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Scrutton, Colin and Powell, John, Editors. Yorkshire rocks and landscape: a field guide. 2006. 3rd edition. Ellenbank Press for the Yorkshire Geological Society.
Under construction - this page is for demonstration purposes only
Figure 19.1 Simplified geological map of the Cayton Bay to Yons Nab area.
Figure 19.2 Sedimentological log of the section between Yons Nab and the Red Cliff Fault.
Figure 19.3 Bioturbated sandstone lens near the base of the Gristhorpe Member. The hammer is 350 mm long. Photo: M. Whyte.

19 The Middle–Upper Jurassic sequence between Cayton Bay and Yons Nab

By Martin Whyte and Mike Romano University of Sheffield

Purpose

To study the succession, depositional history, and palaeontology (including plant beds) of the Middle Jurassic (Lebberston Member) to Upper Jurassic (Lower Calcareous Grit Formation), the Red Cliff Fault, Quaternary tills and examples of mass movement.

Logistics

This section was compiled in 2006 when the printed guidebook was published. Before visiting this site please ensure you have up-to-date contact and access information.

This is a full-day excursion best commenced on a falling tide so that Locality 6 will be reached at low water. If tide times dictate, the excursion may be carried out in the reverse direction. Walking distance is about 5 km.

Take the small track which leaves the A165 in the hollow (TA 068 840] about 200 m south of the traffic lights at the junction between the A165 and the minor road to Cayton. This leads into Killerby Park where cars may be parked for a small fee. Coaches may also be parked here by prior arrangement with Mr D. R. Hindley, Killerby Park, Killerby Cliff, Cayton Bay, Scarborough, North Yorkshire, YO 3NR (tel: 01723 582495].

Note: At high tides water may reach the base of the cliff, especially on the east side of Yons Nab. Care must also be taken at Locality 6 where the rising tide quickly fills gullies on the landward side of the Millepore Bed in front of Yons Nab. Safety helmets must be worn close to the cliff base.

Maps

O.S. 1:50 000 sheet 101 Scarborough & Bridlington; B.G.S. 1:50 000 Sheet 54 Scarborough.

Geological background

The Middle Jurassic of the Yorkshire basin consists largely of fluviatile and deltaic sandstones with marine intercalations (Ravens-car Group). This excursion examines the upward facies transition from one of these marine intercalations (Millepore Bed of the Lebberston Member) through a mixed marine and non-marine sequence (Yons Nab Beds of the Lebberston Member) into non-marine deposits (Gristhorpe Member). This can be contrasted with the more abrupt junctions of the Gristhorpe Member with the overlying marine Scarborough Formation, and of the Scarborough Formation with the deltaic Scalby Formation. The latter contact may represent a depositional break of several million years. The Scalby Formation is the highest subdivision of the Ravenscar Group and in late Middle Jurassic (Callovian) times fully marine conditions were established by a transgression from which a sequence of limestones (Cornbrash Formation), clays (Cayton Clay Formation) and sandstones (Osgodby Formation) were deposited, the latter interrupted by minor phases of tectonic tilting and erosion. In the Upper Jurassic (Oxfordian) deepening marine conditions gave rise to the deposition of widespread silty clays (Oxford Clay Formation), which pass gradually up in a shallowing sequence into the Lower Calcareous Grit Formation. Despite its name the latter is a fine-grained sandstone. It has a calcite cement and is very rich in sponge spicules.

The considerable thickness of rocks which can be examined here is in part due to movement on the Red Cliff Fault. This fault probably has a long history of movement and in the Mesozoic was one of a suite of faults which formed the eastern margin of the Peak Trough (Milsom & Rawson, 1989).

