http://earthwise-staging.bgs.ac.uk/index.php?action=history&feed=atom&title=Paleocene_geology_of_Rum 2026-04-17T00:09:49Z Revision history for this page on the wiki MediaWiki 1.42.3 http://earthwise-staging.bgs.ac.uk/index.php?title=Paleocene_geology_of_Rum&diff=24315&oldid=prev 2015-12-22T21:32:11Z

<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"> <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 22:32, 22 December 2015</td> </tr><tr><td colspan="2" class="diff-lineno" id="mw-diff-left-l5">Line 5:</td> <td colspan="2" class="diff-lineno">Line 5:</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:EGS_RUM_04b.jpg|thumbnail|Panoramic views of the Northern Marginal Zone and Southern Mountains Zone: B. Dibidil river valley. Rhyodacite ignimbrite sheets and sedimentary breccias make up the back wall of Nameless Corrie and the ridge to Ainshval on the left of the photograph. Layered units in the Eastern Layered Intrusion form the distinctive peak of Trollaval in the far centre. Faulted Lewisian gneisses and Torridonian sandstones crop out along the foreshore to the right.]]</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:EGS_RUM_04b.jpg|thumbnail|Panoramic views of the Northern Marginal Zone and Southern Mountains Zone: B. Dibidil river valley. Rhyodacite ignimbrite sheets and sedimentary breccias make up the back wall of Nameless Corrie and the ridge to Ainshval on the left of the photograph. Layered units in the Eastern Layered Intrusion form the distinctive peak of Trollaval in the far centre. Faulted Lewisian gneisses and Torridonian sandstones crop out along the foreshore to the right.]]</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:EGS_RUM_07.jpg|thumbnail|Harrisitic olivines in the Central Intrusion. Individual crystals may reach over 60 cm in length. See text for details.]]</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:EGS_RUM_07.jpg|thumbnail|Harrisitic olivines in the Central Intrusion. Individual crystals may reach over 60 cm in length. See text for details.]]</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;">Media</del>:EGS_RUM_43.jpg| (<del style="font-weight: bold; text-decoration: none;">See image</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;">File</ins>:EGS_RUM_43.jpg|<ins style="font-weight: bold; text-decoration: none;">thumbnail|Schematic representation of possible events leading to the formation of the Central Intrusion. Periodic replenishments of picritic magma (1) rejuvenated the magma chamber causing sliding and slumping (2) and intruded laterally into earlier cumulates (3). Magma fountaining into the chamber (4a) flows off the roof and down the sides as crystal-laden, gravity-driven currents (4b), dislodging crystal mushes as they move, then spread across the floor, reworking cumulate debris and depositing this material and primary crystals on the floor (4c). Movement on faults was accompanied by magma injection, thermal erosion of earlier rocks and their fragmentation to form breccia zones (5). Slides of coherent blocks of cumulate across partly liquefied cumulate led to spectacular slump mélanges (6). (Emeleus et al. [1996]. After Emeleus and Bell [2005].) </ins>(<ins style="font-weight: bold; text-decoration: none;">© NERC</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:EGS_RUM_02.jpg|thumbnail|Simplified geological map of Rum and adjacent islands.]]</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:EGS_RUM_02.jpg|thumbnail|Simplified geological map of Rum and adjacent islands.]]</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:EGS_RUM_09.jpg|thumbnail|Map of Rum showing the location of each excursion as a box.]]</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:EGS_RUM_09.jpg|thumbnail|Map of Rum showing the location of each excursion as a box.]]</div></td></tr> </table>

Scotfot http://earthwise-staging.bgs.ac.uk/index.php?title=Paleocene_geology_of_Rum&diff=24314&oldid=prev 2015-12-22T21:31:39Z

