The complex, herein named the Souter Head subvolcanic complex (SHSC), is hosted by Dalradian semi-pelites of the Southern Highland Group and intrudes the sillimanite core of Barrovian metamorphism in NE Scotland (Kneller & Gillen Reference Kneller, Gillen, Trewin, Kneller and Gillen1987; Stephenson & Gould Reference Stephenson and Gould1995). It is exposed on sea cliffs about 6km S of Aberdeen (Figs 1, 2a, b). While exposure inland is virtually non-existent, the coastal strip presents a near perfectly exposed transect about 0.1 by 1km. It reveals a multistage history of repeated intrusion, breccia formation, hydrothermal activity, mineralisation and faulting.
Figure 1 Geological map of the Souter Head subvolcanic complex. Inset: regional location of Souter Head.
Figure 2
(a) View northwards from Souter Head to Burnbanks Haven. Outcrops of xenolithic granite, breccia, Burnbanks granite and a dolerite pillar can be seen. Inlet in foreground contains a dolerite dyke (see Fig. 1 for detailed geology). (b) Intrusive contact between pink outer Bunstane granite (G) and grey Dalradian metasediment (M). The granite sheets are generally concordant with the dominant fabric in the metasediments. Cove village is in the distance. (c) Breccia composed of randomly orientated metasediment clasts (M) with granite matrix (G). Later quartz (Q) infilling cavities and fractures. (d) Breccia (B) composed mainly of metasediment clasts with rare rounded granite clast (G) cut by pink quartz porphyry dyke (P). (e) Breccia (B) cut by pink felsite dyke ca.5m thick (F). Note large raft of metasediment (MR) (Fig. 1, NJ 0190 9625). (f) Pink xenolithic granite. Xenoliths of grey partially digested metasediment. (g) Pegmatite dyke (pink mineral K-feldspar) cutting inner non-xenolithic granite and both faulted against breccia. (h) Faulted contact between breccia and non-xenolithic granite intruded by quartz porphyry. Early linear alteration zone with quartz veins cutting granite from left to right. All cut by late molybdenite-bearing quartz veins (QM) and associated alteration from top to bottom centre. Rounded pink cores of granite and porphyry upstanding relative to grey altered rock. Quartz vein in (j) is continuation of vein at top centre. (i) Explanatory sketch for (h). (j) Molybdenite-bearing group 2 quartz vein cutting breccia (B) looking S. Inner non-xenolithic granite in background (G) (marked in Fig. 3). (h) shows a continuation of this vein to the south. (k) Linear alteration zone with quartz veins (Q) in non-xenolithic granite faulted against breccia (B). Fresh granite (FG) cores upstanding and surrounded by altered granite (AG).
Previous work has described aspects of the geology, intrusive history, geochemistry, hydrothermal fluids, alteration and mineralisation (Porteous Reference Porteous1973; Kneller & Gillen Reference Kneller, Gillen, Trewin, Kneller and Gillen1987; Lowry Reference Lowry1991). In 2013, the mineralisation and hydrothermal alteration throughout the complex were examined as part of a regional study of gold (Au) mineralisation in the Caledonides of northern Britain (Mark et al. Reference Mark, Rice, Fallick, Trewin, Lee, Boyce and Lee2011; Rice et al. Reference Rice, Mark, Selby and Hill2012, Reference Rice, Mark, Selby, Neilson and Davidheiser-Kroll2016) and some minor Au anomalies were discovered.
This led to a detailed study of the SHSC, which has shown it to be Ordovician rather than Late Caledonian in age, and the only subvolcanic complex of this age known in the Grampian terrane (Mark et al. Reference Mark, Rice and Condon2019). This paper provides the first comprehensive description of the geology, quartz veining, hydrothermal alteration, geochemistry of the intrusives and mineralisation, and presents a model for the evolution of the complex.
1. Regional (NE Scotland) geological setting
The dominant rock types in NE Scotland are Neoproterozoic metasediments of the Dalradian Supergroup (Strachan et al. Reference Strachan, Smith, Harris, Fettes and Trewin2002). The sediments were deposited on the passive margin of the Laurentian continent and deformed and metamorphosed in the Ordovician following collision with an island arc and crustal fragments (the Grampian event of the Caledonian Orogeny; Strachan et al. Reference Strachan, Smith, Harris, Fettes and Trewin2002). During this event the metasediments were intruded by syn- and late-orogenic (mainly) S-type granitic and basic magmas (Oliver Reference Oliver2001; Strachan et al. Reference Strachan, Smith, Harris, Fettes and Trewin2002; Oliver et al. Reference Oliver, Wilde and Wan2008). Four phases of deformation are commonly recognised in NE Scotland, of which the first three include the main compressional and nappe-building phases. It is the classic area for Barrovian- and Buchan-style metamorphism (Strachan et al. Reference Strachan, Smith, Harris, Fettes and Trewin2002).
