https://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&feed=atom&action=historyDalradian rocks of the Loch Leven area - an excursion - Revision history2024-03-28T18:43:33ZRevision history for this page on the wikiMediaWiki 1.41.0https://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=23003&oldid=prevScotfot at 23:46, 30 October 20152015-10-30T23:46:36Z<p></p>
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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;">From: </del>Roberts, J.L. and Treagus, J.E. 1977. 7: [[Dalradian rocks of the South-West Highlands. Scottish Journal of Geology Volume 13 Part 2]] p.165-184'''</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>'''Roberts, J.L. and Treagus, J.E. 1977. 7: <ins style="font-weight: bold; text-decoration: none;">Dalradian rocks of the South-West Highlands. </ins>[[Dalradian rocks of the South-West Highlands. Scottish Journal of Geology Volume 13 Part 2<ins style="font-weight: bold; text-decoration: none;">|Scottish Journal of Geology Volume 13 Part 2. 1977</ins>]] <ins style="font-weight: bold; text-decoration: none;"> </ins>p.165-184'''</div></td></tr>
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</table>Scotfothttps://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=22986&oldid=prevScotfot at 23:25, 30 October 20152015-10-30T23:25:07Z<p></p>
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</table>Scotfothttps://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=22985&oldid=prevScotfot at 23:24, 30 October 20152015-10-30T23:24:24Z<p></p>
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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>'''From: Roberts, J.L. and Treagus, J.E. 1977. 7: [[<del style="font-weight: bold; text-decoration: none;">The </del>Dalradian rocks of the <del style="font-weight: bold; text-decoration: none;">Loch Leven area</del>. Scottish Journal of Geology <del style="font-weight: bold; text-decoration: none;">v </del>13<del style="font-weight: bold; text-decoration: none;">. </del>Part 2]] p.165-184'''</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>'''From: Roberts, J.L. and Treagus, J.E. 1977. 7: [[Dalradian rocks of the <ins style="font-weight: bold; text-decoration: none;">South-West Highlands</ins>. Scottish Journal of Geology <ins style="font-weight: bold; text-decoration: none;">Volume </ins>13 Part 2]] p.165-184'''</div></td></tr>
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</table>Scotfothttps://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=22984&oldid=prevScotfot at 23:23, 30 October 20152015-10-30T23:23:30Z<p></p>
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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>'''From: Roberts, J.L. and Treagus, J.E. 1977. 7: The Dalradian rocks of the Loch Leven area. Scottish Journal of Geology v 13. p.165-184'''</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>'''From: Roberts, J.L. and Treagus, J.E. 1977. 7: <ins style="font-weight: bold; text-decoration: none;">[[</ins>The Dalradian rocks of the Loch Leven area. Scottish Journal of Geology v 13. <ins style="font-weight: bold; text-decoration: none;">Part 2]] </ins>p.165-184'''</div></td></tr>
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</table>Scotfothttps://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=22983&oldid=prevScotfot: /* Locality 25 */2015-10-30T23:15:47Z<p><span dir="auto"><span class="autocomment">Locality 25</span></span></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>The object of this excursion is to examine the evidence that the Stob Ban Synform is an F2 fold which affects an earlier F<sub>1</sub> fold as represented by the Ballachulish Syncline. It was this evidence which Bailey (1960) used as the foundation for his interpretation of the Ballachulish area as a whole. The excursion involves 4 or 5 miles of walking over rough ground and an ascent of some 2500 feet. It may be combined with the ascent of Stob Ban to provide a full day. Starting from Fort William, follow the road up Glen Nevis as far as Archriabhach, where cars may be parked. The party should then walk south up the valley of the Allt a' Choire Dheirg to the junction of this river with the burn which drains the north-west corrie of Stob Ban. Following this burn upstream, the contact of the Mullach nan Coirean Granite can be located near the ruins of an old sheiling at (NN 148 664).</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>The object of this excursion is to examine the evidence that the Stob Ban Synform is an F2 fold which affects an earlier F<sub>1</sub> fold as represented by the Ballachulish Syncline. It was this evidence which Bailey (1960) used as the foundation for his interpretation of the Ballachulish area as a whole. The excursion involves 4 or 5 miles of walking over rough ground and an ascent of some 2500 feet. It may be combined with the ascent of Stob Ban to provide a full day. Starting from Fort William, follow the road up Glen Nevis as far as Archriabhach, where cars may be parked. The party should then walk south up the valley of the Allt a' Choire Dheirg to the junction of this river with the burn which drains the north-west corrie of Stob Ban. Following this burn upstream, the contact of the Mullach nan Coirean Granite can be located near the ruins of an old sheiling at (NN 148 664).