Geology of the Brixton Deverill - East Knoyle district (Wiltshire), 1:10000 sheets ST83NE (Brixton Deverill) and ST83SE (East Knoyle) : part of 1:50000 sheet 297 (Wincanton)

The Brixton Deverill-East Knoyle d i s t r i c t lies at the western endof Salisbury Plain and encompasses the north-western part of the Vale of Wardour. The central part of the d i s t r i c t forms part of a dissected plateau developed on Upper Chalk (Figure 1); this reaches a maximum height of 238 m south-east of Brixton Deverill. In the north-west, there are prominent escarpments capped by the Lewes Chalk on either side of the Wylye valley. In the south, the Mere Fault and associated monoclinal structure play an important part in shaping the landscape. In the west, the chalk rises steeply on the north side of the fault from the clay vale to the south. Between West Knoyle and East Knoyle, the steeply dipping Upper Greensand and Chalk strata give rise to strongly featured ground. The principal drainage in the northern part of the d i s t r i c t is northwards by the River Wylye, the only permanent river on the chalk outcrop and its tributaries. In the south-central area, drainage is eastwards by a series of valleys that coalesce just west of Hindon and ultimately join the River Nadder at Tisbury. In the south, on the clay vale, drainage is southwestwards by tributaries of the River Lodden, and south-eastwards by tributaries of the River Nadder. The lowest point in the d i s t r i c t , c.96 m OD, lies in the southern tract. Soils developed on the Upper Greensand and most of the Chalk are light and w e l l drained. However, s o i l s on the West Melbury Chalk, together with some on the clay-with-flint deposits and Kimmeridge Clay are much heavier and poorly drained. Agriculture is a mixture of arable and pasture, with the latter dominant on the Kimmeridge Clay Vale. There are few woods, with deciduous woods confined mostly to the clay vale and the relatively newly planted coniferous plantations on the Chalk and Upper Greensand. Agriculture is the only industry in the area

Geological notes and local details for 1:10000 sheets TQ01NW, NE, SW and SE: Pulborough and Storrington: part of 1:50000 Sheet 317 (Chichester)

This report describes the geology of 1:10 000 geological sheets TQ 01 NW, NE SW and SE, which cover the country around Pulborough and Storrington, in Sussex. The area falls within the 1:50 000 Chichester (317) Geological Sheet. It was first surveyed on the 'one-inch' scale by H.W. Bristow and F. Drew as part of Old Series One-inch Geological Sheet 9, published in 1864. The descriptive memoir covering this and adjacent sheets was compiled by W. Topley and published in 1875. The area was resurveyed on the 'six-inch scale by Clement Reid in 1890 and G.W. Lamplugh in 1899-1900~and formed part of the New Series 'One-inch' Geological Sheet 317, published in 1902. A descriptive memoir by Clement Reid appeared in 1903

Geology of the Poole-Bournemouth area: part of 1:50 000 Sheet 329 (Bournemouth)

This report summarises the results of the three phases of a three year project to investigate the geology of the Poole-Bournemouth area in Dorset, funded by the Department of the Environment

Geology of Exeter and its environs

A 225 km² area around Exeter, described in this report, extends from the villages of Brampford Speke and Whimple in the north to Aylesbeare, Exminster and Woodbury in the south. It is underlain by Carboniferous, Permian, and Triassic solid formations and by a variety of Quaternary superficial deposits. The Namurian Crackington Formation comprises mainly tightly folded shales with subordinate sandstone interbeds. The Permian rocks consist of a lower, predominantly: breccia, sequence (Whipton Formation, Teignmouth Breccia, Monkerton Member) that thins and disappears northwards against a possibly fault-controlled ridge of Crackington Formation; the breccias are overlain by sandstones and mudstones (Dawlish Sandstone and Aylesbeare Mudstone). Volcanic rocks occur at the base of the Permian sequence and possibly within the Dawlish Sandstone. The latter splits into five alternating sandstone and mudstone members when traced northwards from Exeter into the Crediton Trough (an area of thick Permian sediments). The Aylesbeare Mudstone is divisible south of Aylesbeare into two members, the lower containing impersistent sandstones. It is overlain by the basal Triassic gravels (Budleigh Salterton Pebble Beds) which are in turn succeeded by the Otter Sandstone

Geology of the Cranborne Chase district (Dorset)

This account describes the geology depicted on 1:10 000 sheets ST90NE (Witchampton), ST91SE (Chettle), ST91NE (Sixpenny Handley), SU00NW (Horton), SU01SW (Wimborne St Giles) and SU01NW (Pentridge), which form part of the 1:50 000 scale Ringwood (314) Geological Sheet. The original geological survey on the one-inch scale was by H W Bristow and J Trimmer and published on Old Series Sheet 15 in 1856. The district was geologically surveyed on the 1:10 560 scale by F J Bennett 1896–1899, E E L Dixon 1899–1890 and C Reid in 1894 and 1899. The 1:63 360 scale Ringwood Sheet 314 was first published with drift in 1902 and reprinted in 1948. The sheet was reconstituted from the one-inch scale without geological revision and reprinted on to a 1:50 000 scale base in 1976 and reprinted in 1990. The 1:10 000 scale revision survey was carried out by C R Bristow in 1997 and 1998. Cretaceous macrofossils have been identified by M A Woods, Cretaceous micropalaeontology by I P Wilkinson and Palaeogene palynolog by J A Riding

Geology of the Shepton Mallet area (Somerset)