Excursion details

From the car park take the path that leads directly down a gully to the shore (Figure 19.1). Once on the shore, turn right (east). Killerby Cliffis entirely made of till which has been much affected by mass movement. Several World War II pill boxes can be seen in various stages of descent from the cliff-top. The till fills a pre-glacial valley, which was cut to below present-day sea level, and eastwards the slope of the valley side can be seen in section with rockhead gradually rising from shore level up to the cliff-top. The character of the cliff thus changes and becomes more precipitous, to give the striking face of High Red Cliff. This cliff is composed of three units: the lower vertical part is made of sandy Osgodby Formation (13 m), the upper vertical portions are made of the Lower Calcareous Grit Formation (25 m) and these are separated by the steeply sloping face of the softer Oxford Clay Formation (40 m). In the Oxford Clay minor rhythmic alternations of harder and softer bands, visible here, may represent the effects of small climatic changes related to periodic variations in the Earth's orbit (Milankovitch cycles). It is interesting that rhythms on a similar scale continue into the Lower Calcareous Grit despite the major change in lithology.

Locality 1 [TA 075 841]

The Osgodby Formation can be examined by climbing up at the western end of its main outcrop. At the top the Hackness Rock Member (2 m) consists of sandy berthierinitic (chamositic) oolite and limy sandstone containing belemnites, Gryphaea and occasional ammonites. The underlying Redcliff Rock Member (II m) contains ferruginous sandstones, bands of sandy berthierinitic oolite and is more silty towards its base. Some horizons contain an abundance of bivalves and sparse ammonites. The boundary between the Hackness Rock and Redcliff Members is difficult to locate precisely, though the intervening Langdale Member is missing here due to erosion (Wright 1968)

The underlying Cayton Clay (3 m), Cornbrash Limestone (0.4 m) and Scalby Formations are usually covered by beach sand. However the Cornbrash Limestone Formation can be seen at Locality 2, where it forms a low ledge within the boulders on the upper beach and about 20 m out from the base of the cliff. Between Locality 1 and Locality 2, note the large, differentially weathering, spheroidal concretions (up to 2 m in diameter) developed in the lower part of the Redcliff Rock Member. Fallen blocks of Osgodby, Oxford Clay and Lower Calcareous Grit Formations can also be examined but attest to the considerable dangers of working in this area. The silty clays of the Oxford Clay contain poorly preserved ammonites, while the well-cemented sandstones of the Lower Calcareous Grit show an abundance of branching, network-like, burrow systems (Thalassinoides).

Locality 2 [TA 077 841]

The Cornbrash Limestone Formation is an impure, nodular limestone containing ribbed oysters (Lopha) and occasional specimens of other bivalves (including Trigonia, Pholadomya and Entolium). At its base, U-shaped burrows (Rhizocorallium), preserved in siderite, extend down into greyish silty sandstones which here represent the top (1 m +) of the Scalby Formation. Shales of the Cayton Clay Formation may occasionally be seen beneath boulders between the Cornbrash outcrop and the cliff base. In the cliff the sandstones of the Redcliff Member show oblique, westerly-dipping planes, and fallen blocks contain a fauna of bivalves (including Pinna, Trigonia, Gervillia and Entolium) and belemnites.

From Locality 2 it is best to continue above the zone of slippery green seaweed to where a prominent notice board (Figure 19.1) advises that it is not possible to walk to Filey at shore level. Here the cliff runs inland behind a large, degraded, landslip. Either scramble round the margin of the slip at shore level or climb onto the slip and follow the path which runs close to its outer edge. At the far end the path crosses an active mud flow, where the footing can be very soft and muddy as it descends again to the beach at Locality 4 [TA 080 842].

Here, Low Red Cliff is clearly different in geological character from High Red Cliff as a result of displacements on the Red Cliff Fault. The fault can be traced on the shore from the truncation of beds on its eastern side and the fault plane outcrops on the upper shore. The trace is obscured under the mud flow but the fault reappears in the cliff at the rear of the flow (Locality 3).

Locality 3 [TA 081 841]

Ascend to the west of the mud flow. Evidence of recent movement of the mud flow can usually be detected in longitudinally grooved mud surfaces and transverse crevasse-like gashes. The Red Cliff Fault is a westerly downthrowing normal fault which almost completely cuts out the Oxford Clay. The apparent vertical displacement is thus about 35 m. Small subsidiary faults can be seen on either side. Coarse crystalline calcite occurs in patches along fault planes and in joints within the Oxford Clay Formation, and fragments may be found in the scree at the cliff-foot. Return to Locality 4.