</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>=== Locality 25 ===</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>=== Locality 25<ins style="font-weight: bold; text-decoration: none;">. Pelitic hornfels in contact with the Mullach nan Coirean Granite and Ballachulish Syncline </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>Dark pelitic hornfels is present in contact with the rocks of the Mullach nan Coirean Granite. These rocks are followed upstream to the SE by pale-green calc-silicate rocks representing the Ballachulish Limestone. These rocks are succeeded to the SE. by the Ballachulish Slates, exposed about halfway up the gorge below the corrie. These rocks are followed in turn by another band of pale-green calc-silicate rocks, representing the Ballachulish Limestone, beyond which the Leven Schists are exposed as a pelitic hornfels at the lip of the corrie. Throughout this section, abundant F<sub>2</sub> folds with steeply dipping axial planes are developed, plunging SW and verging NW. The Ballachulish Slates occupy the core of the Ballachulish Syncline on the NW limb of the Stob Ban Synform, and are flanked by Ballachulish Limestone and Leven Schists, as successively older groups on the limbs of the Ballachulish Syncline.</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>Dark pelitic hornfels is present in contact with the rocks of the Mullach nan Coirean Granite. These rocks are followed upstream to the SE by pale-green calc-silicate rocks representing the Ballachulish Limestone. These rocks are succeeded to the SE. by the Ballachulish Slates, exposed about halfway up the gorge below the corrie. These rocks are followed in turn by another band of pale-green calc-silicate rocks, representing the Ballachulish Limestone, beyond which the Leven Schists are exposed as a pelitic hornfels at the lip of the corrie. Throughout this section, abundant F<sub>2</sub> folds with steeply dipping axial planes are developed, plunging SW and verging NW. The Ballachulish Slates occupy the core of the Ballachulish Syncline on the NW limb of the Stob Ban Synform, and are flanked by Ballachulish Limestone and Leven Schists, as successively older groups on the limbs of the Ballachulish Syncline.</div></td></tr>
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</table>Scotfothttps://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=22982&oldid=prevScotfot: /* Locality 25. Summit of Tom Meadhoin */2015-10-30T23:11:02Z<p><span dir="auto"><span class="autocomment">Locality 25. Summit of Tom Meadhoin</span></span></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>Follow the thin band of quartzite south-west until the nose of the Tom Meadhoin Anticline is reached at (NN 095 637). This quartzite is separated from the Tom Meadhoin Quartzite by a banded series of impure quartzites and black slates. These rocks can be examined at a low craig immediately to the north of the Tom Meadhoin Quartzite. A slaty cleavage (S<sub>1</sub>) dips more steeply NW than bedding. Exposures farther downhill, at the nose of the Tom Meadhoin Anticline, show bedding dipping N or NE at a high angle to the slaty cleavage S<sub>1</sub>. These bedding-cleavage relationships indicate that the Tom Meadhoin Anticline is an F<sub>1</sub> fold. (This is confirmed by the observations made at locality 17.) The fold plunges NE at a moderately low angle.</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>Follow the thin band of quartzite south-west until the nose of the Tom Meadhoin Anticline is reached at (NN 095 637). This quartzite is separated from the Tom Meadhoin Quartzite by a banded series of impure quartzites and black slates. These rocks can be examined at a low craig immediately to the north of the Tom Meadhoin Quartzite. A slaty cleavage (S<sub>1</sub>) dips more steeply NW than bedding. Exposures farther downhill, at the nose of the Tom Meadhoin Anticline, show bedding dipping N or NE at a high angle to the slaty cleavage S<sub>1</sub>. These bedding-cleavage relationships indicate that the Tom Meadhoin Anticline is an F<sub>1</sub> fold. (This is confirmed by the observations made at locality 17.) The fold plunges NE at a moderately low angle.</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>===Locality 25. Summit of Tom Meadhoin ===</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>=== Locality 25. Summit of Tom Meadhoin <ins style="font-weight: bold; text-decoration: none;">to North Ballachulish </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>Continue south-west towards the summit of Tom Meadhoin (NN 086 622) across the quartzite outcrop, noting the cross-bedding which can be seen in nearly every exposure. The closure of the Tom Meadhoin Anticline, plunging SW at a moderately low angle, can be traced out SW of the Tom Meadhoin summit, starting on the SE limb and walking around the hinge to the NW limb. Abundant cross-bedding in the quartzite confirms that the fold is an upward-facing anticline. Although the Tom Meadhoin Quartzite lacks a cleavage which might be axial planar to this fold, exposures of banded Leven Schists at the head of a small burn draining north into the Allt Meurach show a slaty cleavage Sx dipping more steeply NW than bedding.</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>Continue south-west towards the summit of Tom Meadhoin (NN 086 622) across the quartzite outcrop, noting the cross-bedding which can be seen in nearly every exposure. The closure of the Tom Meadhoin Anticline, plunging SW at a moderately low angle, can be traced out SW of the Tom Meadhoin summit, starting on the SE limb and walking around the hinge to the NW limb. Abundant cross-bedding in the quartzite confirms that the fold is an upward-facing anticline. Although the Tom Meadhoin Quartzite lacks a cleavage which might be axial planar to this fold, exposures of banded Leven Schists at the head of a small burn draining north into the Allt Meurach show a slaty cleavage Sx dipping more steeply NW than bedding.</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>
