Whitecliff Bay Fossil Hunting

1842 – Nummulites recorded at Whitecliff
Bowerbank noted Nummulites at Whitecliff Bay, an early record in the development of Palaeogene fossil correlation.

1846–1847 – The Palaeogene succession correlated
Joseph Prestwich used the Whitecliff Bay and Alum Bay sections to establish equivalence between island, Hampshire, Sussex and London Basin strata.

1856 – The fluviomarine succession documented
Edward Forbes’s Geological Survey account helped establish the younger Palaeogene succession represented at Whitecliff Bay and its northern continuation.

1862 – Fisher’s Bracklesham bed scheme published
Osmond Fisher divided the well-exposed Whitecliff succession into numbered beds. His scheme remains useful for historical fossil records, although modern formation boundaries differ.

1921 – The Geological Survey account consolidated
H. J. Osborne White’s memoir provided detailed descriptions of the island’s succession, including the Whitecliff section, consolidating earlier observations for later field work.

1937 – Nummulites studied as correlation markers
Work by Curry and by Wrigley and Davies developed study of the large foraminifera that distinguish important horizons in the Whitecliff marine succession.

1955 – Site first notified for conservation
Whitecliff Bay and Bembridge Ledges received its first SSSI notification, recognising the scientific value of the coast.

1967–1968 – Sedimentary structures reveal former conditions
Brian Daley described gypsum pseudomorphs, gutter casts and crack fills in the Bembridge Marls, showing that these beds preserve detailed evidence of sedimentary processes.

1968–1971 – Ostracod faunas systematically studied
Haskins’s studies investigated ostracods through the succession, adding a fine-scale record useful for interpreting environmental and salinity changes.

1968 – Bembridge charophyte-zone type section
Castel designated Whitecliff Bay as the type section for the Bembridge charophyte zone. Its original Oligocene assignment is a historical age interpretation, not an unchanged modern age determination.

1971 – A subtle unconformity recognised
Daley and Edwards identified angular discordance between the Bembridge Limestone and overlying Bembridge Marls in the bay’s northern continuation, recording intra-Palaeogene warping.

1972 – A rodent named from the Bembridge Marls
Bosma and Schmidt-Kittler described Ectropomys exiguus; the type specimen came from the Whitecliff Bay Bembridge Marls.

1974 – Microfossils and fossil algae refine interpretation
Murray and Wright’s foraminiferal study used Whitecliff extensively, while Daley described fossil blue-green algal encrustations on bivalves in the Bembridge Marls.

1980 – Dinoflagellate zonation formalised
Bujak and colleagues’ zonation used Whitecliff Bay as the type locality for eight dinoflagellate cyst assemblage zones, strengthening regional correlation.

1981 – London Clay reference section designated
Chris King designated the Whitecliff section as a Hampshire Basin reference for the London Clay and clarified its constituent depositional cycles and upper sand units.

1983–1988 – Sedimentary cycles reinterpreted
Plint’s work investigated repeated transgression, regression and erosion in the Bracklesham succession, linking the local sedimentary facies to sea-level change.

1985 – Solent stratigraphy and magnetic record developed
Insole and Daley formalised the Solent Group framework, while Townsend and Hailwood demonstrated the Whitecliff section’s value for magnetic-polarity correlation.

1986 – SSSI protection renewed
The site was notified under the Wildlife and Countryside Act on 14 July 1986, protecting its geological exposures and intertidal and cliff habitats.

1990 – Upper Bracklesham boundary clarified
Freshney and colleagues’ grain-size work supported returning Fisher Bed XVII to the Selsey Sand, placing the Barton Clay boundary above the nummulite-rich bed.

1992–1997 – Freshwater limestone cycles investigated
Armenteros and colleagues studied alternating deposition and soil modification in the Bembridge Limestone, helping explain the cyclic architecture of the Whitecliff section.

1997 – Foreshore succession re-examined
Huggett and Gale documented the Thames, Bracklesham and Barton succession using foreshore exposures, adding sedimentological and glaucony evidence to the classic cliff record.

2004 – Mammal-bearing horizons reassessed
Hooker and colleagues reported mammal material from the Bembridge Limestone and Bembridge Marls, extending the evidence used to compare late Eocene faunas and their stratigraphical positions.