The final closure of the Iapetus Ocean in the Silurian introduced a period of continental sedimentation and extensive, mainly granitic, igneous activity (the Newer Granites) extending into the late Devonian. NE Scotland has been largely emergent from the Devonian to the present day, although there may have been a late Cretaceous marine transgression (Harker Reference Harker and Trewin2002). Dolerite dykes of late Carboniferous age are widely distributed and cut the SHSC (Read et al. Reference Read, Browne, Stephenson, Upton and Trewin2002).
2. Geology of the SHSC
2.1. Igneous lithologies and field relationships
The dominant rock types are breccia and red two-mica granites. Minor intrusive phases comprise quartz porphyry, pegmatite, felsite and dolerite, which are present as dykes, sills and pipe-like bodies. The contacts between the dominant rock types are mainly faulted, but in a few places original contacts are preserved. The intrusive complex is composed of outer two-mica granites separated by faults from an inner sequence. The former show intrusive relationships with Dalradian country rocks of the Aberdeen Formation (Munro Reference Munro1986), but the contact between the latter and the Dalradian rocks is not exposed. The relative timing of crystallisation for the inner sequence can be established from field relationships to be, from oldest to youngest: breccia, two-mica granite, pegmatite, quartz porphyry and felsite and, finally, dolerite. Apart from dolerite, all intrusives are cut by quartz veins. These relationships are illustrated and described in the following sections. The SHSC lacks a tectonic foliation and, therefore, emplacement postdates the main episodes of deformation (D1–3) in NE Scotland.
2.2. The outer granites
These previously unrecognised granites, referred to as the Burnbanks (northern contact) and Bunstane (southern contact) granites, are in faulted contact with breccia at the margins of the inner sequence and extend for a few 100m to an intrusive contact with the metasediments (Fig. 1). The intrusive contacts are not readily accessible, but can be viewed from a distance in the cliffs. They are sharp and consist of sheets of granite generally concordant with the dominant (composite) fabric in the metasediments (Fig. 2b). The Burnbanks granite can be examined by an old landing stage accessed with care by a steep path down the cliffs; it is red, medium-grained and contains quartz, albite, microcline, muscovite and biotite, with accessory apatite, pyrite, chalcopyrite, rutile, ilmenite, monazite and zircon. The feldspars are strongly sericitised and the quartz shows undulose extinction. It also contains abundant, elongate, orientated xenoliths of metasediment. The Bunstane granite can only be accessed by boat and was not sampled. The outer granites are considered to be part of the SHSC on the basis of their close spatial and symmetrical relationship to the inner sequence and the similar petrography and age (Mark et al. Reference Mark, Rice and Condon2019) of the Burnbanks granite to the inner sequence.
2.3. The inner sequence
2.3.1. Breccia
The presence of breccia bodies is unique amongst the Ordovician granites of NE Scotland. They are found as three main masses in the northern, central and southern parts of the Souter Head complex (Fig. 1). The southern outer contact is steep and faulted against the Bunstane granite. Large (20m-scale), rotated blocks of metasediment form a marginal zone that extends for about 100m, separating the granite from a finer-grained breccia. The northern outer contact against the Burnbanks granite is sharp and steep and can be accessed in Burnbanks Haven. Contacts between breccia and the inner granites are typically straight, steep and faulted. However, in places, the original contacts are preserved (e.g., NJ 9620 0182) and show continuation (1–5m-scale) between inner granite and the granite matrix of the breccia, demonstrating that these granites intrude and postdate the breccia.
The breccia clasts are mainly semi-pelite, with rare (occasionally foliated) granite, amphibolite and vein quartz (Figs 2c, d). Clasts are typically angular with a few rounded clasts of granite, and poorly sorted. Most are in the 10–20cm-scale, but clasts up to 1m are common and there are a few larger rafts of metasediment up to 30m across (Figs 1, 2e). The orientation of the composite fabric in the metasediment and the foliation in granite clasts is typically random. In places, elongated clasts (e.g., amphibolite) show preferred orientation.
In the southern part of the complex the breccia is mainly clast-supported, whereas in the northern part the breccia is often matrix supported. Here the matrix consists of granite or pegmatite or quartz and contains rare miarolitic cavities with pyrite, calcite and molybdenite (Porteous Reference Porteous1973).