<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"> <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 22:31, 22 December 2015</td> </tr><tr><td colspan="2" class="diff-lineno" id="mw-diff-left-l5">Line 5:</td> <td colspan="2" class="diff-lineno">Line 5:</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:EGS_RUM_04b.jpg|thumbnail|Panoramic views of the Northern Marginal Zone and Southern Mountains Zone: B. Dibidil river valley. Rhyodacite ignimbrite sheets and sedimentary breccias make up the back wall of Nameless Corrie and the ridge to Ainshval on the left of the photograph. Layered units in the Eastern Layered Intrusion form the distinctive peak of Trollaval in the far centre. Faulted Lewisian gneisses and Torridonian sandstones crop out along the foreshore to the right.]]</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:EGS_RUM_04b.jpg|thumbnail|Panoramic views of the Northern Marginal Zone and Southern Mountains Zone: B. Dibidil river valley. Rhyodacite ignimbrite sheets and sedimentary breccias make up the back wall of Nameless Corrie and the ridge to Ainshval on the left of the photograph. Layered units in the Eastern Layered Intrusion form the distinctive peak of Trollaval in the far centre. Faulted Lewisian gneisses and Torridonian sandstones crop out along the foreshore to the right.]]</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:EGS_RUM_07.jpg|thumbnail|Harrisitic olivines in the Central Intrusion. Individual crystals may reach over 60 cm in length. See text for details.]]</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:EGS_RUM_07.jpg|thumbnail|Harrisitic olivines in the Central Intrusion. Individual crystals may reach over 60 cm in length. See text for details.]]</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;">[[Media:EGS_RUM_43.jpg| (See image)]]</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:EGS_RUM_02.jpg|thumbnail|Simplified geological map of Rum and adjacent islands.]]</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:EGS_RUM_02.jpg|thumbnail|Simplified geological map of Rum and adjacent islands.]]</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:EGS_RUM_09.jpg|thumbnail|Map of Rum showing the location of each excursion as a box.]]</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:EGS_RUM_09.jpg|thumbnail|Map of Rum showing the location of each excursion as a box.]]</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:EGS_RUM_08.jpg|thumbnail|Cross-section through the south-east portion of the Rum Central Complex (Askival – Beinn nan Stac – Sound of Rum), illustrating relationships and tectonics along the Main Ring Fault system, after Emeleus (1997) (see pp. 148-49 for full key.) (© NERC)]]</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:EGS_RUM_08.jpg|thumbnail|Cross-section through the south-east portion of the Rum Central Complex (Askival – Beinn nan Stac – Sound of Rum), illustrating relationships and tectonics along the Main Ring Fault system, after Emeleus (1997) (see pp. 148-49 for full key.) (© NERC)]]</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:EGS_RUM_05.jpg|thumbnail|Intricate layering in troctolites (allivalites), showing sedimentary-style features in the Central Intrusion. Locality 4.4, west of the Long Loch, central Rum. Scale: hammer shaft 30 cm. (ELI), the Western Layered Intrusion (WLI), and the Central Intrusion (CI).]]</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:EGS_RUM_05.jpg|thumbnail|Intricate layering in troctolites (allivalites), showing sedimentary-style features in the Central Intrusion. Locality 4.4, west of the Long Loch, central Rum. Scale: hammer shaft 30 cm. (ELI), the Western Layered Intrusion (WLI), and the Central Intrusion (CI).]]</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> <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:EGS_RUM_31.jpg|thumbnail|View of west-dipping layered units in the upper part of the Eastern Layered Intrusion, south side of Hallival. Scale: about 120 m from grassy col to Hallival summit. Photo taken from Askival.]]</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:EGS_RUM_31.jpg|thumbnail|View of west-dipping layered units in the upper part of the Eastern Layered Intrusion, south side of Hallival. Scale: about 120 m from grassy col to Hallival summit. Photo taken from Askival.]]</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:EGS_RUM_58.jpg|thumbnail|Geological map of the north end of the Central Intrusion, Minishal and the country around Sgaorishal and the north-west coast of Rum. Excursion 6. Extract from BGS 1:50,000 map of Rum © NERC [http://www.bgs.ac.uk/data/maps/maps.cfc?method=viewRecord&amp;mapId=11009  Full map and key].]]</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:EGS_RUM_58.jpg|thumbnail|Geological map of the north end of the Central Intrusion, Minishal and the country around Sgaorishal and the north-west coast of Rum. Excursion 6. Extract from BGS 1:50,000 map of Rum © NERC [http://www.bgs.ac.uk/data/maps/maps.cfc?method=viewRecord&amp;mapId=11009  Full map and key].]]</div></td></tr> </table>