Culver/Whitecliff Point at the southern end, the Palaeogene cliff and foreshore section of Whitecliff Bay, and the Bembridge Limestone–Marls at the northern end near Black Rock Point. Howgate is labelled where a source extends beyond the bay; the whole Bembridge Foreland fauna is not transferred.

CHALK GROUP

The southern headland exposes chalk older than the Palaeogene sequence. Fallen blocks can be examined safely away from the cliff, but their exact source bed is not always identifiable.

WHITE CHALK SUBGROUP

The flinty chalk at Whitecliff Point belongs to the upper white-chalk succession. Historic “Upper Chalk” is a broad older term, not a formation.

Portsdown Chalk Formation

The youngest Chalk at the contact is Campanian. Historical descriptions use the Belemnitella mucronata zonal terminology; echinoids and sponges occur in the chalk debris. This bay-end succession is only part of the Culver Cliff Chalk section.

Chalk–Palaeogene unconformity

An irregular, locally pot-holed erosional surface separates the chalk from the flinty basal sand. It represents missing geological time, not a continuously deposited passage bed.

LAMBETH GROUP

At Whitecliff Bay the principal named unit is the Reading Formation.

Reading Formation

Mottled red, grey and purple mudstones form a conspicuous slipped interval above the chalk. They record mainly nonmarine conditions; derived chalk fossils in basal material are reworked rather than evidence of a Chalk-age Reading Formation.

Reading Bottom Bed

The sandy basal interval contains angular and rounded flints, including occasional derived silicified echinoids. It rests on the chalk’s uneven surface and differs from the overlying mottled clay.

Basal laminated marl and mottled clay

Historical descriptions record a thin grey sandy marl above the basal flinty sand, passing into mottled clay. The colour contrasts help identify the lowest Palaeogene beds even where landslips conceal their contacts.

THAMES GROUP

The thin basal marine transgressive unit precedes the thicker London Clay succession.

Harwich Formation

This is the modern formation-level treatment of the thin interval historically called the London Clay Basement Bed or Oldhaven/Tilehurst unit. These historical names refer to the same interval, rather than several successive formations.

Glauconitic and conglomeratic basement interval

Pebbles, locally cemented sand and reworked clay material mark the marine transgression across the Reading deposits. The old guide records Ditrupa and other marine fossils in this basal interval.

London Clay Formation

The succession contains repeated marine mud-to-sand cycles separated by sharp transgressive surfaces. It includes the upper sand members formerly placed in the Bagshot Sands, and in the modern local scheme reaches into the lower part of Fisher’s old Bed I.

Divisions A and B

The lower muddy cycles include shell-bearing clay and septarian concretions. Sharp, locally pebbly or glauconitic bases distinguish depositional cycles; laminated sand and silt become important towards the top of Division B.

Division C and Portsmouth sand transition

Upward coarsening culminates in a conspicuous sand body. The relationship is a cycle within London Clay, not a boundary into a separate Bagshot Formation.

Portsmouth Sand Member

Light-coloured, cross-stratified quartz-rich sand forms one of the obvious yellowish cliff units. It is the lower of the two historically conflated Bagshot sand bodies.

Division D and intervening sandy clay

The two sand members are separated by a comparatively thin muddy interval. This intervening muddy interval remains important for correlation even where cliff weathering makes it inconspicuous.

Whitecliff Sand Member

This second conspicuous sand body overlies the Portsmouth Sand interval and belongs to the London Clay. Older accounts used it in the Bagshot Sands; the modern boundary lies above those obvious sands.

Division E and lower Fisher Bed I

The younger London Clay cycle includes strata once counted among the lowest Bracklesham Beds. Its basal pebbly transgressive event does not coincide with the modern base of the Wittering Formation.

First planktonic-foraminifer marker

The first recorded planktonic foraminifera occur in the London Clay succession around 40 m above the top of the Reading Formation. This is a stratigraphic correlation marker, not a distance along the modern beach.

BRACKLESHAM GROUP

The local group comprises Wittering, Earnley Sand, Marsh Farm and Selsey Sand formations. Fisher’s Roman-numbered beds are historical field divisions, not formal members.

