Seaton Hole, at the western end of Seaton Bay, exposes fossil-bearing Upper Greensand and Chalk beneath White Cliff. Oysters, other bivalves and echinoids are useful finds to recognise in naturally weathered loose material, with rarer ammonites also recorded. Red Triassic mudstones below the Cretaceous rocks reveal a much older chapter of the coast’s history. Visit only when the tide and beach conditions leave a safe route well clear of the unstable cliffs.
FIND FREQUENCY: ♦♦♦ – Shells and echinoid remains occur in local Greensand and Chalk, but many are fragmentary, worn or firmly enclosed. Rare published finds should not be expected on every visit.
CHILDREN: ♦♦ – Seaton’s town beach and promenade are different from this tidal fossil locality. A carefully supervised visit is possible only where there is ample open beach; do not take children beneath unstable cliffs or onto rock armour.
ACCESS: ♦♦ – Parking and facilities are available in Seaton, but the foreshore approach from West Walk is tidal and the signed Coast Path makes a landward diversion around Old Beer Road. The fossil locality is not an all-tide extension of the surfaced promenade.
TYPE: Coastal cliffs and a shingle/rocky foreshore. Inspect loose local rock on the open beach where permitted; leave attached beds, cliff faces and coastal defences undisturbed.
DIRECTIONS
♦ Seaton Hole is at the western end of Seaton Bay, towards Beer. Use a signed public car park in Seaton, such as Orchard or Seaton Jurassic, checking the current charges and conditions. Walk west along the Esplanade and West Walk towards the Hideaway Café.
♦ Beyond the promenade, the beach continues towards Seaton Hole. Use this link only when there is a wide, clear route well away from the cliffs and sea defences. Plan both the outward and return walk around low water, allowing ample time, and turn back if the beach is narrowing.
♦ Follow the signed South West Coast Path’s landward diversion around unstable Old Beer Road. Do not cross the collapsed road or climb over armour boulders to force a through route. Where conditions rule out the beach approach, use the signed landward path and established access only where currently open.
♦ Use an up-to-date map for Seaton Hole at the western end of the bay, and check local signs and Coast Path notices. The River Axe and harbour are at the opposite end of Seaton; they are not the approach to this locality.
FOSSIL HUNTING
The useful fossil-bearing material at Seaton Hole comes chiefly from the Upper Greensand and Chalk of White Cliff, at the western end of Seaton Bay. Look first at loose, naturally fallen stones on the open foreshore, where the rock type can still be recognised. The sands and sandstones are green-grey when fresh and often weather yellow or brown; chalk is white and much finer grained, while the basal chalk limestone can be hard, sandy and green-speckled. This distinction matters: a fossil in a weathered sandstone block belongs to a different part of the succession from one in soft white chalk. New coastal-defence boulders include imported Norwegian rock and must not be used as evidence for the local geology.
Oysters and other bivalves are the most useful starting point in the Upper Greensand. Curved oyster valves, strongly ribbed scallop-like shells and the moulds left after shells dissolved occur in the calcareous sandstone layers and rounded concretions traditionally called cowstones. In the nineteenth-century Whitecliff collections, oysters were recorded as Exogyra conica, E. columba, E. digitata and E. undata; strongly ribbed pectinids included Pecten (Neithea) quadricostatus. These are historical identifications, retained here to connect the finds with the published beds, rather than a freshly revised species checklist. A rounded stone is not automatically a fossil: look for repeated ribs, growth lines, a hinge or a recognisable shell outline.
The lowest cowstone-bearing sands produced a particularly varied recorded fauna, including the ribbed and ornamented bivalves historically called Trigonia aliformis, T. scabricola and T. spectabilis, together with Arca (Cucullaea) carinata, Cardium hillanum and Turritella. Trigoniid moulds can preserve rows of ribs or knobs; a gastropod mould may show the turns of a high-spired shell even when the shell itself is gone. The harder lenses preserve detail better than the surrounding loose sand, but their fossils can be firmly locked in the matrix. Examine naturally weathered surfaces and existing breaks before assuming that a promising lump needs splitting.
A thin, very shelly sandstone near the top of the historical lower division is especially important in the Whitecliff record. Its lowest 15–30 cm contained abundant shell material, with the solitary coral Placosmilia tuberosa, oysters, pectinids, echinoid plates and spines, crinoid fragments and small colonial fossils. The coral may retain a cup with radiating partitions; a cidarid plate can show the rounded boss that carried a spine, while a detached spine can look like a short textured rod. Small crinoid pieces and bryozoans are easily overlooked among shell grit. Published collecting already found this rock difficult to prepare and many specimens were identifiable only as casts, so an intact fossil-bearing block can be more informative than a damaged isolated fragment.
Chert-rich Upper Greensand is harder and generally less rewarding for whole fossils than the best calcareous shell beds. The old Whitecliff log records oyster-rich sandstone, sponge debris and a small fauna including Orbitolina concava, Elasmostoma, Radiopora ornata and Spondylus. Search the sandstone between chert masses and the surfaces of naturally worn blocks. Chert itself may retain ghostly shell fragments or impressions, but an irregular nodule is not necessarily a sponge. Weathering can remove carbonate and leave a cavity, a mould or a concentration of resistant silica; the original shell is often incomplete.
Chalk material adds echinoids, brachiopods and inoceramid bivalves. The lower nodular chalk at the southern end of White Cliff yielded the historically named Cardiaster pygmaeus, Discoidea dixoni, Hemiaster minimus, Cidaris hirudo and Rhynchonella cuvieri; shells called Inoceramus mytiloides were recorded in the succeeding beds. Echinoid tests are recognised by their organised pore rows and five-part pattern, sometimes with a heart-shaped outline. Small brachiopods have two valves, but their symmetry is usually down the middle of each valve; many bivalves instead have similar left and right valves. The chalk can be soft while the fossil shell is brittle, so avoid scraping away detail or forcing out a specimen that is only partly exposed.
The higher chalk at Annis’ Knob, above the Beer end of the White Cliff section, has a separate historical record of Micraster, Echinocorys, brachiopods and small sponges. It also contains the old Holaster planus zone. This is a higher Chalk occurrence, not a fossil zone within the Foxmould. A loose echinoid found on the beach cannot by itself show which bed supplied it, and the high bluff is not an invitation to climb or work beneath the cliff. Record the find as loose beach material unless its source is genuinely established.
Upper Greensand ammonites are unusual here. An Arrhaphoceras specimen from White Cliff is recorded in the Natural History Museum’s Grimsdale collection, with no secure bed provenance in these accounts; a Bindon Sandstone origin is inferred. The older Chalk collections include fossils named Ammonites varians, A. navicularis and Scaphites aequalis; a curved, ribbed whorl fragment can be the first clue. Condensed and reworked beds make the exact horizon particularly important. A Pycnodus crushing-tooth plate was also recorded from the lower Chalk, and De la Beche described fish teeth and vertebrae in a Whitecliff sandstone in 1826. Such finds are useful scientific evidence, not a promise of routine collecting. Photograph an unusual specimen with a scale, keep its matrix where possible, and record the precise beach position and whether it was loose. A fossil’s provenance is often more valuable than an ambitious identification.
The red Triassic mudstones are a different target: the marine shell beds described above belong to the much younger Cretaceous cover. Do not treat green reduction patches, gypsum veins or weathered mudstone shapes as marine fossils. Nor should Jurassic ammonites or Lias boulders be promised for Seaton Hole from records east of the River Axe. Collect only where permitted, in small quantities from loose material, and leave attached beds, cliff faces and coastal defences undisturbed.