Locality 4 [TA 080 842]

The western end of Low Red Cliffis made up of lenticular white sandstones and grey siltstones at the base of the Scalby Formation. In places there is abundant, fine or coarse, coalified plant debris. Some of the plant material is also pyritized and weathering of this has covered the cliff face with a bright yellow sulphurous bloom. The geometry of the channel sandstones is variable, and cross-bedding, soft sediment deformation and mud-flakes can also be seen. About 30 m to the east the underlying Scarborough Formation, a thin development (2.8 m) of limy shales with two brown ironstone bands close to the top (Figure 19.2), can be found at the base of the cliff. Towards the centre of the formation, an abundance of crushed shells, with ribbed oysters (Lopha) and other molluscs (Trigonia, Meleagrinella, gastropods and belemnites), is obvious. In places the basal beds of the Scalby Formation cut down into the Scarborough Formation and the top of the Scarborough Formation is disturbed.

From here to the next headland (Locality 5) one moves gradually down succession within the Gristhorpe Member but exposures are variable depending on the amount of beach cover and till slippages from the cliff-top. Dinosaur footprints may occasionally be seen, both in situ and on loose blocks. Immediately under the Scarborough Formation there is a 1.4 m thick sandstone with fine cross-bedding (some authors include this, as the Helweth Beck Member, within the Scarborough Formation). Other prominent horizons in downward sequence (Figure 19.2) are a sandstone containing vertical rootlets of horsetails (Equisetum), a bioturbated carbonaceous sandstone lens (Figure 19.3) and a carbonaceous siltstone with plant remains (Gristhorpe Plant Bed). The latter rests on a highly bioturbated sandstone with vertical roots which is the basal bed of the Gristhorpe Member (Figure 19.2).

Locality 5 [TA 083 843]

The basal bed of the Gristhorpe Member is well seen where the top bed of the Yons Nab Beds (Lebberston Member) also forms a prominent ledge. On the ferruginous upper surface of this bed can be found internal moulds of bivalve shells and valves, including Pholadomya, Trigonia and Pteroperna. Some of the bivalves are in life position. There are also some large vertical U-shaped burrows. The sequence of the Yons Nab Beds (Figure 19.2) is displayed down the shore between Locality 5 and the prominent ledge of the Millepore Bed (Lebberston Member) (Locality 6). In the upper parts there are alternations of sandstone and shale, and poorly preserved bivalves may be found at several levels. The lower parts of the sequence are, apart from a thin ripple-marked and burrowed sandstone, entirely shale with occasional ironstone bands and concretions. Apart from small burrows the shales are only fossiliferous immediately above the Millepore Bed.

Locality 6 [TA 084 843]

The top of the Millepore Bed is well seen on the foreshore and is a sandy oolitic and bioclastic limestone (2 m) with well-developed cross-bedding. Fragments of the bryozoan, Haploecia straminea, from which the bed derived its name, can be found but are not common at this locality. The lower parts of the Millepore Bed are cross-bedded calcareous sandstones (7 m) which can, at low water, be seen to rest on sandstones of the Sycarham Member.

From Locality 6 look back at the cliff at a strike section of the Gristhorpe Member between Locality 5 and the next headland, Yons Nab (Locality 7). Small channels and other lateral changes can be detected within this sequence. Return to the cliff base close to Locality 5 and walk east along the ledge formed by the top bed of the Yons Nab Beds. Approaching Yons Nab, notice how the bed is removed by a northeast–southwest trending channel which cuts down from the Gristhorpe Member into the Yons Nab Beds.

Locality 7, Yons Nab [TA 085 842]

The complex channel-fill sandstones are well displayed on the shore in front of Yons Nab. To the east the upper beds of the Yons Nab Beds reappear on the eastern side of the channel. Immediately in front of Yons Nab, the siltstones of the Gristhorpe Plant Bed rest on the channel sandstones and are overlain by a bioturbated carbonaceous sandstone. However these beds are often concealed by beach gravels which here usually contain an abundance of pyrite nodules and fragments, some of which show traces of woody structure. At the base of the cliff on the east side of Yons Nab a sandstone with ironstone concretions and plant fragments contains occasional poorly preserved specimens of the fresh-water bivalve Unio.

