- Geology of Yorkshire
In Yorkshire there is a very close relationship between the major topographical areas and the geological period in which they were formed. The Pennine chain of Hills in the west is of Carboniferous origin. The central vale is Permo-Triassic. The
North York Moorsin the north-east of the county are Jurassic in age while the Yorkshire Woldsto the south east are Cretaceous chalk uplands. The plain of Holdernessand the Humberhead levels both owe their present form to the Quaternary ice ages. The strata become gradually younger from west to east.Citation | last =Edwards
first2 =F M
title =The Pennines and Adjacent Areas
series =British Regional Geology
publisher =HMSO. Natural Environment Research Council
accessdate =] Citation | last =Kent
first =Sir Peter
first2 =G D
title =Eastern England from the Tees to the Wash
series =British Regional Geology
publisher =HMSO. Natural Environment Research Council
Much of Yorkshire presents heavily glaciated scenery as few places escaped the great ice sheets as they advanced during the last ice age.
The evolution of the landscape
The oldest rocks in Yorkshire are represented by a number of small inliers of
Palaeozoicareas along the southern margin of the Askrigg block to the north of the Craven fault. This Ingletonian group of folded and cleaved mudstones and sandstones is of disputed age but fossils equate them with the lower Skiddaw group of the Lake Districtwhich are OrdovicianThese rocks were laid down when the area was part of the Avalonialand mass and was positioned about 30° south of the equator.cite book |title=The Geology of Britain: An Introduction |last=Toghill |first=Peter |authorlink= |coauthors= |year=2000 |publisher=Swan Hill Press |location= Shrewsbury|isbn=1 85310 890 1 ]
By the end of the Ordovician period the Avalonian land mass had collided with
Balticaand this event caused a marine regression which was exacerbated by a world wide drop in sea level caused by a period of glaciation.
Silurianperiod Avalonia and Baltica moved rapidly towards Laurentiaat a position about 20°south of the equator. The Iapetus Oceanwhich lay between them was closed. Inliers of the Silurian rocks which were formed at this time occur at Cross Fell, adjacent to the Pennine fault, and at Horton in Ribblesdaleand Austwick, north of the Craven fault.
In the following
Devonianera the land area which is now Yorkshire was in a continental, inland, phase of deposition. There are no proven remaining Devonian deposits in the Yorkshire area and the Carboniferous rock lie unconformably on the Silurian.
Carboniferousdeposits were laid down on and between large pre existing land blocks and intervening troughs.The blocks are known as the Askrigg and Alston blocks.These upstanding areas and the troughs between were actively subsiding into shallow seas which were the result of a global rise in sea levels. These seas contained high levels of calcium carbonate and calcium forming fossils. There are areas of reef deposition around the blocks where the seas were temporarily shallower. The land mass was by now astride the equator. The bordering seas began to be periodically invaded by deltas formed by rivers flowing from the adjacent higher ground.The sand of the deltas became the Millstone Grits of the Yorkshire Pennines. The climate then becamr humid and the delta areas started to support swamps and tropical rain forests. These deltas changed size and shape frequently and were regularly innundated by the sea. They would eventually form the numerous coal seams of the Coal Measure sandstones. Towards the end of the Carboniferous period the Gondwanalandland mass collided with both North America and Eurasia resulting in the Variscan orogeny.The seas between the land masses were closed up and fold mountain ranges were formed along the closure line in many areas. The area of Britain was uplifted and fault lines developed. There was now only one supercontinent of Pangea..
Yorkshire lay in the arid hinterland of Pangea, between 20° and 30° north of the equator. The rocks of this period are dominated by red desert sandstones. The area which is now beneath the North Sea was a dry area of subsidence which was filled with a great thickness of wind blown sands. Later a marine transgression from the north established a shallow saline sea which produced a thickness of dolomitic limestone and significant evaporite deposits as it dried up. This
Zechstein Seahad completely evaporated by the end of the Permian.At the end of the Permian 95 per cent of animals and plants throughout the world became extinct. During the following Triassic period a hot and mainly arid climate continued but with flash floods from the south which deposited pebble beds in the mainly wind deposited Sherwood sandstones. Another mass extinction at the end of this period saw 80 per cent of species disappear from earth.