</table>Scotfothttps://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=22981&oldid=prevScotfot at 23:07, 30 October 20152015-10-30T23:07:52Z<p></p>
<table style="background-color: #fff; color: #202122;" data-mw="interface">
<col class="diff-marker" />
<col class="diff-content" />
<col class="diff-marker" />
<col class="diff-content" />
<tr class="diff-title" lang="en-GB">
<td colspan="2" style="background-color: #fff; color: #202122; text-align: center;">← Older revision</td>
<td colspan="2" style="background-color: #fff; color: #202122; text-align: center;">Revision as of 23:07, 30 October 2015</td>
</tr><tr><td colspan="2" class="diff-lineno" id="mw-diff-left-l158">Line 158:</td>
<td colspan="2" class="diff-lineno">Line 158:</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>The burn exposes Ballachulish Slates in its lower course. Upstream the contact of these rocks with the Leven Schists across the line of the Ballachulish Slide can be located. There is a thin band of quartzite developed within the Leven Schists close to the slide.</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>The burn exposes Ballachulish Slates in its lower course. Upstream the contact of these rocks with the Leven Schists across the line of the Ballachulish Slide can be located. There is a thin band of quartzite developed within the Leven Schists close to the slide.</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>===Locality 23 Line of the Ballachulish Slide ===</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>===Locality 23<ins style="font-weight: bold; text-decoration: none;">. </ins>Line of the Ballachulish Slide ===</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>The line of the Ballachulish Slide, flanked to the SE by Ballachulish Slates and to the NW. by Leven Schists with a thin band of quartzite close to the slide, can be followed south-west across the hillside around the hinges of two F<sub>2</sub> folds. These folds plunge NE at a low angle, forming a synform to the NW and an antiform to the SE. They are complementary to the F2 folds developed on the SE. limb of the Stob Ban Synform. A thin remanent of Ballachulish Limestone, now in the form of calc-silicate, can be located on the NW. limb of the synform. Minor F<sub>2</sub> folds are best seen where they affect the quartzite band between the synform and the antiform.</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>The line of the Ballachulish Slide, flanked to the SE by Ballachulish Slates and to the NW. by Leven Schists with a thin band of quartzite close to the slide, can be followed south-west across the hillside around the hinges of two F<sub>2</sub> folds. These folds plunge NE at a low angle, forming a synform to the NW and an antiform to the SE. They are complementary to the F2 folds developed on the SE. limb of the Stob Ban Synform. A thin remanent of Ballachulish Limestone, now in the form of calc-silicate, can be located on the NW. limb of the synform. Minor F<sub>2</sub> folds are best seen where they affect the quartzite band between the synform and the antiform.</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>
</table>Scotfothttps://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=22980&oldid=prevScotfot at 23:07, 30 October 20152015-10-30T23:07:47Z<p></p>
<table style="background-color: #fff; color: #202122;" data-mw="interface">
<col class="diff-marker" />
<col class="diff-content" />
<col class="diff-marker" />
<col class="diff-content" />
<tr class="diff-title" lang="en-GB">
<td colspan="2" style="background-color: #fff; color: #202122; text-align: center;">← Older revision</td>
<td colspan="2" style="background-color: #fff; color: #202122; text-align: center;">Revision as of 23:07, 30 October 2015</td>
</tr><tr><td colspan="2" class="diff-lineno" id="mw-diff-left-l155">Line 155:</td>
<td colspan="2" class="diff-lineno">Line 155:</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>This excursion deals with the structural relationships of the Tom Meadhoin Anticline which forms the nose of the Kinlochleven Anticline NW of the Stob Ban Synform. It involves walking 6 or 7 miles over rough ground. Doire Ban is best approached from the road which runs south from Fort William through Blarmachfoldach. The track through the Lairig Mhor to Kinlochleven is followed from Blar a'Chaoruinn (where cars may be parked) as far as the sheep-folds at the edge of the forestry wood (NN 101 648). Cross the Allt na Lairige Moire to gain the first exposures in the gully of a stream draining east from Doire Ban. Care should be taken if the river is in spate.