view. (C) Echinoid plate BRSUG 29974-75. (D) Mollusc steinkern BRSUG 29974-50. Scale bar: 1 mm, except for B: 500 µm.
4.3. Other fish remains
4.c.1. Vertebrae
Four abraded vertebral centra were found in the basal bone bed, with a flattened ring shape. Some may be Osteichthyan vertebrae, although this assumption is uncertain due to the state of these specimens (Figure 7B).
4.c.2. Fin rays
Nine fin ray fragments were identified, five from the upper bone bed and four from the basal bone bed.
4.4. Invertebrate fossils
4.d.1. Echinoid plates
Three fragments (Figure 7C) from the basal bone bed resemble echinoid plates as previously identified by Mears et al. (Reference Mears, Rossi, MacDonald, Coleman, Davies, Arias-Riesgo, Hildebrandt, Thiel, Duffin, Whiteside and Benton2016, figure 17i, j) and Landon et al. (Reference Landon, Duffin, Hildebrandt, Davies, Simms and Benton2017, figure 7F, G). The specimens have a flat tile shape, and one side has a few regularly spaced little domes.
4.d.2. Gastropod steinkern
One gastropod steinkern fragment (Figure 7D) was found in the upper bone bed. The specimen presents only half a spiral revolution.
4.d.3. Coprolite
One slender, elongate, cylindrical coprolite with small darker particles on the surface was found in the basal bone bed. The specimen is 1 mm long.
5. Discussion
5.a. Depositional environment
The presence of marcasite in the upper bone bed (Figure 3) and pyrite in both bone beds, alongside the occurrence of black shales and phosphatized remains throughout the deposits of Blue Anchor Point, indicate deposition under anoxic condition (Antia & Sykes Reference Antia and Sykes1979). The quite high level of abrasion of the specimens, such as scales that are all fragmentary, and the presence of sandy bone beds between the mudstones suggest that the bone beds include materials that have been removed from a location near the shore and transported offshore by storm events (Suan et al. Reference Suan, Föllmi, Adatte, Bomou, Spangenberg and Schootbrugge2012). This transportation during storm events is also supported by the presence of cream-coloured rip-up clasts in the basal bone bed that were torn off the Sully Beds underneath (Figure 2C), as at Doniford Bay (Tayler et al. Reference Tayler, Duffin, Hildebrandt, Parker and Benton2023).
Like the other Rhaetian bone bed localities from the Bristol Channel area, Blue Anchor Point was located close to the Western Gate of the Central European Basin (Fischer et al. Reference Fischer, Voigt, Franz, Schneider, Joachimski, Tichomirowa, Götze and Furrer2012; Whiteside et al. Reference Whiteside, Duffin, Gill, Marshall and Benton2016). Also, like nearby Doniford Bay, St Audrie’s Bay and Lilstock (Tayler et al. Reference Tayler, Duffin, Hildebrandt, Parker and Benton2023; Lole Durbin et al. Reference Lole Durbin, Duffin, Hildebrandt and Benton2024), the site was probably several kilometres from shore when the bone beds were deposited. Deposition of bone bed materials in this distal site, probably in quite deep and thus anoxic and euxinic waters, preserved and phosphatized the vertebrate remains in the bone beds (Suan et al. Reference Suan, Föllmi, Adatte, Bomou, Spangenberg and Schootbrugge2012).
5.b. Faunal composition
Counts of 355 specimens from the upper bone bed and 647 from the basal bone bed were identified (Table 1). A third of the total number of specimens are scales. The fish teeth show clear differences between the two bone beds, with Osteichthyans dominant in the lower bone bed, chondrichthyans in the upper bone bed. In the basal bone bed, only 21 of the 135 counted specimens are chondrichthyan teeth (Figure 8A), Lissodus remaining the primary chondrichthyan taxon. Lepidotes is the most represented taxon, even without counting its gill rakers that are only present in the basal bone bed. Gyrolepis, Lissodus and Birgeria represent most of the other taxa in the basal bone bed. Denticles are also mainly present in the basal bone bed. Indeterminate chondrichthyan teeth are the most represented teeth in the upper bone bed. Among the 73 counted specimens of the upper bone bed, the dominant taxon is Lissodus, followed by Rhomphaiodon (Figure 8B). The other taxa, including Osteichthyans, are far less represented.
Table 1. Counts of taxa found in the basal and upper bone beds at Blue Anchor Point
Figure 8. Pie chart presenting relative proportions of taxa counted from the basal (A) and upper (B) bone beds at Blue Anchor Point.