At the end of the Triassic the Rhaetic ocean spread its shallow waters over over the deserts to start the Jurassic period.
A shallow epicontinental sea, normally less than 100m deep, spread over the British area during this period. Britain at this time lay between 30° and 40° north of the equator. However, the Pennines, along with parts of Wales and Scotland were probably above sea level for most of the time. During the early and middle Jurassic an area of uplift around Market Weighton affected the way that sediments were deposited causing thinner bands of Jurassic rocks to be formed immediately north and south of the uplifted block.
The main area of Jurassic deposition in Yorkshire was the North York Moors.
*Lower Jurassic At the beginning of the Jurassic era shales, clays and thin limestones and sandstones were deposited in a shallow sea. These deposits are many metres thick and include layers of ironstone of various thicknesses and the rocks from which alum is extracted.
*Middle Jurassic A period of gradual uplift happened when mudstone and sandstone were deposited on a low lying coastal plain crossed by large rivers. Occasionally this land area was inundated by the sea and at these times calcarious rocks containing marine fossils were deposited. These are the Ravenscar group of rocks. The Oxford clay was deposited at the end of this era.
*Upper Jurassic Towards the end of the Jurassic era the land again sank beneath the sea. At first the sea was shallow and calcareous sandstones and limestones were deposited. These are the Corallian rocks of the Tabular hills towards the south of the area. Overlying the Corallian rocks is the Kimmeridge clay which underlies the Vale of Pickering but this is not exposed on the surface. [cite book |title=Geology of the North York Moors |last= Staniforth|first=Alan |authorlink= |coauthors= |year=1993 |publisher=North York Moors National Park Information Service |location=Helmsley |isbn=0 907480 21 7 ]
Marine conditions continued into the Cretaceous period in the Yorkshire area.
The Cretaceous period lasted for 80 million years. It was during this time that the North Atlantic was formed as North America and Europe drifted apart.To the north of the Market Weighton block only small amounts of deposit were laid down in the early part of the Cretaceous.These were the Speeton clays which are 100m thick and lie directly on the Jurassic deposits at Filey Bay.Above this clay is a 14m thick layer of red chalk coloured by impurities washing from the land. Later in the Cretaceous seawater covered the whole of southern Britain and deposited a layer of chalk up to 550m thick forming a great swathe from Flamborough Head to the Channel coast. At the end of the Cretaceous period there was another mass extinction of life with 75 per cent of all life becoming extinct, including the dinosaurs.
Tertiary, the British land mass drifted northwards from 40°N to its present latitude. It was also moved eastwards by the widening of the Atlantic Oceanand there was violent volcanic activity over north west Britain. It was in this period that the Clevelanddyke was formed, originating from volcanic activity near the Scottish island of Mull. The high and low lands of Britain assumed their present relative positions by the late Tertiary period, about 2 million years ago..
Towards the end of the Tertiary period there were repeated cycles of warmer and cooler climate.Each cycle had a period of about 10,000 years and they became more pronounced in the last two million years. Seventeen cycles of cold and
temperateclimate are recognised in Britain with three positive episodes of actual glaciationbeing confirmed. The latest glacial episode destroyed much of the evidence for former ones but traces do exist. On each occasion ice fields formed on the higher land and sent glaciers down the main valleys. There was scouring of material from the valley sides by the glaciers and this was deposited on lower ground as the ice retreated when the climate became warmer. In Yorkshire the higher land of the North York Moors stood proud of the glaciers, the Pennine valleys show classic glacial features and there was abundant deposition in the Vale of York and Holderness as the ice melted.
The Pennines form an
anticlinewhich extends in a north-south direction, consisting of Millstone Gritand the underlying Carboniferous Limestone. The limestone is exposed at the surface to the north of the range in the North PenninesAONB. In the Yorkshire Dalesthis limestone exposure has led to the formation of large underground cave systems and watercourses, known as "gills" and "pots". These potholes are more prevalent on the eastern side and are amongst the largest in England; notable examples are the chasms of Gaping Gill, which is over convert|350|ft|m|0|abbr=on deep and Rowten Pot, which is convert|365|ft|m|0|abbr=on deep. The presence of limestone has also led to some unusual geological formations in the region, such as the limestone pavements of the Yorkshire Pennines. Between the Northern and Southern areas of exposed limestone, between Skipton and the Peak, lies a narrow belt of gritstone country. Here the shales and sandstones of the Millstone Grit form high hills occupied by moors and peat-mosses with the higher ground being uncultivable and barely fit for pastures.
