OR/15/026 Structure - Revision history

Ajhil: /* Portsoy Shear Zone (PSZ) */

2019-12-03T11:22:49Z

Portsoy Shear Zone (PSZ)

← Older revision		Revision as of 12:22, 3 December 2019
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	The bulk of the evidence for the late stage movement history of the PSZ comes from the Banffshire coastal section and from the western edge of the Morven–Cabrach Pluton in the Glenbuchat district to the south-west. Steep anastomosing shear zones and the overall geometry of the zone suggest that transcurrent movements, probably dominantly dextral, postdated the earlier thrusting across the PSZ. Such movements probably occurred during the Early or Mid Ordovician, as the metamorphic mineralogies in the steep shear zones remained at amphibolite grade. Some of the steep shear zones in the Huntly and Knock plutons (see above), and those affecting the Succoth–Brown Hill and Portsoy mafic-ultramafic intrusions, may relate to this episode. Some of the smaller serpentinite lenses and pods may also have been emplaced during this phase.		The bulk of the evidence for the late stage movement history of the PSZ comes from the Banffshire coastal section and from the western edge of the Morven–Cabrach Pluton in the Glenbuchat district to the south-west. Steep anastomosing shear zones and the overall geometry of the zone suggest that transcurrent movements, probably dominantly dextral, postdated the earlier thrusting across the PSZ. Such movements probably occurred during the Early or Mid Ordovician, as the metamorphic mineralogies in the steep shear zones remained at amphibolite grade. Some of the steep shear zones in the Huntly and Knock plutons (see above), and those affecting the Succoth–Brown Hill and Portsoy mafic-ultramafic intrusions, may relate to this episode. Some of the smaller serpentinite lenses and pods may also have been emplaced during this phase.

	The age of intrusion of the North-east Grampian Basic Subsuite is dated at about 471 to 474  Ma (Dempster et al., 2002<ref name="Dempster 2002">DEMPSTER, T J, ROGERS, G, TANNER, P W G, BLUCK, B J, MUIR, R J, REDWOOD, S D, IRELAND, T R, and PATERSON, B A. 2002. Timing of deposition, orogenesis and glaciation within the Dalradian rocks of Scotland: constraints from U-Pb zircon ages. ''Journal of the Geological Society of London'', Vol. 159, 83–94. </ref>; Condon and Martin, cited in Oliver, 2008<ref name="Oliver 2008">OLIVER, G J H, WILDE, S A, and WAN, Y. 2008. Geochronology and geodynamics of Scottish granitoids from the late Neo-proterozoic break-up of Rodinia to Palaeozoic collision. ''Journal of the Geological Society of London'', Vol. 165, 661–674.</ref> as a personal communication; Carty, 2001; Carty et al., 2012). Pressure (P) and temperature (T) estimates based on the hornfels mineral assemblages (Droop and Charnley, 1985<ref name="Droop 1985"></ref>; Droop et al., 2003<ref name="Droop 2003">DROOP, G T R, CLEMENS, J D, and DALRYMPLE, D J. 2003. Processes and conditions during contact anatexis, melt escape and restite formation: the Huntly Gabbro Complex, NE Scotland. ''Journal of Petrology'', Vol. 44, 995–1029. </ref>) imply that emplacement occurred at a crustal depth of 15 to 18.5  km (4 to 5 kb). These P-T conditions are compatible with estimates derived from metamorphic mineral assemblages in some of the sheared zones immediately west of the Huntly intrusion (Beddoe-Stephens, 1990). The distribution of shear zones and the disordered, complex internal structure of the component elements of the Huntly and Knock plutons can be reconciled if their intrusion occurred coeval with shearing and associated deformation. This would explain:		The age of intrusion of the North-east Grampian Basic Subsuite is dated at about 471 to 474  Ma (Dempster et al., 2002<ref name="Dempster 2002">DEMPSTER, T J, ROGERS, G, TANNER, P W G, BLUCK, B J, MUIR, R J, REDWOOD, S D, IRELAND, T R, and PATERSON, B A. 2002. Timing of deposition, orogenesis and glaciation within the Dalradian rocks of Scotland: constraints from U-Pb zircon ages. ''Journal of the Geological Society of London'', Vol. 159, 83–94. </ref>; Condon and Martin, cited in Oliver, 2008<ref name="Oliver 2008">OLIVER, G J H, WILDE, S A, and WAN, Y. 2008. Geochronology and geodynamics of Scottish granitoids from the late Neo-proterozoic break-up of Rodinia to Palaeozoic collision. ''Journal of the Geological Society of London'', Vol. 165, 661–674.</ref> as a personal communication; Carty, 2001; Carty et al., 2012). Pressure (P) and temperature (T) estimates based on the hornfels mineral assemblages (Droop and Charnley, 1985<ref name="Droop 1985"></ref>; Droop et al., 2003<ref name="Droop 2003"></ref>) imply that emplacement occurred at a crustal depth of 15 to 18.5  km (4 to 5 kb). These P-T conditions are compatible with estimates derived from metamorphic mineral assemblages in some of the sheared zones immediately west of the Huntly intrusion (Beddoe-Stephens, 1990). The distribution of shear zones and the disordered, complex internal structure of the component elements of the Huntly and Knock plutons can be reconciled if their intrusion occurred coeval with shearing and associated deformation. This would explain:

