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\section{Geological setting of the Variscan faults and vein fill}  We studied samples of hydrothermal vein calcite from three areas The geographic location and regional geology  ofCarboniferous limestone in  theBritish Isles: (i) The  Peak District area  of the southern Pennines is shown  inDerbyshire and Staffordshire; (ii) The Gower Peninsula, South Wales, and (iii) The Burren, County Clare, Ireland,  Figure 1.All the locations lie to the north of the Variscan front in the British Isles with faulting and vein fill in each area associated with foreland deformation during the late Carboniferous and early Permian periods.  There are distinct similarities in the general geologic setting of the three areas.  During the  mid-Devonian to the end of the lower Carboniferous Britain was subject to a general  north-south back arc-extension arc stretching  as a result of subduction of the Rheic ocean to the south. Extension was largely accommodated by the development of a series of graben and half graben deep water basins bounded by normal growth faults and with foot wall topographic highs. Amongst In  the Peak District the main  basins are: are  the Edale Gulf, Goyt Trough and Widmerpool Gulf in the Peak District; the Culm basin to the south of the Gower Peninsula, and; the Clare Basin along the axis of the Shannon estuary in the west of Ireland. Gulf.  Dinantian shallow water platform and ramp carbonates accumulated on the topographic highs of the Derbyshire platform  whilst deep water facies limestones and shales were deposited in the basins (Figure 1). basins, Figure 1.  Both extension and carbonate sedimentation ended at the end of the Dinantian and was succeeded by with the onset of thermal subsidence. Subsequent sedimentation included a thin blanket of  Namurian shales and later a range of Westphalian river and deltaic sandstone facies. The total thickness of post Dinantian sediment accumulation on the platform limestones ranged froma  1 to 2km, with correspondingly thicker sequences of 3-4km accumulating in the basins. Towards the end of the Carboniferous, and though in the foreland  Variscan shortening resulted in basin inversion andin the foreland  reactivation of extensional faults with both significant strike slip and reverse components of movement. There is evidence for high pore fluid pressures during the period of faulting with the development of mode I fractures and in places a pervasive mesoscale fracture network. Fracture dimensions range from sub-mm to fault widths of several metres. Fracture and fault vein fill at all the locations is dominated by white, sparry calcite often showing a syntaxial growth pattern with varying degrees of complexity as a result of repeated episodes of movement, brecciation and renewed hydrothermal mineral growth. Details of the sample localities are given below.  (i) Peak District. The Derbyshire platform is largely composed of shallow water Dinantian shelf limestones that show little evidence of deformation. The structural evolution of the area is summarised by Quirk (1991). During the lower Carboniferous NE-SW extension, accompanied by normal faulting produced a series of WNW-ESE trending deep water basins that border the platform. The basins are infilled with thick sequences of Dinantian basin limestones, shales and sands. Rotation of the stress field during the upper Carboniferous as a result of the Varsican orogeny to the south resulted in fault re-activation with a significant strike-slip component of movement. It is these re-activated faults that host the largest mineral veins exposed on the North Derbyshire platform.  The thickness of overburden on the platform is not well constrained. Estimates based on reconstruction of post Dinantian upper Carboniferous stratigraphy range up to 2km, with maximum sediment thickness in the basins of 3km (Colman, 1989). Similarly the temperature conditions during vein formation are not well constrained. Fluid inclusion temperatures obtained from hydrothermal calcite suggest temperatures ranging from 50° to as high as 240°C (Rogers, 1977; Masheder and Rankin, 1988; Rodger, 1996; Kendrick et al., 2002).