Locality 8 [TA 085 841]

From Locality 7 to Locality 8, the cliff shows an ascending sequence through the Gristhorpe Member and the Scarborough Formation, which can be compared with the sequence between Localities 4 and 5 (Figure 19.2). The cross-bedded sandstone below the Scarborough Formation is well exposed here, as are the fossiliferous beds of the Scarborough Formation.

Locality 9 [TA 085 840]

Here a large channel within the Scalby Formation cuts down into the top of the Scarborough Formation.

About 200 m south-southeast of Locality 8 [TA 086 838], climb up the clay slopes to a path that leads to the cliff-top (the lower parts of the path have been destroyed by mass movement). Take the cliff-top path over High Red Cliff back to Killerby Park. This route provides excellent views both of the coast and of the Vale of Pickering. Both Gristhorpe Cliff to the east and the headland of Scarborough Castle to the north show the same middle to upper Jurassic sequence as at High Red Cliff. Alternatively return along the shore to the path down from Killerby Park.

20 Jurassic, Cretaceous and Quaternary rocks of Filey Bay and Speeton

By John Neale past President, Yorkshire Geological Society and John Catt University College London

Purpose

To examine the Devensian glacial deposits, interglacial shell bed, Upper Jurassic Kimmeridge Clay, Lower Cretaceous Speeton Clay and Upper Cretaceous Red* and White Chalks exposed in the coastal cliffs of the southeast part of Filey Bay.

Logistics

This section was compiled in 2006 when the printed guidebook was published. Before visiting this site please ensure you have up-to-date contact and access information.

Parking for a coach or up to to cars is available near the cliff-top at Reighton Sands [TA 140 763]

The coast section is suitable for a large group, and involves an easy walk of about 4 km (plus 4 km return), taking at least 3 hours.

Note: The section is accessible only fora-4 hours on either side of low tide. Hard hats should be worn. Do not stand close to vertical clay sections during and after rain when they are unstable, and do not attempt to walk across soft active mudflows. On the sloping cliffs it is safest to walk only on vegetated areas. The high chalk cliffs beyond are dangerous because of block falls and should not be approached closely at any time. The nature of the Red and White Chalk may be studied in foreshore exposures and fallen blocks away from the cliff base.

Maps

O.S. 1:50 000 Sheet tot Scarborough & Bridlington and 1:25 000 Sheet 301, Scarborough, Bridlington and Flamborough Head; B.G.S. 000 Sheet 55/65 Flamborough & Bridlington.

Geological background

*Thc 'Red Chalk' is now known as the Hunstanton Formation.

In this section the solid rocks have a low, general southerly, dip so that progressively younger rocks occur southward. Marine Jurassic and Lower Cretaceous clays and shales are overlain by the Red and White Chalk. A non-sequence occurs at the top of the Jurassic rocks (Kimmeridgian Stage, c. 146–151 Ma) and the Portland and Purbeck rocks of the south of England are not developed. The succeeding io cm Coprolite Bed is overlain by the Cretaceous Speeton Clay (about loo m), forming the finest marine Lower Cretaceous section in Britain and equivalent to five of six Lower Cretaceous Stages (c. 136–106 Ma). The Ewaldi Marl, Gault Clay and lower Red Chalk above represent the sixth Lower Cretaceous Stage and the remainder of the Red Chalk and overlying White Chalk form a very full sequence of Upper Cretaceous rocks. The latter is best examined further south in the Flamborough area (Excursion 21).

During the Late Devensian Stage of the Quaternary, ice advanced southwards in the western part of the North Sea area and deposited tills blocking the seaward end of the Vale of Pickering. From radiocarbon dating of organic remains found above and below the equivalent glacial deposits in Holderness, the ice invaded eastern Yorkshire about 18 000 years ago and finally melted by about 13 000 years ago. Two main tills were deposited — a lower greyish-brown and an upper reddish-brown till. In Holderness these are known as the Skipsea and Withernsea Tills respectively; there they contain more chalk than the equivalent tills in Filey Bay, because the ice crossed the main Chalk outcrop between the two areas. The two tills were probably deposited by a single two-tiered ice-sheet. The Skipsea Till originated from ice which moved across southeast Scotland, Northumberland and Durham, whereas the Withernsea Till was deposited by ice which came from the Lake District and crossed the Pennines via the Vale of Eden, the Stainmore Gap and Lower Teesdale. The Lake District/Teesdale glacier was superimposed on the Scottish/Northumberland ice off Teesmouth, and both then moved southwards as a two-tiered glacier.