Apart from the urban sprawl of Shepton Mallet, the area is dominantly rural with only a scatter of small hamlets. The area is mostly underlain by Jurassic sediments, with the Blue Lias occupying over 50 per cent of the ground. Carboniferous rocks occur in some of the deeper valleys in the northern part of the area, with the Mercia Mudstone and Penarth groups cropping out mainly in the south-west. Higher parts of the Lias Group, together with the Inferior Oolite and Fuller’s Earth crop out in the east of the area. The highest ground is about 246 m O.D. in the north-east; the lowest ground is about 70 m O.D. in the south-west. The principal drainage is westwards via the River Sheppey in the north, and unnamed streams in the south-west. Outside Shepton Mallet, agriculture is the main industry of the region with a predominance of dairy farming on the heavier soils, and arable farming on the lighter soils developed on the Inferior Oolite. There is very little woodland in the area. In the past, quarrying of limestone (Carboniferous, Blue Lias and Inferior Oolite) was an important industry, but extraction is now limited to the Inferior Oolite in the Doulting area. The Shepton Mallet area of this report comprises 1: 10 000 Sheet ST64SW. Figures in square brackets are National Grid references and fall within 100-km square ST. The grid letters precede the grid numbers

Geology of Sheets SY 99 NE and SE and parts of SY 99 NW and SW Corfe Mullen - Lytchett Minster, Dorset: part of 1:50 000 sheet 329 (Bournemouth)

Some 55 km² of the Corfe Mullen - Lytchett Minster area have been geologically surveyed at the 1:10,000 scale. As a result, the detailed stratigraphical sequence established in the Poole Formation during 1984 has been followed westwards; additionally, sand members within the London Clay have been recognized and mapped over a wide area. Gentle E-W flexures which are superimposed on the regional dip of l° SE, probably overlie faults of pre-Aptian age (mid-Cretaceous). Dinoflagellate floras collected from the clays of the Poole Formation and London Clay allow the various stratal units to be placed within the known dinoflagellate zonal sequence. Landslips developed on the clays of the Reading Formation, and solution-collapse hollows developed over the Chalk have been identified at a number of sites. Many of the clays of the London Clay and Poole Formation have been exploited for bricks, tiles and pottery, but most pits are now disused and mostly backfilled. In addition, extensive reclamation of low-lying ground and tidal flats has occurred. A map showing the extent and nature of the Made Ground is included. Summaries of grading data for sand samples collected in the field are presented graphically. River Terrace Deposits occur at various levels; except in the extreme south and north they have been either built over, or exploited, or are of too limited extent or thickness to form significant resources. An account of the hydrogeology of the district is included. The application of geophysical techniques, principally using the EM 31 and 34 to measure ground conductivity as an aid to geological mapping, is discussed in Appendix 1. A glossary of technical terms appears at the end of the report

Geology of Sheet SZ 19 (Hurn-Christchurch): part of 1:50 000 sheet 329 (Bournemouth)

The original geological survey of the area comprising sheet SZ 19 was made by H W Bristow and J Trimmer at the one-inch to one-mile scale (1:63 360) as parts of Old Sheets 15 and 16 published in 1856 and 1855 Series Geological respectively. The drift deposits were not represented on these maps. Clement Reid resurveyed the area on the six-inch to one-mile scale (1:10,560) in 1893, and his results were incorporated in New Series One-Inch Geological Sheet 329 (Bournemouth), published in 1895 in both Solid and Drift editions, and in the accompanying memoir (Reid, 1898). A second edition of this memoir was produced by H J 0 White, and was published in 1917. White re-examined much of the ground, but the published maps remained unaltered. In 1983 the Institute of Geological Sciences (now British Geological Survey) was commissioned by the Department of the Environment (contract PECD7/1/0103-149/82) to provide new 1:10,000 geological maps of the Poole-Bournemouth area. This contract comprises the survey of ten 1:10,000 sheets, and parts of four others, (Figure 1) over three years, to form a basis for the planning of urban and industrial development, and the safeguarding of mineral and water resources. During 1983, in the first phase of the contract, the four constituent quadrants of Sheet SZ 19 were mapped as follows, under the direction of R W Gallois, District Geologist: SZ 19 NW B J Williams; SZ 19 NE E C Freshney; SZ 19 SW E C Freshney; SZ 19 SE C R Bristow

The Earth: Plasma Sources, Losses, and Transport Processes

This paper reviews the state of knowledge concerning the source of magnetospheric plasma at Earth. Source of plasma, its acceleration and transport throughout the system, its consequences on system dynamics, and its loss are all discussed. Both observational and modeling advances since the last time this subject was covered in detail (Hultqvist et al., Magnetospheric Plasma Sources and Losses, 1999) are addressed

Measurement of the correlation between flow harmonics of different order in lead-lead collisions at √sNN = 2.76 TeV with the ATLAS detector

Correlations between the elliptic or triangular flow coefficients vm (m=2 or 3) and other flow harmonics vn (n=2 to 5) are measured using √sNN=2.76 TeV Pb+Pb collision data collected in 2010 by the ATLAS experiment at the LHC, corresponding to an integrated luminosity of 7 μb−1. The vm−vn correlations are measured in midrapidity as a function of centrality, and, for events within the same centrality interval, as a function of event ellipticity or triangularity defined in a forward rapidity region. For events within the same centrality interval, v3 is found to be anticorrelated with v2 and this anticorrelation is consistent with similar anticorrelations between the corresponding eccentricities, ε2 and ε3. However, it is observed that v4 increases strongly with v2, and v5 increases strongly with both v2 and v3. The trend and strength of the vm−vn correlations for n=4 and 5 are found to disagree with εm−εn correlations predicted by initial-geometry models. Instead, these correlations are found to be consistent with the combined effects of a linear contribution to vn and a nonlinear term that is a function of v22 or of v2v3, as predicted by hydrodynamic models. A simple two-component fit is used to separate these two contributions. The extracted linear and nonlinear contributions to v4 and v5 are found to be consistent with previously measured event-plane correlations