The dominance of Osteichthyan taxa in the basal bone bed is unusual but matches what we observed at nearby Lilstock (Lole Durbin et al. Reference Lole Durbin, Duffin, Hildebrandt and Benton2024). However, there, the dominance by Osteichthyans applied to both the lower and upper bone beds. Further, the lower bone bed at the geographically closer locality of Doniford Bay is dominated by Lissodus teeth (Tayler et al. Reference Tayler, Duffin, Hildebrandt, Parker and Benton2023). The dominance by Osteichthyans is seen also in the basal bone bed across the Bristol Channel at Lavernock, in South Wales (Evans et al. Reference Evans, Duffin, Hildebrandt and Benton2024). In all cases, including Blue Anchor, the locations are at the west end of the Rhaetian outcrop, closest to the western ‘gate’ from which the Rhaetian Transgression progressed, heading from southwest to northeast. Water flooded the Bristol–South Wales area from a gate to the emerging North Atlantic Ocean. These waters reached western localities such as Blue Anchor, Lilstock and Lavernock first and so faunas might be slightly older or might have occupied somewhat different habitats than those found further east.
What is even more surprising is the dominance of Lepidotes teeth at Blue Anchor. This is different from the English Rhaetian bone beds from other localities, where Gyrolepis, Birgeria and Saurichthys generally represent most of the Osteichthyan teeth (Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018) even when Osteichthyans are dominant (Allard et al. Reference Allard, Carpenter, Duffin and Benton2015; Mears et al. Reference Mears, Rossi, MacDonald, Coleman, Davies, Arias-Riesgo, Hildebrandt, Thiel, Duffin, Whiteside and Benton2016; Cavicchini et al. Reference Cavicchini, Heyworth, Duffin, Hildebrandt and Benton2018; Ronan et al. Reference Ronan, Duffin, Hildebrandt, Parker, Hutchinson, Copp and Benton2020; Williams et al. Reference Williams, Duffin, Hildebrandt, Parker, Hutchinson and Benton2022; Lole Durbin et al. Reference Lole Durbin, Duffin, Hildebrandt and Benton2024). Lepidotes is only found in the basal bone bed of the Westbury Formation at Charton Bay, Devon, where there is a greater diversity of Osteichthyan taxa with no clear dominance (Korneisel et al. Reference Korneisel, Gallois, Duffin and Benton2015).
The upper bone bed has a faunal composition similar to that of both bone beds at Doniford Bay (Tayler et al. Reference Tayler, Duffin, Hildebrandt, Parker and Benton2023), and of the basal bone bed at Aust Cliff (Allard et al. Reference Allard, Carpenter, Duffin and Benton2015; Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018) and at sites along the M4–M5 motorway (Slater et al. Reference Slater, Duffin, Hildebrandt, Davies and Benton2016). This faunal composition with dominance of Lissodus and Rhomphaiodon over osteichthyan taxa represented by Gyrolepis, Birgeria and Saurichthys may be characteristic of offshore shallow marine environments (Tayler et al. Reference Tayler, Duffin, Hildebrandt, Parker and Benton2023).
5.c. Differences between the two bone beds
Differences in faunal composition between the two bone beds could relate to differences in deposition. The upper bone bed is much richer in pyrite than the lower bone bed, and uniquely preserves marcasite, both suggesting more anoxic conditions. Both bone beds comprise detrital quartz grains and bone debris washed in from elsewhere, and the more anoxic conditions of the upper bone bed could indicate eventual deposition in deeper waters than the lower bone bed. Deposition of the upper bone bed in deeper water might reflect the generally rising sea level as the Rhaetian transgression proceeded.
5.d. Comparison of the Blue Anchor vertebrate fauna
Here, we review the key taxa from Blue Anchor, and their occurrences in the wider context of the Rhaetian bonebeds of England and across Europe.