A chronological record of fossil discoveries, geological research and conservation milestones at Seaton Hole and Whitecliff.
1825 – An early measured section
W. H. Fitton recorded the Whitecliff succession in detail during his investigations of the rocks beneath the Chalk. Published in 1836, his observations provided an early measured account of the Greensand section beside Seaton Hole.
1826 – Fossil-bearing sandstones described
Henry De la Beche published a description and illustrated section of Whitecliff, distinguishing nine divisions within its chert-bearing sandstones. One coarse-grained layer contained fish teeth and vertebrae with broken shells, providing an early record of vertebrate remains from this exact cliff.
1874 – Beds and fossil assemblages catalogued
C. J. A. Meyer recorded thicknesses and fossil occurrences through the Whitecliff succession as part of a detailed comparison of the coastal Cretaceous rocks. His numbered beds documented fossil-bearing concretions, shell-rich pebble layers, chert beds and the overlying Chalk, establishing a framework used by later investigators.
1887–1888 – A major fall changes the exposure
A large Chalk fall at Whitecliff interrupted the previously continuous exposure of the underlying Greensand. Its debris separated the lower beds to the north from the higher beds to the south, leaving a lasting feature in the section subsequently described by geologists.
1894 – Fossil collecting and stratigraphic reassessment
A. J. Jukes-Browne examined Whitecliff with C. J. A. Meyer, helping them resolve earlier disagreements about the beds near the Greensand–Chalk junction. Geological Survey collecting by J. Rhodes also documented the local Greensand fauna, including fossils from the lower concretions and a hard, shell-rich sandstone higher in the succession.
1900 – Detailed Greensand sections published
A. J. Jukes-Browne and W. Hill published detailed descriptions of the lower sands and overlying chert-bearing beds at Whitecliff. Their account recorded the fault beside Seaton Hole, changes in exposure and individual fossil-bearing horizons, making the locality a key reference section for the Devon Upper Greensand.
1903–1904 – Chalk horizons compared using fossils
Detailed studies by A. W. Rowe and by A. J. Jukes-Browne and W. Hill refined the Chalk succession at Whitecliff and its upper bluff, Annis’ Knob. Fossil sea urchins helped distinguish successive zones, while the very thin limestone at the base of the Chalk was described separately from the thicker beds above.
1984 – Whitecliff becomes a Chalk reference section
I. Jarvis and P. B. Woodroof used Whitecliff as the reference section for the newly defined Seaton Chalk Formation and its subdivisions. Their work distinguished the lower nodular chalk from the overlying flinty chalk and used hardgrounds and other marker beds to compare the condensed local succession with neighbouring exposures.
1985 – Coastal geological protection renewed
The Sidmouth to Beer Coast Site of Special Scientific Interest was renotified under the Wildlife and Countryside Act. Whitecliff lies at its eastern end, within a protected coastal succession valued for its Upper Greensand exposures, hardgrounds, fossil-bearing limestone and Chalk.
1997 – Microfossils reveal changing sea levels
M. B. Hart analysed foraminifera from Beer Roads and Annis’ Knob at the southern end of the Whitecliff section. The microscopic fossils helped identify successive intervals within the Chalk and supported an interpretation of four major sedimentary sequences associated with changing Turonian sea levels.
2001 – The faulted Triassic succession reconstructed
R. W. Gallois used coastal sections and borehole evidence to establish a detailed framework for the Mercia Mudstone Group. The red mudstones in fault-bounded blocks at Seaton Hole and west Seaton were placed within the Seaton Mudstone Member, clarifying their position in the older rocks beside the Cretaceous cliffs.
2001 – World Heritage recognition
Whitecliff was included in the Dorset and East Devon Coast World Heritage Site. The protected coastal section running eastwards from Sidmouth ends at Seaton Hole, recognising the geological importance of these exposures as part of the wider coast.
2004 – Two Greensand type sections established
R. W. Gallois proposed Whitecliff as the type section for both the Foxmould Member and the Whitecliff Chert Member. The adjoining exposures provided a continuous reference for the transition from weakly cemented sands to harder, chert-bearing calcareous beds, separated by a prominent eroded and burrowed surface.
2025 – Seaton Hole coastal defences rebuilt
Coastal protection works completed on 12 December strengthened and widened the rock armour along approximately 600 metres of Seaton Hole beach towards West Walk. The scheme replaced deteriorated defences and reshaped the engineered cliff-base frontage, with the aim of reducing coastal erosion.
GEOLOGY
Seaton Hole exposes a striking break in geological time. Red mudstones formed in the Late Triassic lie beneath marine sandstones of the Early Cretaceous, followed by the pale limestones and chalk of the Late Cretaceous. Much of the intervening record is missing at the contact. The abrupt change is an unconformity: an old land surface was eroded and later flooded by the sea. At White Cliff the lowest Upper Greensand includes fragments of the underlying red mudstone, preserving evidence of that erosion. The Jurassic rocks seen on the coast east of the River Axe are not part of this western Seaton Hole succession.
The local red beds belong to the Seaton Mudstone Member of the Branscombe Mudstone Formation, within the Mercia Mudstone Group. They record dry continental conditions in a low-relief basin, where mud accumulated on intermittently wet plains and flats. Greenish patches and bands reflect changes in the chemical conditions after deposition. Only parts of the member are exposed in the Seaton fault blocks, so its complete regional thickness must not be mistaken for the height or thickness of the red cliffs here.
The Upper Greensand records the later arrival of a shallow sea. Glauconite gives freshly exposed sand a greenish colour, while weathering commonly produces yellow and rusty-brown tones. Some layers remained sandy; others were cemented into hard, fossil-bearing sandstone or shell-rich limestone. The modern Foxmould Member includes the cowstone-bearing sands. Above it, the Whitecliff Chert Member contains conspicuous silica-rich nodules and beds, and the Bindon Sandstone Member includes the upper sandstones. Chert continues into the lower Bindon Sandstone here, so the last chert is not a reliable formation or member boundary. Erosion surfaces, mineralised hardgrounds and changes in sediment character are more dependable.
The Chalk begins with a thin, condensed and locally very hard limestone succession called the Beer Head Limestone Formation. Condensation means that comparatively little rock represents a long interval of time; repeated pauses, erosion, burrowing and mineralisation complicate the fossil record. White Cliff does not contain the thick, complete basal sequence seen at Hooken. Higher up are nodular chalk and then softer flinty chalk, assigned in modern BGS terminology to the Holywell Nodular Chalk and New Pit Chalk formations. The old local name “Seaton Chalk” is useful when reading earlier papers, but is not used here as an extra modern formation. Higher nodular chalk at the Beer end, including Annis’ Knob, belongs to the Lewes Nodular Chalk Formation.
Faulting and the dip of the beds explain why different parts of the succession reach the shore within a short distance. A fault at Seaton Hole brings the Cretaceous rocks against the red Triassic beds; westward and southward around White Cliff, the Greensand–Chalk junction descends towards the Beer end. Fallen and rotated blocks can expose a useful slice of strata, but their present height or tilt is not the original order of an undisturbed cliff. Rockfalls, beach cover and weathering continually change what can be seen. Historic measured logs therefore document the locality’s geology without guaranteeing that every described bed is accessible today.
