https://earthwise.bgs.ac.uk/index.php?title=Holocene_of_Wales&feed=atom&action=historyHolocene of Wales - Revision history2024-03-28T14:01:34ZRevision history for this page on the wikiMediaWiki 1.41.0https://earthwise.bgs.ac.uk/index.php?title=Holocene_of_Wales&diff=27819&oldid=prevDbk: 1 revision imported2016-05-05T09:53:13Z<p>1 revision imported</p>
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</td></tr></table>Dbkhttps://earthwise.bgs.ac.uk/index.php?title=Holocene_of_Wales&diff=27458&oldid=prevAjhil at 09:59, 14 April 20162016-04-14T09:59:56Z<p></p>
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<td colspan="2" style="background-color: #fff; color: #202122; text-align: center;">Revision as of 09:59, 14 April 2016</td>
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<tr><td class="diff-marker" data-marker="−"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #ffe49c; vertical-align: top; white-space: pre-wrap;"><div><del style="font-weight: bold; text-decoration: none;">__notoc__</del></div></td><td colspan="2" class="diff-side-added"></td></tr>
<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>'''From: Howells, M F. 2007. [[British regional geology: Wales|British regional geology: Wales]]. Keyworth, Nottingham: British Geological Survey.'''</div></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>'''From: Howells, M F. 2007. [[British regional geology: Wales|British regional geology: Wales]]. Keyworth, Nottingham: British Geological Survey.'''</div></td></tr>
<tr><td colspan="2" class="diff-side-deleted"></td><td class="diff-marker" data-marker="+"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #a3d3ff; vertical-align: top; white-space: pre-wrap;"><div><ins style="font-weight: bold; text-decoration: none;"></ins></div></td></tr>
<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>[[File:P916214.jpg|thumbnail|Superficial deposits south of the Dyfi estuary (adapted from Godwin, 1943). a Map of Borth Bog b Cross-section, Borth Bog and Dyfi estuary. P916214.]]</div></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>[[File:P916214.jpg|thumbnail|Superficial deposits south of the Dyfi estuary (adapted from Godwin, 1943). a Map of Borth Bog b Cross-section, Borth Bog and Dyfi estuary. P916214.]]</div></td></tr>
<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>[[File:P916215.jpg|thumbnail|Licensed aggregate dredging locations in the Bristol Channel (after James et al., 2005; for current holdings see https://www.thecrownestate.co.uk). P916215.]]</div></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>[[File:P916215.jpg|thumbnail|Licensed aggregate dredging locations in the Bristol Channel (after James et al., 2005; for current holdings see https://www.thecrownestate.co.uk). P916215.]]</div></td></tr>
<tr><td class="diff-marker" data-marker="−"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #ffe49c; vertical-align: top; white-space: pre-wrap;"><div><del style="font-weight: bold; text-decoration: none;">At the beginning of Holocene times, some 10 000 years before present (BP), the climatic amelioration that had been briefly interrupted during the Loch Lomond Stadial (Younger Dryas) continued. A temperate deciduous mixed forest, with regional variations, developed across Wales, particularly below 500 m OD. The forest was progressively modified by increasing human occupation, but the main clearance did not occur until early Roman times, some 2000 years ago.</del></div></td><td colspan="2" class="diff-side-added"></td></tr>
<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><br></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><br></td></tr>