</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>This excursion deals with the structural relationships of the Tom Meadhoin Anticline which forms the nose of the Kinlochleven Anticline NW of the Stob Ban Synform. It involves walking 6 or 7 miles over rough ground. Doire Ban is best approached from the road which runs south from Fort William through Blarmachfoldach. The track through the Lairig Mhor to Kinlochleven is followed from Blar a'Chaoruinn (where cars may be parked) as far as the sheep-folds at the edge of the forestry wood (NN 101 648). Cross the Allt na Lairige Moire to gain the first exposures in the gully of a stream draining east from Doire Ban. Care should be taken if the river is in spate.</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>===Locality 22===</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>===Locality 22<ins style="font-weight: bold; text-decoration: none;">. Ballachulish Slates/Leven Schists and their contact </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>The burn exposes Ballachulish Slates in its lower course. Upstream the contact of these rocks with the Leven Schists across the line of the Ballachulish Slide can be located. There is a thin band of quartzite developed within the Leven Schists close to the slide.</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>The burn exposes Ballachulish Slates in its lower course. Upstream the contact of these rocks with the Leven Schists across the line of the Ballachulish Slide can be located. There is a thin band of quartzite developed within the Leven Schists close to the slide.</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>===Locality 23===</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>===Locality 23 <ins style="font-weight: bold; text-decoration: none;">Line of the Ballachulish Slide </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>The line of the Ballachulish Slide, flanked to the SE by Ballachulish Slates and to the NW. by Leven Schists with a thin band of quartzite close to the slide, can be followed south-west across the hillside around the hinges of two F<sub>2</sub> folds. These folds plunge NE at a low angle, forming a synform to the NW and an antiform to the SE. They are complementary to the F2 folds developed on the SE. limb of the Stob Ban Synform. A thin remanent of Ballachulish Limestone, now in the form of calc-silicate, can be located on the NW. limb of the synform. Minor F<sub>2</sub> folds are best seen where they affect the quartzite band between the synform and the antiform.</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>The line of the Ballachulish Slide, flanked to the SE by Ballachulish Slates and to the NW. by Leven Schists with a thin band of quartzite close to the slide, can be followed south-west across the hillside around the hinges of two F<sub>2</sub> folds. These folds plunge NE at a low angle, forming a synform to the NW and an antiform to the SE. They are complementary to the F2 folds developed on the SE. limb of the Stob Ban Synform. A thin remanent of Ballachulish Limestone, now in the form of calc-silicate, can be located on the NW. limb of the synform. Minor F<sub>2</sub> folds are best seen where they affect the quartzite band between the synform and the antiform.</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>===Locality 24===</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>===Locality 24<ins style="font-weight: bold; text-decoration: none;">. Tom Meadhoin Anticline </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>Follow the thin band of quartzite south-west until the nose of the Tom Meadhoin Anticline is reached at (NN 095 637). This quartzite is separated from the Tom Meadhoin Quartzite by a banded series of impure quartzites and black slates. These rocks can be examined at a low craig immediately to the north of the Tom Meadhoin Quartzite. A slaty cleavage (S<sub>1</sub>) dips more steeply NW than bedding. Exposures farther downhill, at the nose of the Tom Meadhoin Anticline, show bedding dipping N or NE at a high angle to the slaty cleavage S<sub>1</sub>. These bedding-cleavage relationships indicate that the Tom Meadhoin Anticline is an F<sub>1</sub> fold. (This is confirmed by the observations made at locality 17.) The fold plunges NE at a moderately low angle.</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>Follow the thin band of quartzite south-west until the nose of the Tom Meadhoin Anticline is reached at (NN 095 637). This quartzite is separated from the Tom Meadhoin Quartzite by a banded series of impure quartzites and black slates. These rocks can be examined at a low craig immediately to the north of the Tom Meadhoin Quartzite. A slaty cleavage (S<sub>1</sub>) dips more steeply NW than bedding. Exposures farther downhill, at the nose of the Tom Meadhoin Anticline, show bedding dipping N or NE at a high angle to the slaty cleavage S<sub>1</sub>. These bedding-cleavage relationships indicate that the Tom Meadhoin Anticline is an F<sub>1</sub> fold. (This is confirmed by the observations made at locality 17.) The fold plunges NE at a moderately low angle.