Detailed geology and stratigraphy
This account covers Seaton Hole and White Cliff towards King’s Hole, with the higher Chalk reference at Annis’ Knob explicitly distinguished at the Beer end. The modern succession is described from older to younger. Historic Survey logs follow separately where their bed divisions cannot be matched safely to modern boundaries. Measurements describe the exposures recorded by their authors; they are not a new measured section or a statement of present-day access. Historical fossil names are retained as historical records, without silently implying modern taxonomic validation.
Fault and dip recorded in the 1894 Survey visit. The 1900 memoir describes the Seaton Hole fault as striking approximately north–south, with the Whitecliff beds dipping south-west at about 7–8°. These are historical observations of the local structure, not a new survey. Their systematic tilt must be distinguished from the variable orientations of slipped or fallen blocks.
MERCIA MUDSTONE GROUP
Branscombe Mudstone Formation
Seaton Mudstone Member
Local red-mudstone interval. Red-brown to orange-brown mudstones and silty mudstones, locally with green reduction patches and beds, form the Triassic substrate. Higher parts of this member are recorded in the fault blocks at Seaton, between grid references SY 235896 and SY 244898. The complete 115 m member is known from the Chard borehole, not a continuously measurable cliff at Seaton Hole. The Haven Cliff Mudstone Member and Blue Anchor Formation farther east are not imported into this section.
Sub-Cretaceous unconformity. An irregular, burrowed erosion surface separates the red mudstones from the Upper Greensand. Meyer’s observation, reported in the 1900 Survey memoir, described the lowest approximately 3 ft (0.91 m) of dark green clayey sand and a basal layer containing red-mudstone fragments. This is evidence of erosion of the substrate before or during the marine transgression. No separate in-situ Gault or Lias unit is established at this western locality.
SELBORNE GROUP
Upper Greensand Formation
The Upper Greensand is late Albian in age. White Cliff is a type locality for its Foxmould and Whitecliff Chert subdivisions. Green-grey sand, calcareous sandstone, shell-grit limestone and chert alternate through the succession. Modern regional thickness ranges are not substituted for a single local measurement. The six lower sandy packages and sixteen upper beds measured historically are reproduced below, with their original limits and numbering.
Foxmould Member
Sands and cowstone-bearing packages. Glauconitic sand contains lenticular concretions and more continuous beds of calcareous sandstone. These are the cowstones and sandstone “burrs” of older accounts. The present member includes material which early authors divided between Cowstone Beds, Foxmould and supposed sandy Gault equivalents. Those old divisions must not be stacked as separate modern formations. The historical local lower log totals 84½ ft (25.76 m) seen, with the base concealed during the 1894 visit.
Upper shelly sandstone. At the top of the 1900 lower division, a 2½ ft (0.76 m) calcareous sandstone includes a basal 6–12 in (0.15–0.30 m) concentration of shells and other fossils. The published fauna is listed with the lower log. The conspicuous lithology is useful for recognising a loose block, but does not establish a present-day accessible collecting horizon.
Culverhole hardground pair and intervening greensand. Gallois’s modern White Cliff–King’s Hole column distinguishes a lower and upper mineralised surface around a glauconite-rich sandy interval at the Foxmould–Whitecliff Chert transition. These record interruptions and reworking on the sea floor. The BGS framework uses the Culverhole Hardground for the member boundary. The two physical surfaces should be retained in the local account rather than reduced to a generic “change to chert”.
Whitecliff Chert Member
Basal sandstone package. Above the Culverhole hardgrounds, sandstone passes upwards into the lowest distinct cluster of dark chert layers. The figure is a lithological log; individual chert masses are not formal named beds.
Lowest chert-bearing package. Several dark chert horizons occur below the first internal nodular, hardground-bearing sandstone.
First internal hardground. A hardened surface caps nodular, bioturbated sandstone beneath the lowest shelly-pebbly channel lag.
Lowest channel-lag deposit. Pebbly, shell-rich sandstone directly overlies this internal hardground.
Second chert-bearing package. A further group of dark chert layers separates the lowest lag from the middle hardground complex.
Middle complex: lower hardground. Nodular sandstone terminates at the lowest of three closely spaced internal surfaces.
Middle channel-lag deposit. Shelly-pebbly sandstone occurs between the lower and middle surfaces of this complex.
Middle complex: middle hardground. A separate hardened surface overlies the middle channel lag and underlies the pale-concretion interval.
Pale siliceous-concretion interval. Pale siliceous concretions, distinguished from dark chert in the figure key, occur below the upper nodular bed.
Middle complex: upper hardground. The nodular bed is capped by the third surface, completing four internal hardgrounds above the basal Culverhole pair.
Main chert-bearing package. Closely spaced dark chert layers extend above this complex to the upper channel lag.
Upper channel-lag deposit. A third shelly-pebbly sandstone interrupts the chert succession.
Upper chert and terminal nodular package. Further dark cherts precede the nodular, bioturbated sandstone beneath the Whitecliff Hardground. No individual layer thicknesses are invented.
Whitecliff Hardground. The mineralised top of the Whitecliff Chert Member is the lower boundary of the Bindon Sandstone. The overlying glauconite-rich, pebbly interval is the Coarse Band of earlier descriptions. The boundary is recognised by the hardground and associated facies change, not by the highest occurrence of chert.
Bindon Sandstone Member
Bed 1, basal pebbly and glauconitic interval. The basal bed above the Whitecliff Hardground includes coarse glauconitic sediment and reworked clasts. It is shown at King’s Hole in the published correlation section. “Coarse Band” is an informal descriptive name; no independent formal Member rank is assigned to it.
Bed 2, chert-bearing calcarenites. Sandy, shell-fragment-rich limestone contains chert layers. Their presence is important at King’s Hole: the lower Bindon Sandstone belongs above the Whitecliff Hardground even where it remains cherty. The number and thickness of chert beds vary along the coast and are not transferred from another locality.
Bed 3, chert-free sandstone and calcarenite. The succeeding bed is chert-free and shows wavy or inclined bedding in the modern section. Its sand and shell debris reflect deposition and movement by marine currents. No separate, locally measured thickness is stated here because the recovered figure does not justify a precise individual value.
Bed 4, upper cross-bedded and disturbed sandstone. The upper bed includes festoon cross-bedding and disturbed or contorted bedding. Gallois’s King’s Hole column records this package beneath the terminal hardground. Such structures concern sediment movement and deformation before full cementation, not a new geological formation.
Small Cove Hardground. The indurated, burrowed top of the Upper Greensand is the basal surface of the Chalk succession. It separates the Bindon Sandstone from the condensed Beer Head Limestone. The Whitecliff museum ammonite Arrhaphoceras (Natural History Museum C 41977, Grimsdale collection) has uncertain bed provenance and probably came from the Bindon Sandstone; it cannot be used as a securely bed-numbered find.
CHALK GROUP
GREY CHALK SUBGROUP
Beer Head Limestone Formation
The modern BGS formation comprises the condensed Cenomanian limestone below the Humble Point Hardground. The local Hooken and Little Beach subdivisions of Jarvis and Woodroof are retained below as historical named intervals. The current Lexicon lists their former Member names as obsolete and does not retain them as formal subdivisions, so they are not given modern Member bars. White Cliff lacks the Pounds Pool interval seen farther west at Hooken and Beer Head. The regional maximum of 10.4 m at Hooken is not a Whitecliff thickness. The 1903 Whitecliff observations recorded approximately 4 ft (1.22 m) in the north, thinning to 2 ft (0.61 m) towards King’s Hole. These old measurements apply to the authors’ condensed limestone division.
