Robin Hoods Bay Fossil Hunting

1828 – Young and Bird published one of the earliest major fossil accounts of Robin Hood’s Bay
The early work of Young and Bird helped establish Robin Hood’s Bay as an important Lower Jurassic fossil locality. Their account included the zonal ammonite later known as Arnioceras semicostatum, one of the key early Jurassic index fossils associated with the bay.

1843 – Martin Simpson described new ammonite taxa from Robin Hood’s Bay
Simpson’s nineteenth-century work on Yorkshire fossils included important ammonite material from Robin Hood’s Bay. This helped build the bay’s reputation as one of the classic localities for Lower Lias ammonites on the Yorkshire coast.

1855 – Simpson added further ammonite work from the bay
Simpson’s later work continued to expand the known ammonite fauna of Robin Hood’s Bay. Together with the earlier studies, this formed part of the foundation of the bay’s long scientific importance for Lower Jurassic biostratigraphy.

Early records – the type of Psiloceras erugatum was collected from loose blocks on the beach
Robin Hood’s Bay also produced the type of the early Jurassic ammonite Psiloceras erugatum, collected from loose beach blocks. This is one of the notable taxonomic discoveries tied to the locality.

1927–1970 – Leslie Bairstow carried out his classic mapping and collecting of the Lower Lias
Leslie Bairstow devoted decades to detailed mapping and ammonite collecting on the foreshore at Robin Hood’s Bay. His work produced a large-scale geological map and an important ammonite collection, making this one of the great long-term studies of any Yorkshire fossil site.

1960 – Agar highlighted the bay’s unusual erosion and coastal development
Agar’s work drew attention to the unusually well-developed foreshore platform and the way erosion exposes the Jurassic beds at Robin Hood’s Bay. This added geological significance to a site already famous for fossils.

1977 – Robinson further studied the erosion and development of the bay
Later work by Robinson continued the study of how the structure and erosion of Robin Hood’s Bay control fossil exposure. This helped explain why the locality is so important both geomorphologically and palaeontologically.

1996 – Parkinson compiled a detailed gamma-ray log through the Lower Jurassic succession
Modern stratigraphic work by Parkinson logged the Lower Jurassic succession exposed around Robin Hood’s Bay in detail. This helped place the fossil faunas into a much more precise modern framework and reinforced the importance of the bay as a reference section.

Modern understanding – Robin Hood’s Bay remains one of Yorkshire’s classic Lower Jurassic fossil localities
Today Robin Hood’s Bay is best known for its rich Sinemurian and Lower Pliensbachian ammonite faunas, together with belemnites, bivalves, brachiopods, crinoids and occasional vertebrate material. Its importance lies not just in individual finds, but in the exceptional quality and continuity of the foreshore succession.

Section Architecture

Robin Hood’s Bay is not a single simple cliff log. The key section is the extensive foreshore cut across the Robin Hood’s Bay Dome, running from Boggle Hole and Wine Haven on the south side of the bay, around Bay Town and North Cheek, and northward into the Castle Chamber continuation. The base of the Lias is not exposed even at the lowest tides, much of the back of the bay is masked by glacial till and landslip, and small faults radiate across the foreshore from the dome structure, so the locality must be treated as a composite wave-cut platform section rather than a single vertical cliff face.

Lowest Exposure Note

The oldest beds proved in situ on the foreshore belong to the upper part of the Semicostatum Zone, Sauzeanum Subzone, within the Calcareous Shale Member. Older Hettangian and lower Sinemurian ammonites are known from beach material and from the district more generally, but they should not be forced into a false in-situ Robin Hood’s Bay cliff log.

Formal Numbering Note

The RHB labels below are practical page headings only. Formal published bed numbers are retained exactly in each title. The upper Sinemurian and boundary beds mostly follow the Hesselbo & Jenkyns numbering used in the modern GCR summary, whereas parts of the higher lower Pliensbachian north-side section are more commonly cited in the Phelps and Howarth numbering used between North Cheek and Castle Chamber. Where the literature changes numbering system, that change is preserved rather than artificially simplified.

LIAS GROUP

Redcar Mudstone Formation (Lower Jurassic: Hettangian To Pliensbachian; Robin Hood’s Bay Exposures Mainly Upper Sinemurian To Lower Pliensbachian)

The Robin Hood’s Bay dome exposes the classic type sections of the Calcareous Shale, Siliceous Shale, Pyritous Shale and Ironstone Shale members of the Redcar Mudstone Formation. The boundaries between those members are transitional and facies-controlled, so they do not coincide exactly with ammonite-zonal boundaries; this is one of the reasons why the bay has remained so important in British Lower Jurassic correlation.

