The East Cliff and Langdon coast at Dover exposes a classic Chalk succession and a varied marine fauna. Langdon Stairs’ tunnel-and-ladder route offers a demanding approach to the shore, where tides and falling rock require particular care.
FIND FREQUENCY: ♦♦♦ – Loose chalk and flints can yield echinoids and shells, but abundance varies and fresh falls must be avoided.
CHILDREN: ♦ – Unsuitable for young children or anyone uncomfortable with a near-vertical ladder and difficult tidal shore.
ACCESS: ♦ – The National Trust describes a steep descent, tunnel and ladder to Langdon Bay; this is not an easy beach stroll.
TYPE: – Loose chalk and flint fossils on permitted shore, with nationally important strata in the cliffs.
DIRECTIONS
♦ Use the National Trust White Cliffs visitor-centre car park and current signs for Langdon Stairs. The visitor-centre address postcode is CT16 1HJ. For satnav, the National Trust recommends CT15 5NA because CT16 1HJ may direct you to the Eastern Docks ferry terminal. Follow the brown signs and turn into the car park at the sharp bend on Upper Road, before reaching the satnav destination.
♦ The described route descends approximately 85 m by a zigzag path, passes through a roughly 35 m tunnel and ends at a near-vertical ladder about 7 m high. Check the route is open before committing to the descent.
♦ Stay within sight of the ladder and return well before the tide reaches its foot. Do not substitute harbour-groyne scrambling or a long traverse from St Margaret’s Bay.
♦ Ref: 51.13173°N, 1.34699°E
FOSSIL HUNTING
At Dover, the shore reached by Langdon Stairs contains both loose chalk fossils and resistant flint specimens, but the visitor’s search area is much smaller than the East Cliff–Langdon scientific section described in geological papers. Follow the National Trust’s instruction to keep the ladder in sight. Within that limited area, compare the surfaces of detached chalk pieces with the beach shingle rather than following a promising bed along the cliff. Naturally weathered or broken faces can reveal shell edges, sponge outlines and echinoid tests without further damage to the exposure.
Echinoids are among the most rewarding recognisable finds. The local record includes heart-shaped Micraster, more dome-shaped Echinocorys and the thin-tested Sternotaxis. Rows of minute pores, a five-part arrangement of plates and small spine-attachment bumps distinguish a test from an ordinary rounded chalk nodule. Some specimens are flattened, incomplete or filled with chalk; flint examples may preserve an internal mould after the shell has disappeared. Look at the underside as well as the upper surface, but leave fragile chalk around the fossil rather than prising it free.
Shells and sponges broaden the search beyond complete sea urchins. Langdon Bay is the type locality of Inoceramus lamarcki, and its group occurs in sponge-bearing chalk below the Southerham marls. Broad shell fragments or impressions may be all that survives of a large bivalve. Smaller, compact brachiopods occur elsewhere in the succession: Terebratulina lata is recorded abundantly in Bridgewick Marl 1, while the overlying Basal Complex includes Orbirhynchia dispansa and the regular echinoid Gauthieria radiata. These associations explain why different chalk pieces can have very different fossils; an unproven beach block should not be assigned to a named bed from one fragment alone.
The harder, nodular Dover Chalk Rock has yielded small bivalves and gastropods together with a well-studied ammonite fauna. Hyphantoceras reussianum and Scaphites geinitzii are recorded from its upper nodular beds. Ammonites may survive as incomplete impressions or moulds, so a small ribbed or coiled fragment deserves recording even when it is not a complete spiral. They are special finds rather than something to expect on every visit. Photograph both the fossil and its enclosing rock, retain associated fragments together and obtain advice before attempting preparation.
Sponges are present in both chalk and flint, and are well represented in the locality’s photographs. Examine already exposed surfaces for a repeated network of pores or a recognisable body outline; not every cavity in a flint is a sponge. Some patterned chalk records burrowing rather than a body fossil, including Zoophycos in the succession above the Chalk Rock. Loose blocks may have fallen from beds high above the platform, so the bed directly behind a find need not be its source. Limit collecting to a few permitted loose specimens, avoid fresh falls and cliff toes, and leave attached fossils and large blocks undisturbed. The return climb is another reason to favour small, well-recorded finds over a heavy bag of rock.