Wittering Formation

Laminated sands and muds, glauconitic fossil-bearing beds and lignitic material record changes between marginal-marine, estuarine and lower-salinity settings. Its base lies above part of the historical Fisher Bed I.

Fisher Bed IV — Nummulites planulatus horizon

A marine fossil-bearing interval provides an early Bracklesham marker; its larger foraminifera were used in correlation. This historical bed must be distinguished from the younger Nummulites laevigatus bed.

Whitecliff Bay Bed — lignite within Fisher Bed V

The prominent lignite, historically called the Bembridge Coal, lies within the Wittering Formation. Rooted and organic-rich deposits record a period of very shallow or emergent conditions within the broader cyclic succession.

Earnley Sand Formation

Glauconitic marine sand overlies the Wittering succession. Shelly material and large foraminifera make this one of the useful palaeontological intervals on the foreshore when naturally uncovered.

Fisher Bed VII — Nummulites laevigatus Bed

The conspicuous concentration of Nummulites laevigatus is both a collecting feature and a long-used correlation horizon. It belongs to the Earnley interval rather than every green sand in the bay.

Marsh Farm Formation

The intervening heterolithic succession includes laminated mud and fine sand. It records a return towards lower-energy, marginal environments between the more marine Earnley and Selsey intervals.

Selsey Sand Formation

Glauconitic sands contain important marine fossil horizons, including the well-cemented Tellina sandstone near the top and the overlying Nummulites variolarius horizon.

Fisher Bed IX — Campanile-bearing horizon

This molluscan marker is recognised in published correlation of the Whitecliff and mainland sections. Its historical placement must be reconciled against the modern Marsh Farm–Selsey boundary rather than inferred from a list of fossils. Murray and Wright’s published correlation explicitly supports this historical marker; uncertainty concerns its precise placement against modern formation boundaries, not the existence of the named correlation.

Fisher Bed XIV — Brook Bed correlation

The published foraminiferal correlation identifies this marker within the higher Bracklesham succession. It is distinct from the younger Bed XVII nummulite concentration. Murray and Wright’s published correlation explicitly supports this historical marker; uncertainty concerns its precise placement against modern formation boundaries, not the existence of the named correlation.

Fisher Bed XVI — Tellina sandstone

This resistant, cross-bedded sandstone is a useful physical marker in the Selsey Sand. It is below the actual formation top, rather than being used as the Bracklesham–Barton boundary.

Fisher Bed XVII — Nummulites variolarius Bed

This sand-and-silt-dominated fossiliferous interval includes molluscs, abundant foraminifera and the small coral Turbinolia. Grain-size work led to its placement in the Selsey Sand instead of the Barton Clay.

BARTON GROUP

The higher marine clays and sands are followed by the lower-salinity Solent succession. Historical schemes included some of the lowest Barton strata in the Bracklesham Beds.

Barton Clay Formation

Shelly marine muds include the former Huntingbridge division, Fisher Beds XVIII–XIX, under the revised boundary scheme. Foreshore sand and coastal defences have obscured much of this interval at different times.

Nummulites prestwichianus horizon

The lower of the two conspicuous Barton markers is a thin glauconitic sand containing abundant Nummulites prestwichianus.

Nummulites rectus horizon

About 6 m higher in the published Whitecliff section, Nummulites rectus is common in stiff blue-grey mud. This is a local measured separation, not a regional constant or a separate formal member.

Chama Sand Formation

The shell-rich Chama interval marks the sandy transition above the Barton Clay in the modern local framework. Its shallow-marine bivalve assemblage differs from the overlying decalcified sands.

Chama Bed

The characteristic bivalve Chama squamosa occurs in this conspicuous shelly interval. In older accounts it was described at the top of the Barton Clay; this is a historical placement of the same rock body.

Becton Sand Formation

Pale quartz-rich sands precede the Headon Hill Formation. Decalcification helps explain why an apparently promising sand exposure may contain little recognisable shell material.

SOLENT GROUP

The succession comprises Headon Hill, Bembridge Limestone and Bouldnor formations. Its younger beds record predominantly low-salinity environments, with important marine incursions.

Headon Hill Formation

A sequence of distinct muddy and locally calcareous members spans freshwater, brackish and near-marine conditions. The Hatherwood Limestone is absent here; the full Headon Hill type succession from the west of the island is not represented here.