Calcareous Shale Member

Bed RHB1 — Beds 1–12 (part), Lowest Exposed Calcareous Shales (>11 m)

These are the lowest beds seen in situ on the central and south-eastern foreshore at the very lowest tides. They consist mainly of medium-grey mudstones with several harder silty bands forming reefs in the centre of the bay, together with scattered calcareous lenticles and some nodule bands. Arnioceras is common at several levels, including beds conventionally correlated with the Sauzeanum Subzone, and recorded associates include Arnioceras cf. semicostatum, Euagassiceras and Pararnioceras. The lower part of the member was deposited in a relatively proximal muddy shelf setting influenced by storms, and some of the harder bands and scour-related features show stronger current activity than higher in the member.

Bed RHB2 — Beds 12–14, Brooki Subzone Package (2.5 m)

Mudstones with a harder calcareous band near the middle and another near the top. Caenisites, including C. cf. brooki, is recorded from the upper part of this interval and identifies the Brooki biohorizon. Lithologically these beds remain dominantly muddy, but the indurated bands show repeated brief pauses in sedimentation and early cementation on the sea floor.

Bed RHB3 — Beds 14–21, Birchi Subzone Package (7.11 m)

Medium-grey mudstones with silty bands and some nodule horizons, preserving the typical lower Robin Hood’s Bay shelf facies. Promicroceras capricornoides and Microderoceras birchi are recorded from this package. Fossils are more scattered than in some higher Sinemurian intervals, but the beds remain consistently fossiliferous and preserve the gradual upward passage from the lower Sinemurian into richer upper Sinemurian faunas.

Bed RHB4 — Bed 22, Upper Calcareous Shale Member / Obtusum Subzone (1.71 m)

Mudstone with two bands of calcareous nodules yielding Asteroceras, Promicroceras, Xipheroceras and Cymbites. This bed package marks the top of the Calcareous Shale Member at Robin Hood’s Bay and shows the increasingly fossiliferous and nodule-rich character of the upper Sinemurian. Shell beds within the higher part of the member are commonly dominated by broken but little-worn Gryphaea, suggesting winnowing on a sea floor lying around storm wave-base.

Total Exposed Thickness Of Calcareous Shale Member In The Robin Hood’s Bay Dome Section: More Than 22 Metres, With Older Beds Continuing Offshore Beyond The Lowest Tidal Exposure

Siliceous Shale Member

The Siliceous Shale Member is the most obviously cyclic part of the Robin Hood’s Bay Sinemurian succession. Very fine quartz sand occurs as thin beds, scour fills and muddy sand scars within silty mudstone, producing a series of coarsening-upward cycles that can be followed around both sides of the bay. Benthic faunas are concentrated in the sandier tops of cycles and include Gresslya, Pholadomya and Pleuromya, together with rich trace-fossil assemblages including Teichichnus, Rhizocorallium, Ophiomorpha, Diplocraterion and Chondrites. Some scour floors are sealed by dark clay drapes beneath which articulated asteroids, ophiuroids, echinoids and the crinoid Hispidocrinus scalaris have been preserved, showing episodic rapid burial after reworking.

Bed RHB5 — Bed 23, Basal Siliceous Scar (0.6 m)

A calcareous sandstone forming a prominent scar, with a concretionary band immediately below. This is the first strongly recognisable sandy marker above the Calcareous Shale Member and marks the change into the more obviously cyclic Siliceous Shale facies. It represents a firm, current-worked sea floor developed during a coarser pulse in sediment supply.

Bed RHB6 — Beds 24–26, Gryphaea Scar Package (c. 2.75 m)

Silty mudstone with a nodule band near the middle, capped by the hard calcareous Gryphaea Scar of Bed 26. Promicroceras and Epophioceras occur in the softer beds, while the scar itself is rich in Gryphaea and probably provided the source of some large ex situ Asteroceras of stellare type. This interval records repeated shell accumulation and reworking on a storm-influenced marine shelf.

Bed RHB7 — Beds 27–33, Stellare Subzone Package (c. 3.3 m)

Mudstones, silty in part, with scattered lenticles and nodules, overlain by a triple band of siltstone and calcareous concretions, many formed in ammonite body chambers. Asteroceras of the blakei group and Promicroceras are common in the lower part, while Aegasteroceras sagittarium characterizes the upper part. This package contains some of the key stellare-age biohorizon stratotypes for the bay and shows the interplay of muddy background deposition with episodic winnowing and early concretion growth.