A chronological record of fossil discoveries, geological research and scientific milestones associated with Dover.
1818–1819 – Early Chalk succession established
William Phillips described the coastal Chalk succession around Dover, helping to establish a lithological framework for these prominent cliffs.
1819 – An important inoceramid described
James Parkinson’s Inoceramus lamarcki is represented by type material from flint below the Southerham marls in Langdon Bay. The association provides an unusually precise connection between a historic species and the modern measured section.
1874–1876 – Dover linked with continental fossil zones
Hébert’s work in 1874 and Barrois’ in 1876 used the Dover cliffs in comparing British Chalk with fossil-zone successions in France. This helped turn a local cliff section into an international reference.
1899–1900 – Micraster and coastal biozones investigated
Arthur Rowe’s work on variation in Micraster, followed by Rowe and Sherborn’s Kent and Sussex coastal survey, used the Dover cliffs to refine Chalk fossil zones and their field recognition.
1903–1904 – Dover Chalk Rock and Basal Complex described
Jukes-Browne and Hill published detailed cliff sections, including Fan Bay. Their bed descriptions can now be matched with the Southerham and Caburn marls, Bridgewick markers and the condensed ammonite-bearing Dover Chalk Rock.
1981 – Boundary ammonite reported from Langdon Stairs
Gale and Woodroof recorded a juvenile ammonite from within a broken echinoid near the Navigation interval, tentatively identified as Forresteria petrocoriensis. Its identification and stratigraphic implications require caution; it is not a definitive modern boundary marker by itself.
1983–1984 – The Dover Top Rock examined in boundary studies
Detailed work on Langdon Stairs clarified the Navigation hardgrounds and associated fossils during debate over recognition of the Turonian–Coniacian boundary. Later definitions have refined the international boundary criteria.
1987 – Cliffs renotified as an SSSI
The Dover to Kingsdown Cliffs site was renotified for its geological and biological interest. The designation recognises the value of the Chalk sequence as well as its coastal habitats.
1988 – Modern geological memoir published
The British Geological Survey memoir for Ramsgate and Dover described the coastal sections and corrected earlier miscorrelations of prominent flint bands. It remains a major source for local lithology and fossil horizons.
1994 – The cliffs enter a carbon-isotope reference record
Jenkyns and colleagues used the Dover coastal Chalk in a composite carbon-isotope study. The chemical record added another way to correlate the fossiliferous beds with successions elsewhere.
2001 – National synthesis of the Chalk succession
The Geological Conservation Review integrated measured logs, marker beds and fossil distributions from East Cliff, Langdon Bay and Langdon Stairs. It distinguished the Dover Chalk Rock from the younger Dover Top Rock.
2010s onwards – A changed route to Langdon Bay
Loss of part of the old cliff path led to a replacement approach through a former searchlight tunnel and down a near-vertical ladder. The present route differs from the path used in older geological descriptions.
References
Shephard-Thorn (1988), Geology of the country around Ramsgate and Dover
BGS Chalk framework: Newhaven Chalk and Margate Chalk Member
Joe Shimmin (2017), Humble flint sea urchins and the stories they tell
Mortimore, Wood & Gallois (2001), British Upper Cretaceous Stratigraphy, Folkestone to Kingsdown account
May (2003), Kingsdown to Dover, Coastal Geomorphology of Great Britain
BGS Lexicon: Newhaven Chalk Formation
NCC, Dover to Kingsdown Cliffs SSSI citation (UK Fossils-hosted scan)
Natural England: Dover to Kingsdown Cliffs SAC conservation objectives
National Trust: White Cliffs visitor centre to Langdon Stairs trail
National Trust Heritage Records MNA128273: Langdon Stairs
GEOLOGY
The East Cliff–Langdon coast exposes a thick Late Cretaceous marine succession in which changes in the character of the chalk are as important as its familiar white colour. Fine carbonate sediment accumulated on the sea floor, interrupted by clay-rich marl seams, flint-forming intervals and periods when little sediment was deposited or some was removed. The wider East Cliff composite reaches New Pit Chalk near its lower limit, passes through the Lewes Nodular Chalk and Seaford Chalk, and includes a small high-level cap of Margate Chalk within the Newhaven Chalk Formation. These levels are distributed through the cliffs rather than all appearing together on the beach.
