Polyphase Deformation of the High-Grade Metamorphic Rocks along the Neusspruit Shear Zone in the Kakamas Domain: Insights into the Processes during the Namaquan Orogeny at the Eastern Margin of the Namaqua Metamorphic Province, South Africa

: The central part of the Namaqua Metamorphic Province was subjected to intense deformation under high-grade metamorphic conditions up to granulite facies, but also shows greenschist facies overprints denoting the metamorphic nature during the 1.2–1.0 Ga Namaquan Orogeny. This study examines the structural development of the central Kakamas Domain of the eastern Namaqua Metamorphic Province, which has not been extensively studied previously. The compressional orogenic phase is associated with D 1 and D 2 deformation events during which northeast–southwest-directed shortening resulted in southwest-directed thrusting illustrated by an intra-domain thrust and southwest-verging isoclinal folds. The post-tectonic Friersdale Charnockite of the Keimoes Suite is emplaced during the D 3 deformation event. Late reactivation of the intra-domain thrust in the Kakamas Domain to form the Neusspruit Shear Zone during the D 4 event is of a monoclinic nature and is described as a deeply rooted structure with shear direction towards the east. This structure, together with the more local Neusberg Thrust Fault, forms part of an intensely ﬂattened narrow basin in the eastern Namaqua Metamorphic Province. Strain and vorticity indices suggest a transpressional shearing across the Neusspruit Shear Zone and adjacent regions probably initiated during the reactivation of the intra-domain thrust. The ~1.2 to 1.8 km-wide, northwest–southeast striking dextral-dominated Neusspruit Shear Zone constitutes a western regional boundary for the supracrustal Korannaland Group and is composed of steep, narrow zones of relatively high strain, characterised by ductile deformation and penetrative strain.


Introduction
The 1.3-1.0 Ga Namaqua-Natal Metamorphic Province of southern Africa is part of the global Grenvillian age orogenic belts [1][2][3][4][5][6]. It was involved in the formation of the Kalahari Craton [7] and was potentially associated with the assembly of the supercontinent Rodinia [8][9][10]. The Namaqua-Natal Metamorphic Province forms an arcuate belt stretching from the west coast of Namibia to the southeast coast of South Africa (e.g., [3,[11][12][13][14] and references therein). It is divided into two sectors, namely the western Namaqua and eastern Natal sectors [13]. The Namaqua Metamorphic Province or Namaqua Sector (Figure 1) is of interest in this study and is subdivided into subprovinces. Regional stratigraphic and structural studies have, however, confirmed that the subprovinces host a number of tectonostratigraphic domains distinguished based on tectonic history, metamorphic grade and lithostratigraphic criteria, and separated by regional scale structural discontinuities. Although there is no consensus on the number of, or names for, these domains, summaries  [13]). The position of the study area is indicated. Abbreviations: P-Pofadder.
The stratigraphy and structure of the Kakamas Domain are loosely defined compared to other domains to the west [39,40] and those closer to the Archean Kaapvaal Craton in the east [1,21]. The Kakamas Domain has seen comparatively little research done compared to more recent work to the west in southern Namibia [3,38]. Despite the presence of volcanogenic massive sulphide (VMS) deposits in the adjacent Areachap Domain, there is little to no known mineralisation in the Kakamas Domain, apart from the presence of pegmatites [16]. An early investigation in the Kakamas Domain by [41] focused on phacoliths of charnockitic monzogranite-porphyry of an area around Keimoes, which was later classified as the Friersdale Charnockite of the Keimoes Suite [16,22,37], and references therein. Another study [25], however, focused on the structural and metamorphic evolution of an area around Kakamas and Keimoes. More recently, Reference [6] investigated the structure and stratigraphy of an area near Kakamas. In addition, there have been several recent detailed geochemical and geochronological studies with regards to the Mesoproterozoic crustal evolution and emplacement ages of various syn-and/or post-tectonic intrusions in the Kakamas Domain [4,22,37,38,42,43]. There has, however, been little recent work done on the structural evolution of the Kakamas Domain.
In light of the investigations associated with the Kakamas Domain, this study concentrates on the understanding of the processes taking place at high-grade metamorphic conditions during the Namaqua Orogeny in an area east of the Neusspruit Shear Zone and south of the Orange River ( Figure 2). As the Neusspruit Shear Zone is a prominent intra-terrane shear zone within the Kakamas Domain, this paper contributes to the understanding of the structural-metamorphic development around such structures in the eastern Namaqua Sector.