Hooken Nodular Limestone, historical local interval. A thin remnant of this shell-detrital limestone interval is reported at White Cliff. In the older A/B/C scheme it corresponds to division A 2; the underlying A 1/Pounds Pool division is not established here. The full type-section thickness and fauna at Hooken are therefore not assigned to Seaton Hole.
King’s Hole Hardground. This surface caps the historical Hooken interval and marks the base of the Little Beach interval. It forms part of the condensed basal Chalk succession. The full regional hardground fauna is not treated as a collection made at King’s Hole merely because the surface bears that name.
Little Beach Bioclastic Limestone, historical local interval. The shell-rich limestone above the King’s Hole Hardground is the dominant part of the thin local basal Chalk sequence in the modern interpretation. The older Whitecliff description distinguishes compact yellowish-white shelly limestone from a greener, phosphatic upper part. Its fossils and clasts may include reworked material, so fossil age and the final deposition of the enclosing bed need not be identical.
Humble Point Hardground. This caps the Beer Head Limestone in the current BGS scheme. It separates the Grey Chalk succession from the overlying Pinnacles interval, which older publications included within Beer Head Limestone. That historical inclusion is not followed here.
WHITE CHALK SUBGROUP
Holywell Nodular Chalk Formation
Pinnacles Glauconitic Limestone, historical local interval. The thin glauconitic interval between the Humble Point and Haven Cliff hardgrounds is reported at White Cliff in the Jarvis–Woodroof interpretation. BGS places its regional equivalents with the basal Holywell Nodular Chalk, including the Plenus Marls–Melbourn Rock interval, rather than in Beer Head Limestone. This is a condensed late Cenomanian interval; the name alone does not imply that the thicker Pinnacles type section at Hooken is present at Seaton Hole.
Haven Cliff (Neocardioceras) Hardground. This surface forms the top of the historical Pinnacles interval and the base of the Connett’s Hole interval. It is a named marker recognised in the Whitecliff scheme, despite being named after another locality. The old “base of Seaton Chalk” is therefore a position within the modern White Chalk succession, not the base of the entire Chalk Group.
Connett’s Hole Nodular Chalk, historical local interval. Defined at White Cliff with 13.5 m preserved, this local unit runs from the Haven Cliff Hardground to Flinty Hardground 5. It comprises nodular chalk and hardgrounds, with sand and glauconite at the base. BGS relates this local unit to the Holywell Nodular Chalk; that broad correlation does not provide a new bed-by-bed remeasurement of the boundary. The older name remains useful for recognising the published local section.
Beer Stone-equivalent beds. The 1903 Whitecliff log tentatively identified a 5 ft (1.52 m) interval of grey-streaked, less nodular chalk as the equivalent of the Beer Stone. The authors explicitly distinguished its appearance from the quarried freestone at Beer. It is a correlation, not evidence that the complete quarry lens or quarry fauna occurs at Seaton Hole.
West Ebb Marl. The regional local-member scheme recognises this marl above the Beer Stone interval as an important marker. The full Whitecliff log from the defining 1984 paper was not recovered, so no exact Whitecliff thickness, sublayer count or fossil list is assigned to this marl here.
Branscombe Hardground. This is a major omission surface within the local lower Chalk scheme. It removes very different amounts of strata along the coast. At White Cliff, additional chalk and hardgrounds survive above it within the historical Connett’s Hole interval, so it must not simply be equated with the top of that interval or with Flinty Hardground 5. The strongly condensed relationship at Hooken is not transferred here.
Upper Connett’s Hole interval and correlation limits. The local historical member scheme and modern formation scheme are not identical. Chalk above the Branscombe Hardground and below Flinty Hardground 5 is retained here as a separately identified interval, without assigning every intervening nodular bed to a precise modern boundary. Tocher’s 1984 thesis records approximately 9 m and eight separate hardgrounds in this expanded Whitecliff interval, compared with their merged expression farther west. The defining published graphic log is still required to resolve all eight individually and complete a modern bed-by-bed reconciliation.
Flinty Hardground 1. Tocher’s 1984 review of the Whitecliff succession reports the first appearance of Mytiloides cf. labiatus between the Branscombe Hardground and this horizon. It is therefore a separately documented numbered marker. No thickness or position within the 1894 numerical beds is inferred.
Flinty Hardground 5. The uppermost numbered flinty hardground caps the historical Connett’s Hole Nodular Chalk and underlies the Beer Roads Flinty Chalk. Its position is explicitly specified by the BGS review of the local scheme.
New Pit Chalk Formation
Beer Roads Flinty Chalk, historical local interval. The unit named from the east side of Beer Beach begins above Flinty Hardground 5. Soft white chalk contains repeated flint and marl seams. It is broadly the local equivalent of the New Pit Chalk and is associated with the Terebratulina lata zone. The historical continuation at the north side of Beer Harbour is given separately below, so that its measured and estimated beds are not mistaken for measurements at the Seaton Hole end of the cliff.
Rowe’s Two Foot Band (Common Hill Marl). This local marker is correlated by BGS with New Pit Marl 1. The “two foot” label is historical, not an independently measured Seaton Hole thickness. Its regional correlation is useful for reading the published Beer Roads succession.
Rowe’s Four Foot Band. The second named marl-band marker is correlated with New Pit Marl 2. A measured Whitecliff thickness and a direct match to the nineteenth-century numbered beds are not asserted.
Lewes Nodular Chalk Formation
Annis’ Knob higher-Chalk interval. The high bluff above the northern side of Beer Harbour, at the southern end of the White Cliff section, exposes nodular, flinty chalk of the old Holaster planus and Micraster cortestudinarium zones. It is treated as a distinct higher-level reference, not as a bed accessible on the Seaton Hole beach. The measured 1894 packages are given below. No complete Seaford Chalk succession is inferred here from nearby coastal localities.
Annis’ Knob Flint and zonal-boundary caution. A conspicuous nodular flint course cuts the bluff. Earlier workers placed a convenient zonal division at this lithological marker, but subsequent fossil collecting put the faunal change higher. The flint is a useful rock marker, not a universally exact boundary between the two echinoid zones. BGS discusses its correlation with the Breaky Bottom Flint farther east as probable, not certain.
Historic measured sections: how to read the following beds
The following logs preserve the individual packages actually published for Whitecliff and its Beer-end continuation. Each author’s numbering is separate. Their widths, colours and fossil lists are observations from older exposures, not new formal beds. They supplement the modern account above; they must not be added to it as extra thickness. Imperial measurements are retained with approximate metric conversions.
De la Beche’s 1826 Whitecliff subdivisions
The nine numbered sandstone packages were described from top down. Their individual thicknesses were not supplied. “Green earth” is the author’s terminology for the green granular constituent. These early lithological divisions are kept distinct from both Meyer’s numbering and the modern members. Their main value is the record of alternating sandstone/chert packages and the vertebrate-bearing Bed 8.
1826 Bed 1. Yellowish-white sandstone. No numerical thickness was given.
1826 Bed 2. Nodules of compact light-coloured sandstone, connected by sandstone containing green earth. No numerical thickness was given.
1826 Bed 3. Yellowish-brown sandstone containing chert seams. No numerical thickness was given.
1826 Bed 4. Yellowish sandstone containing some green earth and numerous quartz grains. No numerical thickness was given.
1826 Bed 5. Nodules of chert in yellowish-brown sandstone. No numerical thickness was given.
1826 Bed 6. Sandstone rich in green earth mixed with nodules of light-coloured sandstone. No numerical thickness was given.
1826 Bed 7. Yellowish-brown sandstone with chert seams. No numerical thickness was given.
1826 Bed 8. Coarse-grained sandstone with fish teeth and vertebrae, broken shells and other debris. No numerical thickness was given.