Lissodus minimus was originally described (as Acrodus minimus) from the basal Rhaetian Bone Bed at Aust Cliff by Louis Agassiz (Agassiz Reference Agassiz1839; Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018). Since then it has been recorded from virtually every Rhaetian site in the UK (e.g. Sykes et al. Reference Sykes, Cargill and Fryer1970; Allard et al. Reference Allard, Carpenter, Duffin and Benton2015; Korneisel et al. Reference Korneisel, Gallois, Duffin and Benton2015; Nordén et al. Reference Nordén, Duffin and Benton2015; Lakin et al. Reference Lakin, Duffin, Hildebrandt and Benton2016; Mears et al. Reference Mears, Rossi, MacDonald, Coleman, Davies, Arias-Riesgo, Hildebrandt, Thiel, Duffin, Whiteside and Benton2016; Slater et al. Reference Slater, Duffin, Hildebrandt, Davies and Benton2016; Landon et al. Reference Landon, Duffin, Hildebrandt, Davies, Simms and Benton2017; Cavicchini et al. Reference Cavicchini, Heyworth, Duffin, Hildebrandt and Benton2018; Tayler et al. Reference Tayler, Duffin, Hildebrandt, Parker and Benton2023; Lole Durbin et al. Reference Lole Durbin, Duffin, Hildebrandt and Benton2024) and throughout northwest Europe including France, Belgium, The Netherlands, Germany, Switzerland, Austria and Poland (e.g. Deecke Reference Deecke1926; Duffin & Gazdzicki Reference Duffin and Gazdzicki1977; Duffin Reference Duffin1980, Reference Duffin1985, Reference Duffin2001; Duffin et al. Reference Duffin, Coupatez, LePage and Wouters1983; Duffin & Delsate Reference Duffin and Delsate1993; Cuny Reference Cuny1995; Diependaal & Reumer Reference Diependaal and Reumer2021). Older German records suggest that the species is found in the Hauptmuschelkalk, Trochitenkalk, Keuperdolomit and Dachsteinkalk (Deecke Reference Deecke1926), giving a stratigraphic range of Ladinian to Rhaetian, although these records require verification.
Formerly Hybodus minor, Rhomphaiodon minor was also first described from the basal Bone Bed at Aust Cliff (Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018). Like L. minimus, it appears to be a standard member of the Rhaetian microvertebrate fauna, being found throughout the British Isles and northwest Europe, including the UK (e.g. Deecke Reference Deecke1926; Duffin & Gazdzicki Reference Duffin and Gazdzicki1977; Duffin et al. Reference Duffin, Coupatez, LePage and Wouters1983; Duffin & Delsate Reference Duffin and Delsate1993; Cuny Reference Cuny1995; Allard et al. Reference Allard, Carpenter, Duffin and Benton2015; Korneisel et al. Reference Korneisel, Gallois, Duffin and Benton2015; Nordén et al. Reference Nordén, Duffin and Benton2015; Lakin et al. Reference Lakin, Duffin, Hildebrandt and Benton2016; Mears et al. Reference Mears, Rossi, MacDonald, Coleman, Davies, Arias-Riesgo, Hildebrandt, Thiel, Duffin, Whiteside and Benton2016; Slater et al. Reference Slater, Duffin, Hildebrandt, Davies and Benton2016; Landon et al. Reference Landon, Duffin, Hildebrandt, Davies, Simms and Benton2017; Cavicchini et al. Reference Cavicchini, Heyworth, Duffin, Hildebrandt and Benton2018; Diependaal & Reumer Reference Diependaal and Reumer2021; Williams et al. Reference Williams, Duffin, Hildebrandt, Parker, Hutchinson and Benton2022; Tayler et al. Reference Tayler, Duffin, Hildebrandt, Parker and Benton2023; Lole Durbin et al. Reference Lole Durbin, Duffin, Hildebrandt and Benton2024). Deecke (Reference Deecke1926) also records it from the Lettenkohlesandstein (Middle Norian), and Struckmann (Reference Struckmann1871) records it from the Upper Muschelkalk (Ladinian) of Germany, records which require verification. Tackett et al. (Reference Tackett, Zierer and Clement2023) suggested that Rhomphaiodon sp. was part of a Late Triassic elasmofauna from Nevada (USA). Duffin (Reference Duffin1993) described R. minor from the Steinmergelgruppe (Middle Norian) of Medernach in Luxembourg, giving it a suggested stratigraphic range from Ladinian to the Rhaetian.
Pseudodalatias barnstonensis was first described from the Rhaetian of Barnstone in Nottinghamshire (Sykes Reference Sykes1971) and, although a rather rare component of Late Triassic faunas it has since been recorded from numerous Rhaetian sites in the UK (e.g. Sykes Reference Sykes1974; Allard et al. Reference Allard, Carpenter, Duffin and Benton2015; Nordén et al. Reference Nordén, Duffin and Benton2015; Slater et al. Reference Slater, Duffin, Hildebrandt, Davies and Benton2016; Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018; Williams et al. Reference Williams, Duffin, Hildebrandt, Parker, Hutchinson and Benton2022), France (Cuny Reference Cuny1995), the Netherlands (Diependaal & Reumer Reference Diependaal and Reumer2021), Belgium (Duffin & Delsate Reference Duffin and Delsate1993) and Germany (Barth et al. Reference Barth, Franz, Heunish, Kustatscher, Thies, Vespermann and Wolfgramm2014). Complete dental strips from the lower dentition have also been described from the Norian of northern Italy (Tintori Reference Tintori1980).