The landscape of the Pennines is generally upland areas of high
moorlandindented by the more fertile valleys of the region's various rivers.
The Yorkshire Coalfield
The coalfield area is underlain by
Coal Measureswhich consist mainly of mudstone with beds of sandstone and many seams of coal.The sandstones resist erosion so they form a recurring pattern of escarpments that stand out from the shallow mudstone floors of the valleys. The major rivers crossing the area have carved broad valleys which have been glaciated and are floored by fertile alluvial deposits.Citation | last =Rayner
first =D H
first2 =J E (Eds.)
title =The Geology and Mineral Resources Of Yorkshire
publisher =Yorkshire Geological Society
The Magnesian Limestone Belt
The Magnesian Limestone belt forms a narrow north- south oriented strip of undulating land on the eastern edge of the Pennines overlooking the Vale of York.The magnesian limestone deposits were laid down in an evaporating inland sea in the Permian period. They are made up of a lower layer of
dolomiteand dolomitic limestones, which form the dominant landscape feature, overlain by red mudstone with gypsum. The upper layer is made of a similar sequence. There are numerous swallow holes caused by the underground dissolution of limestone and gypsum.The sequence can be seen clearly where it is cut by rivers in the Nidd gorge at Knaresborough, the Wharfe valley at Wetherbyand the Don gorge near Doncaster.The York and Escrick glacial moraines swing north and merge north of Wetherby to cover the magnesian limestone with glacial deposits. In the Bedalearea and northwards thes deposits are so extensive as to mask the limestone topography. South of Wetherby there is only a thin layer of glacial deposits overlying the limestone. The soils here are from the limestone and clay deposits and are generally very fertile.
Beneath the drift deposits of the vale of York lie
Triassicsandstone and mudstone, and lower Jurassicmudstone but these are completely masked by the surface deposits. These deposits include glacial till, sand and gravel and both terminal and recessional moraines left by receding ice sheets at the end of the last ice age. The Escrick moraine extends across the vale from west to east and the York moraine, 8 miles further north, forms a similar curving ridge from York eastwards to Sand Hutton. To the north of these ridges are deposits of clay, sand and gravel left by a glacial lake. There are also areas of river alluvium consisting of clay, silt and sand deposited by the main rivers and streams. [cite web
title =The Vale of York
publisher =Natural England
accessdate =2008-02-08 ]
North York Moors
The geology of the North York Moors is dominated by rocks of the
Jurassicage.They were mostly laid down in tropical seas 205 to 142 million years ago. Fluctuations in sea level produced different rock types varying from shales to sandstones and limestones derived from coral. These marine and delta deposited rocks are superbly exposed on the Yorkshire coast from Staithes to Filey. [cite book |title=The Dinosaur Coast |last=Osborn |first=Roger|authorlink= |coauthors=Bowden; Alistair |year=2005 |publisher=North York Moors National Park |location=Helmsley |isbn=0 907480 88 8 ]
Subsequently, about 30 million years ago, the land was uplifted and tilted towards the south by earth movements. The upper layers of rock were eroded away and the older rocks were exposed in places. Because of the tilt the oldest rocks became exposed in the north. These are the bands of shales and ironstones on the northern scarp of the moors and Cleveland Hills. The middle layers form the sandstones of the high moors and the youngest layers of limestone form the tabular hills. In the dales where the rivers have cut through the younger rocks there are also exposures of older shales, ironstone and sandstone. Rosedale is an example of this. [cite book |title=The North York Moors Landscape Heritage |last=Spratt |first=D A |authorlink= |coauthors=Harrison |year=1989|publisher=North York Moors National Park |location=Helmsley, Yorkshire |isbn=0 907480 58 6 ] During the
Quaternaryera, the last 2 million years, the area has experienced a sequence of glaciations. The most recent glaciation, the Devensian, ended about 20,000 years ago. The higher parts of the North York Moors were not covered by the ice sheets but glaciers flowed southwards on either side of the higher land mass.