<tr><td class="diff-marker" data-marker="−"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #ffe49c; vertical-align: top; white-space: pre-wrap;"><div>At the maximum growth of the Late-Devensian ice sheet, about 21 000 BP, sea level was at its lowest, approximately 100 m below present OD. From Late Devensian into Holocene times, sea level changes were induced by melting of the ice sheet and isostatic rebound, and between 18 000 and 15 000 years BP there was a temporary land bridge between Wales and Ireland. Current sea level was attained about 5000 years ago, although movements have continued. The principal postglacial deposits, apart from the extensive tracts of river alluvium, occur in the vicinity of the coast where, locally, swathes of blown sand impede drainage and separate large tracts of alluvium from the shoreline. Such relationships are common, but the most notable are probably those between Porthcawl and Swansea, east of Pendine, at Ynyslas [[Media:P916214.jpg|(P916214)]] near Borth, at Morfa Harlech, at Newborough Warren on Anglesey and at the mouth of the Vale of Clwyd between Abergele and Prestatyn. In Cardigan Bay, the beach material is mainly transported northwards and in many instances, for example at Ynyslas, ridges of beach gravels form a foundation for the dunes. At Ynyslas, the dunes separate the submerged forest and associated beds on the foreshore from Borth Bog to the east; the site has been extensively studied and provides an important record of coastal and environmental changes over the past 7000 years. The submerged forest beds are most commonly exposed at or below high-water mark in a setting where they could not be formed at the present time; tree bases in growth positions are common. In the excavation for the major dock and shoreline installations in Glamorgan, postglacial peat beds were particularly well exposed, down to 30 m below current sea level at Barry. The peat beds are interbedded with marine and estuarine clays, which contain a characteristic fauna that indicates some pauses in the gradual drowning. At Crymlyn Bog (Swansea), the youngest peat, up to 12 m thick, at and above current sea level, was probably formed some 3000 years ago. Associated with the plants in the peat beds are insect remains and mammal bones, particularly of deer species that no longer frequent the Welsh countryside. In the bays of south Wales, the peat beds have yielded flint artefacts, indicating that the forests were temporarily dry enough to encourage Neolithic and early Bronze Age human habitation.</div></td><td class="diff-marker" data-marker="+"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #a3d3ff; vertical-align: top; white-space: pre-wrap;"><div><ins style="font-weight: bold; text-decoration: none;">At the beginning of Holocene times, some 10&nbsp;000 years before present (BP), the climatic amelioration that had been briefly interrupted during the Loch Lomond Stadial (Younger Dryas) continued. A temperate deciduous mixed forest, with regional variations, developed across Wales, particularly below 500&nbsp;m&nbsp;OD. The forest was progressively modified by increasing human occupation, but the main clearance did not occur until early Roman times, some 2000 years ago.</ins></div></td></tr>
<tr><td colspan="2" class="diff-side-deleted"></td><td class="diff-marker" data-marker="+"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #a3d3ff; vertical-align: top; white-space: pre-wrap;"><div> </div></td></tr>
<tr><td colspan="2" class="diff-side-deleted"></td><td class="diff-marker" data-marker="+"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #a3d3ff; vertical-align: top; white-space: pre-wrap;"><div>At the maximum growth of the Late-Devensian ice sheet, about 21<ins style="font-weight: bold; text-decoration: none;">&nbsp;</ins>000 BP, sea level was at its lowest, approximately 100 m below present OD. From Late Devensian into Holocene times, sea level changes were induced by melting of the ice sheet and isostatic rebound, and between 18<ins style="font-weight: bold; text-decoration: none;">&nbsp;</ins>000 and 15<ins style="font-weight: bold; text-decoration: none;">&nbsp;</ins>000 years BP there was a temporary land bridge between Wales and Ireland. Current sea level was attained about 5000 years ago, although movements have continued. The principal postglacial deposits, apart from the extensive tracts of river alluvium, occur in the vicinity of the coast where, locally, swathes of blown sand impede drainage and separate large tracts of alluvium from the shoreline. Such relationships are common, but the most notable are probably those between Porthcawl and Swansea, east of Pendine, at Ynyslas [[Media:P916214.jpg|(P916214)]] near Borth, at Morfa Harlech, at Newborough Warren on Anglesey and at the mouth of the Vale of Clwyd between Abergele and Prestatyn. In