The breccia is interpreted as forming by the explosive release of volatiles from an underlying magma chamber, which shattered the country rock, as evidenced by rotated angular and rounded clasts. The presence of granite matrix in places suggests the bottom of the breccia column is exposed. Such breccias are classified as igneous cemented breccias or intrusion breccias and are common in subvolcanic stocks forming at levels in the range 1–10km (Sillitoe Reference Sillitoe1985; Seedorf et al. Reference Seedorf, Dilles, Proffett, Einaudi, Zurcher, Stavast, Johnson, Barton, Hedenquist, Thompson, Goldfarb and Richards2005).
2.3.2. The inner granites
These are found as two masses separated by breccia (Fig. 1). The northern mass contains a weak and patchy foliation and abundant xenoliths, and is interpreted as a contact facies (Fig. 2f). The foliation is defined by biotite, which is enclosed by other minerals displaying an igneous texture and is interpreted as a magmatic foliation (Paterson et al. Reference Paterson, Vernon and Tobisch1989). The southern block lacks both foliation and xenoliths. Marked variation in foliation occurs across E–W structures in the northern mass (e.g., NJ 9617 0185) and may reflect later rotation along these structures. Xenoliths are mainly composed of semi-pelite with rare amphibolite. They range up to 20m in diameter with variable shape and degree of assimilation. The density of xenoliths decreases towards the southern contact.
The granites are red, medium-grained and composed of quartz, showing weak undulose extinction, oligoclase, orthoclase, muscovite and biotite. There is also moderate sericitisation of feldspar and weak chloritisation of biotite. Accessory minerals include apatite, zircon, monazite, garnet and magnetite. The southern granite mass also contains finely disseminated pyrite (with inclusions of pyrrhotite and galena) and microcavities containing epidote and barite. The presence of muscovite and garnet indicates that these granites are strongly peraluminous.
2.3.3. Pegmatite
Pegmatites are unfoliated and composed of quartz, red K-feldspar, muscovite and biotite. They occur as small 1–5m-scale irregular bodies and lenses, and as linear veins up to 90cm wide that can be traced for up to 70m along strike (Figs 1, 2g). The veins strike between N–S and NNE–SSW and are mainly found cutting the inner granites, whereas the irregular bodies typically occur in breccia.
2.3.4. Quartz porphyry
Red quartz porphyry is mainly found cutting breccia as linear and anastomosing dykes (up to 1.5m wide) with a predominant NW–SE orientation (Fig. 2d). It is essentially restricted to the central breccia body. In one locality (NJ 9616 0173) the quartz porphyry intrudes along the faulted contact between non-xenolithic granite, pegmatite and breccia, and thus postdates all three (Figs 1, 2h, i). The phenocrysts are mainly quartz (up to 2mm) with undulose extinction, microcline and albite (both up to 0.5mm), with small amounts (<1%) of biotite and muscovite. The matrix contains the same minerals, but muscovite is more common, together with sparse manganese–iron garnet. There are also trace amounts of biotite, monazite, xenotime and zircon.
2.3.5. Felsite
Red felsite occurs as dykes reaching up to 5m thick (Fig. 2e), which are cut by N–S vertical and easterly dipping quartz veins. The main minerals in a fine-grained groundmass are quartz, sodic plagioclase, K-feldspar and minor muscovite. K-feldspar occurs as sector-zoned microphenocrysts and also in lace-textured, radiating intergrowths with quartz. There are accessory amounts of monazite, apatite, rutile and zircon. Pyrite, sericite and kaolinite alteration of feldspar are locally common. Some of the coarser muscovite may be primary. The felsites are post-breccia and pre-quartz veins and, thus, of a comparable age to the SHSC. However, felsites have geochemical differences (see Section 4.1) and occur outwith the complex (e.g., Porteous Reference Porteous1973) and may be unrelated to it.
2.3.6. Dolerite
There are small exposures of dolerite dykes (up to 5m wide) throughout the complex. They cut all the main rock types and felsite, lack quartz veins and are not significantly hydrothermally altered. The dykes have similar NNE–SSW and E–W orientations to dolerite dykes outcropping along the coast near Souter Head and to Carboniferous quartz dolerite dykes found elsewhere in Aberdeenshire (Stephenson & Gould Reference Stephenson and Gould1995). They are considered to be Carboniferous quartz dolerites (Kneller & Gillen Reference Kneller, Gillen, Trewin, Kneller and Gillen1987) and are not considered further herein.