Synechodus rhaeticus (formerly assigned to Palaeospinax) was described from isolated dorsal fin spines from Rhaetian deposits at Aust Cliff and Holwell, and then on the basis of distinctive isolated teeth (Duffin Reference Duffin1982, Reference Duffin1998b ) which have been recovered from numerous other sites in the UK (Allard et al. Reference Allard, Carpenter, Duffin and Benton2015; Nordén et al. Reference Nordén, Duffin and Benton2015; Mears et al. Reference Mears, Rossi, MacDonald, Coleman, Davies, Arias-Riesgo, Hildebrandt, Thiel, Duffin, Whiteside and Benton2016; Whiteside et al. Reference Whiteside, Duffin, Gill, Marshall and Benton2016; Cavicchini et al. Reference Cavicchini, Heyworth, Duffin, Hildebrandt and Benton2018; Ronan et al. Reference Ronan, Duffin, Hildebrandt, Parker, Hutchinson, Copp and Benton2020), Belgium and Luxembourg (Godefroit et al. Reference Godefroit, Cuny, Delsate and Roche1998), Germany (Sander et al. Reference Sander, Wintrich, Schwermann and Kindlimann2016) and France (Cuny et al. Reference Cuny, Hunt, Mazin and Rauscher2000). Pseudocetorhinus pickfordi was also originally described from Holwell (Reference DuffinDuffin 1998a ). Its geographical range has since been expanded to include numerous other UK sites (Allard et al. Reference Allard, Carpenter, Duffin and Benton2015; Korneisel et al. Reference Korneisel, Gallois, Duffin and Benton2015; Nordén et al. Reference Nordén, Duffin and Benton2015; Mears et al. Reference Mears, Rossi, MacDonald, Coleman, Davies, Arias-Riesgo, Hildebrandt, Thiel, Duffin, Whiteside and Benton2016; Slater et al. Reference Slater, Duffin, Hildebrandt, Davies and Benton2016; Cavicchini et al. Reference Cavicchini, Heyworth, Duffin, Hildebrandt and Benton2018; Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018), plus outcrops in Germany (Barth et al. Reference Barth, Franz, Heunish, Kustatscher, Thies, Vespermann and Wolfgramm2014; Sander et al. Reference Sander, Wintrich, Schwermann and Kindlimann2016), France (Cuny Reference Cuny1995; Cuny et al. Reference Cuny, Hunt, Mazin and Rauscher2000) and Luxembourg (Godefroit et al. Reference Godefroit, Cuny, Delsate and Roche1998).
The tiny teeth of Parascylloides turnerae were probably long confused morphologically with posterior teeth of Rhomphaiodon minor. Since their original description from Barnstone in Nottinghamshire and the Hildesheim area of northern Germany (Thies et al. Reference Thies, Vespermann and Solcher2014) they have been recorded from a small number of Rhaetian sites in the UK (Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018; Moreau et al. Reference Moreau, Duffin, Hildebrandt, Hutchinson, Parker, Carpenter and Benton2021) and The Netherlands (de Lange et al. Reference De Lange, Chenal, Diependaal and Reumer2023).
The geographical and stratigraphical distribution of the various actinopterygian taxa found at Blue Anchor is quite similar to that of the chondrichthyan elements of the assemblage. Complete, articulated specimens of Sargodon tomicus occur in the Calcare di Zorzina (Middle Norian) and Argilliti di Riva di Solto (?Upper Norian) of the Italian Lombardy Alps (Tintori Reference Tintori1983), while isolated incisiform and molariform teeth have been recorded from the Rhaetian of Britain, France, Belgium, Germany, Switzerland, Austria and Poland (Deecke Reference Deecke1926; Duffin & Gazdzicki Reference Duffin and Gazdzicki1977; Duffin et al. Reference Duffin, Coupatez, LePage and Wouters1983; Duffin & Delsate Reference Duffin and Delsate1993; Cuny Reference Cuny1995; Sander et al. Reference Sander, Wintrich, Schwermann and Kindlimann2016). Tackett et al. (Reference Tackett, Zierer and Clement2023) note its presence in the Late Triassic fauna of Nevada while Deecke (Reference Deecke1926) also records it from the Upper Muschelkalk (Ladinian) and Lettenkohle (Carnian) of Germany (cf. Deecke Reference Deecke1926), giving it a stratigraphic range of Ladinian to Rhaetian.