</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>===Locality 25===</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>===Locality 25<ins style="font-weight: bold; text-decoration: none;">. Summit of Tom Meadhoin </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>Continue south-west towards the summit of Tom Meadhoin (NN 086 622) across the quartzite outcrop, noting the cross-bedding which can be seen in nearly every exposure. The closure of the Tom Meadhoin Anticline, plunging SW at a moderately low angle, can be traced out SW of the Tom Meadhoin summit, starting on the SE limb and walking around the hinge to the NW limb. Abundant cross-bedding in the quartzite confirms that the fold is an upward-facing anticline. Although the Tom Meadhoin Quartzite lacks a cleavage which might be axial planar to this fold, exposures of banded Leven Schists at the head of a small burn draining north into the Allt Meurach show a slaty cleavage Sx dipping more steeply NW than bedding.</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>Continue south-west towards the summit of Tom Meadhoin (NN 086 622) across the quartzite outcrop, noting the cross-bedding which can be seen in nearly every exposure. The closure of the Tom Meadhoin Anticline, plunging SW at a moderately low angle, can be traced out SW of the Tom Meadhoin summit, starting on the SE limb and walking around the hinge to the NW limb. Abundant cross-bedding in the quartzite confirms that the fold is an upward-facing anticline. Although the Tom Meadhoin Quartzite lacks a cleavage which might be axial planar to this fold, exposures of banded Leven Schists at the head of a small burn draining north into the Allt Meurach show a slaty cleavage Sx dipping more steeply NW than bedding.</div></td></tr>
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</table>Scotfothttps://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=22979&oldid=prevScotfot at 23:03, 30 October 20152015-10-30T23:03:50Z<p></p>
<a href="https://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=22979&oldid=22978">Show changes</a>Scotfothttps://earthwise.bgs.ac.uk/index.php?title=Dalradian_rocks_of_the_Loch_Leven_area_-_an_excursion&diff=22978&oldid=prevScotfot at 22:53, 30 October 20152015-10-30T22:53:04Z<p></p>
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<td colspan="2" style="background-color: #fff; color: #202122; text-align: center;">Revision as of 22:53, 30 October 2015</td>
</tr><tr><td colspan="2" class="diff-lineno" id="mw-diff-left-l176">Line 176:</td>
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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;"><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"></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>The basic excursion (omitting the extensions to localities 30-33) may be accomplished in a day. Cars and coaches may be parked in several convenient lay-bys on the A82 and a bus service runs along the same road between Kinlochleven and Fort William. Low tide is of marginal advantage for some exposures.</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>The basic excursion (omitting the extensions to localities 30-33) may be accomplished in a day. Cars and coaches may be parked in several convenient lay-bys on the A82 and a bus service runs along the same road between Kinlochleven and Fort William. Low tide is of marginal advantage for some exposures.</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>===Locality 28<del style="font-weight: bold; text-decoration: none;">===</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>=== Locality 28 Glen Coe Quartzite—Binnein Schist—Binnein Quartzite, upper limb of Kinlochleven Anticline <ins style="font-weight: bold; text-decoration: none;">===</ins></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>Glen Coe Quartzite—Binnein Schist—Binnein Quartzite, upper limb of Kinlochleven Anticline<del style="font-weight: bold; text-decoration: none;">. </del>Parking at quarry (NN 123 611) and lay-byes on both sides of road nearby. Both the shore and road-side exposures from (NN 120 610) to (NN 127 613) give an almost continuous section. The western-most exposure and the headland to the east exhibit typical impure Glen Coe Quartzite with abundant cross-bedding and locally slump structures, pebble beds and mud slithers. The beds can be seen to be involved in a large F<sub>1</sub> fold pair, with axial-planar S<sub>1</sub>, plunging steeply N. In pelitic beds a widely spaced strain-slip cleavage is developed related to the major F<sub>4</sub> deflection of strike across Loch Leven.</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>Parking at quarry (NN 123 611) and lay-byes on both sides of road nearby. Both the shore and road-side exposures from (NN 120 610) to (NN 127 613) give an almost continuous section. The western-most exposure and the headland to the east exhibit typical impure Glen Coe Quartzite with abundant cross-bedding and locally slump structures, pebble beds and mud slithers. The beds can be seen to be involved in a large F<sub>1</sub> fold pair, with axial-planar S<sub>1</sub>, plunging steeply N. In pelitic beds a widely spaced strain-slip cleavage is developed related to the major F<sub>4</sub> deflection of strike across Loch Leven.</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"></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>To the east of the headland the quartzite grades transionally into the Binnein Schist, which can be demonstrated, from small scale cross-bedding, to be older. These beds are dominated by a NE striking strain-slip cleavage, S<sub>2</sub> and the related F<sub>2</sub> minor folds. Garnet and white K-feldspar porphyroblasts are syn-tectonically related to this deformation. The glaciated exposures at the eastern end of the shore exposures show good examples of small-scale F<sub>1</sub> closures folded by F<sub>2</sub>; in the road-side exposures above, the plunge of F<sub>1</sub> can be seen to vary from steep to gentle to the N and the vergence indicates a synform to the east.