Cardigan Bay, the beach material is mainly transported northwards and in many instances, for example at Ynyslas, ridges of beach gravels form a foundation for the dunes. At Ynyslas, the dunes separate the submerged forest and associated beds on the foreshore from Borth Bog to the east; the site has been extensively studied and provides an important record of coastal and environmental changes over the past 7000 years. The submerged forest beds are most commonly exposed at or below high-water mark in a setting where they could not be formed at the present time; tree bases in growth positions are common. In the excavation for the major dock and shoreline installations in Glamorgan, postglacial peat beds were particularly well exposed, down to 30<ins style="font-weight: bold; text-decoration: none;">&nbsp;</ins>m below current sea level at Barry. The peat beds are interbedded with marine and estuarine clays, which contain a characteristic fauna that indicates some pauses in the gradual drowning. At Crymlyn Bog (Swansea), the youngest peat, up to 12 m thick, at and above current sea level, was probably formed some 3000 years ago. Associated with the plants in the peat beds are insect remains and mammal bones, particularly of deer species that no longer frequent the Welsh countryside. In the bays of south Wales, the peat beds have yielded flint artefacts, indicating that the forests were temporarily dry enough to encourage Neolithic and early Bronze Age human habitation<ins style="font-weight: bold; text-decoration: none;">.</ins></div></td></tr>
<tr><td colspan="2" class="diff-side-deleted"></td><td class="diff-marker" data-marker="+"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #a3d3ff; vertical-align: top; white-space: pre-wrap;"><div> </div></td></tr>
<tr><td colspan="2" class="diff-side-deleted"></td><td class="diff-marker" data-marker="+"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #a3d3ff; vertical-align: top; white-space: pre-wrap;"><div><ins style="font-weight: bold; text-decoration: none;">Inland, solifluction processes have been active on hillslopes, and landslips are a prominent feature, and potential hazard, particularly within the deeply dissected valleys across the coalfield in south Wales. The postglacial sea-level changes and variations in the drainage patterns caused extensive terracing of the river alluvium. Most of the gentle upland slopes in Wales are covered with thin peat, which thickens locally in depressions, for example on Plynlimon. One of the most distinctive, romantic and probably thickest swathes of peat is that across Migneint, west of Arenig Fawr, which includes Llyn Conwy close to the source of the Conwy river. The River Teifi, near Tregaron, flows through one of the largest valley peat bogs (Cors Caron), which formed in the floor of the moraine-dammed lake; the oldest peat has been dated at about 10&nbsp;000 years BP, dating the melting of the ice a little earlier</ins>.</div></td></tr>
<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><br></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><br></td></tr>
<tr><td class="diff-marker" data-marker="−"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #ffe49c; vertical-align: top; white-space: pre-wrap;"><div><del style="font-weight: bold; text-decoration: none;">Inland</del>, <del style="font-weight: bold; text-decoration: none;">solifluction processes have been active on hillslopes, and landslips are a prominent feature, and potential hazard, particularly within the deeply dissected valleys across the coalfield in south Wales. The postglacial </del>sea-<del style="font-weight: bold; text-decoration: none;">level changes </del>and <del style="font-weight: bold; text-decoration: none;">variations </del>in the <del style="font-weight: bold; text-decoration: none;">drainage patterns caused extensive terracing of the river alluvium</del>. <del style="font-weight: bold; text-decoration: none;">Most of </del>the <del style="font-weight: bold; text-decoration: none;">gentle upland slopes in Wales are covered with thin peat</del>, which <del style="font-weight: bold; text-decoration: none;">thickens locally in depressions, for example on Plynlimon. One of the most distinctive</del>, <del style="font-weight: bold; text-decoration: none;">romantic </del>and <del style="font-weight: bold; text-decoration: none;">probably thickest swathes of peat </del>is that <del style="font-weight: bold; text-decoration: none;">across Migneint</del>, <del style="font-weight: bold; text-decoration: none;">west of Arenig Fawr</del>, <del style="font-weight: bold; text-decoration: none;">which includes Llyn Conwy close </del>to the <del style="font-weight: bold; text-decoration: none;">source </del>of <del style="font-weight: bold; text-decoration: none;">the Conwy river. The River Teifi, near Tregaron</del>, <del style="font-weight: bold; text-decoration: none;">flows through one of </del>the <del style="font-weight: bold; text-decoration: none;">largest valley peat bogs (Cors Caron), </del>which <del style="font-weight: bold; text-decoration: none;">formed in the floor </del>of <del style="font-weight: bold; text-decoration: none;">the moraine-dammed lake; the oldest peat has </del>been <del style="font-weight: bold; text-decoration: none;">dated at about 10 000 years BP, dating </del>the <del style="font-weight: bold; text-decoration: none;">melting </del>of the <del style="font-weight: bold; text-decoration: none;">ice a little earlier</del>.</div></td><td class="diff-marker" data-marker="+"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #a3d3ff; vertical-align: top; white-space: pre-wrap;"><div><ins style="font-weight: bold; text-decoration: none;">Offshore</ins>, sea-<ins style="font-weight: bold; text-decoration: none;">bed sediments can be broadly divided into mobile sediments </ins>and <ins style="font-weight: bold; text-decoration: none;">gravelly lag deposits, which are actively involved </ins>in the <ins style="font-weight: bold; text-decoration: none;">current marine process</ins>. <ins style="font-weight: bold; text-decoration: none;">Where mobile sediments are absent, </ins>the <ins style="font-weight: bold; text-decoration: none;">sea bed is mantled by a shelly or pebbly gravel and coarse sand deposit</ins>, which <ins style="font-weight: bold; text-decoration: none;">undergoes constant winnowing and reworking</ins>, and <ins style="font-weight: bold; text-decoration: none;">it </ins>is <ins style="font-weight: bold; text-decoration: none;">this process </ins>that <ins style="font-weight: bold; text-decoration: none;">forms the mobile layer. In both St George’s Channel and Cardigan Bay</ins>, <ins style="font-weight: bold; text-decoration: none;">the gravelly deposits pass laterally into giant sand waves</ins>, <ins style="font-weight: bold; text-decoration: none;">up </ins>to <ins style="font-weight: bold; text-decoration: none;">40&nbsp;m high, and tidal sand ridges. In </ins>the <ins style="font-weight: bold; text-decoration: none;">central part </ins>of <ins style="font-weight: bold; text-decoration: none;">Tremadog Bay</ins>, the <ins style="font-weight: bold; text-decoration: none;">sand passes laterally into mud in </ins>which <ins style="font-weight: bold; text-decoration: none;">considerable volumes </ins>of <ins style="font-weight: bold; text-decoration: none;">gas have </ins>been <ins style="font-weight: bold; text-decoration: none;">recorded. Similar sand waves are well developed to </ins>the <ins style="font-weight: bold; text-decoration: none;">south and west </ins>of <ins style="font-weight: bold; text-decoration: none;">Gower in </ins>the <ins style="font-weight: bold; text-decoration: none;">Bristol Channel</ins>.</div></td></tr>
<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><br></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><br></td></tr>