2.3.7. Quartz veins
Quartz veins and attendant hydrothermal alteration are an important component of the complex (Fig. 3). All the main rock units and felsite and quartz porphyry are cut by quartz veins and affected by hydrothermal alteration to a varying extent. The quartz veins are generally straight-sided, massive and lack vugs, and they fall into two main groups. The earliest (group 1) comprises veins occurring within linear alteration zones, principally cutting the non-xenolithic granite and predating the quartz porphyry. These veins will be discussed in Section 2.3.8. The second (group 2) and most abundant consists of veins, which postdate the porphyry and cut the main rock units and the contacts between them (Figs 2h–j). This second group consists mainly of two sets of N–S-striking veins, one vertical and the other dipping easterly at a shallow angle, a minor E–W-orientated set and two NE–SW striking veins (Fig. 4). The order of emplacement from oldest to youngest is (1) N–S vertical; (2) N–S easterly dipping; and (3) E–W. The two N–S-orientated sets are best developed cutting the granites where, for example, ten easterly dipping veins (1–2cm thick) were recorded in a 100m traverse across the non-xenolithic granite.
Figure 3 Distribution of hydrothermal alteration and main quartz veins in the SHSC.
Figure 4 Orientation of group 2 quartz veins. Most fall into two sets: N–S vertical and N–S dipping E.
The N–S vertical veins are up to 50cm thick and the largest can be traced for at least 125m. They contain sparse K-feldspar and pyrite cubes. The N–S easterly dipping set are up to 20cm thick and contain occasional pyrite-rich lenses. These veins cut all main rock units. The E–W set is thin (up to 5cm) and contains quartz only. One of the NE–SW striking veins is 30cm thick and contains thin margin-parallel bands and clusters of muscovite and molybdenite (Fig. 2j). It can be traced for over 50m and cuts breccia, non-xenolithic granite and quartz porphyry (Fig. 2h, i).
2.3.8. Hydrothermal alteration
This is widespread and linked to quartz veining (Fig. 3). The most intense alteration occurs in numerous linear vertical zones in the non-xenolithic granite associated with group 1 quartz veins (Fig. 2h, i, k). The zones are orientated N–S and NNE–SSW, and are typically up to 4m wide but are more extensive at intersections. They are characterised by stockwork veining, thin cm-scale zone parallel vertical (group 1) quartz veins and intense argillic (kaolinite) alteration. In places, granite in the zones is intensely shattered so that only mineral fragments, mainly quartz and micas, can be recognised. All feldspar has been altered to kaolinite, which dominates the fine-grained matrix. Typically, the alteration zones are truncated at faulted breccia contacts (Fig. 2k), but in places the largest zones extend for a few metres into the breccia. The alteration zones associated with the group 2 quartz veins are narrow (up to 1m), patchy, less intense and lack stockwork veining. The main alteration mineral is sericite rather than kaolinite. Away from all veins, weak alteration is pervasive and widespread and comprises sericite, kaolinite, chlorite, pyrite, epidote and barite.
2.3.9. Minerals of economic interest
Molybdenite is the only mineral of potential economic interest, found mainly in quartz veins, with minor amounts in the breccia accompanying calcite within miarolitic cavities (Porteous Reference Porteous1973) and as coatings on fractures. Quartz vein-hosted molybdenite occurs with pyrite in N–S easterly dipping veins and in thin veins in NNE–SSW alteration zones, but is most abundant in the single NE–SW-striking vein (Fig. 2j). Molybdenite is confined to the central part of the complex.
2.3.10. Field relations between the breccia and inner granites
These have proved controversial in the past and are critically important for reconstructing the events leading to the formation of the SHSC. The non-xenolithic granite has been interpreted as a large block in the breccia (Munro Reference Munro1986) or as an intrusive body extending into the breccia (Porteous Reference Porteous1973; Lowry Reference Lowry1991). The presence of transitional contacts between granite and the granite matrix of the breccia supports the latter interpretation. The occurrence of a weak and patchy foliation in the xenolithic granite, which varies in orientation across E–W-trending linear structures, led Porteous (Reference Porteous1973) and Lowry (Reference Lowry1991) to interpret this granite mass as three large clasts hosted by breccia (i.e., the breccia postdates the granite). However, this is not supported by transitional contacts (recognised by Lowry Reference Lowry1991) (e.g., NJ 9620 0182), which indicate that the granites are intruding and, therefore, postdate the breccia. The rotation of the foliation across structures may be due to subsequent deformation that preceded pegmatite emplacement.
3. Structure
Although the contacts of the outer granites with the country rocks are intrusive (Fig. 2b), the internal contacts between the dominant rock types, granite and breccia are steep and generally faulted. The complex is strongly fractured along two main directions, E–W and N–S, best seen in the granites. The coastal topography is strongly influenced by these and other fracture sets, e.g., the well-defined narrow NNE–SSW inlets and the steep E–W faces of the inlets forming Souter Head itself (Figs 1, 2a). The various dykes, sills and quartz veins show varying orientations. Thus, pegmatites are N–S to NNE–SSW, porphyries are NW–SE and E–W, felsites are N–S and NW–SE, dolerite dykes NNE–SSW and E–W, linear alteration zones N–S and NNE–SSW and quartz veins mainly N–S. These variations (dolerite dykes excepted) reflect changing stress regimes possibly linked to rapid exhumation (Mark et al. Reference Mark, Rice and Condon2019).