Totland Bay Member

The local member is much thinner than at Totland Bay because of erosion below the overlying Colwell Bay interval. It records freshwater and brackish settings and includes a mammal-bearing lens known as WB1.

Basal bright-green mud — 1.7 m

The measured section begins with bright-green mud above the Becton Sand contact. This lower muddy interval differs from the paler lignitic beds above.

Pale-grey lignitic mud — 2.8 m

Several lignitic layers occur in this pale mud. The WB1 mammal lens was recorded within a green clay interval approximately 3 m above the member base, with freshwater gastropods and a transition towards lignite; do not treat it as a continuous bone bed.

Muddy fine sand with basal ironstone — 1.8 m

Pale-grey, muddy fine sand begins with sandy ironstone, forming a distinct change above the underlying lignitic mud.

Upper pale-green shelly marl — 1.8 m

Marl with shell bands forms the upper part of the measured Totland interval. Brackish assemblages occur towards the member top.

Colwell Bay Member

A thick marine to lower-salinity interval begins at an erosional contact. The basal Brockenhurst Bed has the richest marine fauna in the Headon Hill Formation here; the Venus Bed higher up is abundant in shells but less diverse.

Basal blue-grey sandy mud and shell beds — 12.9 m

This lower package starts at an erosion surface and contains shell-rich layers, including the basal Brockenhurst interval. Its fauna documents stronger marine influence than the preceding member.

Pale-grey mud with basal oysters — 1.2 m

An oyster-rich base distinguishes this muddy interval from the much thicker sandy mud below.

Shelly blue-grey sandy mud — 4.1 m

The upper half is particularly shell-rich. This measured interval is distinct from the basal Brockenhurst fauna; the shelly muds do not form a single bed.

Pale-yellow fine sand passing to dark-green mud — 3.2 m

The upward change from sand into darker mud records another change in energy and sediment supply within the member.

Fine pale-green sand to grey-green mud — 1.6 m

A thinner sand-to-mud package overlies the preceding interval and adds to the internal cyclicity.

Upper green molluscan mud — 5.8 m

The uppermost measured Colwell interval is green to green-grey mud with lymnaeid gastropods, showing the return to a lower-salinity fauna.

Linstone Chine Member — historical local correlation

A 1.5 m pale-green fine sandstone is included under this name in the GCR measured table. The companion stratigraphical account calls its presence at Whitecliff questionable, so the regional correlation remains uncertain.

Cliff End Member

The local section returns to predominantly low-salinity muddy deposition above the Colwell interval. Two measured muddy packages are distinguishable.

Lower grey-green mud — 8.0 m

The lower muddy package has a subdued colour and is distinct from the mottled mud above.

Upper green mud with red mottling — 4.0 m

Red mottling develops in the upper package, recording post-depositional modification of the muddy substrate.

Lacey’s Farm Limestone Member

The local expression is 6.7 m of green marl with concretions and calcareous bands, rather than the massive limestone body developed at the western type area. Mammal material has been recorded within this interval.

One Foot Bed

A cream-coloured limestone approximately 0.30 m thick lies within the local calcareous interval. Its historical name describes the thin bed, not the thickness of the entire member.

Fishbourne Member

The measured local package is 10.9 m of grey to grey-green shaly mud with intermittent Viviparus bands. Published modern summaries give slightly different totals; this source measurement does not imply current cliff-survey precision.

Osborne Member

A 10.4 m measured muddy interval is black at its base, changes through grey and grey-green mud, and becomes red-and-green mottled near the top. Mammal occurrences are localised; the mottled floodplain facies should not be described as uniformly marine or wholly barren.

Seagrove Bay Member — traditional Whitecliff subdivision

This upper Headon Hill interval is retained in the GCR measured succession. Later nomenclatural work associates much of the Whitecliff interval with the Osborne unit; the traditional subdivision is described explicitly rather than presented as a settled modern correlation.

Basal yellow sandstone — 0.7 m

An erosional base introduces the sandy interval above Osborne mudstones.

Mottled green mud with concretions — 4.8 m

Green mud with brown mottling and local calcareous concretions makes up the largest part of the traditionally defined member here.