The Lewes Nodular Chalk gives much of the lower succession its distinctive texture. Hard, rough, sometimes iron-stained nodular layers alternate with softer chalk, marls and flint bands. The Southerham, Caburn and Bridgewick markers allow geologists to relate individual exposures around Langdon Bay and the historical Langdon Stairs section. Fossils also change with position: Langdon Bay is the type locality of the bivalve Inoceramus lamarcki, whose original specimen came from flint below the Southerham marls. Such a recorded horizon provides much more information than a shell identified only as coming from Dover.
The Dover Chalk Rock is an especially condensed part of this succession, where several ammonite-bearing nodular beds record slow accumulation and early cementation. Its lower bed contains a different ammonite assemblage from the upper beds, which include Hyphantoceras reussianum and Scaphites geinitzii. Higher up, the Navigation Hardgrounds form the historically named Dover Top Rock. These are separate hardened sea-floor surfaces, not another name for the older Chalk Rock. Together with further hardgrounds above, they show that the chalk sea left a discontinuous record containing pauses and reworked sediment.
Above Shoreham Marl 2, the Seaford Chalk becomes smoother and more uniformly white, with prominent flints and shell-debris-rich intervals. Its Belle Tout, Cuckmere and Haven Brow bed packages differ in fossil content as well as their marker bands. Much of this younger succession lies high in the cliff, so fallen blocks can bring material from levels far above the adjacent platform. Subsequent wave action breaks down chalk and leaves more resistant flint on the shore. That mixing explains why beach finds are useful evidence of the local fauna but cannot automatically be assigned to the bed directly behind them.
Explore the formations, individual beds and marker horizons at Dover.
East Cliff/Athol Terrace, Langdon Bay and Langdon Stairs, east of Dover Harbour. Aker’s Steps and Shakespeare Cliff west of the harbour are separate reference sections, not the descent in this guide.
CHALK GROUP
The bedrock was deposited in a marine setting during the Late Cretaceous. Fine carbonate sediment is interspersed with clay-rich marl seams, fossil-rich horizons and surfaces recording pauses or erosion on the sea floor.
WHITE CHALK SUBGROUP
The account follows the exposed succession from older to younger beds. Historic Lower, Middle and Upper Chalk divisions do not coincide with all the modern formation boundaries.
New Pit Chalk Formation
The lowest part of the East Cliff composite reaches the Glynde Marls beneath the entry of persistent nodular chalk. Most of the route down Langdon Stairs begins higher in the succession, so the underlying New Pit Chalk should not be presented as a beach-wide exposure.
Glynde Marls
These clay-rich marker seams, historically called the Maxton Marls in Kent, occur below the main nodular-chalk entry. The Dover East Cliff composite includes them, whereas the lowest recorded Langdon Stairs bench is considerably younger. Individual Glynde seams are not separately measured in the cited East Cliff description.
Lewes Nodular Chalk Formation
Rough, iron-stained nodular chalk alternates with softer chalk, marl seams and repeated flint bands. This is a Turonian to Coniacian succession, including the condensed Dover Chalk Rock and the higher hardgrounds of the Dover Top Rock. The 50 m historical Langdon Stairs log is a measured geological section, not a promise that the reconstructed access path exposes every old bench.
Glynde Beds
Iron-stained nodular sponge beds beneath the Southerham flints show that nodular chalk begins well below the historical Basal Complex. These are especially important in the East Cliff/Athol Terrace and lower Langdon Bay composite. Bivalves of the Inoceramus lamarcki group are common in the nodular sponge beds below Southerham Marl 1.
Southerham Tubular Flints
Mixed small tubular and large nodular flints lie below Southerham Marl 1. They are recorded at beach level between Langdon Stairs and the eastern arm of Dover Harbour. Langdon Bay is the type locality of Inoceramus lamarcki; its holotype came from flint below the Southerham marls, probably this large-nodule horizon.
Southerham Marl 1
The lower seam is a conspicuous plastic marl above the Southerham flints. It forms one of the two historically described marl seams in the lower Langdon Bay succession.
Southerham Marl 2
A second marl lies above Southerham Marl 1, separated by chalk. The pair corresponds to Jukes-Browne and Hill’s older description of two marls approximately four feet apart; that historical measurement should not be treated as a constant coast-wide spacing. The chalk between the two marls has yielded Subprionocyclus hitchinensis. Micraster corbovis, thin-shelled Sternotaxis plana and terebratulid brachiopods are also recorded around the paired-marl interval.