In interglacial periods before the Late Devensian glaciation the eastern end of the Vale of Pickering was an estuary. Sediment which accumulated in the estuary during an interglacial dated by the amino acid method to approximately 200 000 years ago forms the Speeton Shell Bed, which occurs between the Speeton Clay and glacial deposits on New Closes Cliff.

Excursion details

The lane from the A165 at Reighton village to Reighton Sands traverses several drumlins with long axes orientated north-northwest—south-southeast, a local direction of ice movement parallel to the Chalk escarpment. From Reighton Sands car park follow the sloping track to the shore and turn right (southeastwards). The cliffs cut in Pleistocene and Mesozoic clays for the next 2 km are continually changing because of landslipping and coast erosion, so it is impossible to give exact locations of good exposures. Usually about go% of the cliffs are occupied by landslips, many of which are rotational slips. In situ exposures have vertical faces and approximately horizontal planes between till and gravel units.

About 500 m east-southeast of Reighton Gill solid rocks appear in the cliffs from beneath the tills. However sand may be stripped from the beach to provide foreshore exposures of the solid rocks from the Gill onwards. They are divided into Beds A–F, F being the lowest; Beds B–E constitute the Speeton Clay. Minor folding in the argillaceous rocks results from the weight of the Chalk above or the pressure of Quaternary ice.

Locality 1. The cliff section from below the car park to the seaward end of the ravine called Reighton Gill [TA 142 763] to [TA 144 762] exposes the Late Devensian tills.

Approximately half the cliff is formed of the greyish-brown Skipsea Till, often obscured by downslipped masses of the overlying reddish-brown Withernsea Till. Thin gravels are often seen between the two tills or in the lower part of the Withernsea Till. At Reighton Gill the junction between the two tills rapidly descends to about a quarter of the cliff height, and within the Withernsea Till on the southeast side of the Gill there is a 2–3 m thick gravel, which rises rapidly in the cliff section for about too m southeastwards. Near its southeastern extremity, there is a large contorted raft of grey Jurassic (Kimmeridge, Oxford or Liassic) clay high in the cliff in the Withernsea Till.

Southeast of Reighton Gill, the glacially disturbed surface of Mesozoic clays rises at approximately 88 m/km from below sea level to approximately 30 m O.D. on New Closes Cliff [TA 147758]

In places the surface is overlain by a thin chalky gravel sometimes containing estuarine shells, the lateral equivalent of part of the Speeton Shell Bed (Locality 2). The overlying tills are usually less well exposed on the sloping, densely vegetated cliffs than they are on either side of Reighton Gill, but a few metres of weathered Withernsea Till is usually visible at the top of the cliff.

Stone orientation measurements show that Skipsea Till ice flowed northeast–southwest in the Reighton area, whereas the parent ice of the Withernsea Till moved north-northwest–south-southeast, parallel to the long axes of the drumlins, which must be composed mainly of Withernsea Till. The lower part of the tiered ice-sheet preserved the regional ice movement direction, but the upper part was controlled by the local topography, notably the direction of the Chalk escarpment.

Locality 2, New Closes Cliff [TA 147 758], some 500 m southeast of Reighton Gill.

Approximately halfway up the cliff [TA 1475 7585] the Speeton Shell Bed is usually exposed between an eroded and contorted surface of Speeton Clay and the Late Devensian Skipsea Till (Figure 20.1). It consists of 2–5 m of sandy loam, grey below but weathered brown in upper layers, lying between two beds of chalk-flint gravels. Shells within the sandy loam include the bivalves Macoma balthica, Scrobicularia piperata, Cardium edule and Mytilus edulis, and gastropods Littorina littorea, L. rudis, Hydrobia ulnae and Utriculus obtusus, an assemblage indicating temperate estuarine conditions; many of the same species are in fact common in the modern Humber estuary. A microfauna also indicates deposition in shallow brackish water. The chalky gravels above and below the Shell Bed probably accumulated by gelifluction in cold periods, so the whole sequence represents a cold–warm–cold oscillation.