<tr><td class="diff-marker" data-marker="−"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #ffe49c; vertical-align: top; white-space: pre-wrap;"><div><del style="font-weight: bold; text-decoration: none;">Offshore</del>, <del style="font-weight: bold; text-decoration: none;">sea-bed sediments can be broadly divided into mobile sediments </del>and <del style="font-weight: bold; text-decoration: none;">gravelly lag deposits</del>, which <del style="font-weight: bold; text-decoration: none;">are actively involved </del>in the <del style="font-weight: bold; text-decoration: none;">current marine process</del>. <del style="font-weight: bold; text-decoration: none;">Where mobile sediments are absent, </del>the <del style="font-weight: bold; text-decoration: none;">sea bed is mantled by a shelly or pebbly gravel and coarse </del>sand <del style="font-weight: bold; text-decoration: none;">deposit</del>, <del style="font-weight: bold; text-decoration: none;">which undergoes constant winnowing and reworking</del>, <del style="font-weight: bold; text-decoration: none;">and it </del>is this <del style="font-weight: bold; text-decoration: none;">process </del>that <del style="font-weight: bold; text-decoration: none;">forms </del>the <del style="font-weight: bold; text-decoration: none;">mobile layer</del>. <del style="font-weight: bold; text-decoration: none;">In both St George’s Channel </del>and <del style="font-weight: bold; text-decoration: none;">Cardigan Bay</del>, the <del style="font-weight: bold; text-decoration: none;">gravelly deposits pass laterally into giant sand waves</del>, up to <del style="font-weight: bold; text-decoration: none;">40 </del>m <del style="font-weight: bold; text-decoration: none;">high</del>, <del style="font-weight: bold; text-decoration: none;">and tidal sand ridges. In </del>the <del style="font-weight: bold; text-decoration: none;">central part </del>of <del style="font-weight: bold; text-decoration: none;">Tremadog Bay</del>, the <del style="font-weight: bold; text-decoration: none;">sand passes laterally into mud in which considerable volumes of gas have been recorded. Similar sand waves are well developed </del>to the <del style="font-weight: bold; text-decoration: none;">south and west </del>of <del style="font-weight: bold; text-decoration: none;">Gower in </del>the <del style="font-weight: bold; text-decoration: none;">Bristol Channel</del>.</div></td><td class="diff-marker" data-marker="+"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #a3d3ff; vertical-align: top; white-space: pre-wrap;"><div><ins style="font-weight: bold; text-decoration: none;">These offshore</ins>, <ins style="font-weight: bold; text-decoration: none;">unconsolidated sands </ins>and <ins style="font-weight: bold; text-decoration: none;">gravels are an important economic resource</ins>, which <ins style="font-weight: bold; text-decoration: none;">have been dredged </ins>in the <ins style="font-weight: bold; text-decoration: none;">outer Severn estuary [[Media:P916215</ins>.<ins style="font-weight: bold; text-decoration: none;">jpg|(P916215)]] and in </ins>the <ins style="font-weight: bold; text-decoration: none;">linear tidal </ins>sand <ins style="font-weight: bold; text-decoration: none;">ridge</ins>, <ins style="font-weight: bold; text-decoration: none;">Nash Sand</ins>, <ins style="font-weight: bold; text-decoration: none;">close to Porthcawl. It </ins>is <ins style="font-weight: bold; text-decoration: none;">in </ins>this <ins style="font-weight: bold; text-decoration: none;">area </ins>that the <ins style="font-weight: bold; text-decoration: none;">proposed Severn Barrage is likely to be sited; the idea for a barrage was originally put forward by Thomas Telford in the early 19th century</ins>. <ins style="font-weight: bold; text-decoration: none;">There have been two detailed investigations, an ‘outer’ location between Breaksea Point </ins>and <ins style="font-weight: bold; text-decoration: none;">Warren Point</ins>, <ins style="font-weight: bold; text-decoration: none;">and an ‘inner’ location between Lavernock Point and Brean Down. Sediment along </ins>the <ins style="font-weight: bold; text-decoration: none;">line of the inner location is less than 1&nbsp;m thick</ins>, <ins style="font-weight: bold; text-decoration: none;">except at sandbanks where it is </ins>up to <ins style="font-weight: bold; text-decoration: none;">10&nbsp;</ins>m <ins style="font-weight: bold; text-decoration: none;">in places. The superficial sediments are underlain variously by Carboniferous limestone</ins>, <ins style="font-weight: bold; text-decoration: none;">in </ins>the <ins style="font-weight: bold; text-decoration: none;">vicinity </ins>of <ins style="font-weight: bold; text-decoration: none;">the Holm islands</ins>, <ins style="font-weight: bold; text-decoration: none;">Triassic mudstone, and Lower Jurassic limestone and mudstone. The deep-water channel between </ins>the <ins style="font-weight: bold; text-decoration: none;">Holm islands determined this </ins>to <ins style="font-weight: bold; text-decoration: none;">be </ins>the <ins style="font-weight: bold; text-decoration: none;">prospective site </ins>of the <ins style="font-weight: bold; text-decoration: none;">turbines</ins>.</div></td></tr>
