Floyd, P.A., Exley, C.S. & Styles, M.T. 1993. Igneous Rocks of South-west England, Geological Conservation Review Series No. 5. JNCC, Peterborough, ISBN 0 412 48850 7.
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This site has a unique section through a pelitic roof pendant in a granite pluton. Its late-stage and metasomatic minerals and textures in the granite and country rock, reflect the influence of magmatic volatile constituents.
Introduction
There are several places where contacts between Cornubian granites and their country rocks can be seen, but this section
A detailed field description and petrography was given by Hall (1930), general accounts of the petrogenesis are included in Exley and Stone (1982) and Exley et al. (1983), and details of the origin of the Li- and F-rich granite come from Stone (1975, 1979, 1984). The origin of the roof complex has been explained by Stone (1969), Bromley and Holl (1986) and Badham (1980).
Rinsey Cove, or Porthcew, is on the south coast of Cornwall immediately to the east of Rinsey Head and about 4 km north-west of Porthleven. The Tregonning–Godolphin Granite pluton, which meets the coast here, is composed of two variants; the more northerly Godolphin facies consisting of fine-grained, megacrystic biotite granite (Type C,
Tourmalinization is common in xenoliths which are found in all stages of assimilation, and acicular tourmaline appears on the underside of the country rocks near the cliff top at the eastern side of Rinsey Cove.
The rocks which make up the roof and pendant, which occupy most of the Cove, are Mylor Slate Formation metasediments which, although predominantly dark and pelitic, contain semipelite and psammite and thus have a striped or banded appearance. The place of the Mylor Slate Formation in a wider context of stratigraphy and structure has been discussed by Leveridge et al. (1984) and Leveridge and Holder (1985). The rocks also contain numerous quartz veins, both contorted and cross-cutting, much of the silica for which seems to have been derived from the mobilization of quartz within the rocks by the compression and heat of metamorphism. The local structure, better seen here than at many contacts, consists of recumbent folds, on the limbs of which are minor folds resulting from an earlier deformation. There are two cleavages, of which the more striking (originally termed S2 but now redesignated S3 to correspond with the regional chronology) is subhorizontal and undisturbed by the granite (Stone and Lambert, 1956; Stone, 1966).
In addition to being folded, the metasediments have been thermally metamorphosed to spotted hornfelses, with the development of cordierite, andalusite (locally chiastolite) and, through metasomatism, tourmaline. Corundum, present in the Land's End metasediments at Priest's Cove, has not been found, and migmatization, like that associated with the Dartmoor Granite at Burrator and Leusdon Common, is absent.
On the west side of Rinsey Cove, the contact dips towards the Cove at 20–30°, cutting across the flat-lying cleavage, but is 'stepped' along joints in units from 0.5 to 4 m high, demonstrating emplacement of the granite by stoping and subsidence; disorientated xenoliths and apophyses of granite show how the magma penetrated the killas and prised blocks away. Coarse granite and aplite–pegmatite layers up to 3-m-thick are present. At the head of the cove, a cave has been eroded along the contact which here shows evidence of having been faulted and mineralized. The eastern contact is nearly vertical and may be either intrusive or faulted. The main body of the granite has a medium-grained texture almost up to the contact where there are 1-m-thick pegmatite and pegmatitic patches nearby. A smaller, elliptical pendant or large xenolith about 15 m across and also accompanied by pegmatitic patches is exposed between tide marks on the shore a few metres to the south.
It is considered that the magma producing the Tregonning Granite evolved from the Godolphin magma as a consequence of the deep-seated separation of a fluorine- and OH-rich fraction and ion exchange to enrich the Tregonning magma in Li, Na and Al at the expense of Fe, Ca and Mg. Biotite was thus replaced by zinnwaldite, and plagioclase became more albitic. This process is demonstrated elsewhere in the St Austell mass (discussed below, Tregargus Quarries). The sheets of the roof complex at Rinsey indicate the building up of a later, volatile-rich residuum under a relatively impermeable roof. The lithium-mica leucogranite represents a direct continuation of magmatic melt evolution, whereas the aplite represents a crystallized silicate liquid, and the pegmatite replaces aplite which was metasomatized by a K-rich aqueous fluid (Stone, 1969; Manning, 1982; Exley and Stone, 1982; Exley et al., 1983; Manning and Exley, 1984; Pichavant and Manning, 1984). The roof complexes of other granites, for instance Land's End (seen near Cape Cornwall and Porthmeor Cove), are much simpler because of the absence of the lithium-mica granite component, while the related sheets of Megiliggar Rocks, a short distance to the southeast, are both thicker and more complex. The difference between aplitic and pegmatitic textures could, however, equally be a result of pressure variations following successive openings of the rock initiated by the movement of foundering blocks, as suggested by Bromley and Holl (1986). Badham (1980) combined features of both these explanations, accepting the variations in fluid compositions but emphasizing the importance of physical conditions in determining textures. The lithium-bearing micas from the Tregonning Granite and its leucogranite sheets, whose exact compositions were uncertain for many years, have now been identified as zinnwaldite and lepidolite respectively (Stone et al., 1988).
The only other exposures of this type of granite are found in the western part of the St Austell mass, but in this case they are intruded into granite. Moreover, the roof complex, seen only in china clay pits in the vicinity of Hensbarrow Beacon, has not developed as distinctive a display of leucogranite, aplite and pegmatite as that at Rinsey Cove.
This site shows outstanding sections through the upper part of one of the plutons of the Cornubian Granite mass and its junction with the older sedimentary rocks which it has intruded, baked and altered. Here may be seen evidence of how the granite was emplaced when still molten rock, by the undermining and dislodgement of blocks of the surrounding rocks by forcefully penetrating joints and fissures (a process called stoping), followed by subsidence of blocks into the magma. Blocks thus prised off from the country-rock walls and a possible hanging mass of baked sediments are seen to be surrounded by granite. In time, the molten granite would have assimilated the blocks, but here they have survived because the granite cooled and solidified before this could happen. The site has a well-developed roof complex, the upper-formed product of the granite magma. Although still of granite composition, the component pegmatite, aplite and leucogranite of the complex differ in detail from one another and from the earlier-crystallized granite as a result of losing some constituents of early crystals, increased concentration of volatiles, and interactions between the constituents.