Scotfot http://earthwise-staging.bgs.ac.uk/index.php?title=Paleocene_geology_of_Rum&diff=24313&oldid=prev 2015-12-22T21:30:21Z

<p><span dir="auto"><span class="autocomment">The Central Intrusion (CI)</span></span></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"> <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 22:30, 22 December 2015</td> </tr><tr><td colspan="2" class="diff-lineno" id="mw-diff-left-l81">Line 81:</td> <td colspan="2" class="diff-lineno">Line 81:</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 Central Intrusion (CI) ====</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 Central Intrusion (CI) ====</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>This intrusion intrudes both the Eastern and Western layered intrusions [[Media:EGS_RUM_06.jpg| (See image)]], cutting a north–south swathe through them from the Long Loch to Papadil [[Media:EGS_RUM_02.jpg| (See image)]]. Although layered peridotites and troctolites are present, the intrusion is characterised by igneous breccias (Donaldson, 1973). The breccias occur in approximately north–south zones, tens to hundreds of metres in width, in which angular to subangular blocks and megablocks of peridotite and troctolite are embedded in predominantly feldspathic peridotite matrices (Volker and Upton, 1990). The troctolite clasts commonly display layering, which dips steeply in all directions although generally remaining fairly uniform in direction within a clast. Large or small individual clasts may record complex events involving crystal sedimentation, or the disruption and/or replacement of layered structures. In turn, layered structures in the enclosing peridotite record considerable disturbance and disruption, commonly suggesting that clasts and blocks subsided into incompetent surroundings, probably crystal mushes (Excursion 4). Elsewhere, layered structures may appear slumped, or disturbed by avalanches of ‘pebbly’ peridotite debris and by dropstones (Excursion 4). Much of the debris within the breccias resembles fragments of peridotite and troctolite from the earlier intrusions. West and south of the Long Loch, large rafts of troctolite are many tens of metres in extent. These megablocks have steeply dipping layering and were probably derived from the ELI. Layered structures are especially well developed in the troctolites and feldspathic peridotite exposed in the CI west of the Long Loch where slump structures, graded bedding, flame structures and other features suggesting ‘soft sediment’ deformation are much in evidence (Excursion 4). On the western slopes of Trollaval there is a progressive increase of dip in the ELI units when traced westwards, indicating that at some stage substantial masses of layered rocks sagged towards the Central Intrusion and probably broke off and subsided into it (cf. [[Media:EGS_RUM_06.jpg| (See image)]], (<del style="font-weight: bold; text-decoration: none;">Figure43</del>)&lt;nowiki&gt;; Volker and Upton, 1990; Emeleus &lt;/nowiki&gt;''et al.'', 1996; O’Driscoll ''et al.'', 2007b).</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>This intrusion intrudes both the Eastern and Western layered intrusions [[Media:EGS_RUM_06.jpg| (See image)]], cutting a north–south swathe through them from the Long Loch to Papadil [[Media:EGS_RUM_02.jpg| (See image)]]. Although layered peridotites and troctolites are present, the intrusion is characterised by igneous breccias (Donaldson, 1973). The breccias occur in approximately north–south zones, tens to hundreds of metres in width, in which angular to subangular blocks and megablocks of peridotite and troctolite are embedded in predominantly feldspathic peridotite matrices (Volker and Upton, 1990). The troctolite clasts commonly display layering, which dips steeply in all directions although generally remaining fairly uniform in direction within a clast. Large or small individual clasts may record complex events involving crystal sedimentation, or the disruption and/or replacement of layered structures. In turn, layered structures in the enclosing peridotite record considerable disturbance and disruption, commonly suggesting that clasts and blocks subsided into incompetent surroundings, probably crystal mushes (Excursion 4). Elsewhere, layered structures may appear slumped, or disturbed by avalanches of ‘pebbly’ peridotite debris and by dropstones (Excursion 4). Much of the debris within the breccias resembles fragments of peridotite and troctolite from the earlier intrusions. West and south of the Long Loch, large rafts of troctolite are many tens of metres in extent. These megablocks have steeply dipping layering and were probably derived from the ELI. Layered structures are especially well developed in the troctolites and feldspathic peridotite exposed in the CI west of the Long Loch where slump structures, graded bedding, flame structures and other features suggesting ‘soft sediment’ deformation are much in evidence (Excursion 4). On the western slopes of Trollaval there is a progressive increase of dip in the ELI units when traced westwards, indicating that at some stage substantial masses of layered rocks sagged towards the Central Intrusion and probably broke off and subsided into it (cf. [[Media:EGS_RUM_06.jpg| (See image)]], (<ins style="font-weight: bold; text-decoration: none;">[[Media:EGS_RUM_43.jpg| (See image)]]</ins>)&lt;nowiki&gt;; Volker and Upton, 1990; Emeleus &lt;/nowiki&gt;''et al.'', 1996; O’Driscoll ''et al.'', 2007b).</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>A distinctive structure is found in feldspathic peridotites north-east of Loch MacIver (Loch an Dornabac). Radiating, bifurcating crystals of plagioclase up to 40 cm in length, enclosing myriads of minute olivine crystals, occur in seaweed-like masses as much as 1 m in diameter, scattered through the normal feldspathic peridotite. These ‘poikilo-macro-spherulitic’ feldspars grew &#039;&#039;in situ&#039;&#039;, possibly from a hydrous feldspathic magma (Excursion 4; Donaldson &#039;&#039;et al.&#039;&#039;, 1973). Other cases of &#039;&#039;in-situ &#039;&#039;crystallisation are apparent in the CI and around Harris where radiating crystals of olivine reach lengths of up to several tens of centimetres (cf. [[Media:EGS_RUM_07.jpg| (See image)]]).</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>A distinctive structure is found in feldspathic peridotites north-east of Loch MacIver (Loch an Dornabac). Radiating, bifurcating crystals of plagioclase up to 40 cm in length, enclosing myriads of minute olivine crystals, occur in seaweed-like masses as much as 1 m in diameter, scattered through the normal feldspathic peridotite. These ‘poikilo-macro-spherulitic’ feldspars grew &#039;&#039;in situ&#039;&#039;, possibly from a hydrous feldspathic magma (Excursion 4; Donaldson &#039;&#039;et al.&#039;&#039;, 1973). Other cases of &#039;&#039;in-situ &#039;&#039;crystallisation are apparent in the CI and around Harris where radiating crystals of olivine reach lengths of up to several tens of centimetres (cf. [[Media:EGS_RUM_07.jpg| (See image)]]).</div></td></tr> </table>

Scotfot http://earthwise-staging.bgs.ac.uk/index.php?title=Paleocene_geology_of_Rum&diff=24312&oldid=prev 2015-12-22T21:29:06Z

<p><span dir="auto"><span class="autocomment">The Central Intrusion (CI)</span></span></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"> <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 22:29, 22 December 2015</td> </tr><tr><td colspan="2" class="diff-lineno" id="mw-diff-left-l83">Line 83:</td> <td colspan="2" class="diff-lineno">Line 83:</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 intrusion intrudes both the Eastern and Western layered intrusions [[Media:EGS_RUM_06.jpg| (See image)]], cutting a north–south swathe through them from the Long Loch to Papadil [[Media:EGS_RUM_02.jpg| (See image)]]. Although layered peridotites and troctolites are present, the