Bed RHB8 — Beds 33–38, Denotatus Subzone Package (c. 4.95 m)

Mudrock with scattered calcareous nodules, lenticles and a distinct denotatus nodule band in Bed 37. Eparietites impendens and allied forms occur low in the package, and Eparietites denotatus is frequent in the nodule band, which is one of the important denotatus biohorizon levels of the bay. This is a richly ammonitic upper Siliceous Shale interval in which the sandy phases are less visually dominant than below, but nodule formation and faunal concentration remain strong.

Bed RHB9 — Beds 38–42, Simpsoni Subzone Package (c. 2.1 m)

A silty seam and nodular mudstone at the base yield Oxynoticeras simpsoni and Gagaticeras of the exortum group; higher up, Bed 41 is a calcareous nodule band with locally abundant Gagaticeras of the gagateum group, and Bed 42 is mudstone with a harder silty band near the top. This is one of the most historically important parts of the whole Robin Hood’s Bay succession because it includes the classic simpsoni and gagateum-type faunas on which much early Sinemurian biostratigraphy was founded.

Bed RHB10 — Bed 43, Double Band (0.4 m)

The famous Double Band is a conspicuous bipartite bed of bioturbated fine sandstone, best seen on the north side of Boggle Hole at the base of a small promontory. It is one of the most useful field markers in the entire bay. Rich trace fossils include Diplocraterion, Teichichnus, Ophiomorpha and Chondrites. The bed marks a short-lived influx of sand and benthic colonization in otherwise mud-dominated shelf sedimentation.

Bed RHB11 — Beds 44–53 (lower part), Upper Oxynotum Package (c. 7.5 m)

Above the Double Band lies a thicker upper Oxynotum package of mudstones with calcareous concretions, resistant silty bands and a major silty sandstone pair represented by Bed 51. Large Oxynoticeras of the oxynotum group occur in the lower part, with rarer Bifericeras bifer and related forms, while Bed 44 may represent the oxynotum biohorizon itself. These beds show repeated alternation between quieter mud accumulation and stronger event deposition, still on a shallow offshore shelf.

Bed RHB12 — Beds 53 (upper band)–55, Densinodulum Subzone Package (1.2 m)

A thin but important sandy and nodular package. The upper band of Bed 53 is a silty calcareous bed with small nodules yielding Crucilobiceras densinodulum, overlain by mudstone and then a second thin sandy bed. This interval probably includes the lymense biohorizon and marks the first clearly recognised densinodulum fauna in the bay.

Bed RHB13 — Beds 56–60, Raricostatum Subzone Package (c. 3.7 m)

Mudrock with a thin sandy siltstone band above, followed by silty mudstone with abundant crushed Echioceras of the raricostatum group and capped by Bed 60, a nodule-bearing mudstone yielding Echioceras cf. intermedium and Eoderoceras. This subzone is especially notable because crushed ammonites become relatively abundant in the shales themselves, not just in discrete nodules.

Bed RHB14 — Beds 61–67, Macdonnelli Subzone Package (c. 6.4 m)

Silty mudstones with ferruginous and calcareous lenticles and nodules, including the prominent East Scar of Bed 63. Leptechioceras of the planum and macdonnelli groups, together with Eoderoceras and Radstockiceras, identify the macdonnelli fauna. The member remains distinctly sandy and cyclic here, but the ammonite assemblage changes decisively from oxynotid-dominated faunas below into echioceratid and eoderoceratid assemblages characteristic of the highest Sinemurian.

Bed RHB15 — Bed 68, Landing Scar (0.8 m)

A silty sandstone, bioturbated in its upper part, forming Landing Scar at Bay Town. Leptechioceras of the meigeni group are recorded from this bed. It is one of the clearest practical field datums in the bay and marks the top of the obviously sandy Siliceous Shale facies before the darker boundary mudstones above.

Total Thickness Of The Siliceous Shale Member In The Robin Hood’s Bay Composite Section: Approximately 34 Metres

Pyritous Shale Member

The Pyritous Shale Member comprises dark grey to black pyritic mudstones spanning the uppermost Sinemurian and lowest Pliensbachian boundary interval. It is much darker and less overtly sandy than the member below, although scour fills occur near its base and top. Benthic fossils are relatively sparse, bioturbation is mainly pyritized Chondrites with subordinate Rhizocorallium, Ophiomorpha and Teichichnus, and the whole facies records a relative deepening and more dysaerobic sea floor.