	* the presence of Lower Zone cumulates at both the western and eastern margins of the Huntly Pluton, and the local occurrences of smaller cumulate lenses within the intrusions		* the presence of Lower Zone cumulates at both the western and eastern margins of the Huntly Pluton, and the local occurrences of smaller cumulate lenses within the intrusions

Ajhil: /* Portsoy Shear Zone (PSZ) */

2019-12-03T11:22:15Z

Portsoy Shear Zone (PSZ)

← Older revision		Revision as of 12:22, 3 December 2019
Line 56:		Line 56:
	The bulk of the evidence for the late stage movement history of the PSZ comes from the Banffshire coastal section and from the western edge of the Morven–Cabrach Pluton in the Glenbuchat district to the south-west. Steep anastomosing shear zones and the overall geometry of the zone suggest that transcurrent movements, probably dominantly dextral, postdated the earlier thrusting across the PSZ. Such movements probably occurred during the Early or Mid Ordovician, as the metamorphic mineralogies in the steep shear zones remained at amphibolite grade. Some of the steep shear zones in the Huntly and Knock plutons (see above), and those affecting the Succoth–Brown Hill and Portsoy mafic-ultramafic intrusions, may relate to this episode. Some of the smaller serpentinite lenses and pods may also have been emplaced during this phase.		The bulk of the evidence for the late stage movement history of the PSZ comes from the Banffshire coastal section and from the western edge of the Morven–Cabrach Pluton in the Glenbuchat district to the south-west. Steep anastomosing shear zones and the overall geometry of the zone suggest that transcurrent movements, probably dominantly dextral, postdated the earlier thrusting across the PSZ. Such movements probably occurred during the Early or Mid Ordovician, as the metamorphic mineralogies in the steep shear zones remained at amphibolite grade. Some of the steep shear zones in the Huntly and Knock plutons (see above), and those affecting the Succoth–Brown Hill and Portsoy mafic-ultramafic intrusions, may relate to this episode. Some of the smaller serpentinite lenses and pods may also have been emplaced during this phase.