Caburn Beds
This informal interval lies between the Southerham and Caburn marl levels. It includes nodular sponge-bearing chalk and distinctive flints; it is a bed package within the Lewes formation, not a member.
Caburn Sponge Bed
Tough, nodular, sponge-bearing chalk occurs in the Caburn interval beneath Caburn Marl. The sponge bed and associated small flints form distinctive markers in the lower Langdon Stairs succession.
Caburn Flints
Small pink, irregularly pitted or carious flints occur with the Caburn Sponge Bed beneath Caburn Marl. Their distinctive texture is shared with the correlative Sussex horizon.
Caburn Marl
This seam was recorded on the lowest bench of the historical Langdon Stairs log. It is the grey marl that forms an open crevice in older descriptions of the lower cliff sequence. The surface beneath the marl has yielded Micraster michelini.
Ringmer Beds
The Ringmer interval follows the Caburn marl level and leads into the Bridgewick markers. It includes the flints and marl seams historically grouped in the Basal Complex at Dover.
Bridgewick Flints
The flints form part of the Basal Complex below the Dover Chalk Rock. Their association with the Bridgewick marls was formerly used in mapping the base of Upper Chalk, a boundary distinct from the modern formation scheme. Echinoids include Micraster michelini, M. corbovis and Sternotaxis plana.
Bridgewick Marl 1
The lower prominent Bridgewick marl is the grey seam in Bed 6 of the old Jukes-Browne and Hill section. It lies within the flint-and-marl Basal Complex. Terebratulina lata is abundant in the marl and has its last recorded occurrence here; above it, Orbirhynchia dispansa and the regular echinoid Gauthieria radiata characterise the Basal Complex.
Bopeep Flints
This distinct named flint horizon belongs to the same Basal Complex and separates parts of the Bridgewick marl succession. It should not be merged with the older Bridgewick flints.
Bridgewick Marl 2
The second named marl lies within the smooth chalk of historical Bed 3 below the Chalk Rock. It is distinct from the first Bridgewick marl and the intervening flints.
Bridgewick Marl 3
This higher Bridgewick marl completes the named marl succession below the Chalk Rock. The brachiopod genus Cretirhynchia first appears above it; the named species C. cuneiformis and C. minor are recorded from the younger Chalk Rock nodular beds 2 and 3.
Kingston Beds
The Kingston interval is strongly condensed in the Dover Chalk Rock. Its nodular layers and ammonite assemblages represent a shorter rock thickness than their equivalents in more expanded chalk sections.
Dover Chalk Rock
This informal condensed interval consists of several nodular chalk beds separated by softer layers. It represents the upper hardground suite of the more extensive Chalk Rock farther west in England, rather than the whole Berkshire–Wiltshire succession.
Dover Chalk Rock: nodular bed 1
The lower ammonite-bearing nodular bed contains Subprionocyclus hitchinensis and Yezoites bladenensis, with bivalves including Inoceramus perplexus and Mytiloides costellatus. It lacks the Hyphantoceras fauna characteristic of the next beds.
Dover Chalk Rock: nodular bed 2
The second nodular bed belongs to the upper ammonite assemblage, including Hyphantoceras reussianum, Eubostrychoceras saxonicum and Scaphites geinitzii. Small gastropods, bivalves and brachiopods also occur; the upper-bed fauna is shared with nodular bed 3. The combined upper-bed brachiopod fauna includes Orbirhynchia reedensis, Cretirhynchia cuneiformis, C. minor and Gibbithyris subrotunda.
Dover Chalk Rock: nodular bed 3
The third nodular bed shares the upper Chalk Rock ammonite assemblage with bed 2. The absence of Subprionocyclus from these upper beds distinguishes their fauna from bed 1, while the resistant nodular lithology records condensation and early sea-floor cementation.
Lewes Marl position
The Lewes Marl is occluded within the condensed Chalk Rock succession at Dover rather than forming the obvious clay seam seen in expanded sections elsewhere. Its position is established by correlation with the surrounding marker beds.