intrusion is characterised by igneous breccias (Donaldson, 1973). The breccias occur in approximately north–south zones, tens to hundreds of metres in width, in which angular to subangular blocks and megablocks of peridotite and troctolite are embedded in predominantly feldspathic peridotite matrices (Volker and Upton, 1990). The troctolite clasts commonly display layering, which dips steeply in all directions although generally remaining fairly uniform in direction within a clast. Large or small individual clasts may record complex events involving crystal sedimentation, or the disruption and/or replacement of layered structures. In turn, layered structures in the enclosing peridotite record considerable disturbance and disruption, commonly suggesting that clasts and blocks subsided into incompetent surroundings, probably crystal mushes (Excursion 4). Elsewhere, layered structures may appear slumped, or disturbed by avalanches of ‘pebbly’ peridotite debris and by dropstones (Excursion 4). Much of the debris within the breccias resembles fragments of peridotite and troctolite from the earlier intrusions. West and south of the Long Loch, large rafts of troctolite are many tens of metres in extent. These megablocks have steeply dipping layering and were probably derived from the ELI. Layered structures are especially well developed in the troctolites and feldspathic peridotite exposed in the CI west of the Long Loch where slump structures, graded bedding, flame structures and other features suggesting ‘soft sediment’ deformation are much in evidence (Excursion 4). On the western slopes of Trollaval there is a progressive increase of dip in the ELI units when traced westwards, indicating that at some stage substantial masses of layered rocks sagged towards the Central Intrusion and probably broke off and subsided into it (cf. [[Media:EGS_RUM_06.jpg| (See image)]], (Figure43)&lt;nowiki&gt;; Volker and Upton, 1990; Emeleus &lt;/nowiki&gt;&#039;&#039;et al.&#039;&#039;, 1996; O’Driscoll &#039;&#039;et al.&#039;&#039;, 2007b).</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 intrusion intrudes both the Eastern and Western layered intrusions [[Media:EGS_RUM_06.jpg| (See image)]], cutting a north–south swathe through them from the Long Loch to Papadil [[Media:EGS_RUM_02.jpg| (See image)]]. Although layered peridotites and troctolites are present, the intrusion is characterised by igneous breccias (Donaldson, 1973). The breccias occur in approximately north–south zones, tens to hundreds of metres in width, in which angular to subangular blocks and megablocks of peridotite and troctolite are embedded in predominantly feldspathic peridotite matrices (Volker and Upton, 1990). The troctolite clasts commonly display layering, which dips steeply in all directions although generally remaining fairly uniform in direction within a clast. Large or small individual clasts may record complex events involving crystal sedimentation, or the disruption and/or replacement of layered structures. In turn, layered structures in the enclosing peridotite record considerable disturbance and disruption, commonly suggesting that clasts and blocks subsided into incompetent surroundings, probably crystal mushes (Excursion 4). Elsewhere, layered structures may appear slumped, or disturbed by avalanches of ‘pebbly’ peridotite debris and by dropstones (Excursion 4). Much of the debris within the breccias resembles fragments of peridotite and troctolite from the earlier intrusions. West and south of the Long Loch, large rafts of troctolite are many tens of metres in extent. These megablocks have steeply dipping layering and were probably derived from the ELI. Layered structures are especially well developed in the troctolites and feldspathic peridotite exposed in the CI west of the Long Loch where slump structures, graded bedding, flame structures and other features suggesting ‘soft sediment’ deformation are much in evidence (Excursion 4). On the western slopes of Trollaval there is a progressive increase of dip in the ELI units when traced westwards, indicating that at some stage substantial masses of layered rocks sagged towards the Central Intrusion and probably broke off and subsided into it (cf. [[Media:EGS_RUM_06.jpg| (See image)]], (Figure43)&lt;nowiki&gt;; Volker and Upton, 1990; Emeleus &lt;/nowiki&gt;&#039;&#039;et al.