Huddart, D. & Glasser, N.F. 2007. Quaternary of Northern England. Geological Conservation Review Series No. 25, JNCC, Peterborough, ISBN 1 86107 490 5.
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N.F. Glasser
The site at Burbage Brook, contains an assemblage of sediments and landforms that are significant for studies of rock weathering, periglacial processes and landscape evolution in the Pennines. The Pennine tors are at the heart of a long-standing controversy concerning the nature of deep weathering and tor formation in the British Isles. There currently are two main theories that can account for tor formation. The first entails a two-stage model of weathering and stripping (Linton, 1955, 1964) and the second requires only a single cycle of denudation under periglacial conditions (Palmer and Radley, 1961; Palmer and Nielson, 1962). Much of this debate has focused on the tors of the Pennines, which are developed in Millstone Grit. One of the characteristics of the Pennine tors is that commonly they are developed on the edge of escarpments. Palmer and Radley (1961) termed these features 'edge tors', although they are also widely known in the literature as 'scarp-edge tors' (Cunningham, 1964, 1965). This site is noted for its particularly well-developed scarp-edge tors.
The landform–sediment assemblage at Burbage Brook includes a variety of escarpments, tors, structural benches, solifluction deposits, weathering features, blockfields, blockslopes and a Devensian Late-glacial soil. The site has been used by Linton (1964) to illustrate his theory of tor formation and by Cunningham (1965), who identified and described in detail eight tors on Mother Cap Moor as part of his discussion of the south Pennine tors. A detailed description of the geomorphology of the Burbage basin is given by Said (1969). This area of the Pennines was also used in the pioneering work on slope form and slope evolution (Young, 1961; Carson and Petley, 1970) and in attempts to establish a denudation chronology for the British uplands (Johnson and Rice, 1961; McArthur, 1970, 1971, 1977, 1981).
Burbage Brook occupies an area of c. 3.5 km2 of Hathersage Moor, some 10 km to the west of Sheffield. These moorland slopes form a broad valley containing the Burbage Brook. Geologically, rocks of Namurian (Upper Carboniferous) age dominate the area (the 'Millstone Grit' of Eden et al., 1957). At Burbage Brook these are primarily massive sandstones, siltstones and mudstones of the Chatsworth Grit and the Middle Grit Group. A number of prominent cliff faces and scars, including those at Millstone Edge and Burbage Edge, define the upper slopes of the Burbage valley. In places, these cliffs reach heights of up to 30 m and immediately below them are accumulations of detached blocks. Large boulder fields extend for a considerable distance below the edges. On the eastern side of Burbage Brook are a series of continuous scarps and slopes. The area to the west of Burbage Brook is generally more broken up and consists of a number of tors, including those at Higger Tor, Carl Wark, Winyards Nick and Over Owler Tor
The tors of the Burbage area can be subdivided into two main types (Linton, 1964). These are the higher tors and the lower tors. The higher tors are located on the top of free faces, on the back slope of cuestas and on ridge summits. They exhibit evidence of deep weathering along joints and bedding planes. Large weathering pits are common on their summits. There are no free faces of corresponding height in the immediate vicinity. The lower tors are those immediately in front of free faces. They show little evidence of deep weathering along joints and bedding planes. Weathering pits are less common on their summits, but where these do occur they are shallow and widely spaced. Well-developed weathering pits have convex lips, an inner wall and floor. Some pits are crossed by open joints and cracks, possibly of periglacial origin. A second type of weathering is evident in the form of honeycomb weathering on the sloping surfaces of free faces, tor plinths and blocks. Overall, the honeycomb weathering appears to be less common than the weathering pits.
Said (1969) completed the most comprehensive study of the geomorphology of the area
Soil and vegetation currently cover most of the Burbage Brook catchment. Beneath this cover, the sedimentary evidence is exposed mainly in stream-cut sections along the course of the Burbage Brook. These show evidence for several phases of river aggradation and incision
Said (1969) also described slope profiles across the shale–grit and shale–sandstone lithologies. Convex slopes occur on highly jointed grit or sandstone lithologies. Free faces (edges) are restricted to the more massive grit outcrops, particularly near summit crests. Bedding planes and joints on the edges commonly are weathered, particularly on the flaggy sandstones. Slope profiles commonly are covered by head material, although this is deeper and better developed on concave slopes than on convex slopes. The size, location and morphology of boulder accumulations are also controlled to a certain extent by lithology. The blocks are not rounded corestones but show considerable variation in degree of roundness. They are more angular on interfluves and at the foot of free faces, but relatively more rounded at a distance. Large differences in the roundness of sandstone and grit fragments are apparent. Sandstone fragments tend to be more angular whereas the grit fragments are relatively more rounded. All shapes of grit blocks can be found, including oblate, equant, bladed and prolate. Glacial erratics are also noted in the area, but these generally are rare.