	The age of intrusion of the North-east Grampian Basic Subsuite is dated at about 471 to 474  Ma (Dempster et al., 2002<ref name="Dempster 2002">DEMPSTER, T J, ROGERS, G, TANNER, P W G, BLUCK, B J, MUIR, R J, REDWOOD, S D, IRELAND, T R, and PATERSON, B A. 2002. Timing of deposition, orogenesis and glaciation within the Dalradian rocks of Scotland: constraints from U-Pb zircon ages. ''Journal of the Geological Society of London'', Vol. 159, 83–94. </ref>; Condon and Martin, cited in Oliver, 2008<ref name="Oliver 2008">OLIVER, G J H, WILDE, S A, and WAN, Y. 2008. Geochronology and geodynamics of Scottish granitoids from the late Neo-proterozoic break-up of Rodinia to Palaeozoic collision. ''Journal of the Geological Society of London'', Vol. 165, 661–674.</ref> as a personal communication; Carty, 2001; Carty et al., 2012). Pressure (P) and temperature (T) estimates based on the hornfels mineral assemblages (Droop and Charnley, 1985<ref name="Droop 1985">DROOP, G T R, and CHARNLEY, N. 1985. Comparative geobarometry of pelitic hornfelses associated with the newer gabbros: a preliminary study. ''Journal of the Geological Society of London'', Vol. 142, 53–62.</ref>; Droop et al., 2003<ref name="Droop 2003">DROOP, G T R, CLEMENS, J D, and DALRYMPLE, D J. 2003. Processes and conditions during contact anatexis, melt escape and restite formation: the Huntly Gabbro Complex, NE Scotland. ''Journal of Petrology'', Vol. 44, 995–1029. </ref>) imply that emplacement occurred at a crustal depth of 15 to 18.5  km (4 to 5 kb). These P-T conditions are compatible with estimates derived from metamorphic mineral assemblages in some of the sheared zones immediately west of the Huntly intrusion (Beddoe-Stephens, 1990). The distribution of shear zones and the disordered, complex internal structure of the component elements of the Huntly and Knock plutons can be reconciled if their intrusion occurred coeval with shearing and associated deformation. This would explain:		The age of intrusion of the North-east Grampian Basic Subsuite is dated at about 471 to 474  Ma (Dempster et al., 2002<ref name="Dempster 2002">DEMPSTER, T J, ROGERS, G, TANNER, P W G, BLUCK, B J, MUIR, R J, REDWOOD, S D, IRELAND, T R, and PATERSON, B A. 2002. Timing of deposition, orogenesis and glaciation within the Dalradian rocks of Scotland: constraints from U-Pb zircon ages. ''Journal of the Geological Society of London'', Vol. 159, 83–94. </ref>; Condon and Martin, cited in Oliver, 2008<ref name="Oliver 2008">OLIVER, G J H, WILDE, S A, and WAN, Y. 2008. Geochronology and geodynamics of Scottish granitoids from the late Neo-proterozoic break-up of Rodinia to Palaeozoic collision. ''Journal of the Geological Society of London'', Vol. 165, 661–674.</ref> as a personal communication; Carty, 2001; Carty et al., 2012). Pressure (P) and temperature (T) estimates based on the hornfels mineral assemblages (Droop and Charnley, 1985<ref name="Droop 1985"></ref>; Droop et al., 2003<ref name="Droop 2003">DROOP, G T R, CLEMENS, J D, and DALRYMPLE, D J. 2003. Processes and conditions during contact anatexis, melt escape and restite formation: the Huntly Gabbro Complex, NE Scotland. ''Journal of Petrology'', Vol. 44, 995–1029. </ref>) imply that emplacement occurred at a crustal depth of 15 to 18.5  km (4 to 5 kb). These P-T conditions are compatible with estimates derived from metamorphic mineral assemblages in some of the sheared zones immediately west of the Huntly intrusion (Beddoe-Stephens, 1990). The distribution of shear zones and the disordered, complex internal structure of the component elements of the Huntly and Knock plutons can be reconciled if their intrusion occurred coeval with shearing and associated deformation. This would explain:

	* the presence of Lower Zone cumulates at both the western and eastern margins of the Huntly Pluton, and the local occurrences of smaller cumulate lenses within the intrusions		* the presence of Lower Zone cumulates at both the western and eastern margins of the Huntly Pluton, and the local occurrences of smaller cumulate lenses within the intrusions