1826 Bed 9. Yellowish-brown sandstone with chert seams. No numerical thickness was given.
1826 unnumbered lower unit 1. Greenish-yellow or brown sands equivalent to Foxmould; more green earth than at Lyme, and reported chert nodules. Separate unnumbered lower division; do not assign to a numbered bed or force modern correlation.
1826 unnumbered lower unit 2. Sands rich in green earth containing fossils and indurated portions compared with Lyme, apparently with more iron pyrites. The paper compares fauna to the preceding Lyme account but does not individually assign each named taxon to White Cliff. Keep comparative statement rather than import the Lyme list.
1826 PlateXVI: additional labelled packages
The original White Cliff drawing separates the overlying Chalk into three broad flint-based divisions and a compact basal bed. These are historical descriptive packages, not modern formations. The accompanying enlarged sandstone drawing repeats the text’s alternation of chert-bearing beds and green-grained sandstone, including the fish-bearing layer; it adds no numerical thicknesses.
1826 plate package 1. Chalk with numerous flints. This is a separately labelled interval in the descending White Cliff drawing; no numerical thickness is given.
1826 plate package 2. Chalk in which flints are more rare. This is a separately labelled interval in the descending White Cliff drawing; no numerical thickness is given.
1826 plate package 3. Chalk without flints. This is a separately labelled interval in the descending White Cliff drawing; no numerical thickness is given.
1826 plate package 4. Compact bed with quartz grains. This is a separately labelled interval in the descending White Cliff drawing; no numerical thickness is given.
1826 plate: upper sandstone annotations. The simplified drawing labels yellowish-white sandstone with green earth near its upper and lower parts and chert nodules. Below it are yellow sandstone with chert seams and sands of varied colours. These graphic observations are retained without forcing a one-to-one match to the numbered text beds.
1826 plate: lower sands and Cow Stones. The lower drawing labels greenish-yellow sands, with chert nodules, above green-earth-rich sands containing indurated nodules labelled Cow Stones. The nodules are components of the sand, not an additional thickness-bearing bed.
Meyer’s 1874 numbered succession: Whitecliff observations
The original twenty-bed scheme was regional, but the observations below retain only its Whitecliff measurements and explicitly localised fossils. Beds are listed upwards. They are historical units, not twenty newly defined local beds or a modern formation scheme. Regional thicknesses are labelled as such. In particular, the old measurements near the Greensand–Chalk contact differ markedly from later logs and must not be forced into a precise modern correlation.
1874 Bed 1. Greenish sandy argillaceous strata; basal grit of small subangular pebbles or fragments of underlying rocks. The printed thickness is 3 ft; explicit White Cliff value. Whitecliff-labelled fossils: Arca carinata.
1874 Bed 2. Clay-rich sand with abundant green earth, dark greyish to pale brownish green; fossiliferous partly hardened nodules near top. The printed thickness is 15 ft; explicit White Cliff value. Whitecliff-labelled fossils: Hemipneustes Greenovii, Pecten orbicularis (small variety), Cardium Hillanum, Lucina orbicularis, Pectunculus umbonatus, Trigonia spectabilis. The local fossils were casts and impressions in indurated nodules.
1874 Bed 3. Buff and greyish marly sands with large rounded, spongiform concretions. The printed thickness is 40 ft; explicit White Cliff value. Whitecliff-labelled fossils: Exogyra conica, Exogyra laevigata, Pecten orbicularis (variety).
1874 Bed 4. Light yellowish, slightly marly sands with irregular concretions; upper sandstone-pebble shingle bed with broken Pecten and Exogyra valves. The printed thickness is 25 ft (?); explicit White Cliff headline; uncertainty printed. Whitecliff-labelled fossils: Pecten (broken valves), Exogyra (broken valves). The four sublayers total 24½ft, although the printed total is 25 ft; both values are retained.
The following sublayers are listed downwards, exactly as the source presents the local subsidiary log.
1874 Bed 4, 4 a. 1 ft (approximately 0.30 m). Argillaceous sand.
1874 Bed 4, 4 b. 1.5 ft (approximately 0.46 m). Dark greyish sandy clay with pyrites.
1874 Bed 4, 4 c. 2 ft (approximately 0.61 m). Greenish grey sand crowded with sandstone pebbles and broken shells.
1874 Bed 4, 4 d. 20 ft (approximately 6.10 m). Sands with irregular concretions.
1874 Bed 5. Light-coloured sand with nodular or tabular chert. The printed thickness is 25 ft; explicit White Cliff headline. The three explicit sublayers total 22½ft, conflicting with the 25 ft headline; no artificial correction is made.
The following sublayers are listed downwards, exactly as the source presents the local subsidiary log.
1874 Bed 5, upper layer. 12 ft (approximately 3.66 m). Sand with chert in layers.
1874 Bed 5, middle layer. 3.5 ft (approximately 1.07 m). Bed of sandstone pebbles with broken shells.
1874 Bed 5, lower layer. 7 ft (approximately 2.13 m). Sand with chert.
1874 Bed 6. Light-coloured, locally almost white sand passing into sandstone. The printed thickness is 1 ft; explicit White Cliff value.
1874 Bed 7. Explicitly absent at Whitecliff (0 ft). The regional bed comprises sandstone pebbles and oyster fragments; it is recorded here as an absence, not added to the local thickness.
1874 Bed 8. Buff sand beds, irregularly structured, with zones of sandstone pebbles. The printed thickness is 5 ft; explicit White Cliff value.
1874 Bed 9. Buff sandstone of sugary appearance with fine green grains and quartzose-grit layers. The printed thickness is 5 ft; explicit White Cliff value.
1874 Bed 10. Rubbly yellowish quartzose sands in a chalky matrix. The printed thickness is 6 ft; explicit White Cliff value. Whitecliff-labelled fossils: Rhynchonella gallina.
1874 Bed 11. Yellowish quartzose sand with fine green grains in a semicrystalline chalky matrix. The printed thickness is 2 ft; explicit White Cliff value.
1874 Bed 12. Compact nodular rubbly bed with green and quartz grains in chalky matrix; uneven upper surface, locally iron-stained boundary. The printed thickness is 1 ft; explicit White Cliff value. Whitecliff-labelled fossils: Ammonites varians, Scaphites aequalis, Cardium (allied to C. Hillanum), Cardium Mailleanum, Ostrea (allied to O. normaniana), Rhynchonella Schloenbachi.
1874 Bed 13. Grey or brown chalk containing green grains, quartz grains and phosphatic nodules. The printed thickness is 4 ft; explicit White Cliff value. Whitecliff-labelled fossils: Ammonites navicularis, Rhynchonella dimidiata, Rhynchonella Mantelliana. Meyer noted casts and possible reworking in this bed regionally, without diagnosing each Whitecliff specimen individually.
1874 Bed 14. Hard nodular chalk containing fine quartz grains. The printed thickness is 4 ft; explicit White Cliff value.
1874 Bed 15. Creamy white or yellowish semicrystalline sandy chalk, correlated historically with Beer Stone of the quarries. The printed thickness is 5 ft; explicit White Cliff value.
1874 Bed 16. Hard nodular sandy chalk without flints, semicrystalline; historically correlated with the quarry Bastard Freestone. The printed thickness is 8 ft; explicit White Cliff value. The later 1903 memoir considered the printed 8 ft probably a misprint for 18 ft; the two observations are not silently reconciled.
