Document Type : European UNESCO Geoparks: Original Article


School of Geography, Earth & Environmental Sciences, University of Plymouth, Drake Circus, Plymouth PL4 8AA, UK


The Permian breccias, conglomerates and sandstones of the English Riviera UNESCO Global geopark were deposited in quite harsh, desert environments just north of the Permian Equator. Body fossil evidence is completely lacking but rare trace fossils provide evidence of a land-based community. There is a variety of traces present, probably indicative of the presence of a range of unknown animals. Though these animals cannot be identified, their occurrence is important in the understanding of the biodiversity of these Permian environments.


Main Subjects


The English Riviera UNESCO Global Geopark is located on the east-facing coastline of South Devon (Figs 1, 2). It lies within the Variscan Orogenic Belt, which crosses South-West England from west to east.




Figure 1. Geological map of Devon, based on published data of the British Geological Survey.





Figure 2. Simplified geological map of the English Riviera UNESCO Global Geopark.



The main tectonic events were in the Carboniferous, when the Rheic Ocean finally closed (Leveridge and Shail 2011 and references therein). At this time, South-West England was located just north of the Equator (Hart, 2012, fig. 2), and included in the ‘super-continent’ of Pangaea. With a major southern-hemisphere glaciation in progress, sea levels were low, and much of Pangaea was terrestrial and subject to – at the palaeolatitude of the English Riviera – desert-like conditions.




Figure 3. Generalized stratigraphy of the Permian rocks exposed on the south Devon coast between Torbay and Exmouth. All thicknesses and lithologies are, laterally, highly variable. After Gallois and Mather (2016) and reproduced with permission of the Ussher Society.





 Figure 4. A)Folded sediments of the Meadfoot Group at the southern end of Goodrington Beach. Note that the red staining is the result of being overlain by the uncomformable conglomerates of the Permian succession (Figure 4B) that are exposed in Waterside Cove. The ‘Taenidium’-rich horizon lies just above the coarse-grained, basal conglomerate.

  In the Torquay area (Figs 2, 3), the folded strata of the Devonian are overlain by the terrestrial deposits of the Permian, and this major unconformity is seen immediately south of Goodrington (Fig. 4A, B) and in Waterside Cove. The lowermost sediments are coarse breccias and conglomerates, with interbedded finer-grained sandstones and rare siltstones which can be traced along the coastline of Devon north of Torquay (Benton et al. 2002; Gallois and Mather 2016; Coram and Radley 2016). In the lower parts of the succession, west of the River Exe, most of the sediments were deposited intermittently during rare flooding events, such as those seen in modern Middle Eastern wadis (Hart 2012, fig. 17A, B). The breccias and conglomerates are dominated by rounded to sub-angular boulders and cobbles of the local Devonian limestones, occasional fragments of slate and rare igneous rocks (not including the Dartmoor granite, which was intruded close to the Carboniferous/Permian boundary; see Chesley et al. 1993). These are not encouraging environments in which to look for body fossils but, in a few places, trace fossils are known. These provide the only evidence of life-forms existing in the harsh environments of these Pangaea deserts and are, therefore, exceptionally important.



The English Riviera UNESCO Global Geopark is located on the eastern coastline of South Devon (Figs 1, 2). The boundary of the Geopark territory is that of the Torbay Unitary Authority and, as such, follows no geological or physical features. While the coastline provides the obvious access to the geological features, there are many inland quarries which are, unfortunately, either overgrown, built over, or infilled. In a few locations there are exposures in roadside cuttings.

The marine area of Tor Bay is enclosed between two, prominent headlands; Hope’s Nose in the north and Berry Head in the south. These headlands are composed of resistant Devonian rocks, while the intervening area (forming the ‘bay’) is formed mainly of softer, Permian sandstones, conglomerates and breccias.