The shelly loam often contains narrow shrinkage cracks, probably formed during brief periods of exposure at low water during deposition of the Shell Bed. The loam and chalky gravel above and below are also contorted and faulted. Edwards (in Ellis, 1987) identified two episodes of disturbance: a strong earlier episode of north–south compression which affected the sandy loam, lower chalk gravel and underlying Speeton Clay, and a later weaker northeast–southwest compression which contorted the upper chalk gravel and refolded some of the earlier folds. The later force corresponds with the direction of movement of the lower part of the Late Devensian glacier, which deposited the Skipsea Till. The earlier force raised the eroded top of the Speeton Clay to approximately 28 m higher than its predicted regional level at Reighton, the folds in this clay indicating an outcrop compression of approximately 2:1. The earlier force also pushed the Shell Bed to its present position on New Closes Cliff from a much lower original level of deposition.

The earlier (north–south) force probably resulted from the only other known glaciation of East Yorkshire, which deposited the Basement Till of Holderness, during the Wolstonian Stage (130 000–186 000 years ago) or earlier. A thin layer of Basement Till also occurs locally above the Speeton Shell Bed on New Closes Cliff, but this is probably a large erratic raft picked up by the late Devensian glacier and deposited in the lowest part of the Skipsea Till. Provisional amino acid dating of Macoma balthica shells from the Speeton Shell Bed suggests deposition in the Ilfordian Interglacial (186 000–245 000 years ago), which implies that the glaciation resulting in initial disturbance of the Speeton Shell Bed and in deposition of the Basement Till was late Wolstonian.

The Upper Jurassic Kimmeridge Clay (F Bed) is exposed in New Closes Cliff, where it appears from beneath the till, and is also seen from time to time in beach exposures (Figure 20.2). The maximum thickness is 225 m but only the uppermost part is seen in this section. It consists of black pyritic shales and paper shales with large dolomite concretions. White flattened ammonites (Pectinitites pectinatus) are abundant, as are small molluscs similarly preserved.

The basal Cretaceous E Bed, the Coprolite Bed (0.1 m), seen in the area of New Closes Cliff, looks hard and cindery and represents the slowly accumulating sweepings of the old sea floor. It consists of rolled and fragmentary phosphatic and pyritic bivalves, ammonites and bones. In the 19th century some 500 tons of coprolites (phosphate content 57–61%) were mined annually until 1869 when a landslip closed the workings. The old wooden adit props may still be seen occasionally emerging from the eroded base of the cliff.

The D Beds (14.21 m, Berriasian, Valanginian and Hauterivian (part) Stages) are well seen in New Closes Cliff, and consist of black, blue and brown clays which may be glauconitic, pyritic or selenitic. In this, and subsequent beds up to the Red Chalk, brown phosphatic nodules of various shapes and sizes are common and provide evidence of the very slow accumulation of these deposits on the old sea floor. The D Beds are characterized by ammonites and the robust square-sectioned belemnite Acroteuthis. Bivalves, brachiopods and crustacea also occur and large plesiosaur bones have been found in the higher D Beds. Four thin yellow beds indicate ancient volcanic ashes. The top bed is the Compound Nodular Bed (0.30 m), a series of isolated fossiliferous nodules showing two generations of nodule development indicative of very slow formation.

Locality 3, Middle Cliff [TA 148 757]

The C Beds (39.02 m, Hauterivian Stage) consist of light and dark grey clays characterized by the torpedo-shaped belemnite Hibolites jaculoides. Ammonites occur throughout with Endemoceras and uncoiled forms such as Aegocrioceras and Crioceratites commonest in the lower part and Simbirskites in the upper part. These indicate the Hauterivian Stage, although there is still some uncertainty about the exact position of the boundary with the overlying Barremian Stage. A wide variety of other fossils occurs. Some of the phosphatic nodules contain the 'Speeton Shrimp' Meyeria ornata.