Lewes Tubular Flints
The characteristic tubular flints remain recognisable despite condensation of the surrounding chalk. Associated fossil records include Micraster leskei, Mytiloides striatoconcentricus and M. incertus.
South Street Beds
The published lower Langdon Stairs log identifies a South Street interval above the condensed Chalk Rock/Lewes flint succession and below the Navigation interval. It belongs to the softer chalk succeeding the principal nodular rock beds.
Navigation Beds
This informal package includes the streaky Zoophycos chalk and the Navigation hardground complex. The hardened upper levels form the Dover Top Rock.
Cuilfail Zoophycos Beds
Streaky softer chalk below the Navigation Hardgrounds contains conspicuous Zoophycos traces. It was recorded around the first corner above the bottom of the historical Langdon Stairs path; Sternotaxis placenta and Micraster normanniae occur in this part of the succession.
Navigation Hardgrounds: the Dover Top Rock
A complex of hardened chalk surfaces forms the historical Dover Top Rock. These are submarine omission surfaces, produced when sediment accumulated slowly or was removed. They are distinct from the older, ammonite-bearing Dover Chalk Rock. The hardground complex is well documented in the historical Langdon Stairs section.
Navigation Marls
Clay-rich seams overlie the Navigation hardground complex and provide close correlation between the cliff sections. Historical placement of the Turonian–Coniacian boundary here has changed as international boundary definitions have been refined; a marl seam should not be equated uncritically with a modern stage boundary. At East Cliff a shell-rich bed about 0.7 m above the marls contains Cremnoceramus deformis erectus with C. waltersdorfensis, an important local boundary-transition record.
Cliffe Beds
The interval above the Navigation marls contains the Cliffe Flint and is capped by the Cliffe Hardground. The associated fossils and omission surfaces aid correlation across the condensed Dover succession.
Cliffe Flint
A conspicuous large flint marker occurs beneath the Cliffe Hardground. Its stratigraphic position, together with adjacent chalk surfaces, is more reliable for correlation than the shape of an isolated beach flint.
Cliffe Hardground
A hardened surface above the Cliffe Flint forms the lower of the prominent post-Navigation hardgrounds. Brachiopods recorded as Cretirhynchia subplicata are especially common in the interval between this and the Hope Gap Hardground.
Hope Gap Beds
This interval lies between the Cliffe and Hope Gap hardgrounds. It contains a prominent flint marker and abundant small rhynchonellid brachiopods in parts of the chalk.
Hope Gap Flint
This large flint horizon is associated with the Hope Gap hardground complex. It is a separate named marker from the Cliffe Flint below and the sheet-flint associated with the higher Beeding interval.
Hope Gap Hardground
A conspicuous omission surface caps the Hope Gap interval. The echinoid assemblage includes forms identified as Micraster decipiens, recorded in older zonal terminology as M. cortestudinarium.
Beeding Beds
The post-Hope Gap interval includes the Beeding Marl and associated sheet-flint, terminating at the Beeding hardground surface. It is an informal package, not a formal member.
Beeding Marl
A marl seam provides a marker between the Hope Gap and Beeding hardground intervals. A conspicuous tabular sheet-flint in this part of the succession was historically used to correlate the Micraster cortestudinarium Zone.
Beeding Hardground
Another hardened chalk surface follows the Beeding Marl interval. It belongs to the repeated succession of hardgrounds and flints, rather than constituting a separate member or formation.
Light Point Beds
Chalk between the Beeding and Light Point hardground surfaces forms the Light Point interval. Its upper omission surface carries glauconitic staining and reworked chalk pebbles.
Light Point Hardground
The upper surface of this conspicuous Langdon Stairs hardground is glauconitised and carries a lag of glauconitised pebbles. It records sea-floor cementation followed by erosion and reworking before chalk deposition resumed.
Beachy Head Sponge Beds
In the upper Langdon Stairs succession, nodular sponge-bearing chalk bands alternate with softer chalk crowded with Zoophycos traces. Large Micraster turonensis characterises these beds; the underlying Light Point–Beachy Head interval contains large Cremnoceramus crassus crassus.
Shoreham Marl 1
The lower of the two Shoreham marls lies above the nodular sponge-bed succession. It remains within the upper Lewes Nodular Chalk Formation.
Shoreham Tubular Flints
Strongly developed tubular flints occur between the two Shoreham marls. Their position within the paired-marl interval makes them an important field marker.
