TheHighland Boundary Fault is a majorfault zone[1] that traverses Scotland fromArran andHelensburgh on the west coast toStonehaven in the east. It separates two different geologicalterranes which give rise to two distinct physiographic terrains: theHighlands and theLowlands, and in most places it is recognisable as a change in topography. Where rivers cross the fault, they often pass through gorges, and the associated waterfalls can be a barrier tosalmon migration.[2]
The fault is believed to have formed in conjunction with the Strathmoresyncline to the south-east during theAcadian orogeny in atranspressive regime that caused the uplift of the Grampian block and a smallsinistral movement on the Highland Boundary Fault.[3][4]
One of the earliest and most prominent references to the Highland Boundary Fault was byGeorge Barrow in 1912 ʻOn the Geology of Lower Dee-side and the Southern Highland Borderʼ, which highlights the nature of the rocks accompanying the Highland Border and describes the mineral zones associated with metamorphism.[5] In the same publication, Barrow also outlines the ʻHighland Faultʼ and the areas where he believes there are planes of overthrust. Barrowʼs description of the structural nature of the rocks along the Highland Border suggests that rocks along both ends of the fault plane are indistinguishable from one another, with nobrecciation.
Aligned southwest to northeast fromLochranza on Arran, the Highland Boundary Fault bisectsBute and crosses the southeastern parts of theCowal andRosneath peninsulas, as it passes up theFirth of Clyde. It comes ashore near Helensburgh, then continues throughLoch Lomond. The loch islands ofInchmurrin,Creinch,Torrinch, andInchcailloch all lie on the Highland Boundary Fault.[6]From Loch Lomond the Highland Boundary Fault continues toAberfoyle, thenCallander,Comrie andCrieff. It then forms the northern boundary ofStrathmore and reaches the North Sea immediately north of Stonehaven near the ruinedChapel of St. Mary and St. Nathalan.[4][7]Aeromagnetic maps of Great Britain and Northern Ireland show that the Highland Boundary Fault can be traced fromIreland to the region ofGreenock. In these areas, the Highland Boundary Fault is seen to be dividing a northerly low area from a southerly high area.[8] The fault is often considered a terrane boundary: the Midland Valley terrane lies to the south whilst the Southern Highlands or Grampian terrane lies to the north[9]In 1970, Hall and Dagley identified the Highland Boundary Fault as coincident with a regional magnetic feature dividing a string of negative anomalies in the north from positive ones in the south.[8] On discovering this, Hall and Dagley concluded that the observed trend, which followed the length of theDalradian trough, transition from positive to negative anomalies. This linear feature of magnetic anomalies has since been referred to as the Fair Head–Clew Bay line.[10]
At present, it is believed that the Highland Boundary Fault was active during two main orogenic events associated with theCaledonian orogeny: theGrampian orogeny in theEarly Ordovician and theAcadian orogeny in theMiddle Devonian.[3] The fault allowed theMidland Valley to descend as a major rift by up to 4,000 m (13,000 ft) and there was subsequent vertical movement. This earlier vertical movement was later replaced by a horizontal shear. A complementary fault, theSouthern Uplands Fault, forms the southern boundary for the Central Lowlands.[3][4]The age of the Highland Boundary Fault has been inferred to be between Ordovician to middle Devonian and through several generations it has been interpreted as agraben-bounding normal fault, a major sinistralstrike-slip fault, a northwest-dippingreverse fault orterrane boundary.[3] The reason the precise nature of the fault is still unknown is because there is little evidence of a continuous fault plane on the surface. More recently, seismic activities marking the fault line have been analysed to show that the 2003 Aberfoyle earthquake had ahypocentre at 4 km (2+1⁄2 mi) depth and was caused by an oblique sinistral strike-slip fault withnormal movement. The fault plane was estimated to be dipping at 65° NW.[3]
To the north and west of the Highland Boundary Fault lie hard Precambrian and Cambrian metamorphic rocks: marine deposits metamorphosed toschists,phyllites andslates, namely the Dalradian Supergroup and theHighland Border Ophiolite suite.[3] To the south and east areOld Red Sandstone conglomerates and sandstones: softer, sedimentary rocks of the Devonian and Carboniferous periods.[4] Between these areas lie the quite different rocks of theHighland Border Complex (at one time called the Highland Boundary Complex[11]), a weakly metamorphosed sedimentary sequence of sandstones, lavas, limestones, mudstones and conglomerates. These make up a zone which is found discontinuously along the line of the fault and which is up to1.2 kilometres (3⁄4 mi) in width.[12]
The Dalradian Supergroup consists ofmetasedimentary rocks which underwent polyphase deformation and metamorphism during the Precambrian and early Paleozoic.[3][4] The oldest Dalradian rocks (theGrampian Group) were deformed and metamorphosed around 750 Ma. The deposition of younger Dalradian sediments continued until 590 Ma, when the sediments underwent transformation to thegreenschist facies during the Proterozoic and Ordovician.[3]
Modeling of gravity and magnetic data along the fault has confirmed the presence of an extensiveophiolite suite. The Dalradian metasedimentary rocks are overlain by anobductedophiolite that is continuous for at least several kilometres on either side of the Highland Boundary Fault. The models generated from magnetic data suggest that the ophiolite is only slightly displaced vertically by the fault.[3]
TheOld Red Sandstone is amagnafacies of red beds andlacustrine deposits from theLate Silurian to theCarboniferous. The NE segment of the Highland Boundary Fault is marked by an abrupt change in the dip of the Old Red Sandstone from around 20° to near-vertical and subsequently exposes the Old Red Sandstone basement.[3]
It is currently believed that there were two main displacement events along the Highland Boundary Fault: the Acadian, and the post-Acadian.[3][13][14]
Evidence for the Acadian displacement event is based on the geochemical study of detrital garnets in the Lower Old Red Sandstone on the Northern limb of theStrathmore Basin. These garnets were linked to those in isolated Dalradian sediments in the northwest, providing evidence for post-Early Devonian (Acadian) movement to be only few tens of kilometers.[13][14]
In addition, theLintrathenignimbrite, which is present at the base of the Lower Devonian sequence was traced along the fault and it was found that the displacement was both short and lateral.[3][13]
The post-Acadian movements are highlighted in the stratigraphy of the region. The Lower Old Red Sandstone is unconformably overlain by Upper Old Red Sandstone, where the Upper Old Red Sandstone is tilted close to the Highland Boundary Fault.[3]
The boundary is used as a natural barrier to prevent northwards movement of grey squirrels, thus protecting the only red squirrel population in the Highlands.[15]