Geological Setting
The Namaqua Metamorphic Province is subdivided into various subprovinces (Figures 1 and 2), defined by distinctive stratigraphic units bounded by structural discontinuities. The domains and subprovinces were variably deformed and metamorphosed during the 1.2-1.0 Ga Namaqua Orogeny. Although the precise geometry remains controversial, there is evidence that the rocks of the Gordonia Subprovince (comprising the Kakamas and Areachap domains- Figure 1) are stratigraphically and structurally distinct from those of the Bushmanland Subprovince to the west [24]. The Gordonia Subprovince is separated from the Kheis Terrane at its eastern boundary by the Brakbosch Fault east of 22 • E and along the Trooilapspan Shear Zone west of 22 • E ( Figure 2). The western boundary is along the Hartbees River Thrust Zone east of 20 • E and along the Swartrand Fault west of 20 • E [16,44] (Figure 2). The southern portion of the Gordonia Subprovince extends to the Kenhardt region, where it disappears beneath younger Palaeozoic cover rocks [13]. The Gordonia Subprovince is transected by Mesoproterozoic faults and shear zones trending mostly northwest-southeast (Figure 2), some of which are major structures of regional importance [1,5,6,13,16,25].
A close relationship between metamorphism and deformation is demonstrated in the Namaqua Sector, which is subjected to different types of tectonics [5]. In the west and south of the Namaqua Sector, metamorphic studies revealed anti-clockwise P-T-t paths [45] interpreted as convective heat transfer by crustal melting and intrusive magma, which thickened the crust [45,46], without crustal stacking [5]. Another study [47], however, proposed that anti-clockwise P-T-t paths are related to advective heat flow combined with intrusive magmatism during compression rather than extension. The central, eastern, and northern parts of the Namaqua Sector, by contrast, show clockwise P-T-t paths as a result of tectonic stacking, associated with advective heat transfer related to voluminous intrusive magma. This is reflected in the granulite facies conditions experienced by the Kakamas Domain, although the tectonic processes are linked to crustal extension [38,48,49].
The Kakamas Domain was first investigated by [50] when they published their memoir on the geology of an area around Kakamas. The Kakamas Domain consists of severely reworked Mesoproterozoic magmatic and supracrustal rocks [16,24,25,38], and was subjected to various tectonic events, including voluminous magmatic emplacement, thrusting, shearing, thickening, and uplift of the crustal sequence, due to a consistent stress regime with a general movement towards the Kaapvaal Craton [13,20,27]. Investigations to the west in the Bushmanland Subprovince [39,40,[51][52][53][54], and to the east in the Areachap Domain ( Figure 1) [55][56][57] have established the occurrence of base metal mineralization, which is not yet identified in the Kakamas Domain.
The Kakamas Domain was subjected to a polyphasic metamorphism comprising four distinguishable events. The first event (M 1 ) occurred at 1220-1180 Ma [48] and reached granulite facies conditions of high-T, low-P metamorphism with temperatures between 800 and 900 • C, and pressure of about 5 kbar [48]. Similar conditions were established in the Aggeneys Domain [58]. This event is related to the emplacement of various S-and A-type granitoids associated with anatexis in the metapelites [38,48].
The M 3 metamorphic event occurred at T =~350 • C and P =~2.5 kbar conditions [25], and has been interpreted as a retrogressive event, producing greenschist facies conditions, marked by the presence of secondary minerals such as muscovite, epidote, and chlorite in the supracrustal rocks [16,25]. It is therefore concluded that the geochronologic evidence points to the episodic nature of metamorphic events in the Kakamas Domain.
The Neusberg Mountain ( Figure 3) is underlain by highly deformed magmatic rocks metamorphosed to amphibolite to granulite facies conditions, along with calc-silicates, and feldspathic quartzites of the Korannaland Group [16,25,41,50]. This supracrustal succession is restricted to the Gordonia Subprovince and comprises metamorphosed sedimentary rocks [16] (Figure 3). The Neusberg Mountain occurs as a highly deformed northwesttrending belt, intruded by various granitoids. The area under discussion (Figures 2 and 3) has been described as a high-T, low-P type of metamorphic environment [25], where conditions decrease from granulite facies at its western boundary along the Hartbees River Thrust (T = 650-750 • C; P = 5 kbar) [60], to lower amphibolite facies in the east near Keimoes (T =~550 • C; P =~2 kbar) [61]. In addition, evidence of retrograde greenschist facies overprinting has been reported [16,25,60]. Petrographic and metamorphic investigations by [25,61], amongst others, emphasize the polyphase metamorphic nature of the Kakamas Domain. The Kakamas Domain underwent various deformation events. Previous investigations have identified four main deformation events in the Kakamas Domain during the 1.2-1.0 Ga Namaqua Orogeny, e.g., [6,16,25,26]; the correlation of these events on a regional scale remains, however, problematic. The early deformation event, D 1 , is recorded as compressional deformation at 1197 ± 5 Ma based on detrital zircon ages, supported by metamorphic ages at 1194 ± 23 Ma [20]. The planar fabric (S 1 ) in the pre-tectonic plutons (the Kakamas Suid Gneiss, Riemvasmaak Gneiss and Warm Zand leucogneiss) is defined by a foliation that is co-planar to the lithological banding and is attributed to large-scale transposition during D 1 [6,27,62]. The D 2 deformation event has been reported as the main folding phase and is expressed by the formation of tight to isoclinal subvertical northwest-trending F 2 folds and a regional axial planar fabric (S 2 ), which is parallel to the transposed S 0 /S 1 banding [6,16,25,63]. The D 2 deformation event is constrained to have occurred between~1155 Ma and 1100 Ma as it has been associated with syn-tectonic granite intrusions [38,42]. The subsequent D 3 deformation event is characterised by open east-west-trending F 3 folds and is associated with post-tectonic magmatism [35,42], illustrated by the emplacement of the Friersdale Charnockite at 1080 ± 13 Ma [43]. The D 4 deformation event is related to dextral strike-slip faulting along major regional shear zones and faults, e.g., [37,56], between 1040 and 1020 Ma [48,64].