Seaford Chalk Formation
Smooth, relatively pure white chalk contains conspicuous flint bands and distinct intervals rich in inoceramid bivalve shell debris. The lower Belle Tout interval is exposed on the upper historical Langdon Stairs section. Higher Cuckmere and Haven Brow beds belong to the wider East Cliff/high-cliff composite, not the whole stair route.
Shoreham Marl 2
The upper Shoreham marl marks the base of the Seaford Chalk Formation in the modern lithostratigraphic scheme. Above it, smoother white chalk succeeds the rougher, frequently nodular chalk below.
Belle Tout Beds
This informal lower division extends from Shoreham Marl 2 to the Seven Sisters Flint Band. Three groups of marl seams interrupt the shell-debris-bearing chalk. The Belle Tout, Cuckmere and Haven Brow names are informal bed packages here, not formal members.
Belle Tout Marl 1
The lowest named marl group within the Belle Tout Beds is distinguished in the measured Dover succession. It belongs to the lower shell-debris-bearing chalk above Shoreham Marl 2; its individual seams must be recognised in context rather than assigned from loose chalk. The foraminiferal entry of Stensioeina exsculpta exsculpta is placed close to this marl in the published Dover log; S. granulata granulata enters lower, above Shoreham Marl 2.
Hope Point Marls: historical Langdon Stairs description
The older Kent description records thin marls around a tabular flint about 6.8 m above the base of its Micraster coranguinum Zone at Langdon Stairs. A roughly 0.5 m band of grey-streaked chalk lies beneath. These legacy markers lie within the lower Seaford marl-bearing succession now described using the Belle Tout scheme; the historic zonal datum must be retained when using the measurement.
Belle Tout Marl 2 complex
A middle group of closely associated marl seams interrupts the Belle Tout chalk. The composite nature of this marker is retained rather than reducing the whole lower Seaford succession to a single unnamed marl. The published log places the entry of Loxostomum eleyi just above the complex.
Belle Tout Marl 3
The highest of the three named Belle Tout marl groups occurs below the Seven Sisters Flint Band. Together, the three groups subdivide the otherwise similar white chalk.
Inoceramid shell-debris horizons
Shell fragments of Platyceramus and Volviceramus characterise parts of the Belle Tout succession. In the Dover measured section they extend from about 3.5 m above Shoreham Marl 2 to the two Cuckmere Flint Bands; these measured offsets should not be transferred unchanged to every point along the coast. A separate calcarenitic horizon 2.7 m above Shoreham Marl 2 at East Cliff contains Volviceramus koeneni and the lowest recorded Platyceramus mantelli.
Seven Sisters Flint Band
A semi-continuous, partly tabular flint band caps the Belle Tout Beds. Older local names include East Cliff Semi-Tabular Flint and Oldstairs Bay Flint. It is measured about 17 m above the Shoreham marls at Dover and reaches lower levels along the northward-dipping coast towards Hope Point.
Cuckmere Flint Band 1
The lower of the two Cuckmere flint bands lies above the Seven Sisters marker. It is part of the flinty basal interval of the Cuckmere Beds, close to the top of the abundant shell-debris succession.
Cuckmere Flint Band 2
The upper Cuckmere flint band completes the pair recorded roughly 2 m above the Seven Sisters Flint at Dover. This is a separate horizon, not an alternative name for the Seven Sisters marker.
Cuckmere Beds
The interval between the basal flints and Michel Dean Flint is comparatively poor in macrofossils, hence the historical name Barren Beds. It can be examined in the East Cliff composite, but lies high in the cliffs beyond Langdon. Trace fossils occur, some tentatively linked with unsilicified Bathichnus, together with two iron-stained sponge beds.
Lower iron-stained sponge bed in the Cuckmere Beds
The lower of two iron-stained sponge horizons interrupts the otherwise relatively macrofossil-poor chalk of the Cuckmere Beds.
Upper iron-stained sponge bed in the Cuckmere Beds
A second iron-stained sponge horizon occurs higher in the Cuckmere interval, separated from the lower sponge bed by chalk.
Michel Dean Flint
This named flint marks the top of the Cuckmere Beds and the transition into the Haven Brow interval. Large cylindrical flints occur within the broader overlying succession, but isolated fallen examples cannot always be assigned to one named band.