In the absence of slickensides and offset structures, the sense and amount of movement along the faults cannot be determined. An exception is a right lateral wrench fault (NJ 9605 0172) that displaces a vertical felsite dyke by about 20m and is sealed by a N–S quartz vein (Fig. 1). All significant movement along granite–breccia contacts ceased before emplacement of quartz porphyry and group 2 quartz veins. These show limited deformation and, therefore, most of the structural features in the complex are of Ordovician age. Post-Ordovician deformation involved reactivation of some NNE and EW structures during the Permo-Carboniferous and emplacement of dolerite dykes.
4. Geochemistry
The purposes of the geochemical analysis were: (1) to assist in the description and classification of this magmatic-hydrothermal system; (2) combined with field data, to assess the economic potential of the SHSC; and (3) to compare the granitic rocks in the SHSC with others in the Grampian terrane to assess the potential of the region for further mineralisation of this type. A representative sample of the various rock types from the inner sequence, together with hydrothermally altered granite and quartz veins, were analysed for major elements, rare-earth elements (REEs) and trace elements (Table 1). A composite sample of chips from outcrops of the breccia–granite matrix with hydrothermal quartz was analysed for trace elements only.
Table 1 Souter Head major elements, rare-earth elements (REEs) and trace elements (all ppm except Au ppb and S %). Abbreviations: NXG = non-xenolithic granite; XG = xenolithic granite; Peg = pegmatite; QP = quartz porphyry; Dol = dolerite; S vein = sulphide lens in Group 2 quartz vein; Mo vein = main molybdenite vein; AltNXG = granite from linear alteration zone; Bx matrix = igneous matrix from intrusion breccia (analysed for trace elements only); N/A = not analysed. Selected bulk crust values from Rudnick & Gao (Reference Rudnick, Gao, Holland and Turekian2003) in ppm for As (2.5), Bi (0.18), Mo (0.8), Pb (11) and in ppb for Au (1.3). Analyses by ALS Minerals, Loughrea, Co. Galway.
4.1. Fresh rock
All the intrusives are silica- and alkali-rich, with silicon dioxide (SiO2) and potassium oxide (K2O)+sodium oxide (Na2O) values in the ranges 70–78% and 6–9%, respectively (Table 1). Apart from aluminium oxide (Al2O3) (13.7–15.1%), no other major oxide exceeds 3.07%. The Souter Head suite is all strongly peraluminous (i.e., Al2O3/CaO + Na2O + K2O > 1.1).
Multi-element variation patterns for the inner granites show typical granitic characteristics when normalised against mantle compositions, i.e., a background of increasing right-to-left enrichment and the commonly observed troughs for niobium (Nb), strontium (Sr), phosphorus (P) and titanium (Ti) (Fig. 5a, b). The latter probably reflect fractionation by mineral phases such as plagioclase, biotite and apatite at some time during the history of the magma or of its source (Halliday et al. Reference Halliday, Stephens and Harmon1981; Halliday & Stephens Reference Halliday and Stephens1984; Tarney & Jones Reference Tarney and Jones1994). When the same suite of elements is normalised against bulk crust (not shown) values lie close to 1.0 (range 0.3–4.4, mean 1.7; bulk crust values from Rudnick & Gao Reference Rudnick, Gao, Holland and Turekian2003).
Figure 5 Multi-element variation diagrams for the SHSC. (a, b) Normalised against primitive mantle values from Lyubetskaya & Korenaga (Reference Lyubetskaya and Korenaga2007). Elements are arranged in order of increasing incompatibility (right to left) with respect to the mantle source (Sun & McDonough Reference Sun and McDonough1989). The figures represent the integrated effects of all the processes that have contributed to the formation of the granites and, generally, these cannot be individually identified. (c) Normalised against chondrite values from Korotev et al. Reference Korotev, Ziegler, Jolliff, Irving and Bunch2009. (d) Comparison of the non-xenolithic granite from Souter Head with the Aberdeen granite (Ordovician) and Late Caledonian granites (Tarney & Jones, Reference Tarney and Jones1994, fig. 8).
All units show enrichment in light rare-earth elements (LREE) and the strongest enrichments occur in the inner granites, probably reflecting the presence of more apatite and monazite (highest phosphorus pentoxide (P2O5) values; Table 1; Fig. 5c).