</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>To the east of the headland the quartzite grades transionally into the Binnein Schist, which can be demonstrated, from small scale cross-bedding, to be older. These beds are dominated by a NE striking strain-slip cleavage, S<sub>2</sub> and the related F<sub>2</sub> minor folds. Garnet and white K-feldspar porphyroblasts are syn-tectonically related to this deformation. The glaciated exposures at the eastern end of the shore exposures show good examples of small-scale F<sub>1</sub> closures folded by F<sub>2</sub>; in the road-side exposures above, the plunge of F<sub>1</sub> can be seen to vary from steep to gentle to the N and the vergence indicates a synform to the east.</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"></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>The eastern-most shore exposures and those of the road-side above provide a transition into Binnein Quartzite, which from cross-bedding can be demonstrated to be older. F<sub>1</sub> folds in exposures above the road plunge steeply north and face down to the west. The synform to the east must be a downward-facing F<sub>1</sub> anticline.</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>The eastern-most shore exposures and those of the road-side above provide a transition into Binnein Quartzite, which from cross-bedding can be demonstrated to be older. F<sub>1</sub> folds in exposures above the road plunge steeply north and face down to the west. The synform to the east must be a downward-facing F<sub>1</sub> anticline.</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>===Locality 29<del style="font-weight: bold; text-decoration: none;">===</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>=== Locality 29 Binnein Quartzite—Eilde Schist, upper limb of Kinlochleven Anticline (NN 130 613 - NN 133 613) <ins style="font-weight: bold; text-decoration: none;">===</ins></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>Binnein Quartzite—Eilde Schist, upper limb of Kinlochleven Anticline (NN 130 613 - NN 133 613)A lay-by is situated at the eastern end of the exposures. Start at western end of the shore section. The typical pure Binnein Quartzite exhibits westerly younging crossbedding and is involved in a large F<sub>1</sub> fold-pair plunging N. Again, the vergence indicates a major synform to the east. Most of the exposures of the shore section are on the short limb of this fold-pair and exhibit spectacular minor folding with axial planar S<sub>2</sub>. Characteristic ellipsoidal iron-rich spots are elongated in S1. Locally the first structures are deformed by the S<sub>2</sub> strain-slip cleavage, crossing in its usual clockwise sense giving a steep intersection lineation.</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>A lay-by is situated at the eastern end of the exposures. Start at western end of the shore section. The typical pure Binnein Quartzite exhibits westerly younging crossbedding and is involved in a large F<sub>1</sub> fold-pair plunging N. Again, the vergence indicates a major synform to the east. Most of the exposures of the shore section are on the short limb of this fold-pair and exhibit spectacular minor folding with axial planar S<sub>2</sub>. Characteristic ellipsoidal iron-rich spots are elongated in S1. Locally the first structures are deformed by the S<sub>2</sub> strain-slip cleavage, crossing in its usual clockwise sense giving a steep intersection lineation.</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"></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>At the eastern end of the section the quartzite grades into the Eilde Schists with smallscale graded silty bands (demonstrating that they are older) and sedimentary dykelets. The more pelitic beds to the east are dominated by F<sub>2</sub>.</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>At the eastern end of the section the quartzite grades into the Eilde Schists with smallscale graded silty bands (demonstrating that they are older) and sedimentary dykelets. The more pelitic beds to the east are dominated by F<sub>2</sub>.</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>===Locality 30<del style="font-weight: bold; text-decoration: none;">===</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> </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>Eilde Schist—Eilde Quartzite, upper limb of Kinlochleven Anticline<del style="font-weight: bold; text-decoration: none;">. </del>From the previous locality walk about 1.5 km east along the A82 until the first roadside exposures of Eilde Quartzite are reached (NN 146 618). Strike NE up the hillside keeping to the east of the small burn. The transitional beds of the Eilde Quartzite/Schist junction can be located at about 500 feet. Cross-bedding (demonstrating the quartzite is older), S<sub>1</sub> and its steep N-plunging intersection with bedding can be seen in the quartzose beds; once again these relationships indicate that a major F<sub>1</sub> downward-facing anticline still lies to the east. In the pelitic beds the wide strain-slip cleavages of S<sub>3</sub> and S<sub>4</sub> strike E-W and N-S respectively. The hinge of a large subsidiary fold to the Kinlochleven Anticline can be seen on the prominent quartzite face on the hillside above. The fold is a synform, but from the cross-bedding and the axial-planar S<sub>1</sub> cleavage, it can be shown to be a downward-facing Fx anticline.