Ajhil: /* Nature of the PSZ and KSZ and their relation to deformation history */

2019-12-03T11:21:24Z

Nature of the PSZ and KSZ and their relation to deformation history

← Older revision		Revision as of 12:21, 3 December 2019
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	As noted above the Portsoy Shear Zone marks the site of an earlier lineament that has controlled the depositional pattern and thus the nature of the Dalradian stratigraphy, particularly within the Argyll Group. It also marks the western extent of geophysically distinct sub-Dalradian basement that may well reflect a fundamental difference between the Buchan area and the remainder of the Grampian Highlands. The structural and metamorphic history also differs considerably across the PSZ, although in the Huntly and Glenfiddich districts the boundary between the low P–high T Buchan-type metamorphism and the higher P–high T Barrovian-type metamorphism clearly lies to the west of the PSZ (Beddoe-Stephens, 1990<ref name="Beddoe 1990">BEDDOE-STEPHENS, B. 1990. Pressures and temperatures of Dalradian metamorphism and the andalusite-kyanite transformation in the north-east Grampians. ''Scottish Journal of Geology'', Vol. 26, 3–14. </ref>). Unfortunately, the lack of inland exposure, complexity of the igneous and sedimentary sequences in the PSZ, and spatially variable nature of the ductile and brittle structures related to the PSZ in the Huntly district, all serve only to pose more questions about the history of this zone and its role in the wider tectonic evolution of the area. The borehole and limited outcrop evidence show that deformation and shearing have accompanied and in part controlled emplacement of the Ordovician North-east Grampian Basic Subsuite, dated at about 474 to 472 Ma.		As noted above the Portsoy Shear Zone marks the site of an earlier lineament that has controlled the depositional pattern and thus the nature of the Dalradian stratigraphy, particularly within the Argyll Group. It also marks the western extent of geophysically distinct sub-Dalradian basement that may well reflect a fundamental difference between the Buchan area and the remainder of the Grampian Highlands. The structural and metamorphic history also differs considerably across the PSZ, although in the Huntly and Glenfiddich districts the boundary between the low P–high T Buchan-type metamorphism and the higher P–high T Barrovian-type metamorphism clearly lies to the west of the PSZ (Beddoe-Stephens, 1990<ref name="Beddoe 1990">BEDDOE-STEPHENS, B. 1990. Pressures and temperatures of Dalradian metamorphism and the andalusite-kyanite transformation in the north-east Grampians. ''Scottish Journal of Geology'', Vol. 26, 3–14. </ref>). Unfortunately, the lack of inland exposure, complexity of the igneous and sedimentary sequences in the PSZ, and spatially variable nature of the ductile and brittle structures related to the PSZ in the Huntly district, all serve only to pose more questions about the history of this zone and its role in the wider tectonic evolution of the area. The borehole and limited outcrop evidence show that deformation and shearing have accompanied and in part controlled emplacement of the Ordovician North-east Grampian Basic Subsuite, dated at about 474 to 472 Ma.

	Major westward shearing on the PSZ was proposed by Baker (1987)<ref name="Baker 1987">~~BAKER, A J. 1987. Models for the tectonothermal evolution of the eastern Dalradian of Scotland. Journal of Metamorphic Geology, Vol. 5, 101–118.~~ </ref> and Beddoe-Stephens (1990)<ref name="Beddoe 1990"></ref> to explain the marked change in metamorphic pressures demonstrated across the zone with the increase in pressure to the west of at least 2  kb. This westward translation is accepted here and must have taken place on a gently eastward dipping structure. Movement clearly post-dates the D1 deformation events both in the Buchan area and farther west as the D1 structures and metamorphic pattern are disrupted. If the movement along the PSZ and KSZ are linked, as seems likely, this thrust translation would relate to the main secondary deformation seen to the north-west of the PSZ. The steepening of the PSZ occurred subsequent to the main westward translation. However, a zircon U-Pb TIMS age of 468.5 ± 0.5  Ma from a variably deformed and steeply inclined pegmatitic granite vein at Portsoy Harbour implies that subvertical lateral movements occurred just after 470  Ma, i.e. only shortly after the main deformation. It is unclear as to how (or even whether) the secondary deformation found to the west of the PSZ relates to that to the east.		Major westward shearing on the PSZ was proposed by Baker (1987)<ref name="Baker 1987"></ref> and Beddoe-Stephens (1990)<ref name="Beddoe 1990"></ref> to explain the marked change in metamorphic pressures demonstrated across the zone with the increase in pressure to the west of at least 2  kb. This westward translation is accepted here and must have taken place on a gently eastward dipping structure. Movement clearly post-dates the D1 deformation events both in the Buchan area and farther west as the D1 structures and metamorphic pattern are disrupted. If the movement along the PSZ and KSZ are linked, as seems likely, this thrust translation would relate to the main secondary deformation seen to the north-west of the PSZ. The steepening of the PSZ occurred subsequent to the main westward translation. However, a zircon U-Pb TIMS age of 468.5 ± 0.5  Ma from a variably deformed and steeply inclined pegmatitic granite vein at Portsoy Harbour implies that subvertical lateral movements occurred just after 470  Ma, i.e. only shortly after the main deformation. It is unclear as to how (or even whether) the secondary deformation found to the west of the PSZ relates to that to the east.

