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The Geology and Geodynamics of the Northumberland Trough Region

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The Geology and Geodynamics of the Northumberland Trough Region Research Institute for the Environment, Physical Sciences & Applied Mathematics The geology and geodynamics of the Northumberland Trough Region: Insights from mathematical modelling Linda Austin1 Stuart Egan1, Stuart Clarke1 & Gary Kirby2 & Dave Millward3 1Earth Sciences and Geography, School of Physical and Geographical Sciences, Keele University, Keele, Staffordshire, ST5 5BG, United Kingdom. 2British Geological Survey, Kingsley Dunham Centre, Keyworth, Nottingham, NG12 5GG, United Kingdom. 3British Geological Survey, Murchison House, West Mains Road, Edinburgh, EH9 3LA, United Kingdom. Introduction The numerical modelling of the interaction of geological and geodynamic processes has proved to be a valuable tool for explaining the causes and magnitude of regional subsidence and uplift in response to continental tectonics. In particular, geodynamic modelling can be used to investigate the effects of deep processes that are poorly constrained by subsurface and surface data. In this work, we apply 2D and 3D numerical modelling techniques, combined with the analysis of surface and subsurface data, to investigate the structural, stratigraphical and geodynamic evolution of the Carboniferous block and basin structure of northern England. Two dimensional and three dimensional mathematical modelling techniques combined with the analysis of surface and subsurface data have been applied and developed to investigate the structural, stratigraphical and geodynamic evolution of the Northumberland Trough Region. In particular, to provide insights into the importance of deep processes, such as depth-dependent extension, and how they interact with basin-controlling processes such as sedimentary infill. The Northumberland Trough Region includes the Northumberland Trough, its westerly continuation, the Solway Basin, the Alston Block, a geomorphological high situated to the south of the Northumberland Trough, the Vale of Eden Basin to the west of the Alston Block and the StainmoreTrough to the south of the Alston Block (Figure 1). ult 50Km n Fa into Alw lt ault Fau n F ood indo lt erw Sw Fau ath xley Fe Hau lt au e F Northumberland Trough cki no Gil Hexham in Newcastle-Upon-Tyne as B ay Maryport-Stublick-Ninety lw Carlisle om Fault System So Fath V a P l e e n Alston Alston Block n o i Durham f n e E F d a e u tem n lt lt Sys Fau Penrith B nowle a utterk s le-B Lake District Block neda in e-Lu gh ehous Trou Clos more Stain Figure 1. Location of Study area. The Northumberland Trough Region comprises a major east-west orientated asymmetrical half-graben system that extends across northern England into the northern Irish Sea. Base map © 2009 Google - Imagery © 2009 TerraMetric The region lies within the tectonic framework of the Iapetus Suture Zone, which has resulted from continental collision between Laurentia to the north and Avalonia to the south, opposing margins of the Iapetus or 'proto-Atlantic' ocean (Beamish and Smythe, 1986; Soper et al., 1992). The region has subsequently experienced a number of extensional, compressional and wrench tectonic events throughout Late Palaeozoic, Mesozoic and Cenozoic times. These events have led to a complex subsidence-uplift history that cannot be adequately explained by basin formation due to simple uniform lithosphere extension. 1 m d s h m e e e o e c e e a a g i i t h r g r r o g t a s Remarks including Major Regional Events Legend M t Tectonics Sedimentation e e E p A a A y r S P S E S E 65.5 ±0.3 West East Maastrichtian Extension with 70.6 ±0.6 Campanian transtension 83.5 ±0.7 Santonian Upper 85.8 ±0.7 Coniacian s 89.3 ±1.0 u Turonian 93.5 ±0.8 o Cenomanian e 99.6 ±0.9 c Albian Extension a t 112.0 ±1.0 Aptian e r 125.0 ±1.0 C Barremian Lower 130.0 ±1.5 Opening of the Atlantic Ocean in the Hauterivian 136.4 ±2.0 west and subsidence of the North Sea Valanginian Basin to the east (Ziegler, 1990). 