Sandstone and sandy limestone — 0.8 m

A mud parting interrupts this relatively resistant calcareous and sandy interval.

Upper mud and pale-green siltstone — 2.8 m

Dark-green mud passes upwards into pale-green siltstone immediately before the Bembridge Limestone succession.

Bembridge Limestone Formation

The measured local sequence alternates limestone and marl. Its thickness and repeated soil-modified intervals make Whitecliff a key section; it lies below, not above, the Bembridge Marls.

Basal marl and thin limestone — 1.8 m

Pale-grey marl begins with a thin limestone bed at the base of the formation.

Lower principal limestone — 2.3 m

Pale-brown limestone, greyer towards the base, contains a lignitic interval near its middle. This is not an entirely homogeneous carbonate bed.

Middle marl and mud — 1.3 m

Grey muddy sediment darkens downwards and contains Corbicula. The middle muds are among the formation’s documented mammal-bearing horizons.

Gastropod limestone — 0.7 m

A pale-brown limestone above the middle mud contains gastropods, marking renewed carbonate deposition.

Upper white limestone — 1.4 m

White limestone has a conglomeratic base, recording reworking at the start of this carbonate interval.

Top pale-green marl — 1.2 m

This 1.2 m marl, with a burrowed upper surface, is retained from the historical measured table that included it at the top of Bembridge Limestone. Later boundary revision assigns marl and clay above the highest limestone to the Bouldnor Formation. The measured bed is preserved here with its historical placement explained; its thickness has not been silently shifted or combined with a different section.

Bouldnor Formation

Only the lower part of this formation is relevant to the bay’s exposed succession. The higher Hamstead and Cranmore members recorded at northern island sites are outside this exposed succession.

Bembridge Marls Member

The lower Bouldnor succession includes an oyster-rich basal marine incursion, muddy lagoonal beds and higher fining-upward cycles. Mammal-bearing localities occur at several levels; some published aggregate faunal lists also include the adjacent Howgate continuation.

Basal shelly mud and sand — 1.4 m

Grey-green mud interbeds with shelly sand and mud. The distinctive Bembridge Oyster Bed is especially well developed at Whitecliff and belongs at the base of this member.

Marine muddy sand — 0.4 m

Light green-grey muddy sand with marine fossils overlies the basal shelly package.

Dark mud with discontinuous limestone — 0.9 m

Green-black mud includes an interrupted argillaceous limestone near its middle. The local equivalent of the Insect Limestone has very few insects and should not be confused with the insect-rich occurrence at Gurnard.

Mud with basal pyritised shell band — 1.2 m

Dark green-grey mud begins with a pyritised concentration of shells. This marker is distinct from the oyster-rich basal package.

Thick mottled mud with sand lenses — 9.0 m

Green-grey mud is mottled red and contains sandy lenses. Localised mammal-bearing marls were sampled around 11.5 m above the main Bembridge Limestone; that figure is a measured stratigraphic position, not a distance along the beach.

Light marl with siltstone bands — 0.9 m

A lighter green-grey marl with thin siltstone beds succeeds the thick mottled interval.

Mud with occasional sandstone bands — 1.2 m

Grey-green mud contains sparse sandstones, preceding the more conspicuous siltstone marker.

Gypsum-pseudomorph siltstone — 1.4 m

Grey-green siltstone contains gastropods and erosional structures together with casts or replacements of former gypsum crystals. Associated structures illuminate emergence, flow and early deformation of the sediment.

Upper green-grey shelly mud — approximately 18 m

Mud with shell bands forms the upper measured part of this published section. Exposure varies, and the exact position of any loose fossil must not be inferred simply from its occurrence near the northern end of the beach.

Superficial plateau gravel and beach cover

Quaternary gravel caps parts of the sequence; modern sand and shingle conceal much of the foreshore between episodes of scouring. Neither is a member of the Bouldnor Formation.

References

Hopson and Farrant (2015), Geology of the Isle of Wight
Benton, Cook and Hooker (2005), Whitecliff Bay, GCR 32
Daley and Balson (1999), Whitecliff Bay, GCR 15
Murray and Wright (1974), Palaeogene Foraminiferida and palaeoecology, Special Papers in Palaeontology 14
Ian West (2002), Whitecliff Bay field guide