	The discontinuous sheet-like nature of the porphyritic granite intrusions that comprise the approximately 600  Ma Keith–Portsoy Granite cannot be ascribed solely to the subsequent shearing and deformation. Emplacement seems to have been controlled by a pre-existing lineament, along which the lenticular granite sheets and pods were emplaced. The KSZ has subsequently reactivated this structure, which may well have been initiated during deposition of the Argyll Group sediments. This part of the Dalradian succession formed during a period of general crustal extension and localised instability, as shown by the presence of several small but deep rift basins, and the occurrence of widespread basic igneous activity. This was followed by continental break-up and the consequent opening of the Iapetus Ocean. Although emplacement of the Keith–Portsoy Granite was coeval with the extrusion of mafic lavas and intrusion of abundant dolerite sheets farther south-west around Tayvallich, regional considerations and global plate reconstructions suggest that the full rift–drift transition did not occur until around 570  Ma. Any small amounts of granitic magma generated by the crustal melting as continental extension progressively developed would likely migrate along pre-existing or newly formed lineaments.		The discontinuous sheet-like nature of the porphyritic granite intrusions that comprise the approximately 600  Ma Keith–Portsoy Granite cannot be ascribed solely to the subsequent shearing and deformation. Emplacement seems to have been controlled by a pre-existing lineament, along which the lenticular granite sheets and pods were emplaced. The KSZ has subsequently reactivated this structure, which may well have been initiated during deposition of the Argyll Group sediments. This part of the Dalradian succession formed during a period of general crustal extension and localised instability, as shown by the presence of several small but deep rift basins, and the occurrence of widespread basic igneous activity. This was followed by continental break-up and the consequent opening of the Iapetus Ocean. Although emplacement of the Keith–Portsoy Granite was coeval with the extrusion of mafic lavas and intrusion of abundant dolerite sheets farther south-west around Tayvallich, regional considerations and global plate reconstructions suggest that the full rift–drift transition did not occur until around 570  Ma. Any small amounts of granitic magma generated by the crustal melting as continental extension progressively developed would likely migrate along pre-existing or newly formed lineaments.

Ajhil at 11:20, 3 December 2019

2019-12-03T11:20:57Z

← Older revision		Revision as of 12:20, 3 December 2019
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	==Early deformation structures==		==Early deformation structures==
	The most common early structural feature in most parts of the Huntly and Turriff districts is a pervasive slaty or continuous cleavage or schistosity (S1) that is generally orientated near-parallel to the bedding. In the low-grade, greenschist-facies, turbiditic Southern Highland Group rocks that lie in the broad hinge zone of the Turriff Syncline, S1 is the only penetrative structure present, and in places it is axial planar to open to tight, medium-scale folding (F1) typically with gentle northerly plunging axes. This early folding is best seen on the Banffshire coast between Banff and Gardenstown, but is undoubtedly present in the lower parts of the Deveron valley in the Huntly district. An exception to this F1 fold pattern is found farther south-east in the gorge section of the River Ythan, east of Fyvie where lithologically similar Southern Highland Group mixed arenites and schistose semipelites, have been metamorphosed under lower amphibolite facies conditions to give cordierite and andalusite. A penetrative early cleavage (S1) is prominent, but there is little evidence of F1 folding. In contrast secondary folding is well seen. Farther west to the north of the Insch Pluton, Fettes (1968<ref name="Fettes 1968">Fettes, D J. 1968. Metamorphic structures of Dalradian rocks in north-east Scotland. Unpublished PhD thesis, University of Edinburgh.</ref>, 1970<ref name="Fettes 1970">~~FETTES, D J. 1970. The structural and metamorphic state of the Dalradian rocks and their bearing on the age of emplacement of the basic sheet. ''Scottish Journal of Geology'', Vol. 6, 108–118.~~ </ref>) documented the regional pattern of the S1 cleavage, and showed that it predated pluton emplacement. In the Aberchirder area S1 strikes approximately north–south, but as the Insch Pluton is approached it swings progressively clockwise, to strike east–west around the northern end of the Rhynie outlier. Farther west again at the western end of the Boganclogh sector of the Insch Pluton the S1 cleavage swings back anti-clockwise to strike north-east to south-west. Typically its dip ranges from about 75° to vertical.		The most common early structural feature in most parts of the Huntly and Turriff districts is a pervasive slaty or continuous cleavage or schistosity (S1) that is generally orientated near-parallel to the bedding. In the low-grade, greenschist-facies, turbiditic Southern Highland Group rocks that lie in the broad hinge zone of the Turriff Syncline, S1 is the only penetrative structure present, and in places it is axial planar to open to tight, medium-scale folding (F1) typically with gentle northerly plunging axes. This early folding is best seen on the Banffshire coast between Banff and Gardenstown, but is undoubtedly present in the lower parts of the Deveron valley in the Huntly district. An exception to this F1 fold pattern is found farther south-east in the gorge section of the River Ythan, east of Fyvie where lithologically similar Southern Highland Group mixed arenites and schistose semipelites, have been metamorphosed under lower amphibolite facies conditions to give cordierite and andalusite. A penetrative early cleavage (S1) is prominent, but there is little evidence of F1 folding. In contrast secondary folding is well seen. Farther west to the north of the Insch Pluton, Fettes (1968<ref name="Fettes 1968">Fettes, D J. 1968. Metamorphic structures of Dalradian rocks in north-east Scotland. Unpublished PhD thesis, University of Edinburgh.</ref>, 1970<ref name="Fettes 1970"></ref>) documented the regional pattern of the S1 cleavage, and showed that it predated pluton emplacement. In the Aberchirder area S1 strikes approximately north–south, but as the Insch Pluton is approached it swings progressively clockwise, to strike east–west around the northern end of the Rhynie outlier. Farther west again at the western end of the Boganclogh sector of the Insch Pluton the S1 cleavage swings back anti-clockwise to strike north-east to south-west. Typically its dip ranges from about 75° to vertical.

