Dr Robin Shail

Cornubian Batholith

The Early Permian igneous rocks of SW England and the adjacent continental shelf form one of the major magmatic provinces of the UK. The best known expression of felsic magmatism is the Cornubian Batholith, comprising composite granite plutons, stretching eastwards from beyond the Isles of Scilly, through Cornwall, to Dartmoor in Devon. It is associated with subtantial rhyolite / microgranite intrusive sheets ('elvans') and the remnants of formerly more extensive rhyolite lavas. The smaller and separate Haig Fras Batholith crops out on the sea floor almost 100 km NW of the Isles of Scilly.











Contemporaneous mafic igneous rocks

Less well known are the mafic igneous rocks that occur: (1) around Exeter, at or near the base of Permian post-Variscan sedimentary successions (lamprophyre and basalt lavas / sills), (2) in the pre-Permian Variscan basement further west (lamprophyre dykes), and (3) within the Permian post-Variscan sedimentary basins of the western English Channel and SW Approaches.

Why do the granites occur where they do and how was so much magma generated ?

Magmas were generated over a 25 Ma period from c. 295 to 270 Ma, primarily by extensional thinning of continental lithosphere previously thickened during Variscan convergence. Mafic igneous rocks resulted from mantle partial melting and felsic igneous rocks largely by partial melting of the lower crust, albeit strongly influenced by underplating / emplacement of mantle-derived melts. Felsic magmatism was restricted to relatively narrow zones in the immediate lower plate / footwall of the Rhenohercynian / Rheic suture (generating the Cornubian Batholith) and the frontal segment of the Bristol Channel Fault Zone (generating the Haig Fras Batholith). The thermal evolution of the lithosphere and onset of partial melting was controlled by superposition of post-Variscan extension and Variscan convergence (see figure above).

Work undertaken with others includes recognition of the role of extensional tectonics and mantle melting in lamprophyre and granite generation within the province (Shail and Wilkinson, 1994Shail et al., 2003; Dupuis et al., 2015; Dupuis et al. 2016; Simons et al. 2016), characterisation of the composite nature of granite plutons (Powell et al., 1999; Salmon and Shail, 1999; Simons et al. 2016), magmatic state fabric development (Kratinová et al., 2003; Kratinová et al., 2010), contact aureole tectonics and emplacement (Hughes et al., 2009; Pownall et al., 2012), characterisation of zircon chemistry (Breiter et al. 2016) and LA-ICPMS dating of zircons (Neace et al. 2016).