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<tr><td class="diff-marker" data-marker="−"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #ffe49c; vertical-align: top; white-space: pre-wrap;"><div><del style="font-weight: bold; text-decoration: none;">These offshore, unconsolidated sands and gravels are an important economic resource, which have been dredged in the outer Severn estuary [[Media:P916215.jpg|(P916215)]] and in the linear tidal sand ridge, Nash Sand, close to Porthcawl. It is in this area that the proposed Severn Barrage is likely to be sited; the idea for a barrage was originally put forward by Thomas Telford in the early 19th century. There have been two detailed investigations, an ‘outer’ location between Breaksea Point and Warren Point, and an ‘inner’ location between Lavernock Point and Brean Down. Sediment along the line of the inner location is less than 1 m thick, except at sandbanks where it is up to 10 m in places. The superficial sediments are underlain variously by Carboniferous limestone, in the vicinity of the Holm islands, Triassic mudstone, and Lower Jurassic limestone and mudstone. The deep-water channel between the Holm islands determined this to be the prospective site of the turbines.</del></div></td><td colspan="2" class="diff-side-added"></td></tr>
<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>== Bibliography ==</div></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>== Bibliography ==</div></td></tr>
<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>BEVINS, R E, HORAK, J M, EVANS, A D, and MORGAN, R. 1996. Palaeogene dyke swarm, north-west Wales: evidence for Cenozoic sinistral fault movement. ''Journal of the'' ''Geological Society of London'', Vol. 153, 177–180.</div></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>BEVINS, R E, HORAK, J M, EVANS, A D, and MORGAN, R. 1996. Palaeogene dyke swarm, north-west Wales: evidence for Cenozoic sinistral fault movement. ''Journal of the'' ''Geological Society of London'', Vol. 153, 177–180.</div></td></tr>
</table>Ajhilhttps://earthwise.bgs.ac.uk/index.php?title=Holocene_of_Wales&diff=27818&oldid=prevDbk at 08:47, 14 April 20162016-04-14T08:47:36Z<p></p>
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<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>'''From: Howells, M F. 2007. [[British regional geology: Wales|British regional geology: Wales]]. Keyworth, Nottingham: British Geological Survey.'''</div></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>'''From: Howells, M F. 2007. [[British regional geology: Wales|British regional geology: Wales]]. Keyworth, Nottingham: British Geological Survey.'''</div></td></tr>
<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>[[File:P916214.jpg|thumbnail|Superficial deposits south of the Dyfi estuary (adapted from Godwin, 1943). a Map of Borth Bog b Cross-section, Borth Bog and Dyfi estuary. P916214.]]</div></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>[[File:P916214.jpg|thumbnail|Superficial deposits south of the Dyfi estuary (adapted from Godwin, 1943). a Map of Borth Bog b Cross-section, Borth Bog and Dyfi estuary. P916214.]]</div></td></tr>
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<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>JOHN, B S. 1970. Pembrokeshire. 267–314 in ''The glaciations of Wales and adjoining'' ''regions''. LEWIS, C A (editor). (London: Longman.)</div></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>JOHN, B S. 1970. Pembrokeshire. 267–314 in ''The glaciations of Wales and adjoining'' ''regions''. LEWIS, C A (editor). (London: Longman.)</div></td></tr>
<tr><td class="diff-marker" data-marker="−"></td><td style="color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #ffe49c; vertical-align: top; white-space: pre-wrap;"><div><del style="font-weight: bold; text-decoration: none;"></del></div></td><td colspan="2" class="diff-side-added"></td></tr>