Bed RHB16 — Beds 69–70, Aureolum–Aplanatum Boundary Package (c. 2.4 m)

Grey to dark-grey mudstones with a siltstone horizon and nodule bands, capped by a red-weathering nodular horizon. Paltechioceras aureolum occurs in the lower part, while the top carries Paltechioceras aplanatum, Eoderoceras and probable Gleviceras. These beds include the aureolum and aplanatum biohorizon stratotypes and form the immediate pre-boundary uppermost Sinemurian sequence at Wine Haven.

Bed RHB17 — Bed 71, Donovani Horizon And Pliensbachian Boundary Interval (c. 2.3 m Combined Boundary Package)

This is the key international boundary bed package of Robin Hood’s Bay. Bed 71 includes uppermost Sinemurian mudstone below and the small but crucial pyritized Bifericeras donovani fauna near the top, with rare juvenile Apoderoceras and Gleviceras. In the detailed Wine Haven boundary log the ratified base of the Pliensbachian lies within this donovani horizon, just above the upper concretionary siderite bed. Lithologically the interval shows the gradual change from pale grey and buff sandy mudstone below into silty dark-grey shale above, and stratigraphically it is one of the most important Lower Jurassic boundaries in Europe.

Bed RHB18 — Beds 72–101, Pyritous Shales Proper (21 m)

Dark mudrocks with bands of ferruginous nodules and concretions forming the main body of the Pyritous Shale Member. Large Apoderoceras occur at least in the lower part, and Phricodoceras is also recorded. Thin-shelled benthos occurs chiefly near the base and top of the member, but otherwise the facies is relatively low-diversity and pyrite-rich. This interval records the continuation of relatively deep, stressed shelf deposition after the stage boundary, before the more obviously banded lower Ironstone Shale facies develops above.

Total Thickness Of The Pyritous Shale Member At Robin Hood’s Bay: About 26 Metres Including The Boundary Package

Ironstone Shale Member

Member Note

The lower Ironstone Shale Member is exceptionally well exposed on the north side of Robin Hood’s Bay between Bay Town and Castle Chamber. It comprises alternating dark and pale silty mudstones, ferruginous nodule bands, sideritic concretions and locally sandy units. The lower part, especially across the Polymorphus, Brevispina and Jamesoni subzones, forms the classic “Banded Shales”, in which the paler beds are coarser grained, more carbonate-rich and benthos-rich, while the darker beds are more organic and finer grained. From around the Ibex Zone upward, large Pinna become a conspicuous feature, locally in life position and elsewhere current-sorted parallel to bedding. Because published numbering changes within this member, both numbering systems are retained exactly below.

Bed RHB19 — Beds 102–106, Upper Taylori Transition Beds

Mudstones with bands of calcareous nodules forming the transition from the dark Pyritous Shale Member into the lower Ironstone Shale facies. Although less fossiliferous in published summaries than the beds above, these beds are important because they show that the lithological shift at the base of the Ironstone Shale Member is gradual rather than abrupt.

Bed RHB20 — Beds 107–?113 (part), Polymorphus Subzone Banded Shales (c. 9.5 m)

Alternating dark and pale mudstones, in part silty, with ferruginous nodules and concretions. Polymorphites is the characteristic ammonite, and the facies is the classic lower “Banded Shales” expression of the Ironstone Shale Member. The alternation of paler, coarser, more benthos-rich beds with darker, finer, more organic beds is especially clear in this part of the member and has been central to discussion of climatic cyclicity and shallow-marine shelf sedimentation in the Cleveland Basin.

Bed RHB21 — Beds ?113 (?part)–?116 (?part), Brevispina Subzone Banded Shales (c. 3.5 m)

Dark-and-pale mudstone alternations with ferruginous nodules and concretions, yielding Platypleuroceras, including P. brevispina, and allied polymorphitids. Lithologically similar to the beds below, these strata continue the banded shallow-shelf rhythm but with a distinct ammonite fauna and slightly more persistent concretion horizons.

Bed RHB22 — Beds ?117 (?part)–121 (part), Jamesoni Subzone Banded Shales (c. 7 m)

Mudstone alternations, dark and pale, in part silty, with ferruginous nodules. Published faunal records are less complete here than in some other subzones, but Uptonia jamesoni and Lytoceras occur in the upper part. These beds complete the Jamesoni-Zone banded shale development and are important because they bridge the transition into the higher, more fossil-rich Ibex-Zone part of the north-side section.

