5 Beer to Charlton Bay



66 to 89 million years ago (MYA).

Upper chalk. The Chalk Group exposed within the Jurassic Coast World Heritage Site (WHS) comprises up to 400 metres of chalks composed dominantly of calcareous nannofossils. Traditionally, the succession is divided into the Lower, Middle and Upper Chalk, although this classification is inappropriate in east Devon. On the coast of Purbeck the Chalk forms spectacular cliffs at Bat’s Head and White Nothe between Worbarrow Bay and Lulworth Cove and at Ballard Head. In East Devon it is about 100 metres thick, and is seen within the cliffs between Lyme Regis and Branscombe, and occurs as isolated outliers between Branscombe and Sidmouth. The Upper Chalk consists of variously nodular, flinty, slightly marly and smooth white chalks which display conspicuous bedding that is picked out by lines of flints, marls and beds of harder chalk. Diverse calcitic faunas of bivalves, brachiopods, belemnites, corals, echinoderms, bryozoans, serpulid worms, fish and a few reptiles have been found in the Upper Chalk within the Jurassic Coast WHS. The sections in the vicinity of Beer, and between White Nothe and Ballard are particularly valuable as reference sections for the chalks of southern England.

90 to 94 MYA.

Middle chalk. The Middle Chalk is present throughout the area, the lower part comprising very fossiliferous hard nodular limestone. In east Devon this yields important ammonite faunas of the latest Cenomanian and earliest Turonian age that are not found elsewhere in the UK, in addition to abundant bivalves of the genus Mytiloides. The Chalk in the Beer area includes the famous Beer Stone, a soft inoceramid-rich chalk that hardens into a fine ornamental building stone on exposure to the air. The overlying, softer, New Pit Formation is locally flinty in east Devon and while poorly fossiliferous in the field, nevertheless contains an highly diagnostic and abundant fauna of planktonic foraminifera, ostracods and calcareous nannofossils, all of which can be used for regional and international


95 to 100 MYA.

The Lower Chalk comprises marly chalks, often rhythmically bedded, which are rather sparsely fossiliferous in the field, but which contain abundant microfossils typical of the Cenomanian Stage. The basal bed of the Lower Chalk (also known as the Basement Bed or Glauconitic Marl) locally contains an abundant macrofauna of beautifully preserved phosphatised ammonites and other molluscs which are very important for inter-regional correlation. The Lower Chalk shows progressive onlap to the west with a basal conglomerate of the chalk facies younging from West Purbeck (Middle Cenomanian) westwards to Devon (late Cenomanian). The Lower Chalk is absent in west Dorset and east Devon, where it is replaced by a succession of thin, fossiliferous, sandy limestones called the Beer Head or Cenomanian Limestones.

101 to 109 MYA.

The Upper Greensand Formation within the Jurassic Coast World Heritage Site (WHS) is a glauconite-rich succession of sandstones and calcarenites, with thin sandy limestones (usually concentrations of shell debris) and dark brown splintery cherts. In east Devon the chert-rich sandstones reach their maximum thickness (c. 25 metres). In this area, the cherts are characterised by the presence of sedimentary bedding. Trace fossils and other macrofauna visible within the silica concentrations confirm that the cherts are replacement features within the diagenetic history of the sediment. The uppermost sandstones in west Dorset and east Devon are characterised by glauconite-rich cross-bedded sandstones that form a quite distinctive building stone. The macrofauna is dominated by the bivalves, especially Exogyra spp., although gastropods and echinoids are also well known. The Perinflatum Subzone is an important phosphatised horizon at the top of the formation in Punfield Cove. The microfauna is quite restricted due to preservational problems, although the sandstones of east Devon have yielded Orbitolina sefini.

110 to 112 MYA.

The Gault Clay and the Upper Greensand formations within the Jurassic Coast WHS are generally sandy in character. At Swanage and in the Lulworth area the Gault is a poorly-fossiliferous silty clay and the sand content increases both westwards and up-succession. In east Devon the Gault is inseparable from the overlying Upper Greensand. Ammonites are often abundant: over 100 species have been recorded from the Gault and Upper Greensand in Purbeck. Microfossils are quite rare, with much of the formation decalcified and badly weathered.


199 to 200 MYA

Blue Lias. This unit is well exposed near Lyme Regis. The Triassic/Jurassic boundary is drawn 2.5 metres above the base of this unit which comprises small-scale rhythms of anoxic shale (produced under low oxygen conditions), oxic shale and thin limestones. The limestones are full of neritic and benthic fossils indicating small shallowing-upward rhythms probably resulting from environmental control following orbitally-forced climatic changes. The unit is richly fossiliferous. A level at the top (Saurian Shales) was a major source of fossil reptiles. The limestones were formerly a source of hydraulic cement. The Hettangian Stage is represented by the lower half of the Blue Lias (Planorbis Zone to Angulata Zone) and the Sinemurian commences in Bed 21 with the Bucklandi Zone. Note that the base of the Jurassic still has to be defined by the International Union of Geological Sciences (IUGS). Succeeds the Penarth Group, probably without a significant stratigraphic break; it comprises grey, fossiliferous, calcareous mudstones and limestones of marine origin. The base of the Jurassic is placed within Blue Lias Formation at the stratigraphic appearance of ammonites of the genus Psiloceras. This major stratigraphic boundary is exposed in the section between Pinhay Bay and Seven Rock Point, west of Lyme Regis at a level 2.5 metres above the base of the group. Beds in the group below this level (Pre-planorbis Beds or Ostrea Beds) are assigned a latest Rhaetian (latest Triassic) age.


201 to 208 MYA

Penarth group. Exposed discontinuously in the faulted and landslipped area between Culverhole Point and Pinhay Bay; it rests disconformably upon the Mercia Mudstone. The group comprises black, fossiliferous shales (Westbury Formation) overlain by grey-green, brackish-water to marine mudstones and marine limestones (Lilstock Formation) and is dated biostratigraphically as Rhaetian age.

209 to 237 MYA

Mercia Mudstone. Exposed between Sidmouth and Branscombe, between Seaton Hole and Culverhole Point, and at Charton Bay; it succeeds the Otter Sandstone conformably. It is overlain, above an angular unconformity, by westward overstepping Cretaceous rocks; continuity of exposure of the group is broken between Branscombe and Seaton by a combination of faulting and the effect of this unconformity. Between Weston Mouth and Branscombe, and at Charton Bay, exposure is affected by landslip. The group consists largely of red-brown mudstones, with some grey-green or silty beds. Fossiliferous dolomitic sandstones and grey-green mudstones (Weston Mouth Sandstone Member) are exposed around Weston Mouth, and higher beds near Branscombe contain large amounts of gypsum. The highest unit in the group, seen east of Seaton, comprises mainly grey-green sediments (Blue Anchor Formation). The dominant sediments of the group accumulated in playas and sabkhas under subaerial and subaqueous conditions; water was of mixed continental and marine origin, and evaporitic conditions resulted in the formation of gypsum and, elsewhere in the Wessex Basin, halite. The Weston Mouth Sandstone represents a brief estuarine episode. The Blue Anchor Formation represents a transition from dominantly continental to dominantly marine influences. Magnetostratigraphic work indicates that the base of the group is Ladinian (Late-Mid Triassic) in age. Carnian-Rhaetian ages are indicated by palynomorphs from the middle and upper parts of the Group.