Cox, B.M. & Sumbler, M.G. 2002. British Middle Jurassic Stratigraphy. Geological Conservation Review Series, No. 26, JNCC, Peterborough, ISBN 1 86107 479 4.
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The coastal exposure of the Oxford Clay Formation at Ham Cliff, at the east end of Weymouth Bay in Dorset, spans the Callovian–Oxfordian stage boundary
The site has been noted by Arkell (1947a) and Cope (1969) but the most recent and fullest account is that of Callomon and Cope (1995) on which the following details, including bed numbers, are based. The measured section is in the cliff but Bed 1, at the base, extends downwards for up to a metre into the beach below high-water mark
| Thickness (m) | |
| Oxford Clay Formation | |
| 5: Clay, dark, slightly fissile, richly fossiliferous with abundant ammonites, including macroconch and microconch Quenstedtoceras cf. woodhamense Arkell at base, Q. mariae (d'Orbigny) and Q. woodhamense at 0.7 m above base, and typical Cardioceras scarburgense (Young and Bird) with common Gryphaea dilatata J. Sowerby at 1.5 m above base; ammonites crushed but with body chambers preserved in yellowish-brown slightly phosphatized marlstone | up to 11.5 |
| 4: Clay, dark, slightly fissile, very sparsely fossiliferous with scattered ammonites (Quenstedtoceras cf. paucicostatum (Lange)); fairly persistent bands of brown, ferruginous mudstone at 1.8 and 2.2 m above base; in upper part of bed, ammonites crushed and with phosphatized body chambers; tenacious in upper 0.3 m | 4.5 |
| 3: Pyritic shell-detrital bed forming persistent, but not always prominent, marker; locally with lenticular, brown ironstone | 0.10 |
| 2: Clay, slightly pyritic, weathering more flaky; sparsely fossiliferous with Quenstedtoceras lamberti (J. Sowerby) often with uncrushed pyritic inner whorls; thin ironstone in lenses near sharp base | 0.75 |
| 1: Clay, pale-grey, fairly tough, non-laminated, calcareous; occasional thin (0.01–0.03 m), lenticular layers of brown ferruginous mudstone or ironstone at or near top; shell-plaster of crushed white ammonites at top forming slight ledge and marker; common Quenstedtoceras praelamberti Douvillé at 0.75 m below cliff base with Q. (Eboraciceras) sp. and Euaspidoceras sp. up to 0.50 m below cliff base; scattered Q. praelamberti above but becoming abundant in top 0.3 m with profuse Q. lamberti sensu stricto and Q. flexicostatum (Phillips), fairly common Kosmoceras sp., occasional Hecticoceras sp., Alligaticeras sp. and Peltoceras sp. | seen to c. 3.0 |
The ammonite faunas of beds 1–4 indicate the Upper Callovian Lamberti Zone and Subzone (including the praelamberti, lamberti and paucicostatum biohorizons). The older Henrici Subzone of the Lamberti Zone is not reached. The ammonites of Bed 5 indicate the Lower Oxfordian Mariae Zone. The boundary between these two zones is usually indicated by the transition from ammonites of the group of Q. lamberti to those of the Q. mariae group. Callomon and Cope (1995) described this as a 'matter of some delicacy and possibly to some degree arbitrary' when the faunal successions are seemingly continuous as at Ham Cliff. In the Midlands, the zone and stage boundary coincides with the top of the Lamberti Limestone, a condensed 'event horizon' that also marks the boundary between the Stewartby and Weymouth members of the Oxford Clay Formation (the Middle and Upper Oxford Clay of traditional usage). The Stewartby Member is a predominantly pale- to medium-grey, commonly smooth-textured, variably silty, calcareous, generally rather poorly fossiliferous, blocky mudstone with ammonites and other macrofauna usually preserved as pyritic internal moulds (see Crookhill Brickpit GCR site report, this volume). The Weymouth Member is a predominantly pale-grey, blocky, smooth-textured, calcareous mudstone, generally only slightly silty but with thin dark-grey, carbonaceous beds with striking interburrowing at some levels as well as thin calcareous siltstones; although generally poorly fossiliferous, large Gryphaea are characteristic and the ammonite fauna is usually pyritized and occasionally associated with sideritic mudstone nodules (Cox et al., 1992). At Ham Cliff, where the succession is relatively expanded, the two members cannot be differentiated on the basis of lithology alone and there appears to be no detectable lithological change or marker bed comparable with the Lamberti Limestone such as is developed elsewhere.
The praelamberti, lamberti and paucicostatum biohorizons are now widely recognized in Europe (Thierry et al., 1997). The paucicostatum Biohorizon is of particular importance in the definition of the Callovian–Oxfordian stage boundary: It was first recognized as a separate faunal biohorizon by Marchand (1979) who referred the species to the genus Cardioceras but Callomon and Cope (1995) considered that the morphological affinities seemed closer to Q. lamberti. Whatever the generic assignment, the paucicostatum Biohorizon is now taken as the youngest and final part of the Callovian Stage throughout much of north-west Europe (Fortwengler and Marchand, 1994). On the Yorkshire coast, which had previously been considered as the best area for a British reference section for the Callovian–Oxfordian stage boundary (see Osgodby Point GCR report, this volume), the boundary succession is much thinner than at Ham Cliff; for example, the paucicostatum Biohorizon is only 0.15 m thick compared with c. 4.2 m at Ham Cliff.
The succession at Ham Cliff is in ammonitiferous clay facies without major non-sequence and may justifiably be considered as potentially the most important, and certainly the most complete, Callovian–Oxfordian stage boundary section in Britain. The facies is more favourable than that at comparable sections elsewhere in Europe for the recovery of microfossils as well as for chemostratigraphy and magnetostratigraphy. The section is thus a most important one for international correlation of the base of the Oxfordian Stage.