140.2 ±3.0 Berriasian 145.5 ±4.0 Compression c i Tithonian o 150.8 ±4.0 z Upper Kimmeridgian 155.7 ±4.0 o Oxfordian s 161.2 ±4.0 e Callovian c 164.7 ±4.0 i M Bathonian s 167.7 ±3.5 s Middle Bajocian Uplift of the North Sea Dome(Ziegler, a r 171.6 ±3.0 1990). Erosion u Aalenian J 175.6 ±2.0 Toarcian 183.0 ±1.5 Erosion of Permo-Triassic and younger Pliensbachian sediments has removed a large amount Lower 189.6 ±1.5 Duration Sinemurian of sedimentary cover. The thickness 196.5 ±1.0 and extent of rocks that have been of Hettangian Event 199.6 ±0.6 eroded are poorly constrained. There Rhaetian are considerably more Triassic and 203.6 ±1.5 Upper Norian Jurassic sediments preserved in the c 216.5 ±2.0 north-west of England than in the north- i Carnian s 228.0 ±2.0 east of England (Chadwick et al. 1995). s Ladinian a i Middle 237.0 ±2.0 r Anisian T 245.0 ±1.5 Olenkian Lower 249.7 ±0.7 In late Permian to early Triassic times, Induan there was a transition from a 251.0 ±0.4 Changhsingian predominantly marine to a continental Lopingian 253.8 ±0.7 environment across northern England Wuchiapingian 260.4 ±0.7 (Clarke, 2009). Capitanian n 265.8 ±0.7 a Guadalupian Wordian i 268.0 ±0.7 m Roadian r 270.6 ±0.7 To the west of the Pennines, east-west e Kungurian orientated extension reactivated large P 275.6 ±0.7 Artinskian fault structures in the underlying Cisuralian 284.4 ±0.7 Sakmarian Carboniferous strata. 294.6 ±0.8 Asselian Uplift of the Carboniferous basins 299.0 ±0.8 resulted in considerable erosion of the n Gzhelian a i Carboniferous strata during the n s Upper 303.9 ±0.9 a u Kasimovian v Permian Period. l o y 306.5 ±1.0 r s n Middle Moscovian e Variscan Orogeny- Collision between n f i 311.7 ±1.1 e Pennine Coal Measures Avalonian part of Larussia to the north P n Lower Bashkirian Group o 318.1 ±1.3 n and Gondwana to the south. Towards c a b i Upper Serpukhovian i r p the end of the Variscan Orogeny the p 326.4 ±1.6 i Yoredale Group a o s s Middle Visean i Whin Sill Suite was intruded. z C s 345.3 ±2.1 s i Border Group o Tournasian M Lower The extensional phase of the e 359.2 ±2.5 l Famennian Northumberland Trough's evolution is a Upper 374.5 ±2.6 characterised by a close association Frasnian P n 385.3 ±2.6 b e t w e e n s e d i m e n t a t i o n a n d a i Giventian contemporaneous faulting. n 391.8 ±2.7 Middle (Chadwick et al. 1995) o Eifelian v 397.5 ±2.7 e Emsian Emplacement of North Pennines 407.0 ±2.8 Basement D Lower Pragian Batholith during the later part of the 411.2 ±2.8 Caledonian Orogeny (Le Bas, 1982). Lockovian 416.0 ±2.8 Pridoli 418.7 ±2.7 Ludfordian Ludlow 421.3 ±2.6 Gorstian Caledonian Orogeny- Collision n 422.9 ±2.5 between Laurentia to the north and a i Homerian r Avalonia to the south resulting in the Wenlock 426.2 ±2.4 u l Sheinwoodian closure of the Iapetus Ocean i 428.2 ±2.3 S Telychian 436.0 ±1.9 Llandovery Aeronian 439.0 ±1.8 Rhuddanian 443.7 ±1.5 Figure 2. Tectono-stratigraphic chart detailing the tectonic and stratigraphic history of the Northumberland Trough 2 Previous research conducted on the subsidence mechanism of the Northumberland Trough Region has presented several explanations. Bott (1976) and Leeder (1976) presented theories that attributed the subsidence to a combination of regional thinning of the crust by creep of the lower crustal material to the south where the mid-European marginal sea was closing by subduction of the northern continental margin, and wedge subsidence of the upper crust to form the block and trough structures. Leeder (1982) proposed an alternative theory based on the stretching mechanism of the McKenzie model, pure shear. This theory proposes an initial extension event, which thinned the lithosphere by stretching during Dinantian times, resulting in the block and trough structures. The initial stretching event caused the asthenosphere to rise, raising the temperature gradient. Subsequently, as the lithosphere cooled during the Westphalian stage, regional thermal subsidence affected both the block and trough regions. Bott et al. (1984) suggested a subsidence mechanism, based on geodynamic observations, which is a modification of these two previous hypotheses with more emphasis on the lithosphere stretching with subordinate thermal effects. The Westphalian subsidence observed is considerably greater than the maximum amount of subsidence predicted by the McKenzie model, indicating that thermal subsidence was not the only factor affecting subsidence during the upper Carboniferous Period. The Westphalian succession is almost twice as thick as that of the Namurian, indicating an increased rate of subsidence rather than the expected exponential decay as a result of thermal subsidence. One of the aims of this research is to produce several end-member geological and geodynamic models for the possible evolution of the basin which simulate these hypotheses and comment on their feasibility. Cross-Sections The analyses of surface data from fieldwork and subsurface geophysical data have been used to produce regional cross-sections showing present day structure and stratigraphy across the region. Several north-south orientated cross-sections have been produced across the area, positioned as shown in Figure 3, in order to show regional variations in basin depth and burial history, as well as the position and magnitude of movement along major faults.
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