1874 Bed 17. Marly, locally nodular chalk with pale grey or yellow bands, dispersed finger-like flints and a basal zone of large flints. The printed thickness is about 10 ft; regional bed estimate; White Cliff included in stated outcrop, not a separately labelled measurement. This estimate is not a separate Whitecliff measurement.
1874 Bed 18. More or less nodular chalk with numerous flints, mainly in layers. The printed thickness is about 40 ft; regional bed estimate; White Cliff explicitly part of the outcrop. This estimate is not a separate Whitecliff measurement. Whitecliff-labelled fossils: Terebratula semiglobosa.
1874 Bed 19. Hard chalk without flints; greyish marly band about 3 ft thick above its middle. The printed thickness is about 15 ft; regional estimate; White Cliff included in bed-outcrop statement. This estimate is not a separate Whitecliff measurement. Whitecliff-labelled fossils: Inoceramus Cuvieri.
1874 Bed 20. White chalk with numerous flints. The printed thickness is not given for White Cliff; 60 ft explicitly Beer Head only; do not assign to White Cliff. Neither the 60 ft Beer Head description nor the 70 ft regional table value is applied here. Whitecliff-labelled fossils: Galerites albo-galerus, Spondylus spinosus, Ostrea, Crania ignabergensis, Terebratula carnea, Terebratulina gracilis, Terebratulina striata.
1900 Survey lower-division log, Whitecliff, shown below in upward order
The source published these six packages in descending order without bed numbers. The labels L 1–L 6 below are editorial cross-references only, with L 1 at the top. The sum is 84½ft (25.76 m) seen. It is not a complete measured thickness of the modern Foxmould Member.
L 6 — Basal dark, wet greensand. 15 ft (approximately 4.57 m). Very dark green, wet sand was visible for this thickness in 1894; its base was concealed. The separately recorded 1874 basal 3 ft and the estimated total 18–20 ft below the lowest cowstone do not form additional beds.
L 5 — Lowest cowstone-bearing sands. 15 ft (approximately 4.57 m). Dark grey to green sand with large lens-shaped calcareous concretions. This is the lower package from which the richest recorded cowstone fauna was obtained.
L 4 — Clayey sand with irregular sandstone courses. 30 ft (approximately 9.14 m). Dark purplish-grey, clay-rich sand with calcareous sandstone beds at uneven intervals. The historical fossils Exogyra conica and Serpula (Vermicularia) concava were common.
L 3 — Sands with extensive sandstone layers. 8 ft (approximately 2.44 m). Soft greenish-grey sand containing laterally persistent calcareous sandstone layers.
L 2 — Light-grey sands with sparse concretions. 14 ft (approximately 4.27 m). Soft light-grey sands containing scattered rounded calcareous concretions.
L 1 — Upper hard shelly sandstone. 2.5 ft (approximately 0.76 m). Hard brownish calcareous sandstone; its basal 6–12 in (0.15–0.30 m) was rough, glauconitic and rich in fossils. The shell-bed fauna is listed separately below.
Lower cowstone fauna, historical names. Echinospatagus murchisonianus, Hemipneustes greenovi, Serpula (Vermicularia) concava, Serpula polygonalis, Anatina sp., Arca (Cucullaea) carinata, Cardium hillanum, Cytherea caperata, Exogyra undata, Lucina orbicularis, Inoceramus sulcatus, Pecten orbicularis, Pectunculus umbonatus, Trigonia aliformis, Trigonia scabricola, Trigonia spectabilis, Venus immersa, Turritella sp.. These are the Whitecliff records attributed in the memoir to Meyer and/or Rhodes’s 1894 Survey collecting. Names are reproduced as historic determinations; no new species-level revision is implied.
Upper shelly-sandstone fauna, historical names. Placosmilia tuberosa, Cidaris, Pentacrinus, Porosphaera, Ceriopora papularia, Serpula, Terebratella pectita (?), Anomia sp., Ostrea frons, Exogyra conica, Exogyra columba, Pecten dutemplei, Pecten (Neithea) quadricostatus, Lima semisulcata, Cardium, Opis (?), Cucullaea, Pectunculus umbonatus, Cyprina angulata (?), Trigonia affinis (= excentrica), Venus immersa (?), Turritella sp.. The published common forms include the coral, Exogyra conica and the strongly ribbed pectinid. Several identifications were doubtful and many specimens were casts; those reservations are retained.
1900 Survey upper-division log, Whitecliff to King’s Hole
The source’s descending numbering is retained: Bed 1 is the highest and Bed 16 the lowest. The total is 65½ft (19.96 m). This old “Chert Beds” division spans more than the modern Whitecliff Chert Member, including strata now assigned to Bindon Sandstone. Its bed numbers must not be confused with Gallois’s Bindon Beds 1–4.
1900 Bed 1. 8 ft (approximately 2.44 m). Nodular calcareous sandstone, less cemented downwards, with occasional sandy chert nodules. The printed occurrence table records Cidaris, Rhynchonella schloenbachi (Cidaris as spines and plates).
1900 Bed 2. 3 ft (approximately 0.91 m). Yellow sandstone with large brown chert masses.
1900 Bed 3. 1.5 ft (approximately 0.46 m). Soft, relatively coarse yellow-green sand containing quartz and glauconite.
1900 Bed 4. 4 ft (approximately 1.22 m). Soft yellowish sandstone with lens-like brown chert layers.
1900 Bed 5. 4 ft (approximately 1.22 m). Hard nodular greenish calcareous sandstone, weathering into rough lumps and becoming less nodular below. Exogyra digitata was recorded as common. The printed occurrence table records Orbitolina concava, Cidaris, Ostrea frons, Exogyra digitata, Cardium (Cardium as a cast; Cidaris as spines and plates).
1900 Bed 6. 12 ft (approximately 3.66 m). Grey sandstone with dark-grey chert, with smaller cherts in the upper part.
1900 Bed 7. 3 ft (approximately 0.91 m). Rough, shell-rich sandstone weathering brown and containing abundant separate Exogyra valves. The printed occurrence table records Cidaris, Ceriopora sp., Exogyra digitata (Cidaris as spines and plates).
1900 Bed 8. 7 ft (approximately 2.13 m). Yellowish sand and sandstone with irregular grey chert masses; the higher cherts were strongly iron-stained, and hard buff calcareous layers occurred near the base.
1900 Bed 9. 3.5 ft (approximately 1.07 m). Grey glauconitic sand with fine-grained calcareous sandstone concretions.
1900 Bed 10. 4 ft (approximately 1.22 m). Grey glauconitic sand with black chert.
1900 Bed 11. 3 ft (approximately 0.91 m). Grey sandstone with broken shells and abundant pieces described as calcareous sponge; occasional chert occurred in its upper part. The printed occurrence table records Ceriopora sp., Exogyra columba, Pecten (Neithea) quinquecostatus.
1900 Bed 12. 3 ft (approximately 0.91 m). Hard grey calcareous sandstone with black chert.
1900 Bed 13. 5 ft (approximately 1.52 m). Brownish loamy sand with a middle layer of large irregular chert and hard calcareous lumps above and below.
1900 Bed 14. 2 ft (approximately 0.61 m). Dark-grey glauconitic sand grading down into dark-green clayey sand, with calcareous sandstone lumps at the base.
1900 Bed 15. 1.5 ft (approximately 0.46 m). Rough nodular green-grey calcareous sandstone containing sandstone pebbles and fossils. The printed occurrence table records Elasmostoma sp., Radiopora ornata, Exogyra columba, Lima semisulcata, Spondylus sp..