Haven Brow Beds
The highest sections reached in historical studies enter this informal upper Seaford division. Basal beds contain shell debris of Cladoceramus; blocks from falls between Langdon Stairs and St Margaret’s Bay have provided material from this otherwise high cliff interval.
Baily’s Hill Flint
A named flint marker within the Haven Brow succession lies above Michel Dean Flint. It belongs to the interval that supplies large paramoudra flints to the beach, although shape alone does not prove a fallen specimen came from this band.
Bedwell’s Columnar Flint Band
Large columnar paramoudra flints characterise this higher marker. The northward dip brings progressively younger Seaford strata closer to beach level towards Kingsdown; very large fallen flints remain heavy, hazardous blocks rather than manageable collecting targets.
Whitaker’s 3-inch Flint Band
A conspicuous sheet-like flint marker lies near the top of the south Kent cliffs, below the yellow Barrois’ Sponge Bed. Its historical name is a correlation label, not a guarantee that every exposure is exactly three inches thick.
Barrois’ Sponge Bed
A yellow sponge-rich bed, a short distance above Whitaker’s 3-inch Flint, caps the local Seaford Chalk. The surface immediately above it is the boundary with the overlying Margate Chalk facies of the Newhaven Chalk Formation.
Newhaven Chalk Formation
Only a small, high-level part of this younger formation occurs in the local coastal sections. Its marl-poor Margate facies is distinct from the underlying Seaford Chalk. The south Kent exposures preserve a much smaller part of the succession than the more extensive sections on Thanet.
Margate Chalk Member
Largely flintless chalk caps the highest parts of the Dover–Kingsdown cliff succession. Most exposures are inaccessible cliff-top material. Historical poor exposures in a shallow construction-railway cutting near Langdon Hole are not a recommendation to enter that cutting today.
References
Shephard-Thorn (1988), Geology of the country around Ramsgate and Dover.
May (2003), Kingsdown to Dover, Coastal Geomorphology of Great Britain.
BGS Lexicon: Newhaven Chalk Formation.
BGS Chalk framework: Newhaven Chalk and Margate Chalk Member.
SAFETY
The ladder foot can be covered by the tide. Check the current National Trust advice, tide times and weather, and make an early return.
Chalk falls are unpredictable. Keep away from cliffs and fresh blocks, avoid scrambling over large debris and carry no load that makes the ladder unsafe.
EQUIPMENT
Wear sturdy footwear with a strong grip and carry a small bag, individual padding, labels and a hand lens. Bring suitable clothing, drinking water and a charged phone.
For a beachcombing visit, leave hammers, chisels and digging tools at home. Do not carry heavy rocks or overfill a bag on slippery ground.
CLEANING AND TREATING
Label each find with its locality, date and, if known, the bed or source rock. Pack fragile chalk fossils separately and support thin shells with their matrix.
Start with gentle dry brushing and gradual room-temperature drying. Do not force matrix from echinoid tests or use acids, bleach or routine varnish. Leave unusual or important specimens unprepared for specialist assessment.
IDENTIFY YOUR FINDS
Need help identifying a fossil? Share clear photos, where you found it and its size with the community.
FURTHER READING
Joe Shimmin (2017), Humble flint sea urchins and the stories they tell
Mortimore, Wood & Gallois (2001), British Upper Cretaceous Stratigraphy, Folkestone to Kingsdown account
Shephard-Thorn (1988), Geology of the country around Ramsgate and Dover
May (2003), Kingsdown to Dover, Coastal Geomorphology of Great Britain
NCC, Dover to Kingsdown Cliffs SSSI citation (UK Fossils-hosted scan)
Natural England: Dover to Kingsdown Cliffs SAC conservation objectives
National Trust: White Cliffs visitor centre to Langdon Stairs trail
National Trust Heritage Records MNA128273: Langdon Stairs
ACCESS RIGHTS
This coast is protected for geological and wildlife interest. SSSI or SAC designation does not itself give a right of entry or a collecting permit. Use lawful public access and comply with landowner rules and current notices.
Restrict any permitted collecting to modest amounts of already loose common material. Do not hammer the cliffs, quarry hardgrounds, excavate or take research samples without the relevant owner or manager’s permission and any protected-site consent required.
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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