The multi-element pattern of the inner granites is similar to that of the nearby Ordovician Aberdeen granite and different to those of the Late Caledonian granites of the eastern Grampians, which have more pronounced troughs (Fig. 5d).
Pegmatite is more depleted in thorium (Th), uranium (U), Nb, LREE, Sr and zirconium (Zr) than the inner granites, probably reflecting increased fractionation of plagioclase, biotite, rutile, phosphates and zircon (Fig. 5a, c).
The most obvious differences in the suite are between the youngest member, the porphyry, and the other members. It shows marked troughs in barium (Ba), Sr, europium (Eu) and Ti, and a flatter REE profile probably representing further fractionation of feldspar, rutile and phosphates (Fig. 5b, c). The porphyry contains the highest levels of sodium (Na), rubidium (Rb) and heavy rare-earth elements (possibly hosted by groundmass garnet).
The felsite pattern is most like the inner granites, but is smoother and has only one strong trough (Ti) and the REE pattern is flatter, suggesting a different history (Fig. 5b, c). These geochemical differences, together with the regional distribution of felsite, suggest that, while of a similar age (see Section 2.3.5), it is not genetically related to the SHSC. Other felsites in the region, whose age is poorly constrained, may be Ordovician also.
4.2. Mineralisation and alteration
Pyrite lenses in the easterly dipping quartz veins contain anomalous quantities of As (109ppm), Bi (900ppm), Mo (4150ppm) and Au (60ppb) (Table 1). However, the only heavy metal found in anomalous quantities in the main quartz–molybdenite vein and the breccia–granite matrix is Mo at 3790 and 41ppm, respectively. The absence of heavy metals such as tin (Sn) and tungsten (W) is discussed later.
Non-xenolithic granite from a linear alteration zone has much less calcium oxide (CaO), Na2O and Sr, and higher loss on ignition (LOI) than outside the zone (Table 1). This reflects plagioclase replacement by kaolinite. Altered granite contains weakly anomalous As (31ppm), Mo (14ppm), W (5ppm) and Au (10ppb).
The remaining igneous rocks show no significant enrichments in the economically important elements noted in the veins or other potentially valuable elements such as copper (Cu) and zinc (Zn). There are scattered slightly higher levels compared to bulk crust of As, Au, Bi, Mo and lead (Pb) (Table 1). There is no strong evidence of a link between metal enrichment and fractionation; for example, the most fractionated rock, the quartz porphyry, is not enriched. More likely, the widespread hydrothermal alteration is probably responsible for these weak enrichments.
5. Discussion
5.1. The SHSC and the late-tectonic S-type granites of NE Scotland
The petrography, geochemistry, field relations and age of the SHSC clearly link it to the late-tectonic S-type granites of NE Scotland (Strachan et al. Reference Strachan, Smith, Harris, Fettes and Trewin2002). Specifically, these include the presence of two micas, peraluminous affinity, high silica content, similar trace element compositions, sharp contacts between outer granites and country rocks and numerous partially digested xenoliths (Tarney & Jones Reference Tarney and Jones1994; Strachan et al. Reference Strachan, Smith, Harris, Fettes and Trewin2002; Appleby et al. Reference Appleby, Gillespie, Graham, Hinton, Oliver and Kelly2010). A unique feature of this complex is the presence of subvolcanic intrusion breccias.
Various features of the SHSC in common with other granites of this group are consistent with the dominant involvement of continental crust in its formation. These include common partially digested metasediment xenoliths, high silica content, strongly peraluminous nature and rock/bulk crust ratios for many trace elements close to one. Appleby et al. (Reference Appleby, Gillespie, Graham, Hinton, Oliver and Kelly2010) have argued for an additional infracrustal component in the Nigg Bay granite 5km N of the SHSC. The dominant crustal component in the magmas and emplacement during rapid exhumation (Mark et al. Reference Mark, Rice and Condon2019) suggest that decompressional melting of the upper crust was a key factor in melt production (Oliver Reference Oliver2001).
5.2. Unique preservation of the upper levels of the igneous complex
Souter Head is the only Ordovician granitic complex known in the Grampian terrane, where the upper levels are preserved. It is also close to Late Caledonian granites (Mount Battock and Hill of Fare, Fig. 6), which are more deeply eroded. This paradox could be explained by pre-Devonian movements on the nearby Dee fault and perhaps partly by downfaulting following collapse of the magma chamber roof (see Section 5.3). The truncation of the Aberdeen granite against this fault (Fig. 6) is consistent with significant downthrow to the S. There was later reverse movement on this fault to preserve Devonian sediments around Aberdeen.
Figure 6 Relationship of the SHSC to the Aberdeen granite, nearest Late Caledonian granites and the Dee and Highland Boundary Faults.