1900 Bed 16. 1 ft (approximately 0.30 m). Soft green sand with thin grey partings.
Upper-division fauna, historical names. Orbitolina concava, Elasmostoma sp., Cidaris, Ceriopora sp., Radiopora ornata, Rhynchonella schloenbachi, Ostrea frons, Exogyra columba, Exogyra digitata, Pecten (Neithea) quinquecostatus, Lima semisulcata, Spondylus sp., Cardium. Cardium was recorded as a cast and Cidaris as spines and plates. The original printed table has been checked against the scan: its occurrences are assigned individually to Beds 1, 5, 7, 11 and 15 above.
1903 basal Chalk contact. The source describes a generally even contact, locally penetrated by angular pockets and fissures filled from above. Similar hardness on both sides made the boundary less obvious in the cliff than its stratigraphical importance might suggest.
1903 lower and central limestone layers. The thicker northern blocks contained Ceriocava ramulosa near the base, which the authors interpreted as evidence of Meyer’s Bed 10. The central rock was compact yellow-white shelly limestone with scattered glauconite and abundant quartz grains. This historical inference differs from the later interpretation that the Pounds Pool interval is absent at White Cliff; it is not converted into an asserted modern Pounds Pool occurrence.
1903 upper limestone, division B. Greener limestone contained coarser glauconite, brown-green staining and partly phosphatised lumps, with fewer fossils than below. The authors described this upper layer as about 1 ft (0.30 m), varying between 10 and 18 in (0.25–0.46 m), while the underlying limestone varied more strongly in thickness.
1903 interpretation of division C. The authors did not recognise a continuous C bed at White Cliff, recording only glauconitic sand nests in the base of the overlying Turonian limestone. The later recognition of a very condensed Pinnacles interval uses a revised local scheme; the older observation is retained without claiming uniform absence or equivalence.
1903 Survey lower-Chalk log, southern Whitecliff
These beds are listed upwards, as in the source. Beds 1–7 total 34½ft (10.52 m); Bed 8 adds 7½ft (2.29 m). The old Rhynchonella cuvieri-zone boundary was placed tentatively at the top of Bed 7. These numerical beds are not silently equated with modern formation boundaries or with the full 13.5 m Connett’s Hole type interval.
1903 Bed 1. 3 ft (approximately 0.91 m). Very hard, rough nodular yellow-white limestone with scattered quartz and glauconite, especially at the base; it is sharply separated from the limestone below.
1903 Bed 2. 6 ft (approximately 1.83 m). Hard yellowish nodular chalk.
1903 Bed 3. 5 ft (approximately 1.52 m). Less hard grey-streaked chalk with few nodules, divided into two beds by a distinct surface; tentatively correlated with Beer Stone.
1903 Bed 4. 9 ft (approximately 2.74 m). Rough nodular chalk with a basal course of very hard yellow nodules.
1903 Bed 5. 8 ft (approximately 2.44 m). Nodular chalk with a basal course of hard yellow nodules and a few flints near the top.
1903 Bed 6. 1 ft (approximately 0.30 m). Hard nodular grey-streaked chalk with some flints and a yellow-nodule layer at its top.
1903 Bed 7. 2.5 ft (approximately 0.76 m). Hard white, grey-streaked chalk containing flints and capped by yellow nodules.
1903 Bed 8. 7.5 ft (approximately 2.29 m). Softer whitish chalk, with a basal black-flint layer, scattered flints and yellow nodules at the top. The author was uncertain whether to include this bed in the lower or succeeding fossil zone.
1903 Bed 1 fauna. Cardiaster pygmaeus, Cidaris hirudo, Discoidea dixoni, Hemiaster minimus, Rhynchonella cuvieri. Cidaris was represented by spines. These historical records belong to the basal nodular chalk in this log, not to the Upper Greensand.
1903 Beds 2–3 fauna. Inoceramus mytiloides, Rhynchonella cuvieri, Cidaris hirudo, Discoidea dixoni, Hemiaster minimus, Galerites subrotundus, Pycnodus. The fish was represented by a palate or crushing-tooth plate. The published record combines the two beds, so the fossils are not assigned separately to Bed 2 or Bed 3.
1903 continuation at the north side of Beer Harbour
This is the Beer-end continuation of the Whitecliff account, not a separate measured log at Seaton Hole. The original numbering continues upwards from Bed 8. Beds 14–17 are visual estimates, and an additional upper interval of about 20 ft (6.10 m), including a dark-grey marl, was described at southern Whitecliff without a new bed number.
1903 Bed 9. 3 ft (approximately 0.91 m). White chalk with numerous black flints and some yellowish lumps.
1903 Bed 10. 7 ft (approximately 2.13 m). Soft chalk, initially flint-free and becoming flinty above; the historical Terebratulina gracilis var. lata was recorded.
1903 Bed 11. 8 ft (approximately 2.44 m). Soft chalk with abundant flints, partly in layers and partly scattered; the same small brachiopod was common.
1903 Bed 12. A nearly continuous black-flint layer; the source gives no separate thickness.
1903 Bed 13. 3 ft (approximately 0.91 m). Grey-veined, marly, flint-free chalk.
1903 Bed 14. 15 ft (approximately 4.57 m). Chalk with scattered flints; the thickness was estimated by eye because the upper beds were inaccessible.
1903 Bed 15. 4 ft (approximately 1.22 m). Chalk containing two nodular-flint layers; thickness estimated by eye.
1903 Bed 16. 6 ft (approximately 1.83 m). Flint-free chalk with a soft marly lower part forming a recess; thickness estimated by eye.
1903 Bed 17. 20 ft (approximately 6.10 m). Flinty chalk with layers and scattered nodules; thickness estimated by eye.
Unnumbered upper chalk-and-marl interval. Approximately 20 ft (6.10 m) of higher chalk, including a dark-grey marl, was reported at southern Whitecliff. This is an old estimate with an uncertain zonal placement, not an extra precisely measured modern member.
1904 Survey account of the 1894 Annis’ Knob section
The following eight packages are listed downwards, as in the source. A 1–A 8 are editorial labels only. They describe the higher bluff at the Beer end of White Cliff and are not collecting directions. Historical zonal interpretations differed between Jukes-Browne and Rowe; this account preserves the rock observations without treating the prominent flint as a proven faunal boundary.
A 1 — Annis’ Knob package. 10 ft (approximately 3.05 m). Chalk with many flint layers, some flints hollow, and hard nodular lumps lower down. The source records Micraster cortestudinarium, Terebratula carnea, Porosphaera globularis and Inoceramus.
A 2 — Annis’ Knob package. 10 ft (approximately 3.05 m). Hard rough nodular chalk with numerous flints and a yellowish rocky top containing brown phosphate fragments; Micraster was common.
A 3 — Annis’ Knob package. 7.5 ft (approximately 2.29 m). Hard rough nodular chalk with flints and a very hard yellowish upper bed. Historical fossils include Echinocorys scutatus, Micraster, Rhynchonella reedensis and a doubtful Parasmilia coral.
A 4 — Annis’ Knob package. 1 ft (approximately 0.30 m). Soft grey-white chalk without flints.
A 5 — Annis’ Knob package. 0.5 ft (approximately 0.15 m). Conspicuous black-flint course. This is the prominent lithological marker discussed in the disputed historical zonal correlation.
A 6 — Annis’ Knob package. 12 ft (approximately 3.66 m). Rough chalk with scattered flints and nodular layers. Recorded fossils include Holaster planus, Micraster leskei, Micraster cortestudinarium, Terebratula carnea and Rhynchonella reedensis.