Bed RHB23 — Bed 121 (part) And Beds 1–4, Arietiforme To Valdani Interval (c. 3.9 m)

The published numbering changes at this level. The basal part includes dark-and-pale mudstone alternations with ferruginous lenticles, followed by ferruginous nodule bands and alternating dark and pale silty mudstones. Recorded faunas include Cymbites in the lower part, Liparoceras cheltiense in Beds 2–3, and Acanthopleuroceras lepidum in Bed 4b, with Acanthopleuroceras maugenesti in the ferruginous nodule band at Bed 1. This is the incoming of classic Ibex-Zone liparoceratid–acanthopleuroceratid faunas on the north side of the bay.

Bed RHB24 — Beds 5–18, Rotundum To Luridum Interval (c. 20.1 m)

Mainly dark mudstones with ferruginous nodule bands below, passing upward into darker silty mudstones and concretion-rich beds of Luridum age. Characteristic ammonites include Beaniceras crassum, B. luridum, Liparoceras heptangulare, L. naptonense and Lytoceras. From about this level upward through much of the Ibex Zone, large Pinna become conspicuous and may be seen either in life position or current-sorted parallel to bedding, giving one of the most distinctive faunal signatures of the Robin Hood’s Bay lower Pliensbachian. The beds record shallow-marine mud sedimentation with strong current influence, episodic storm reworking and repeated siderite growth.

Bed RHB25 — Beds 19–35, Sparsicosta Interval (15.5 m)

Darker grey mudstones below, generally becoming more silty upward and including a sandy unit toward the middle, with calcareous ferruginous nodules and one especially important oolitic ironstone level. The fauna of Beds 21–29 includes Aegoceras maculatum var. atavum, Androgynoceras heterogenes, A. sparsicosta, Liparoceras heptangulare, L. naptonense, Pagophylloceras and Lytoceras. Bed 21 is particularly significant: it is a nodular oolitic ironstone with large subvertical burrows filled with chamositic ooliths and represents the lowest Jurassic level in the Cleveland Basin where true oolitic ironstone is developed. Higher in the interval, shell-rich beds, woody debris and continuing Pinna levels indicate increasingly active, shallow, current-swept shelf conditions.

Bed RHB26 — Beds 36–40, Maculatum Interval (2.7 m)

Silty mudstone with ferruginous nodule bands yielding Androgynoceras maculatum and its heterogenes–leckenbyi variants. This is the uppermost Ironstone Shale Member interval included in the core Robin Hood’s Bay lower Pliensbachian succession. The beds are comparatively finer than some of the coarser Ibex-Zone intervals below, but the facies remains shallow marine and transitional upward toward the basal sandy Staithes Sandstone sea-floor.

Staithes Sandstone Formation (Pliensbachian)

Formation Note

Only the lower part of the Staithes Sandstone Formation is included here, where it comes down to shore level at Castle Chamber and the immediate northward continuation. The formation is dominated by bioturbated siltstones and fine sandstones with small-scale coarsening- and fining-upward cycles, wave ripples, gutter casts and shell-rich horizons. The base is taken at the distinctive ferruginous shelly Oyster Bed.

Bed RHB27 — Bed 41, Oyster Bed (0.2 m)

A ferruginous concretionary shell band forming the base of the Staithes Sandstone Formation in the Castle Chamber continuation. Aegoceras ?capricornus is recorded. This thin but distinctive bed is one of the sharpest practical lithological markers in the whole Robin Hood’s Bay lower Pliensbachian succession.

Bed RHB28 — Beds 42–45, Capricornus Beds (c. 1.5 m)

Siltstones with a band of ferruginous nodules and concretions, carrying Aegoceras capricornus, A. lataecosta and allied forms. These beds are already much sandier and more bioturbated than the Ironstone Shale Member below, reflecting the arrival of a shallower and more energetic shelf regime.

Bed RHB29 — Beds 46–48, Crescens Interval (c. 1.6 m)

Siltstone with ferruginous concretions, including a basal nodule band. Aegoceras crescens occurs, including forms transitional upward toward Oistoceras angulatum. This is a classic transitional shallow-water ammonite-bearing interval in the lower Staithes Sandstone.