Trace fossils

A trace fossil, or ichnofossil (Greek, ikhnos, trace, track) is any disturbance or modification of sediment caused by the activities of an animal (or, in some cases, plants). Traces can range from the obvious borings in shells, reptile footprints and worm burrows to pervasive mottling as a result of the complete mixing of sediment. Trace fossils are, therefore, a record of biological activity but can only rarely be linked to any specific animal. The International Commission on Zoological Nomenclature (ICZN) adjudicates on the names of trace fossils, and although many ichnologists consider structures formed by plants as trace fossils and have also given them names, these are not recognized as such by the International Code of Botanical Nomenclature (ICBN) which deals with plants (including algae and fungi).

There are several published classifications of trace fossils, most of which are based on their presumed mode of formation or their assumed purpose. For example, domichnia (dwellings), repichnia (creeping and crawling), fodinichnia (feeding by deposit feeders), pasichnia (surface feeding traces) and cubichnia resting traces) are all in wide usage and originate from work by Seilacher (1953). The simplest classifications refer only to the morphology and do not imply any direct mode of formation. Trace fossils from the Permian rocks of Devon can be classified as endichnial, a structure preserved within the sediment, or exichnial traces (on the sediment surface). The latter are crustacean trails (Shapter 1842) and reptile footprints (Clayden 1902) preserved on the surfaces of Permian sandstones in inland quarries.

Presumed annelid burrows were recorded by Pengelly (1864) in the Torbay Breccia at Goodrington, and Ussher (1877) observed the presence of ‘numerous annelid tracks’ in the Watcombe Formation above Watcombe Cove (Fig. 2). Henson (in Selwood et al. 1984) noted that ‘thin burrows were common’ in the tops of graded sedimentation units in the Watcombe Formation in outcrops in the Watcombe valley.

Some of the best-known examples of trace fossils are from the Goodrington area, especially in Waterside Cove. These have been described by Laming (1969), Henson (1971), Perkins (1971), Ridgeway (1974, 1976), Pollard (1976), Selwood et al. (1984), Gallois and Mather (2016), Coram and Radley (2016) and Falcon-Lang (2019).

Structures attributable to animal burrows are generally rare. They are, however, relatively abundant in a few thin (



While trace fossils are known from a few places within the English Riviera UNESCO Global Geopark, there are two significant locations in Waterside Cove and Watcombe Cove where such fossils are regularly encountered. These, and other locations outside the Geopark, have recently been described by Gallois and Mather (2016) and Coram and Radley (2016).


Waterside Cove

Endichnial burrows are relatively common at a few stratigraphical levels in-situ and in fallen blocks of the lowest part of the Torbay Breccia near Waterside Cove (Figs 2, 3), and in fallen blocks of Watcombe Formation at Watcombe Cove. They occur in sandstone interbeds within the predominantly breccia-rich successions.

At the southern end of Goodrington Sands, south of Paignton, is an outcrop of Meadfoot Group (Lower Devonian) sandstones and siltstones that are spectacularly folded into recumbent, north-ward verging, overfolds (Fig. 4A). These are stained red by the overlying Permian succession, with the unconformity visible by the railway bridge, as well as in Waterside Cove (Fig. 4B) to the south.

The burrows observed on the foreshore rock platforms are large (1 m long), unbranched, both straight and sinuous, with well-developed meniscus fills (Fig. 5A).  The Waterside Cove trace fossils have been illustrated by Laming (1969, fig. 3) and Perkins (1971, fig. 38). The latter suggested that the burrows had been created by a worm-like creature that could ingest small pebbles, though this appears to be rather unlikely. A detailed description of the burrows is provided by Henson (1971) who thought that they were most probably made by reptiles for occupation or in search of food. In the most complete description of the Waterside Cove burrows to date, Ridgeway (1974) concluded that the trace fossils were made by primitive burrowing reptiles and that the variations in size were related to animal size.  Pollard (1976) confirmed this interpretation and suggested that the burrows might have been formed by limbed amphibians or reptiles during aestivation rather than as dwelling or feeding burrows. Pollard (1976) concluded that the Waterside Cove examples could “probably be named” Beaconites cf. antarcticus (Vialov 1962), and the name Beaconites has often been used since that time.