5.3. Magmatic-hydrothermal evolution of the complex
The excellent exposures of contact relationships in the coastal transect permit a cross-section of the complex (Fig. 7) and the magmatic-hydrothermal evolution of the complex to be reconstructed in some detail (Fig. 8a–f). Rapid exhumation (Mark et al. Reference Mark, Rice and Condon2019) may have been partly responsible for the repeated fracturing and explosive activity described in the following sections. The evolutionary sequence presented here requires the inner granites to postdate the intrusive breccia (see Section 2.3.1) and interprets the Burnbanks and Bunstane granites and granite clasts in the breccias as remnants of an early carapace.
Figure 7 Cross-section of the SHSC. Quartz veins omitted for clarity.
Figure 8 Evolution of the SHSC. (a) Emplacement of a peraluminous granite magma in the upper crust. Volatiles collect in the roof. (b) Magma chamber explodes with formation of breccia bodies. (c) Chamber roof and breccias collapse into chamber. Magma invades blocks of breccia. Superstructure omitted for clarity. (d) System cools and new chamber forms at depth. Further movements fracture the roof. Fractures filled by volatile-rich fluid to form pegmatites and linear alteration zones and minor molybdenite mineralisation. (e) Further cooling and new chamber forms. Fractionation generates the quartz porphyry magma. (f) Cooling continues, N–S fracturing, hydrothermal activity and formation of group 2 quartz veins and Mo–Bi–As–Au mineralisation. Hydrothermal activity possibly linked to deeper chamber.
5.3.1. Stage 1
Emplacement of a peraluminous granite magma in the upper crust and carapace formation (Fig. 8a). During cooling, volatiles collected in the magma chamber roof, which eventually exploded, forming large breccia bodies (Fig. 8b). As fluid pressures subsided, the roof and breccias collapsed into the chamber. Blocks of breccia were invaded by magma to give a partial igneous matrix (Fig. 8c). This magma cooled to form the inner granites. The present distribution of breccia units reflects this collapse, with later adjustments straightening the contacts (Figs 1, 7). The evidence for the early age of this event is the sealing and crosscutting of contacts by porphyry and quartz veins.
5.3.2. Stage 2
Following cooling and reforming of the chamber roof it was refractured along N–S and NNE–SSW directions. Fractures were best developed in granite due to its greater competency. Residual volatile-rich portions of this magma were injected into fractures to form pegmatites and linear alteration zones (Fig. 8d). Volatile-rich magma also invaded breccia to form small irregular bodies of pegmatite. Whereas pegmatites represent passive injection of fluids, the linear alteration zones record the injection of high-pressure fluids from a breached cupola. These caused hydraulic fracturing and intense alteration along the fractures. Later fluids produced quartz veins and minor Mo mineralisation. This episode of volatile release resulted in further collapse of the chamber and adjustments along granite–breccia contacts causing truncation of pegmatites and linear alteration zones (Fig. 2g, k).
5.3.3. Stage 3
New chamber established in which strong crystal fractionation occurred to generate quartz porphyry magma. The chamber was disrupted by NW–SE and E–W fractures into which magma was intruded (Fig. 8e). The porphyry intruded a major breccia–granite contact and marked the end of movement along this contact (Fig. 2h, i).
5.3.4. Stage 4
The complex cooled rapidly, possibly caused by rapid exhumation (Mark et al. Reference Mark, Rice and Condon2019), before further complex-wide fracturing and multiple episodes of hydrothermal activity, possibly linked to a deeper chamber (Fig. 8f). N–S quartz veins cut some of the main breccia–granite contacts, showing that movement had ceased along these. This stage marks the end of magmatic and hydrothermal activity, which lasted about 1Ma (Mark et al. Reference Mark, Rice and Condon2019)
5.4. Classification of mineralisation
The styles and location of Mo mineralisation, composition of intrusives and evidence of progressive fractionation indicate a granite-related vein-type deposit (Lowry Reference Lowry1991; Cerny et al. Reference Cerny, Blevin, Cuney, London, Hedenquist, Thompson, Goldfarb and Richards2005). Specifically, the styles are Mo occurring in quartz veins within granite-hosted alteration zones and also in breccia-hosted veins near to granite.
According to Cerny et al. (Reference Cerny, Blevin, Cuney, London, Hedenquist, Thompson, Goldfarb and Richards2005), granite-related systems are typically emplaced at depths of 1.5–5km. Intrusion breccia, various brittle features and porphyritic textures in the SHSC are consistent with these depths. Dominant kaolinite alteration in the linear alteration zones as opposed to muscovite is atypical of these deposits. However, muscovite may have been replaced by kaolinite during a younger thermal event at ca.405Ma linked to nearby Late Caledonian granites (Fig. 6) (Mark et al. Reference Mark, Rice and Condon2019).
