Tourmalinisation
Tourmalinisation is the metasomatic replacement of feldspars and micas by the mineral tourmaline. The reaction is complex but involves the circulation of hydrothermal fluids rich in both the elements boron and fluorine. This process is widespread in the Cornish granites, and if allowed to go to completion will form a rock of granite origin where all the feldspars and micas have been replaced, forming a rock containing quartz and tourmaline only.
Tourmaline is common in all of the granites, and dominates the mineralogy in many. Such rocks are called luxullyanites after the village of Luxullyan on the St. Austell Granite. Large tourmaline crystals occur in veins and pegmatites.
The majority of the tourmalines are black in hand specimen (yellow or blue in thin section) and are of the sodic varieties schorl and elbaite. Variations in colour arise due to trace and major element variations. The red/pink variety rubellite occurs in some localities but is rare and has been overcollected.
Greisens
Greisens are a rock composed of quartz and muscovite mica formed by the breakdown of feldspars by metasomatic and hydrothermal activity. Greisens are commonly associated with tin - tungsten mineralised veins; i.e. the ore minerals cassiterite and wolframite respectively.
The reactions involved are:
SnCl2 + 3(K,Na)AlSi3O8 + 2H2O ->
SnO2 + KAl3Si3O10(OH)2 + 6SiO2 + 2NaCl + H2
tin chloride + feldspar + water -> cassiterite + muscovite + quartz + halite + hydrogen
The zone of greisenisation is generally thin. At Cligga Head (Day 5), near Perranporth, greisens are only a few centimetres thick, bordering narrow cassiterite veins. The greisen minerals are associated with chlorite and tourmaline.
Kaolinisation
The breaking down of feldspars to the clay mineral kaolinite by metasomatic and/or meteoric fluids. The china clays (Day 6) of the Cornish granites are by far the most economically valuable material to be extracted from the region. They occur in funnel - shaped bodies developed to a greater or lesser degree in all the granitic bodies, but are at their best in the St. Austell granite where they have been extensively worked.
The conversion of feldspars ((K,Na)AlSi3O8) to kaolinite Al4Si4O10(OH)8 is generally associated with the processes of weathering by groundwaters. However, the large scale and the depth of the funnel shaped kaolinite bodies suggests that they were formed by processes more extensive than just surface weathering. It is, therefore, assumed that the mineralisation occurred as a result of the circulation of meteoric waters plus recharge from hydrothermal solutions derived from the granites.
Ore Mineralisation
The deposition of metallic elements carried in hydrothermal fluids to form ore deposits. Two types of mineralisation are important in Cornwall:
tin-tungsten mineralisation, associated with greisens, and
copper-lead-zinc-iron-arsenic mineralisation.
Ultramafic igneous rock bodies, in the form of ophiolites are a common feature of orogenic belts, representing suture zones formed as oceanic basins close. An ophiolite is a sliver of oceanic crust that has been overthrust onto continental crust during continent-continent collision. Ophiolites rarely sit on the sutures and are usually transported some distance away from it along thrust faults, and such is the case with the Lizard Complex of western Cornwall (Lizard Peninsula - Day 8).
Ideally, an ophiolite should have a sequence, from bottom to top, comprising peridotite and pyroxenites overlain by gabbros, a swarm of "sheeted dykes" and finally pillow lavas and cherts representing the ancient seafloor.
Generally when an ophiolite is emplaced they are tilted over and dissected and so all these components may not be present. Such slivers of ophiolite may show overprinting effects as a result of regional metamorphism or may still retain the characteristics of sea-floor metamorphism. More often than not (and this is certainly the case with the Lizard Complex) the bulk of the preserved material are peridotites and these are generally serpentinised. The Lizard Complex contains a sequence of rocks including partially serpentinised peridotites, gabbros and metamorphosed basalts and basaltic dykes.
Sea-floor metamorphism
Sea-floor metamorphism is hydrothermally driven, and therefore, at least in part, metasomatic. The rock types that represent the ocean floor, namely pillow basalts and basalt sheet flows (which are very poorly preserved in the Lizard Complex) tend to have been altered to spilites, where the calcic-plagioclases have altered to sodic-plagioclase as a result of ion exchange with salts in seawater. Commonly, these rocks also develop a greenschist assemblage of new minerals, particularly chlorite and epidote.
Serpentinisation
Ultramafic rocks are prone to low temperature alteration and metamorphism. The reason for this is that the minerals that comprise ultramafic rocks are more at home in the mantle, and therefore residence in the upper crust removes them far away from their stability fields. Also, in the mantle there is very little, water, whereas water is abundant in the upper crust and such minerals, namely olivines and pyroxenes, are unstable in the presence of water. Therefore, we are presented with the somewhat unusual case whereby metamorphism is induced in mantle rocks by a decrease in temperatures and pressures rather than an increase!
Serpentinisation produces clay minerals of the serpentine family (lizardite, antigorite and chrysotile), and hydrous minerals such as chlorite, tremolite and talc. These are all derived from the breaking down of the ferromagnesian minerals, olivine and pyroxene. Iron from these minerals is resurrected in the form of Fe-rich clays like smectite and goethite, and oxides such as haematite.
The textures of serpentinites are variable. At simplest, they show a replacement of undeformed olivines from the grain boundaries and fractures inwards. This results in a rock with a networked appearance resembling (vaguely) snake skin from whence the name comes. More often than not they are deformed and exhibit a foliation. Serpentinites are frequently criss-crossed by veins filled with fibrous serpentine and tremolite. These are often pale green in colour (in which case the mineral is the serpentine antigorite).
Phenocrysts of orthopyroxenes may be pseudomorphed (replaced by another mineral whilst retaining habit and possibly internal features) by a complex mixture of talc and tremolite. This mix is given the name bastite, and the porphyroblasts generally show up well, with a pale green colour in the otherwise homogenous serpentinite groundmass, giving strikingly porphyroblastic serpentinites.
The softness, and ability to take a good polish has made serpentinite an ideal material for carving model lighthouses from. These can be purchased at great expense from a number of shops in western Cornwall, and they do in fact show up the textures and variations within the rock admirably.
Cornwall and much of Devon consists of a series of argillaceous and arenaceous sediments that have now been ubiquitously subject to low grade regional metamorphism and which, over extensive areas, have also experienced high grade contact metamorphism, metasomatism and mineralisation associated with intrusion of a major granite batholith. The majority of the meta-sediments are pelites or greywackes and are of Devonian age, although in North Devon a large synclinal structure preserves Carboniferous sediments of similar facies.
All of these rocks were subject to intense deformation during the late Carboniferous to early Permian Variscan Orogeny and the coastal sections (particularly in the vicinity of Bude (Day 9) provide many of the classical examples of fold and thrust geometry that are seen in structural geology textbooks.
he deformation, whilst complex, is generally less complex than that of the Caledonide Orogeny, with a single fold phase providing the dominant structural style. The intrusion of granites occurred towards the end of the Variscan events. Cooling and alteration of the granites and their country rock and the associated mineralisation continued for a very considerable time after emplacement of the granites.
Finally it is important to note that the Carboniferous and Devonian rocks of north Devon and Cornwall are greywackes and slates. Originally these sediments were deposited on a steep slope where substantial sedimentary thicknesses could accumulate. This is in marked contrast to the Devonian and Carboniferous of the Mendips and South Wales. This contrast has major palaeogeographical implications which we have to consider.