	The ‘Slate Hills’ lie along the northern flank of the Insch Pluton and stretch from Hill of Kirkney [NJ 502 315] in the west, via Wishach Hill and Hill of Foudland, to Hill of Tillymorgan [NJ 652 348] in the east. These hills are underlain by dominantly pelitic and semipelitic turbiditic units of the Macduff Formation (Southern Highland Group), termed the Hill of Foudland Pelite Member, and have an outcrop width of 1 to 2.5  km. The bulk of this pelitic unit has been hornfelsed by the Insch Pluton with ‘spotted slates’ typically developed. The ‘spots’ are mostly porphyroblasts of chlorite after biotite. Cordierite, andalusite and fibrolitic sillimanite are also present in the inner parts of the metamorphic aureole. The dominant structure in these pelitic rocks is normally a steep slaty S1 cleavage. Bedding is only seen locally and typically lies subparallel to the cleavage. It is difficult to recognise any small- and medium-scale F1 fold structures in these fine-grained slaty rocks but cleavage-bedding relationships do imply that they may be present in parts (see below for details). A second deformation phase, D2, is superimposed on rocks of the ‘Slate Hills’, overprinting the metamorphic aureole of the Insch Pluton (Fettes, 1970)<ref name="Fettes 1970"></ref>.		The ‘Slate Hills’ lie along the northern flank of the Insch Pluton and stretch from Hill of Kirkney [NJ 502 315] in the west, via Wishach Hill and Hill of Foudland, to Hill of Tillymorgan [NJ 652 348] in the east. These hills are underlain by dominantly pelitic and semipelitic turbiditic units of the Macduff Formation (Southern Highland Group), termed the Hill of Foudland Pelite Member, and have an outcrop width of 1 to 2.5  km. The bulk of this pelitic unit has been hornfelsed by the Insch Pluton with ‘spotted slates’ typically developed. The ‘spots’ are mostly porphyroblasts of chlorite after biotite. Cordierite, andalusite and fibrolitic sillimanite are also present in the inner parts of the metamorphic aureole. The dominant structure in these pelitic rocks is normally a steep slaty S1 cleavage. Bedding is only seen locally and typically lies subparallel to the cleavage. It is difficult to recognise any small- and medium-scale F1 fold structures in these fine-grained slaty rocks but cleavage-bedding relationships do imply that they may be present in parts (see below for details). A second deformation phase, D2, is superimposed on rocks of the ‘Slate Hills’, overprinting the metamorphic aureole of the Insch Pluton (Fettes, 1970)<ref name="Fettes 1970"></ref>.

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