A 7 — Annis’ Knob package. 10 ft (approximately 3.05 m). Hard rough flinty chalk with small light-brown phosphate pieces. Recorded fossils include Holaster planus, Rhynchonella plicatilis, Terebratulina gracilis var. lata (doubtful in the source), Terebratula carnea and Cyphosoma radiatum.
A 8 — Annis’ Knob package. 1 ft (approximately 0.30 m). Rough chalk full of very hard yellowish lumps and some pale-brown phosphate, seen for this thickness; the base was not established.
Faulted higher chalk beside the bluff. The 1904 account notes a small east-downthrowing fault beside the path, exposing approximately 20 ft (6.10 m) of higher, less nodular chalk with hollow flints. This is a structural repetition or juxtaposition, not an additional bed to add above the measured column.
Evidence limits
The nineteenth-century logs are unusually detailed, but they pre-date modern member boundaries and do not provide a safe one-to-one conversion. The complete 1984 Whitecliff graphic log was not available for independent inspection, and some historic figure measurements remain unresolved. Accordingly, this is a detailed source-led account with stated gaps, not a claim that every modern numbered Chalk hardground has been fully remeasured or correlated. Quarry-only faunas, the full Hooken succession, the east-Axe Triassic–Jurassic section and other localities’ bed thicknesses have been excluded. Exposure and access must be checked separately on the day.
References
De la Beche, H.T. (1826). On the Chalk and Sands beneath it (usually termed Green-sand) in the Vicinity of Lyme Regis, Dorset, and Beer, Devon. Transactions of the Geological Society of London, second series,2,109–118; Whitecliff pp 115–116 and PlateXVI.
Meyer, C.J.A. (1874). On the Cretaceous rocks of Beer Head and the adjacent cliff-sections, and on the relative horizons therein of the Warminster and Blackdown fossiliferous deposits. Quarterly Journal of the Geological Society,30,369–393.
Tocher, B.A. (1984). Palynostratigraphy of uppermost Albian to basal Coniacian (Cretaceous) sediments of the western Anglo-Paris Basin. PhD thesis, City of London Polytechnic.
Mortimore, R.N., Wood, C.J. & Gallois, R.W. (2001). British Upper Cretaceous Stratigraphy. GCR 23, Southern Province chapter; regional correlation context only.
Gallois, R.W. (2001). The lithostratigraphy of the Mercia Mudstone Group of the south Devon coast. Geoscience in south-west England,10,195–204.
Gallois, R.W. (2004). The stratigraphy of the Upper Greensand (Cretaceous) of south-west England. Geoscience in south-west England,11,21–29.
Gallois, R.W. & Owen, H.G. (2018). The stratigraphy of the mid Cretaceous (Albian) Upper Greensand Formation of the Wessex Basin and South West England, UK. Acta Geologica Polonica,68,161–180.
Hopson, P.M. (2005). A stratigraphical framework for the Upper Cretaceous Chalk of England and Scotland. BGS Research Report RR/05/01.
Hopson, P.M., Wilkinson, I.P. & Woods, M.A. (2008). A stratigraphical framework for the Lower Cretaceous of England. BGS Research Report RR/08/03.
British Geological Survey. Lexicon: Beer Head Limestone Formation.
Edwards, R.A. & Gallois, R.W. (2004). Geology of the Sidmouth district. BGS Sheet Explanation.
British Geological Survey (2011). Geology of south Dorset and south-east Devon and its World Heritage Coast. Special Memoir.
Jukes-Browne, A.J. & Hill, W. (1900). The Cretaceous rocks of Britain, Volume I: The Gault and Upper Greensand of England. Geological Survey memoir.
Jukes-Browne, A.J. & Hill, W. (1903). The Cretaceous rocks of Britain, Volume II: The Lower and Middle Chalk of England. Geological Survey memoir.
Jukes-Browne, A.J. & Hill, W. (1904). The Cretaceous rocks of Britain, Volume III: The Upper Chalk of England. Geological Survey memoir.
West, I.M. Beer and Seaton, Geological Field Guide. University of Southampton.
SAFETY
Rockfalls and landslips can occur without warning. Keep well away from the cliff foot, overhangs and fresh fall debris; never climb the cliffs to reach a fossil. East Devon District Council relays the Coastguard’s advice to remain at least the height of the cliff away from its base. If the tide or beach shape prevents a safe separation, do not enter that section. Coastal defences do not make the cliffs safe.
Check tides, weather and sea conditions before setting out. The beach link from West Walk can disappear as the tide rises, and wet rock and steep shingle make walking harder. Leave ample time to return and never use the armour as an escape route. The low-tide window varies with sea conditions; no fixed safe crossing time is given.
Wear footwear with good grip, keep children closely supervised and obey barriers and warning signs. Seaton beach has no lifeguard service. Carry a charged phone, tell someone your plans and, if somebody is cut off or in danger at the coast, call 999 or 112 and ask for the Coastguard.
EQUIPMENT
Take current tide information, a charged phone, water, weatherproof clothing and sturdy footwear. A camera, hand lens, scale and notebook help distinguish shell moulds and record their position without damaging them.
For any small loose finds that may be taken under current local arrangements, use soft wrapping, a rigid container and a label recording the exact beach sector and rock type. Do not bring tools for excavating cliff-foot sand or attached beds. The hard armour boulders are coastal infrastructure, not fossil-collecting material.
CLEANING AND TREATING
Photograph the naturally exposed surface before attempting any cleaning. Shells in weathered Greensand can be fragile even where the surrounding block is hard; a mould may be the only surviving record. Use gentle dry brushing only where the surface is sound and stop if grains or shell fragments detach.
Avoid acid, bleach, varnish and forceful scraping. Chalk fossils can be brittle, and a partly exposed specimen is easily damaged while removing matrix. Keep matching naturally broken pieces and the locality label together; seek specialist advice before preparing an unusual find.
IDENTIFY YOUR FINDS
Need help identifying a fossil? Share clear photos, where you found it and its size with the community.
FURTHER READING
Seaton Coastal Defence Scheme: completed works and access information
South West Coast Path: Sidmouth to Seaton and current route information
Natural England: Sidmouth to Beer Coast SSSI
East Devon District Council: cliff safety
Seaton Town Council: travel and parking
ACCESS RIGHTS
White Cliff at Seaton Hole forms the eastern end of Sidmouth to Beer Coast SSSI and belongs to the Jurassic Coast World Heritage Site. These designations protect important geological and biological features. Public beach access does not by itself establish permission to remove specimens: follow local notices and confirm the relevant landowner’s collecting requirements.
Where collecting is permitted, take only a small number of loose, naturally fallen specimens on the open foreshore, retaining their locality information. Do not excavate cliffs or attached beds, damage coastal defences or disturb vegetation and wildlife. Proposed excavation or other work that could affect the SSSI needs the landowner’s and Natural England’s advice and any necessary consent.
The official coastal-defence project reports completion and restored access in December 2025, using approximately 6,500 tonnes of imported Norwegian rock along about 600 m of the shore. This does not certify every route for a later visit. Check current signs, council notices and the Coast Path’s permanent Old Beer Road diversion; do not mistake the imported armour for naturally fallen local fossil-bearing rock.
Natural England’s management statement discusses responsible geological collecting but does not itself grant consent. Consult the official site record for the citation and management information.
It is important to follow our ‘Code of Conduct’ when collecting fossils or visiting any site. Please also read our ‘Terms and Conditions‘
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