Rocks of Devonian, Triassic and Jurassic age are known to be present in the subsurface of the island from boreholes and interpreted seismic reflection profiles. Up to 389 m of presumed Devonian sedimentary rocks been proved by six boreholes drilled on the island, consisting ofclaystone, siltstone, sandstone and quartzite, similar in type to other dated Devonian sequences. A nearly full Triassic succession has been drilled, reaching a maximum thickness of 450 m. Sandstones of the Sherwood Sandstone Group are overlain by claystones and siltstones of the Mercia Mudstone Group and limestones of the Penarth Group. A complete Jurassic succession is shown by the boreholes at Arreton, reaching over 1400 m in thickness, comprising mainly mudstones of the Lias Group, oolitic limestones of the Inferior and Great Oolite Group, claystones of the Kellaways and Oxford Clay Formations, bioclastic limestones of the Corallian Group, organic-rich mudstones of the Kimmeridge Clay Formation, limestones of the Portland Group and the lower part of the Purbeck Group. The entire sequence presents sedimentation in a shallow water environment.
A complete section is found in the subsurface, but only the upper part of the succession is exposed from Compton Bay to Brighstone Bay and at Sandown Bay, in the core of two broad anticlines. In the Arreton boreholes the Wealden Group reaches a total of 620 m. The exposed sequence comprises the upper part of the Wessex Formation and the overlying Vectis Formation. The Wessex Formation consists of red mudstones with some interbedded sandstones laid down in a freshwater and floodplain environment. The Vectis Formation consists of grey mudstones, deposited in a shallow water lacustrine to lagoonal setting, with some evidence of marine influence. The type section for the formation is in Brighstone Bay.
The Chalk Group consists of a sequence of chalky limestones with some interbedded marls. The age of the sequence ranges from Cenomanian through to Campanian, The upper boundary is an unconformity across which rocks of Maastrichtian to Paleocene age are missing.
Palaeogene
Rocks of Palaeogene age rest unconformably on the Upper Cretaceous sequence on the Isle of Wight. Most of the Palaeocene is missing, in common with all of onshore UK. The Palaeogene strata were deposited in a shallow water marine environment, which was affected by repeated changes in relative sea level, causing cycles of transgression and regression.
The Lambeth Group is well exposed at the southern end of Alum Bay and Whitecliff Bay at the western and eastern ends of the island. This Thanetian sequence is represented by the Reading Formation, a thin sequence of mainly claystones with variable amounts of sands, varying from 25 – 40 m in thickness.
Thames Group
On the Isle of Wight this group comprises the YpresianLondon Clay Formation, which reaches up to 160 m in thickness. The formation is a sequence of mainly claystones, although to the east of the island the formation contains sandstones of the Whitecliff and Portsmouth Sand Members.
The Bracklesham Group is of Ypresian to Lutetian in age. Its type section is along the cliffs in Whitecliff Bay.
Barton Group
This sequence is of Lutetian to Priabonian in age. It comprises a mixture of clays, fine sands, sandy clays and clayey sands. The stratigraphy exposed at the two ends of the island are somewhat different.
The outcrops of Quaternary age are relatively poorly understood.
Structure
Deposition of the Triassic, Jurassic and lowermost Cretaceous sequences was controlled by two large west-east trending, south-dipping normal faults, the Needles Fault and the Sandown Fault, which have an overlapping en-echelon geometry. Reactivation of these faults over part of their lengths during the Paleogene inversion event produced the structures that control the current outcrop patterns. The two main structures are the Brighstone and Sandown Anticlines, which relate to reactivation of the Needles and Sandown Faults respectively. These anticlines have steep, locally vertical northern limbs, forming the monoclinal structures seen at The Needles, Alum Bay and Whitecliff Bay. In the centre of the island the shortening is transferred between the fault zones, forming the zone of lower dips and north-south strike between Calbourne and Garston's Down. To the north of the monoclines the Paleogene sequence is deformed into a gentle syncline, the Bouldnor Syncline.