Quartz porphyry is the youngest known intrusion and several parameters – i.e., Rb/Sr and ferric oxide (Fe2O3)/ferrous oxide (FeO) ratios of 21.3 and 0.8 respectively, the presence of magnetite and low levels of Sn and W – indicate that the SHSC is in the most oxidised and most evolved category of this class, where, typically, Mo is exclusively concentrated (Cerny et al. Reference Cerny, Blevin, Cuney, London, Hedenquist, Thompson, Goldfarb and Richards2005, fig. 7).
In addition to Mo, small quantities of Au, As and Bi are found in quartz–pyrite veins at Souter Head. Significant concentrations of these metals occur in other granite-related systems, where magmato-hydrothermal processes may have been similar. For example, at Timbarra in Australia, Au and Mo are concentrated by fractional crystallisation of a magnetite-bearing, peraluminous granite magma (Mustard Reference Mustard2001; Mustard et al. Reference Mustard, Ulrich, Kamenetsky and Mernagh2006).
The SHSC is a rare example of Ordovician hydrothermal mineralisation in the Grampian terrane, and the only known example of granite-related mineralisation of this age in this terrane. Quartz-vein-hosted Au–Mo mineralisation of similar age occurs at Curraghinalt in northern Ireland, but there is no known coeval intrusive activity and it is classified as an orogenic Au deposit (Rice et al. Reference Rice, Mark, Selby, Neilson and Davidheiser-Kroll2016).
5.5. Exploration potential of the SHSC and surrounding area
Certain features suggest that the SHSC is prospective for additional Mo and possibly Au mineralisation. These are the large size, lack of exposure, volatile-rich nature and abundant quartz veining. Specifically, the complex could host porphyry-Mo-style stockwork mineralisation (Seedorf et al. Reference Seedorf, Dilles, Proffett, Einaudi, Zurcher, Stavast, Johnson, Barton, Hedenquist, Thompson, Goldfarb and Richards2005) at depth and Au mineralisation in the roof of underlying pluton(s) or disseminated in breccias or in quartz vein complexes.
In a regional context, the period ca.470Ma in the Grampian terrane favoured the generation of large mineralised hydrothermal systems in the upper crust. Key factors were uplift and extension, increasing crustal permeability and magmas accessing the crust along major structures to provide sources of heat and metals (Ashcroft et al. Reference Ashcroft, Kneller, Leslie and Munro1984; Viete et al. Reference Viete, Richards, Lister, Oliver, Banks, Law, Butler, Holdsworth, Krabbendam and Strachan2010; Mark et al. Reference Mark, Rice and Condon2019). Despite deep levels of erosion over much of the terrane, making the preservation of such systems unlikely, the SHSC shows that in favourable circumstances they have survived. Exploration for similar systems to the SHSC should focus, therefore, on areas containing S-type granites, quartz veins and breccias associated with inferred downfaulting such as the sector between the Dee fault and the Highland Boundary fault (Fig. 6).
6. Conclusions
The SHSC is a large late-orogenic intrusive complex showing multiple stages of faulting, magma and breccia intrusion and hydrothermal activity. It was emplaced during a period of rapid exhumation, which may have facilitated repeated faulting, explosive release of volatiles and rapid cooling of the system. The unique preservation of an Ordovician subvolcanic complex in the Grampian terrane could be explained by putative pre-Devonian movements on the nearby Dee fault.
Complex formation was initiated by shallow emplacement of a peraluminous granite magma, explosive release of volatiles and formation of breccias. As the fluid flux subsided the breccia column collapsed into the magma chamber. Reforming of the chamber roof and subsequent rupture led to further volatile release along linear fracture zones and intense wall-rock alteration. Injection of fractionated quartz porphyry dykes is the final magmatic phase observed. Further fracturing and cooling was accompanied by extensive and episodic hydrothermal activity and Mo and Au–Bi–As mineralisation, marking the end of magmatic and hydrothermal activity. The Souter Head magmas were derived largely by melting of upper-crustal Dalradian metasediments. Crystal fractionation under oxidising conditions was responsible for the Mo and Au–As–Bi mineralisation. The mineralisation is a Mo-rich end member of the granite-related style of mineralisation.
The large size, multiple phases of hydrothermal activity and poor exposure indicate that the complex is prospective for further Mo and possibly Au mineralisation. Upper-crustal mineralisation of Ordovician age is preserved in the Grampian terrane in suitable tectonic settings and should be included in an exploration programme.
7. Acknowledgements
We would like to thank Jenny Johnston and Jamie Bowie (School of Geosciences, University of Aberdeen) for drafting the figures.