Said (1969) explained the different sedimentary units of the area as a function of fluctuating climate in the Late-glacial
Detailed study of the different types of edges (free faces) and their morphology led Said (1969) to suggest that these were formed in the cold phase preceding the antepenultimate glaciation. There was also a phase of face development during the penultimate glaciation. Some of the free faces probably survived the last interglacial. The development of free faces was renewed in the last glacial episode and it is likely that periglacial processes shaped much of their present form at that time. The active evolution of free faces ceased with the cessation of cold conditions at the end of the Late-glacial. McArthur (1981), working in the upper Derwent basin, came to similar conclusions regarding the timing of these episodes of periglacial activity. He described 'periglacial slope planations' and argued that these valley-side benches formed through retreat of sandstone and gritstone scarps and associated removal of rock waste by solifluction. McArthur (1981) invoked river incision of 40–50 m following the initiation of scarp retreat to leave the benches in their current position. The upper Derwent basin, however, lies within the limits of the maximum glaciation and it has been suggested that this is a significant factor in their formation (Ballantyne and Harris, 1994). There appears to be strong structural control on the development of the 'periglacial slope planations' described by McArthur (1981), with the lip of each bench underlain by resistant sandstone and the treads cut across shales. It therefore is equally, if not more, plausible to interpret these benches as the products of differential glacial erosion of strata of variable resistance (Ballantyne and Harris, 1994). The role of cryoplanation therefore may be limited in this area simply to scarp retreat and solifluction of regolith over the surfaces of glacially eroded benches.
Said (1969) considered the development of tors to be an integral part of the development of free faces. Whether a tor is produced in any part of a free face is a function of its lithology and structure. For example, he noted that in the Burbage area lenses of massive grit in the free faces are often left as isolated stacks or small tors. Said argued that because this area was ice covered during the antepenultimate glaciation all tors would be destroyed and that the tors in this area therefore cannot be Tertiary in origin. According to Said (1969), therefore, the active evolution of tors ceased at the end of the Late-glacial. This does not of course allow for the possibility that the tors survived beneath cold-based portions of the ice sheet, as demonstrated elsewhere for other tor landscapes (Fitzpatrick, 1963; Sugden, 1968, 1989; Hall, 1985, 1991; Hall and Sugden, 1987; Hall and Mellor, 1988; Hall et al., 1989; Ballantyne, 1994; Kleman, 1994). In contrast, both Linton (1955) and Cunningham (1965) advocated Tertiary deep weathering and argued that the tors were weathered long before the surrounding blocks were exposed.
The roundness of detached blocks was probably acquired subsequent to their detachment from the free faces and other bedrock outcrops. The difference in roundness between sandstone and grit boulders probably is lithological and holds no genetic significance. The blockfields probably formed during the penultimate and last glacial phases, but some may be much older. There is stratigraphical evidence to show that the blockfields were formed in both the Older Dryas and Younger Dryas and that their active evolution ceased at the end of the Late-glacial.
Weathering pits are currently developing on the surface of blocks, but those on the sides of blocks are relict. Pits are initiated on the surface of blocks where large quartz pebbles are removed, and develop through enlargement as a result of wetting–drying cycles, freeze–thaw and organic growth and decay. They cannot be used as evidence of Tertiary weathering because they can develop in a variety of climatic settings. Pit initiation probably began in the last interglacial but was interrupted by the onset of cold conditions during the last glacial. Their development has resumed in the Holocene. The honeycomb weathering on the sloping surfaces of free faces, tor plinths and blocks is interpreted by Said (1969) as weathering of an iron-deficient zone beneath iron crusts. Wherever the crust is punctured, for example by the removal of a quartz pebble, the inner, decomposed, iron-deficient zone is exposed and the pattern develops. The pits are probably of little palaeoclimatic significance.
Other workers have confirmed the overall conclusion of Said (1969) that the landscape of the southern Pennines owes much to relict periglacial processes. In his study of the neighbouring upper Derwent basin, for example, McArthur (1981) concluded that solifluction sheets are essentially immobile under the present-day climatic regime. Similarly, landscape elements such as benches, escarpments and regolith are periglacial in origin, but the dominant landscape-forming processes in the southern Pennines under present climatic conditions are fluvial.
Burbage Brook contains an assemblage of landforms and sediments typical of upland areas in the southern Pennines. It is an important site for the study of tors, edges, and the processes of rock weathering and slope formation. An important element of this site is that it has been used to construct a chronology and regional picture of events during Late-glacial and Holocene times. The evidence from Burbage Brook indicates periods of intense weathering under periglacial climates during the Older and Younger Dryas, followed by a return to fluvially dominated, landscape modification under present climatic conditions.