The presence or absence of burrow linings and walls appears to be crucial and Gallois and Mather (2016) discussed the taxonomic separation of Beaconites and Taenidium. Pollard (1976) had named the Waterside Cove examples as Beaconites based on a comparison with the type material (photographs, not rock specimens) of Vialov’s (1962) B. antarcticus from the Devonian part of the Beacon Supergroup in Antarctica. The burrows described here are much larger than those described by Vialov (1962) but are of a similar size range as those described by Bradshaw (1981). Similar, meniscus-filled traces have also been described as Beaconites from Devonian rocks in South Wales (Allen and Williams 1981; Morrissey and Braddy 2004) and from Carboniferous rocks in County Mayo, Ireland (Graham and Pollard 1982).  D’Alessandro and Bromley (1987), in a comprehensive review of Taenidium and morphologically similar forms, drew attention to the close similarity between Beaconites and Taenidium. They concluded that, until the description of the former had been clarified, unbranched meniscus-filled fossils of the type described from Waterside Cove, should be referred to as Taenidium (Heer 1877).

The most comprehensive discussion of Beaconites and Taenidium is provided by Keighley and Pickerill (1994) who concluded that there had been inconsistent use of both names. Taenidium, it was suggested, should only be applied to un-lined, meniscate, back-filled burrows without a wall created by the occupant. Using the emended definition provided by Keighley and Pickerill (op. cit.) the Waterside Cove traces should be regarded as Taenidium; see Keighley and Pickerill (1994, text-fig. 2, plate 1).

In a brief description of these fossils, Falcon-Lang (2019, p. 78) suggests that they may have been formed by ‘giant’ arthropleurids, though there is little direct evidence for such animals being present in Devon at this time. None of the trace fossils associated with the Taenidium occurrences appear to be comparable to the suggested arthropleurid trace fossils described from the uppermost Carboniferous and lowermost Permian of New Mexico by Schneider et al. (2010).





 Figure 5. A)Taenidium’ meniscus-filled trace fossil from Waterside Cover, south of Goodrington. B) highly burrowed sandstones from Petitor Cove, north of Oddicombe Beach. C) intense bioturbation (?Helminthopsis) of sandstone from Watcombe Cove, north of Oddicombe Beach. In figures 5B and 5C the GB£1.00 coin provides the scale, while in figure 5A it is a pen.


Watcombe Cove and Adjacent Cliffs

At the very northern limit of the English Riviera UNESCO Global Geopark are Oddicombe Beach, Petitor, and Watcombe Cove (Fig. 2). Trace fossils are relatively abundant in fallen blocks of breccia and fine-grained sandstone in the Watcombe Formation (Fig. 3) at Watcombe Cove but less common at Petit Tor Beach, where they comprise straight to gently curved, unbranched, meniscus-filled burrows, mostly 4 to 8 mm in diameter, but with a maximum observed length of 400 mm. They often form complex networks in which burrows are superimposed on one another at angles of mostly 40° to 90° (Fig. 5C). Locally, many burrows coalesce to form irregular disturbed patches up to 90 x 200 mm which may have given access to the sediment-water interface (Fig. 5C). The burrow infillings are lithologically similar to the matrix with curved menisci picked out by grain-size variations in the sandstones.  These burrow systems may be similar to those described as Helminthopsis isp by Lima and Netto (2012) from the Permian of southern Brazil.


 Exichnial Trace Fossils

Exichnial trace fossils have been described by Gallois and Mather (2016) from the Dawlish Sandstone Formation including crustacean trails (Shapter 1842) and reptile footprints. Clayden (1902) reported that trackways of the mammal-like synapsid reptile Cheilichnus bucklandi (Jardine) were relatively common on some of the sandstone bedding planes in an old quarry at Poltimore [SX 971 971] near Exeter (Edwards and Scrivener 1999, plate 3i). Gallois and Mather (op. cit.) also described rare occurrences of small trace fossils from the Torbay Breccia at Livermead and Corbyn Head (in Torbay) as well as from the Teign Breccia at Maidencombe Beach and at Ness Cove, Shaldon. They also report the presence of an irregular, star-shaped ‘disturbance’ with associated cementation in the Corbyn’s Head Member of the Torquay Breccia at Corbyn Head, Torbay, which might be a partially lined trace fossil c.f. Heliophycus Miller and Dyer (1878), a burrow of unknown affinity or the result of plant action.