&#039;&#039;, 1996; O’Driscoll &#039;&#039;et al.&#039;&#039;, 2007b).</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>A distinctive structure is found in feldspathic peridotites north-east of Loch MacIver (Loch an Dornabac). Radiating, bifurcating crystals of plagioclase up to 40 cm in length, enclosing myriads of minute olivine crystals, occur in seaweed-like masses as much as 1 m in diameter, scattered through the normal feldspathic peridotite. These ‘poikilo-macro-spherulitic’ feldspars grew ''in situ'', possibly from a hydrous feldspathic magma (Excursion 4; Donaldson ''et al.'', 1973). Other cases of ''in-situ ''crystallisation are apparent in the CI and around Harris where radiating crystals of olivine reach lengths of up to several tens of centimetres (cf. <del style="font-weight: bold; text-decoration: none;">Figure 7</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>A distinctive structure is found in feldspathic peridotites north-east of Loch MacIver (Loch an Dornabac). Radiating, bifurcating crystals of plagioclase up to 40 cm in length, enclosing myriads of minute olivine crystals, occur in seaweed-like masses as much as 1 m in diameter, scattered through the normal feldspathic peridotite. These ‘poikilo-macro-spherulitic’ feldspars grew ''in situ'', possibly from a hydrous feldspathic magma (Excursion 4; Donaldson ''et al.'', 1973). Other cases of ''in-situ ''crystallisation are apparent in the CI and around Harris where radiating crystals of olivine reach lengths of up to several tens of centimetres (cf. <ins style="font-weight: bold; text-decoration: none;">[[Media:EGS_RUM_07.jpg| (See image)]]</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>During the original survey of Rum (Harker, 1908), many instances were found where the peridotites, troctolites and gabbros in the Layered Centre had been intruded by ‘granophyre’ (microgranite) and ‘felsite’ (porphyritic rhyodacite) from which it was concluded that the felsic rocks were the younger. At first sight the field evidence seems incontrovertible: wherever the mafic rocks are in contact with felsic rocks, there are spectacular breccias in which angular to subrounded mafic rocks are embedded in a network of veins and dykes of fine- to medium-grained microgranite that merge into the adjoining felsic rocks (Excursion 4). Many years later this interpretation was challenged and it is now known that the breccias are intrusion breccias, formed when hot mafic magmas chilled against but also melted or partially melted silicic country rocks. These were principally microgranite and porphyritic rhyodacite, but also sandstones and feldspathic gneisses (Hughes ''et al.'', 1957; Hughes, 1960a; Emeleus, 1997). The relatively low-temperature, rheomorphic felsic melts had burst through and fragmented the chilled and contracting margins of the mafic intrusions, producing (rare) sinuous, rounded liquid-liquid contacts where still-liquid mafic magma chilled against the relatively low-temperature felsic liquids, while in some instances, hybrid rocks were formed when heated felsic magma was able to mingle with mafic magma. Thus, the rocks of the Layered Centre clearly post-date the felsic rocks of Stage 1 [[Media:EGS_RUM_06.jpg| (See image)]], (<del style="font-weight: bold; text-decoration: none;">Figure8</del>). Additional supporting evidence comes from the minor intrusions; basaltic dykes and cone-sheets, which intrude the porphyritic rhyodacite, microgranite and feldspathic sandstones of the Torridon Group, can be followed into the contact zone where they underwent progressive thermal metamorphism and veining by thin silicic stringers. Ultimately, the dykes could no longer be supported by their weakened, partially melted felsic surrounding, whereupon they collapsed and disintegrated, contributing to the mafic blocks in the intrusion breccias. Some of the best examples come from fragmented cone-sheets in upper Dibidil (Hughes, 1960a) but convincing exposures may be examined in the contact zones at the south end of Meall Breac and Cnapan Breaca, at the ELI contact about 3 km east of Hallival, and at the WLI margin at the east end of Harris Bay (Excursions 2, 4b).