Birgeria acuminata and Saurichthys longidens were both established on material from the basal Rhaetian Bone Bed at Aust (Cross et al. Reference Cross, Ivanovski, Duffin, Hildebrandt, Parker and Benton2018) and are common at Rhaetian localities throughout the UK (e.g. Sykes et al. Reference Sykes, Cargill and Fryer1970; Allard et al. Reference Allard, Carpenter, Duffin and Benton2015; Korneisel et al. Reference Korneisel, Gallois, Duffin and Benton2015; Nordén et al. Reference Nordén, Duffin and Benton2015; Lakin et al. Reference Lakin, Duffin, Hildebrandt and Benton2016; Mears et al. Reference Mears, Rossi, MacDonald, Coleman, Davies, Arias-Riesgo, Hildebrandt, Thiel, Duffin, Whiteside and Benton2016; Slater et al. Reference Slater, Duffin, Hildebrandt, Davies and Benton2016; Landon et al. Reference Landon, Duffin, Hildebrandt, Davies, Simms and Benton2017; Cavicchini et al. Reference Cavicchini, Heyworth, Duffin, Hildebrandt and Benton2018; Williams et al. Reference Williams, Duffin, Hildebrandt, Parker, Hutchinson and Benton2022; Tayler et al. Reference Tayler, Duffin, Hildebrandt, Parker and Benton2023; Lole Durbin et al. Reference Lole Durbin, Duffin, Hildebrandt and Benton2024). Both species have since been reported from Rhaetian deposits of France, Belgium, The Netherlands, Poland and Germany (Deecke Reference Deecke1926; Duffin & Gazdzicki Reference Duffin and Gazdzicki1977; Duffin et al. Reference Duffin, Coupatez, LePage and Wouters1983; Cuny Reference Cuny1995; Barth et al. Reference Barth, Franz, Heunish, Kustatscher, Thies, Vespermann and Wolfgramm2014; Sander et al. Reference Sander, Wintrich, Schwermann and Kindlimann2016; Diependaal & Reumer Reference Diependaal and Reumer2021). Birgeria acuminata ranges from the Upper Muschelkalk (Ladinian) to Rhaetian deposits according to Deecke (Reference Deecke1926) and, outside the Rhaetian, S. longidens has also been reported from the Lettenkohle (Carnian). Tackett et al. (Reference Tackett, Zierer and Clement2023) report abundant remains of both taxa from the Late Triassic of Nevada.
Scales and teeth of Gyrolepis albertii have been recorded from Lower Muschelkalk (Anisian) to Rhaetian sediments (Deecke Reference Deecke1926; Duffin & Delsate Reference Duffin and Delsate1993; Cuny Reference Cuny1995; Barth et al. Reference Barth, Franz, Heunish, Kustatscher, Thies, Vespermann and Wolfgramm2014; Diependaal & Reumer Reference Diependaal and Reumer2021) throughout northwest Europe, as well as from the Late Triassic of Nevada (Tackett et al. Reference Tackett, Zierer and Clement2023).
6. Conclusion
The Rhaetian at Blue Anchor Bay includes two bone beds in the Westbury Formation. These differ in their faunas, the lower bone bed containing abundant Osteichthyan teeth, and the upper bone bed being dominated by teeth of hybodont chondrichthyans. The lower bone bed is unusual when compared to those from other Rhaetian localities because normally the faunas of the basal bone bed are also dominated by chondrichthyan teeth. The absence of sharks at Blue Anchor is then a mystery. The upper bone bed, as elsewhere, contains more pyrite than the lower bone bed, as well as marcasite, both indicating more anoxic conditions and perhaps a deeper water deposition site.
Differentiation of the faunas could represent all sorts of biological and geological factors, but the dominance by Osteichthyans in the basal bone beds at western locations such as Blue Anchor, Lilstock and Lavernock, might indicate something about their geographic locations, closest to the source of the Rhaetian Transgression from the nascent Atlantic Ocean to the west. Perhaps, as the transgression flooded eastwards, there were sufficient differences in water depths or habitats, or even in the time it took, to be reflected in the faunal compositions.
Supplementary material
To view supplementary material for this article, please visit https://doi.org/10.1017/S0016756824000268
Acknowledgements
We thank two anonymous referees of the MS for their very helpful comments.
Author contributions
MJB and CJD conceived and supervised the project, MR and CH carried out laboratory work, and MR made all preliminary identifications and wrote the first draft of the paper. All authors contributed to revising the paper.
Competing interests
The authors declare no conflicts of interest.
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