The Permian sites within the English Riviera UNESCO Global Geopark are generally accessible and much safer than some of the Devonian locations (see Hart and Smart this volume). Waterside Cove, Goodrington, Petitor/Oddicombe and Watcombe are backed by cliffs and some (e.g., Oddicombe) are most definitely unstable. All the coastal sections are subject to quite large tidal ranges and should be avoided on rising tides.

Trace fossils are generally rare, occasionally being found on rock surfaces that may, in the summer months, be algae covered. They may be interesting to the specialist, but general visitors may struggle to both find these fossils and understand their significance. As such, they are unlikely to be regarded as important tourist highlights, no matter their palaeontological significance.

Geosites that may potentially be used for pre-university education are quite limited, but are described on-line in the Devon Register of Educational Sites.



Many of the geological sites within the English Riviera UNESCO Global Geopark are recognized as nationally important. Many are on the Geological Conservation Review (GCR) Register, while others are Sites of Special Scientific Interest (SSSI) and National Nature Reserves (NNR); see Page (2004) for a review. While many are under local management, all are under statutory protection by Natural England. These processes have been described by Hart and Smart (this volume).



The presence of trace fossils in the Permian strata of the English Riviera UNESCO Global Geopark demonstrates that life existed in the harsh, desert conditions of the area at that time. These fossils are, the only evidence of such life and their presence can be both interesting, and useful, in debates on Permian palaeoenvironments in Devon.



 Melanie Border is thanked for the provision of some trace fossil images from the English Riviera UNESCO Global Geopark. Mr James Quinn (University of Plymouth) is thanked for providing some of the diagrams. Comments provided by two anonymous reviewers have assisted in the improvement of the final paper.