</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>During the original survey of Rum (Harker, 1908), many instances were found where the peridotites, troctolites and gabbros in the Layered Centre had been intruded by ‘granophyre’ (microgranite) and ‘felsite’ (porphyritic rhyodacite) from which it was concluded that the felsic rocks were the younger. At first sight the field evidence seems incontrovertible: wherever the mafic rocks are in contact with felsic rocks, there are spectacular breccias in which angular to subrounded mafic rocks are embedded in a network of veins and dykes of fine- to medium-grained microgranite that merge into the adjoining felsic rocks (Excursion 4). Many years later this interpretation was challenged and it is now known that the breccias are intrusion breccias, formed when hot mafic magmas chilled against but also melted or partially melted silicic country rocks. These were principally microgranite and porphyritic rhyodacite, but also sandstones and feldspathic gneisses (Hughes ''et al.'', 1957; Hughes, 1960a; Emeleus, 1997). The relatively low-temperature, rheomorphic felsic melts had burst through and fragmented the chilled and contracting margins of the mafic intrusions, producing (rare) sinuous, rounded liquid-liquid contacts where still-liquid mafic magma chilled against the relatively low-temperature felsic liquids, while in some instances, hybrid rocks were formed when heated felsic magma was able to mingle with mafic magma. Thus, the rocks of the Layered Centre clearly post-date the felsic rocks of Stage 1 [[Media:EGS_RUM_06.jpg| (See image)]], (<ins style="font-weight: bold; text-decoration: none;">[[Media:EGS_RUM_08.jpg| (See image)]]</ins>). Additional supporting evidence comes from the minor intrusions; basaltic dykes and cone-sheets, which intrude the porphyritic rhyodacite, microgranite and feldspathic sandstones of the Torridon Group, can be followed into the contact zone where they underwent progressive thermal metamorphism and veining by thin silicic stringers. Ultimately, the dykes could no longer be supported by their weakened, partially melted felsic surrounding, whereupon they collapsed and disintegrated, contributing to the mafic blocks in the intrusion breccias. Some of the best examples come from fragmented cone-sheets in upper Dibidil (Hughes, 1960a) but convincing exposures may be examined in the contact zones at the south end of Meall Breac and Cnapan Breaca, at the ELI contact about 3 km east of Hallival, and at the WLI margin at the east end of Harris Bay (Excursions 2, 4b).</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 scenario outlined above provides an explanation for the absence of good chilled margins to the constituents of the Layered Centre; they were simply destroyed during formation of the intrusion breccias (but see Greenwood &#039;&#039;et al.&#039;&#039;, 1990). The problem is a general one throughout the Hebridean Igneous Province so that the most promising localities to search for good chills (possibly representing rapidly cooled parental magma) are at gabbro/basalt lava contacts, which are lacking on Rum. The problem of the parental magma or magmas of the Layered Centre has exercised investigators since the original survey (e.g. Harker, 1908; Brown, 1956; Emeleus, 1997 and references therein), with the present consensus favouring a magnesium-rich basalt, possibly most closely represented by rare picritic dykes that post-date the Layered Centre (Upton &#039;&#039;et al.&#039;&#039;, 2002).</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 scenario outlined above provides an explanation for the absence of good chilled margins to the constituents of the Layered Centre; they were simply destroyed during formation of the intrusion breccias (but see Greenwood &#039;&#039;et al.&#039;&#039;, 1990). The problem is a general one throughout the Hebridean Igneous Province so that the most promising localities to search for good chills (possibly representing rapidly cooled parental magma) are at gabbro/basalt lava contacts, which are lacking on Rum. The problem of the parental magma or magmas of the Layered Centre has exercised investigators since the original survey (e.g. Harker, 1908; Brown, 1956; Emeleus, 1997 and references therein), with the present consensus favouring a magnesium-rich basalt, possibly most closely represented by rare picritic dykes that post-date the Layered Centre (Upton &#039;&#039;et al.&#039;&#039;, 2002).</div></td></tr> </table>