As the climate became warmer at the end of the ice age the snowfields on the moors began to melt. The meltwater was unable to escape northwards, westwards or eastwards because it was blocked by ice. Huge torrents of water were forced southwards. Water from the Esk valley area flowed southwards gouging out the deep Newtondale valley as it went. Water from the moors formed a vast lake in the area of the Vale of Pickering. Eventually this lake filled its basin and then overflowed at the lowest point which was at Kirkham. Here it cut the steep sided Kirkham gorge. When the glacier finally retreated they left deep deposits of boulder clay and glacial alluvium behind. The boulder clay blocked the eastern end of the Vale of Pickering causing a permanent deviation in the course of the River Derwent. Alluvium from the glaciers covers many areas to the north of the moors and in the Esk valley
Vale of Pickering
The site of the post glacial
Lake Pickering, the vale has a predominantly level topography covered by glacial drift deposits, with some rolling low ground on boulder clay and moraines in the far east. The underlying Jurassic sandstones and mudstones have little direct influence upon the landscape. There are minor outliers of Jurassiclimestone in places at the foot of the Howardian Hillsand the North York Moors, and there is some eroded chalk from the Wolds mixed with sands at the base of the Wolds in the southeast. There are springs associated with calcareous aquifers in places on the periphery of the vale.
The hills are formed from
Cretacious chalk, and make an arc from the Humberestuary west of Kingston upon Hullup to the North Seacoast between Bridlingtonand Scarborough. Here they rise up to form cliffs, most notably at Flamborough, Bempton Cliffsand Filey; Flamborough Headland is designated a Heritage Coast. On the other side of the Humber, the chalk formations continue as the Lincolnshire Wolds.
Most of the area takes the form of an elevated, gently rolling plateau, cut by numerous deep, steep-sided, flat-bottomed valleys of glacial origin. The chalk formation of the hills provides exceptionally good drainage, with the result that most of these valleys are dry; indeed, surface water is quite scarce throughout the Wolds. Typically the valleys are hard to see from above, creating the visual impression that the landscape is much flatter than is actually the case.
Geologically, Holderness is underlain by
CretaceousChalk but in most places it is so deeply buried beneath glacial deposits that it has no influence on the landscape. The landscape is dominated by deposits of till, boulder clays and glacial lake clays. These were deposited during the Devensianglaciation. The glacial deposits form a more or less continuous lowland plain which has some peat filled depressions (known locally as meres) which mark the presence of former lake beds. There are other glacial landscape features such as drumlinmounds, ridges and kettle holes scattered throughout the area.
The well drained glacial deposits provide fertile soils that can support intensive arable cultivation. Fields are generally large and bounded by drainage ditches. There is very little woodland in the area and this leads to a landscape that is essentially rural but very flat and exposed. The coast is subject to rapid marine erosion. [cite web
url = http://www.english-nature.org.uk/Science/natural/profiles%5CnaProfile20.pdf
title = The Plain of Holderness Natural Area Profile
accessdate = 2007-09-16
year = 1977
format = PDF]
During the last ice age, a glacier extended across this area almost to where Doncaster now is. The main glacial front was at Escrick where the Esckrick moraine marks its position. This formed the northern limit of an extensive lake, "Glacial Lake Humber", which was impounded by the blocking of the Humber gap by another ice front. Later the lake was filled with clay sediments which are up to 20 metres thick in some places.These clay sediments are locally overlain by peat deposits forming raised mires. At the base of the peat layers can be found the remains of a buried forest.cite web
title =Humberhead Levels Character Area
publisher =English Nature
accessdate = 2008-01-29 ]
SSSI's in Yorkshire
title =Nature on the Map
publisher =Natural England
accessdate =2008-02-08 ]
* [http://www.bgs.ac.uk/magazine/geology/home.html British Geological Survey]
* [http://www.stratigraphy.org/geowhen/region_Europe.html GeoWhen Database]
* [http://www.dinocoast.org.uk/pdf/forge_valley_geology_trail.pdf Forge Valley Geological Trail leaflet]
* [http://www.natureonthemap.org.uk/map.aspx?m=geology Geological Sites - Nature on the Map]
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