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</table>Dbkhttps://earthwise.bgs.ac.uk/index.php?title=Holocene_of_Wales&diff=27375&oldid=prevAjhil at 08:05, 14 April 20162016-04-14T08:05:25Z<p></p>
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<tr><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>JOHN, B S. 1970. Pembrokeshire. 267–314 in ''The glaciations of Wales and adjoining'' ''regions''. LEWIS, C A (editor). (London: Longman.)</div></td><td class="diff-marker"></td><td style="background-color: #f8f9fa; color: #202122; font-size: 88%; border-style: solid; border-width: 1px 1px 1px 4px; border-radius: 0.33em; border-color: #eaecf0; vertical-align: top; white-space: pre-wrap;"><div>JOHN, B S. 1970. Pembrokeshire. 267–314 in ''The glaciations of Wales and adjoining'' ''regions''. LEWIS, C A (editor). (London: Longman.)</div></td></tr>
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</table>Ajhilhttps://earthwise.bgs.ac.uk/index.php?title=Holocene_of_Wales&diff=27255&oldid=prevDbk: 1 revision imported2016-04-14T06:37:07Z<p>1 revision imported</p>
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</td></tr></table>Dbkhttps://earthwise.bgs.ac.uk/index.php?title=Holocene_of_Wales&diff=27254&oldid=prevBobMcIntosh at 19:43, 7 March 20162016-03-07T19:43:28Z<p></p>
<p><b>New page</b></p><div>'''From: Howells, M F. 2007. [[British regional geology: Wales|British regional geology: Wales]]. Keyworth, Nottingham: British Geological Survey.'''<br />
[[File:P916214.jpg|thumbnail|Superficial deposits south of the Dyfi estuary (adapted from Godwin, 1943). a Map of Borth Bog b Cross-section, Borth Bog and Dyfi estuary. P916214.]]<br />
[[File:P916215.jpg|thumbnail|Licensed aggregate dredging locations in the Bristol Channel (after James et al., 2005; for current holdings see https://www.thecrownestate.co.uk). P916215.]]<br />
At the beginning of Holocene times, some 10 000 years before present (BP), the climatic amelioration that had been briefly interrupted during the Loch Lomond Stadial (Younger Dryas) continued. A temperate deciduous mixed forest, with regional variations, developed across Wales, particularly below 500 m OD. The forest was progressively modified by increasing human occupation, but the main clearance did not occur until early Roman times, some 2000 years ago.<br />
<br />
At the maximum growth of the Late-Devensian ice sheet, about 21 000 BP, sea level was at its lowest, approximately 100 m below present OD. From Late Devensian into Holocene times, sea level changes were induced by melting of the ice sheet and isostatic rebound, and between 18 000 and 15 000 years BP there was a temporary land bridge between Wales and Ireland. Current sea level was attained about 5000 years ago, although movements have continued. The principal postglacial deposits, apart from the extensive tracts of river alluvium, occur in the vicinity of the coast where, locally, swathes of blown sand impede drainage and separate large tracts of alluvium from the shoreline. Such relationships are common, but the most notable are probably those between Porthcawl and Swansea, east of Pendine, at Ynyslas [[Media:P916214.jpg|(P916214)]] near Borth, at Morfa Harlech, at Newborough Warren on Anglesey and at the mouth of the Vale of Clwyd between Abergele and Prestatyn. In Cardigan Bay, the beach material is mainly transported northwards and in many instances, for example at Ynyslas, ridges of beach gravels form a foundation for the dunes. At Ynyslas, the dunes separate the submerged forest and associated beds on the foreshore from Borth Bog to the east; the site has been extensively studied and provides an important record of coastal and environmental changes over the past 7000 years. The submerged forest beds are most commonly exposed at or below high-water mark in a setting where they could not be formed at the present time; tree bases in growth positions are common. In the excavation for the major dock and shoreline installations in Glamorgan, postglacial peat beds were particularly well exposed, down to 30 m below current sea level at Barry. The peat beds are interbedded with marine and estuarine clays, which contain a characteristic fauna that indicates some pauses in the gradual drowning. At Crymlyn Bog (Swansea), the youngest peat, up to 12 m thick, at and above current sea level, was probably formed some 3000 years ago. Associated with the plants in the peat beds are insect remains and mammal bones, particularly of deer species that no longer frequent the Welsh countryside. In the bays of south Wales, the peat beds have yielded flint artefacts, indicating that the forests were temporarily dry enough to encourage Neolithic and early Bronze Age human habitation.<br />