</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>=== Locality 30 Eilde Schist—Eilde Quartzite, upper limb of Kinlochleven Anticline <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>From the previous locality walk about 1.5 km east along the A82 until the first roadside exposures of Eilde Quartzite are reached (NN 146 618). Strike NE up the hillside keeping to the east of the small burn. The transitional beds of the Eilde Quartzite/Schist junction can be located at about 500 feet. Cross-bedding (demonstrating the quartzite is older), S<sub>1</sub> and its steep N-plunging intersection with bedding can be seen in the quartzose beds; once again these relationships indicate that a major F<sub>1</sub> downward-facing anticline still lies to the east. In the pelitic beds the wide strain-slip cleavages of S<sub>3</sub> and S<sub>4</sub> strike E-W and N-S respectively. The hinge of a large subsidiary fold to the Kinlochleven Anticline can be seen on the prominent quartzite face on the hillside above. The fold is a synform, but from the cross-bedding and the axial-planar S<sub>1</sub> cleavage, it can be shown to be a downward-facing Fx anticline.</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"></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>FIG. 6. Geological map (after Treagus, 1974) of the Kinlochleven area (Excursion 6, localities 28-33).</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>FIG. 6. Geological map (after Treagus, 1974) of the Kinlochleven area (Excursion 6, localities 28-33).</div></td></tr>
<tr><td colspan="2" class="diff-lineno" id="mw-diff-left-l196">Line 196:</td>
<td colspan="2" class="diff-lineno">Line 197:</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>If time permits, walk NW. across the dominantly south-west younging Binnein Quartzite to the Eilde Schist junction at (NN 162 625) (cf. Locality 29). Folding in the Eilde Schist is complex, but it is worth continuing NW. to the prominent junction with the Eilde Quartzite above at (NN 159 628). The first few tens of metres are strongly deformed but unambiguous cross-bedding soon shows that the quartzite is inverted. This junction is a slide which has completely removed the Eilde Quartzite on the lower limb of the Kinlochleven Anticline. Looking SE. from here towards the slopes of Garbh Bheinn on the south side of the loch, the Eilde Quartzite can be seen in the core of the synformal nose of the Kinlochleven Anticline; here it is greatly thinned, but not completely removed, on the lower limb. An interesting return route is made by walking NE. and locating the Binnein Quartzite/Schist junction that follows the bend in the Allt Nathrach (NN 166 628). The junction is involved in a large F<sub>2</sub> fold and the transitional beds reveal excellent examples of small-scale interference patterns produced by F<sub>1</sub> and F<sub>2</sub>. Descend to the prominent knoll north of the Nathrach caravan site (NN 163 621). Here the banded Binnein Schist is dominated by micro-folding with an ENE. trending axial-planar cleavage. These exposures are at the hinge of the Loch Leven Antiform; the cleavage and folds related to this major F<sub>3</sub> structure are intensely developed along its hinge zone.</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>If time permits, walk NW. across the dominantly south-west younging Binnein Quartzite to the Eilde Schist junction at (NN 162 625) (cf. Locality 29). Folding in the Eilde Schist is complex, but it is worth continuing NW. to the prominent junction with the Eilde Quartzite above at (NN 159 628). The first few tens of metres are strongly deformed but unambiguous cross-bedding soon shows that the quartzite is inverted. This junction is a slide which has completely removed the Eilde Quartzite on the lower limb of the Kinlochleven Anticline. Looking SE. from here towards the slopes of Garbh Bheinn on the south side of the loch, the Eilde Quartzite can be seen in the core of the synformal nose of the Kinlochleven Anticline; here it is greatly thinned, but not completely removed, on the lower limb. An interesting return route is made by walking NE. and locating the Binnein Quartzite/Schist junction that follows the bend in the Allt Nathrach (NN 166 628). The junction is involved in a large F<sub>2</sub> fold and the transitional beds reveal excellent examples of small-scale interference patterns produced by F<sub>1</sub> and F<sub>2</sub>. Descend to the prominent knoll north of the Nathrach caravan site (NN 163 621). Here the banded Binnein Schist is dominated by micro-folding with an ENE. trending axial-planar cleavage. These exposures are at the hinge of the Loch Leven Antiform; the cleavage and folds related to this major F<sub>3</sub> structure are intensely developed along its hinge zone.</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>===Locality 32<del style="font-weight: bold; text-decoration: none;">===</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>=== Locality 32 The F2 Kinlochleven Antiform <ins style="font-weight: bold; text-decoration: none;">===</ins></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>The F2 Kinlochleven Antiform<del style="font-weight: bold; text-decoration: none;">.