Bed RHB30 — Beds 49–58, Angulatum Interval (c. 6.4 m)

Siltstone with concretionary bands in the upper part and mudstone with ferruginous concretions near the base, yielding Oistoceras angulatum, related transitional forms and Liparoceras divaricosta. The facies is heavily bioturbated in places, but hummocky cross-bedding, wave ripples and minor scour gutters show that these were storm-agitated shallow-marine sands and silts rather than quiet offshore muds.

Bed RHB31 — Beds 59–61, Castle Chamber Floor Sandstone (c. 2.15 m)

Hard ferruginous sandstone forming the floor of Castle Chamber. Oistoceras angulatum is characteristic. The bed has long been one of the key field markers at Castle Chamber because it forms the shelter floor and clearly displays the more arenaceous style of the Staithes Sandstone Formation. Scour at the base indicates energetic erosion before deposition of the sandstone body.

Bed RHB32 — Beds 62–65, Figulinum Interval (0.45 m)

Two bands of red calcareous concretions separated by sandy shale and siltstone, yielding Oistoceras figulinum, O. curvicorne and forms transitional toward later Amaltheus. This is the highest lower Pliensbachian interval included in the core Robin Hood’s Bay page and forms the top of the lower Staithes section before the overlying upper Pliensbachian Amaltheus-bearing sands of the Hawsker continuation.

Higher Continuation Note

Immediately above the lower Staithes beds logged here, the Castle Chamber roof sandstones and the first Amaltheus mark the onset of the upper Pliensbachian Hawsker Bottoms succession. Those younger Stokesi-, Margaritatus- and Toarcian beds are best treated as the Castle Chamber–Hawsker continuation and are not forced into this Robin Hood’s Bay page.

Depositional Environment

The Robin Hood’s Bay succession records repeated shifts across a shallow but fully marine Jurassic shelf on the margin of the Cleveland Basin. The Calcareous Shale Member represents relatively proximal muddy shelf sedimentation with silty storm-influenced beds and local shell concentrations. The Siliceous Shale Member records stronger rhythmic alternation between mud and very fine sand, with scour hollows, sandy foreshore scars, abundant trace fossils and periodic winnowing around storm wave-base. The Pyritous Shale Member marks a relative deepening and more dysaerobic sea floor across the latest Sinemurian to earliest Pliensbachian interval, culminating in the internationally important donovani horizon and the Pliensbachian GSSP at Wine Haven. The Ironstone Shale Member records a return to more strongly cyclical, banded shallow-marine mudstone and siltstone deposition with ferruginous nodules, early oolitic ironstone, large Pinna communities and increasing upward coarsening. The lower Staithes Sandstone Formation completes the section with bioturbated storm-worked silts and fine sands deposited in a shallower, higher-energy shelf setting.

Total Thickness Covered Here: The Howarth Robin Hood’s Bay Composite Succession, From The Lowest Spring-Tide Exposures To The Top Of The Lower Pliensbachian Lower Staithes Sequence, Measures 163.74 Metres

References

Howarth, M.K. (2002). The Lower Lias of Robin Hood’s Bay, Yorkshire, and the work of Leslie Bairstow.
Hesselbo, S.P. & Jenkyns, H.C. (1995). Detailed stratigraphy and sequence stratigraphy of the Hettangian to mid-Pliensbachian Robin Hood’s Bay succession.
Dommergues, J.-L. & Meister, C. (1992) on the Sinemurian–Pliensbachian ammonite succession and the Bifericeras donovani horizon at Wine Haven.
Meister, C. and co-authors (2006). The Global Boundary Stratotype Section and Point (GSSP) for the base of the Pliensbachian Stage, Wine Haven, Robin Hood’s Bay.
Howarth, M.K. (1955, 1973, 1992) on the Pliensbachian and Toarcian ammonite succession of the Yorkshire coast.
Howard, A.S. (1985). Lithostratigraphy of the Staithes Sandstone and Cleveland Ironstone formations of north-east Yorkshire.
Phelps, M. (1985) on the Castle Chamber and lower Staithes Sandstone succession.
Page, K.N. (1992, 1995) on Lower Jurassic biohorizons and Robin Hood’s Bay stratotypes.
British Geological Survey Lexicon: Redcar Mudstone Formation, Calcareous Shale Member, Siliceous Shale Member, Pyritous Shale Member, Ironstone Shale Member and Staithes Sandstone Formation.
Geological Conservation Review accounts: Normanby Stye Batts–Miller’s Nab (Robin Hood’s Bay), North Yorkshire, and Castlechamber to Maw Wyke, North Yorkshire.