Allen JRL & Williams BPJ (1981). Beaconites antarcticus: a giant channel-associated trace fossil from the Lower Old Red Sandstone of South Wales and the Welsh Borders. Geological Journal. 16:255–269.
Benton MJ, Cook E, Turner P (2002). Permian and Triassic red beds and the Penarth Group of Great Britain. Geological Journal. 38(2): 190-190.
Bradshaw MA (1981). Paleoenvironmental interpretations and systematics of Devonian trace fossils from the Taylor Group (lower Beacon Supergroup), Antarctica. New Zealand Journal of Geology and Geophysics.24:615–652.
Chesle  JT, Halliday  AN, Snee LW, Mezger K, Shepherd TJ, Scrivener RC (1993). Thermochronology of the Cornubian batholith in southwest England: Implications for pluton emplacement and protracted hydrothermal mineralization. Geochimica et Cosmochimica Acta, 57: 1817–1835.
Clayden MA (1902). On the occurrence of footprints in the lower sandstones of the Exeter district. Quarterly Journal of the Geological Society of London. 64: 496–501.
Coram RA & Radley JD (2016). Devon’s desert ‘worms’. Geology Today. 32(2): 65–69.
D’Alessandro A & Bromley, RG (1987). Meniscate burrows and the Muensteria-Taenidium problem. Palaeontology. 30: 743–763.
 Edwards RA & Scrivener RC (1999). Geology of the country around Exeter. Memoir for Geological Sheet 325 (England and Wales). London: HMSO
Falcon-Lang H (2019). Localities explained 22: South Devon, UK. Geology Today. 35(2): 73-80.
Gallois RW & Mather JD (2016). Trace fossils in the Permian rocks of South-West England. Geoscience in South-West England. 14(1): 20–28.
Graham TW & Pollard JE (1982). Occurrences of the trace fossil Beaconites antarcticus in the Lower Carboniferous fluviatile rocks of County Mayo, Ireland. Palaeogeography, Palaeoclimatology, Palaeoecology. 38: 257–268.
Hart MB (2012). The geodiversity of Torbay. Report and Transactions of the Devonshire Association for the Advancement of Science, Literature and the Arts. 144: 43–86.
Heer O (1877). Flora Fossils Helvetiae. Die vorweltliche Flora der Schweiz. J. Würster and Co.
Henson MR (1971). The Permo-Triassic rocks of south Devon. Unpublished PhD Thesis, University of Exeter.
Keighley D.G & Pickerill R.K (1994). The ichnogenus Beaconites and its distinction from Ancorichnus and Taenidium. Palaeontology. 37(2): 305–337.
Laming DJC (1969). A guide to the New Red Sandstone of Torbay, Petitor and Shaldon. Report and Transactions of the Devonshire Association for the Advancement of Science, Literature and the Arts. 101: 207–218.
Leveridge BE & Shail  RK (2011). The marine Devonian stratigraphy of Great Britain. Proceedings of the Geologists’ Association. 122(4): 540–567.
Lima JHD & Netto RG (2012). Trace fossils from the Permian Teresina Formation at Cerro Caveiras (S. Brazil). Revista Brasileira Paleontologia. 15(1): 5–22.
Miller SA & Dyer CB (1878). Contribution to paleontology, No. 1. Journal of Cincinatti Society of Natural History. 1: 24–39.
Morrissey LB & Braddy S (2004). Terrestrial trace fossils from the Lower Old Red Sandstone, southwest Wales. Geological Journal. 47: 1–29.
Page KN (2004). A review of the geological heritage of Torbay with guidance for its management and a strategy for sustainable use. Torbay Heritage Forum. Retrieved from:
Pengelly W (1864). On the chronological value of the New Red Sandstone System of Devonshire. Report and Transactions of the Devonshire Association for the Advancement of Science, Literature and the Arts. 1: 31–43.
Perkins JW (1971). Geology explained in South and East Devon. David and Charles, Newton Abbot.
Pollard JE (1976). A problematic trace fossil from the Tor Bay Breccias of south Devon. Proceedings of the Geologists’ Association. 86: 105–108.
Ridgeway JM (1974). A problematical trace fossil from the New Red Sandstone of Devon. Proceedings of the Geologists’ Association. 85: 511–517.
Ridgeway JM (1976). A problematic trace fossil from the Tor Bay Breccias of south Devon. Written discussion of a paper taken as read, reply by the author. Proceedings of the Geologists’ Association.86: 108–109.
Schneider JW, Lucas SG, Werneburg R, Rößler R (2010). Euramerican late Pennsylvanian/early Permian arthropleurid/tetrapod associations – implications for the habitat and paleobiology of the largest terrestrial arthropod. In Lucas SG. et al. (eds), Carb-Permian transition in Cañon del Cobre, New Mexico Museum of Natural History and Science Bulletin. 49: 49–70.
Seilacher A (1953). Studien zur palichnologie. I. Uber die methoden der palichnologie. Neues Jahrbuch für Geologie und Paläontologie, Abhandlungen. 96: 421–452.
Selwood EB, Edwards RA, Simpson S, Chesher JA, Hamblin RJO, Henson MR, Riddols BW & Waters RA (1984).Geology of the Country around Newton Abbot. Memoir for 1:50,000 geological sheet 339. HMSO, London.
Shapter T (1842). The climate of south Devon; and its influence upon health; with short accounts of Exeter, Torquay, Babbacombe, Teignmouth, Dawlish, Exmouth, Budleigh Salterton and Sidmouth.London: John Churchill.
Ussher WAE (1877). The age and origin of the Watcombe Clay. Report and Transactions of the Devonshire Association for the Advancement of Science, Literature and the Arts. 9: 296–300.
 Vialov OS (1962). Problematica of the Beacon Sandstone at Beacon Height West, Antarctica. New Zealand Journal of Geology and Geophysics. 5: 718–732.