</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>Park in Kinlochleven and walk west along the A82 on the south side of the river, branch right along the small road to the pier and pass through the dock gates. A quartzite/schist junction can be located where a small burn descends the cliff (NN 179 618). Note that the junction strikes SSE., rotated by the F3 Loch Leven Antiform and that the crossbedding youngs west towards the schist. This is the Binnein Quartzite/Schist junction on the eastern limb of the F1 Mamore Syncline, a subsidiary fold to the Kinlochleven Anticline.</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>Park in Kinlochleven and walk west along the A82 on the south side of the river, branch right along the small road to the pier and pass through the dock gates. A quartzite/schist junction can be located where a small burn descends the cliff (NN 179 618). Note that the junction strikes SSE., rotated by the F3 Loch Leven Antiform and that the crossbedding youngs west towards the schist. This is the Binnein Quartzite/Schist junction on the eastern limb of the F1 Mamore Syncline, a subsidiary fold to the Kinlochleven Anticline.</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 colspan="2" class="diff-lineno" id="mw-diff-left-l203">Line 203:</td>
<td colspan="2" class="diff-lineno">Line 203:</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"></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>Return to Kinlochleven via the old railway track; inversion of the quartzite can be demonstrated until an exposure of schist is reached where a small burn descends the hillside (NN 184 617); beyond this the quartzite dips steeply west and youngs in the same direction. The schist is the Binnein Schist in the core of the Kinlochleven Antiform. To demonstrate the relation of this structure to the strong S<sub>2</sub> cleavage, it is necessary to climb the hillside south of Kinlochleven (NN 185 615) to the core of Binnein Schist or better still to ascend the prominent crag NE of the town (NN 195 624) where the Eilde Schist/Binnein Quartzite junction is affected by the antiform at a higher structural level.</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>Return to Kinlochleven via the old railway track; inversion of the quartzite can be demonstrated until an exposure of schist is reached where a small burn descends the hillside (NN 184 617); beyond this the quartzite dips steeply west and youngs in the same direction. The schist is the Binnein Schist in the core of the Kinlochleven Antiform. To demonstrate the relation of this structure to the strong S<sub>2</sub> cleavage, it is necessary to climb the hillside south of Kinlochleven (NN 185 615) to the core of Binnein Schist or better still to ascend the prominent crag NE of the town (NN 195 624) where the Eilde Schist/Binnein Quartzite junction is affected by the antiform at a higher structural level.</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>===Locality 33<del style="font-weight: bold; text-decoration: none;">===</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>=== Locality 33 The eastern limb of the Kinlochleven Antiform <ins style="font-weight: bold; text-decoration: none;">===</ins></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>The eastern limb of the Kinlochleven Antiform<del style="font-weight: bold; text-decoration: none;">.</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 Kinlochleven take the road eastwards on the south side of the river until the old bridge is reached at (NN 192 618). Exposures here and in the river show that the Binnein Quartzite/Schist junction to the east should now be located, either on the path to the north of the river or near the pipe-line on the south side. The penetrative cleavage in the semi-pelitic transitional beds looks like Sj and infers that the rocks face down to the west. Close examination, however, particularly of the more pelitic beds, will show that this cleavage is an intense development of the S2 strain-clip cleavage. By inference the F<sub>1</sub> folds on this limb of the Kinlochleven Antiform must face upwards; although occasional F<sub>1</sub> folds can be found in the Eilde Schist, lack of sedimentary structures in the critical exposures does not make this upward facing easy to demonstrate.</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 Kinlochleven take the road eastwards on the south side of the river until the old bridge is reached at (NN 192 618). Exposures here and in the river show that the Binnein Quartzite/Schist junction to the east should now be located, either on the path to the north of the river or near the pipe-line on the south side. The penetrative cleavage in the semi-pelitic transitional beds looks like Sj and infers that the rocks face down to the west. Close examination, however, particularly of the more pelitic beds, will show that this cleavage is an intense development of the S2 strain-clip cleavage. By inference the F<sub>1</sub> folds on this limb of the Kinlochleven Antiform must face upwards; although occasional F<sub>1</sub> folds can be found in the Eilde Schist, lack of sedimentary structures in the critical exposures does not make this upward facing easy to demonstrate.</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>
</table>Scotfot