Scotfot http://earthwise-staging.bgs.ac.uk/index.php?title=Paleocene_geology_of_Rum&diff=24311&oldid=prev 2015-12-22T21:26:01Z

<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"> <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 22:26, 22 December 2015</td> </tr><tr><td colspan="2" class="diff-lineno" id="mw-diff-left-l4">Line 4:</td> <td colspan="2" class="diff-lineno">Line 4:</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:EGS_RUM_04a.jpg|thumbnail|Panoramic views of the Northern Marginal Zone and Southern Mountains Zone: A. Coire Dubh area with Cnapan Breaca and Hallival, viewed from the north-west. Rocks of the Northern Marginal Zone form the low foreground (Coire Dubh Breccia) and the pale crags and exposures on Cnapan Breaca (centre; rhyodacite ash flows). The base of the crags on Cnapan Breaca marks the position of bedded tuffs and fine-grained sandstone. The Marginal Gabbro of the Eastern Layered Intrusion forms the grassy area on the right-hand flank of Cnapan Breaca, and the terraced slopes leading up to Hallival mark the positions of ‘allivalite’ (bytownite troctolite) in layered units in this intrusion. ]]</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:EGS_RUM_04a.jpg|thumbnail|Panoramic views of the Northern Marginal Zone and Southern Mountains Zone: A. Coire Dubh area with Cnapan Breaca and Hallival, viewed from the north-west. Rocks of the Northern Marginal Zone form the low foreground (Coire Dubh Breccia) and the pale crags and exposures on Cnapan Breaca (centre; rhyodacite ash flows). The base of the crags on Cnapan Breaca marks the position of bedded tuffs and fine-grained sandstone. The Marginal Gabbro of the Eastern Layered Intrusion forms the grassy area on the right-hand flank of Cnapan Breaca, and the terraced slopes leading up to Hallival mark the positions of ‘allivalite’ (bytownite troctolite) in layered units in this intrusion. ]]</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:EGS_RUM_04b.jpg|thumbnail|Panoramic views of the Northern Marginal Zone and Southern Mountains Zone: B. Dibidil river valley. Rhyodacite ignimbrite sheets and sedimentary breccias make up the back wall of Nameless Corrie and the ridge to Ainshval on the left of the photograph. Layered units in the Eastern Layered Intrusion form the distinctive peak of Trollaval in the far centre. Faulted Lewisian gneisses and Torridonian sandstones crop out along the foreshore to the right.]]</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:EGS_RUM_04b.jpg|thumbnail|Panoramic views of the Northern Marginal Zone and Southern Mountains Zone: B. Dibidil river valley. Rhyodacite ignimbrite sheets and sedimentary breccias make up the back wall of Nameless Corrie and the ridge to Ainshval on the left of the photograph. Layered units in the Eastern Layered Intrusion form the distinctive peak of Trollaval in the far centre. Faulted Lewisian gneisses and Torridonian sandstones crop out along the foreshore to the right.]]</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;">[[File:EGS_RUM_07.jpg|thumbnail|Harrisitic olivines in the Central Intrusion. Individual crystals may reach over 60 cm in length. See text for details.]]</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:EGS_RUM_02.jpg|thumbnail|Simplified geological map of Rum and adjacent islands.]]</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:EGS_RUM_02.jpg|thumbnail|Simplified geological map of Rum and adjacent islands.]]</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:EGS_RUM_09.jpg|thumbnail|Map of Rum showing the location of each excursion as a box.]]</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:EGS_RUM_09.jpg|thumbnail|Map of Rum showing the location of each excursion as a box.]]</div></td></tr> </table>

Scotfot http://earthwise-staging.bgs.ac.uk/index.php?title=Paleocene_geology_of_Rum&diff=24310&oldid=prev 2015-12-22T21:22:39Z

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