At the eastern end of Middle Cliff an old landslip brings in the higher beds and forms a belt of disturbed ground stretching for about 350 m between there and Black Cliff [TA 153 755]

The clays are largely B Beds but examples of the Red Chalk and White Chalk may also be examined. This is convenient if one does not wish to proceed beyond Speeton Beck [TA 155 754] to see them in situ.

Locality 4, Black Cliff [TA 152 755]

The B Beds are characterized by the pointed cylindrical belemnites Praeoxyteuthis, Anlacoteuthis and thyteuthis, and three divisions are recognized.

The Lower B Beds (20.94 m, Barremian Stage) crop out in Black Cliff and are dark, blue-grey clays with some intercalations of paler clays. Various forms of pyrite are common and glauconite occurs at some horizons. Besides belemnites, shelly fossils include bivalves, gastropods, large fragmentary ammonites and a rare echinoid.

Locality 5, Speeton Beck [TA 155 754]

The beck forms the southern boundary of Black Cliff and provides a stable and easily recognized marker point in this section. It provides access to Speeton Village or the cliff-top path and is an alternative route to a shore-level return to Reighton Gap at the end of the excursion.

The Middle B Beds or Cementstone Beds (9.75 m, Barremian Stage) occur in the upper part of Black Cliff north of Speeton Beck but at beach level south of it. South of the beck the sections are poor, the clays being much obscured by slippage and fallen debris from the high White Chalk cliffs. The black pyritic clays contain seven bands of large impure limestone nodules of which the lowest three are the most persistent. These nodules have approximately the right proportions of clay and limestone for calcining and grinding to make cement and have hence been called 'Cementstones'. In the t9th century they were worked in open workings above Black Cliff and also by adits driven into the cliff. They made a light-coloured Roman cement which set rapidly and did not crack on drying. Over woo tons a year were sent annually to Hull by coaster and later by railway.

The Upper B Beds (9.4 m, Barremian and Aptian Stages) are very pyritic clays with some browner beds. Poorly exposed, most are Barremian but the highest part has yielded Aptian ammonites.

The A Beds (c. 12 m, Aptian and Albian Stages) commence with the Ewaldi Marl, which consists of dark brown streaky clays with green glauconite patches, phosphatic nodules and a basal nodul bed. The typical belemnite is the small torpedo-shaped Neohibolites ewaldi.

The overlying beds consist of red-brown clays with some green-grey clays and a thin (0.2 m) band of glauconite with phosphate nodules ('The Greensand Streak') at the base. The small (2–3 cm long) belemnite 'Neohibolites minimus' indicates an Albian age which is confirmed by rare ammonite finds.

Locality 6, Buckton Cliffs [TA 163 751]

About 600 m east-southeast of Speeton Beck the Red and White Chalk form the impressive Buckton and Bempton cliffs stretching on to Flamborough Head (Excursion 21)

The Red Chalk (up to 30 m, Albian and Cenomanian Stages) is essentially white chalk coloured by ferric oxide, probably derived from Triassic rocks and incorporated in the limy ooze of the sea floor at the time of deposition. As little as 1')/0 of ferric oxide will give a good red colour. The same belemnite occurs as in the previous beds as well as other fossils, notably terebratulid brachiopods. Ammonites show that the bulk of the Red Chalk belong to the Upper Albian. The remainder is placed in the Cenomanian, the lowest stage of the Upper Cretaceous.

The hard limestone of the Chalk Group (about 400 in in the Flamborough area, Upper Cretaceous) forms the high cliffs of Speeton, Buckton and Bempton. The hardness of the chalk in Yorkshire is a result of its calcite cement. Only the flintless lower part (Ferriby Chalk Formation, 44 m) is accessible here, but beware of falling debris and the possibility of being cut off by the rising ride.The formation contains a wide variety of fossils throughout, but they are scattered, often fragmentary and difficult to extract. Bivalves of the genus Inoceramus are the best known.

A black streak visible high in the cliff is the Black Band, which lies just above the base of the predominantly flinty chalks of the overlying Welton Chalk Formation. Boulders from these flinty chalks lie on the beach and some contain good Thalassinoides burrow-fill flints.

Glossary

Bibliography

At all times follow: Countryside code and Code of conduct for geological field work