<br />
Inland, solifluction processes have been active on hillslopes, and landslips are a prominent feature, and potential hazard, particularly within the deeply dissected valleys across the coalfield in south Wales. The postglacial sea-level changes and variations in the drainage patterns caused extensive terracing of the river alluvium. Most of the gentle upland slopes in Wales are covered with thin peat, which thickens locally in depressions, for example on Plynlimon. One of the most distinctive, romantic and probably thickest swathes of peat is that across Migneint, west of Arenig Fawr, which includes Llyn Conwy close to the source of the Conwy river. The River Teifi, near Tregaron, flows through one of the largest valley peat bogs (Cors Caron), which formed in the floor of the moraine-dammed lake; the oldest peat has been dated at about 10 000 years BP, dating the melting of the ice a little earlier.<br />
<br />
Offshore, sea-bed sediments can be broadly divided into mobile sediments and gravelly lag deposits, which are actively involved in the current marine process. Where mobile sediments are absent, the sea bed is mantled by a shelly or pebbly gravel and coarse sand deposit, which undergoes constant winnowing and reworking, and it is this process that forms the mobile layer. In both St George’s Channel and Cardigan Bay, the gravelly deposits pass laterally into giant sand waves, up to 40 m high, and tidal sand ridges. In the central part of Tremadog Bay, the sand passes laterally into mud in which considerable volumes of gas have been recorded. Similar sand waves are well developed to the south and west of Gower in the Bristol Channel.<br />
<br />
These offshore, unconsolidated sands and gravels are an important economic resource, which have been dredged in the outer Severn estuary [[Media:P916215.jpg|(P916215)]] and in the linear tidal sand ridge, Nash Sand, close to Porthcawl. It is in this area that the proposed Severn Barrage is likely to be sited; the idea for a barrage was originally put forward by Thomas Telford in the early 19th century. There have been two detailed investigations, an ‘outer’ location between Breaksea Point and Warren Point, and an ‘inner’ location between Lavernock Point and Brean Down. Sediment along the line of the inner location is less than 1 m thick, except at sandbanks where it is up to 10 m in places. The superficial sediments are underlain variously by Carboniferous limestone, in the vicinity of the Holm islands, Triassic mudstone, and Lower Jurassic limestone and mudstone. The deep-water channel between the Holm islands determined this to be the prospective site of the turbines.<br />
== Bibliography ==<br />
BEVINS, R E, HORAK, J M, EVANS, A D, and MORGAN, R. 1996. Palaeogene dyke swarm, north-west Wales: evidence for Cenozoic sinistral fault movement. ''Journal of the'' ''Geological Society of London'', Vol. 153, 177–180.<br />
<br />
BROWN, E H. 1960. ''The relief and drainage of Wales.'' (Cardiff: University of Wales.)<br />
<br />
CAMPBELL, S, and BOWEN, D Q (editors). 1989. ''Quaternary of Wales''. ''Geological'' ''Conservation Review Series, ''No. 2. (Peterborough: Nature Conservancy Council.)<br />
<br />
GEORGE, T N. 1974. The Cenozoic evolution of Wales. 341–371 in ''The Upper Palaeozoic'' ''and post-Palaeozoic rocks of Wales''. OWEN, T R (editor). (Cardiff: University of Wales Press.)<br />
<br />
GODWIN, H. 1943. Coastal peat beds of the British Isles and North Sea. ''Journal of'' ''Ecology'', Vol. 31, 199–247.<br />
<br />
JOHN, B S. 1970. Pembrokeshire. 267–314 in ''The glaciations of Wales and adjoining'' ''regions''. LEWIS, C A (editor). (London: Longman.)<br />
[[Category:Wales]]</div>BobMcIntosh