Methodology
A two-pronged approach, addressing both the lithostratigraphy and structural analyses, was undertaken in this study. Sampling localities were selected based on accessibility and exposure in the field ( Figure 3). The outcrops of the supracrustal and plutonic rocks were described on the basis of field occurrence and hand specimen, as well as petrographically. Samples of the various gneisses and post-tectonic pluton were collected from relatively fresh homogenous outcrops in the study area ( Figure 3) for thin-section petrographic and microstructural analysis using a Zeiss petrographic microscope and an Olympus X-43 digital camera. Shear sense indicators in the Kakamas Suid Gneiss were assessed by cutting thin sections perpendicular to the foliation ( Figure 4F).
Published geological and structural maps were also used for examination and interpretation of geological features. Mapping was based on topographic and previously published geological maps, aerial-photographs, and digital aerial photos to develop a visual understanding and representation of the study area. The 1:250,000 scale 2820 Upington geological map [65] is used for the regional geology. The published 1:50,000 topographic map (2820 DD Koekoeb) from the Department of Mapping and Survey was used as the base map for the study area, where the geology was interpolated. The orthophoto-map series, at a scale of 1:10,000, combined with the aerial photographs and digital aerial photos, were used to interpret the geology and structures.
The structure observed in the study area consists of a macrofold stretching from the Neusberg (NM) to Vuurkop (VM) Mountains, respectively ( Figure 3). Rather than analysing the heterogeneously deformed macroscopic structure in the study area in one section, it is best understood by dividing the entire structure into three sub-areas where the individual structure can be described as homogeneously deformed ( Figure 3). Various strain features, such as fold axes, axial planes, and foliations, along with shear sense indicators, such as vorticity indicators, were observed and recorded. The fold axes were derived by plotting the poles using a π-diagram, and to do this accurately, we include the poles to planes around each hinge and not just the limbs of the fold. Their orientations were plotted stereographically using the software package Stereonet version 10.0 [66]. The orientations of the fold axis and main foliation plane were determined for each sub-area. The structure in each sub-area is classified based on the attributes of the fold axis and main foliation plane as described by [67]. Various geological and structural maps were compiled using the software packages Surfer version 16 and ArcMap version 10.3.1. Supplementary analytical datasets are given in the Table S1.

Lithostratigraphy
The stratigraphy of the area under consideration consists of supracrustal and plutonic rocks. In this study, detailed mapping revealed a complex distribution of the rocks, which are loosely characterised geochemically and ill-defined geochronologically in the literature. The stratigraphic nomenclature used in this study relates to that of [16,22,25,41,44,65,68]. The recognition of primary sedimentary structures can be a useful tool in the interpretation of severely deformed and metamorphosed rocks. Sedimentary features, such as bedding, gradation, lamination, trough cross-bedding, and the presence of pebbles are, therefore, important features to distinguish between different lithologies in the supracrustal succession and give an idea as to potential protoliths with the view to unravelling the depositional environment. The magmatic rocks were identified and differentiated by means of criteria such as the presence of augen, texture, mineralogy, and the presence of felsic and/or mafic xenoliths. The lithostratigraphy from both the supracrustal and plutonic rocks in the study area are described from the youngest to the oldest lithology based on available ages and field relationships ( Table 1). The contact rocks are also described.  (Table 1). These formations are part of the stratigraphic profile in Figure 4. The Biesie Poort Subgroup is made up of various formations as summarised by [16]. The Puntsit is the only formation of the Biesie Poort Subgroup identified in the study area.

Puntsit Formation
The Puntsit Formation has the widest distribution and is traced to the southern closure of the NM (Figure 3). It builds the topmost succession of the Vuurkop Mountain (VM), where it underlies a rocky ridge due to the presence of wollastonite-bearing calcareous rock. Wollastonite-bearing calcareous rocks occur sporadically between the Neusberg and Vuurkop ( Figure 3) as lenses of about 1.5 m length, and approximately 10 to 40 cm width. The wollastonite-bearing calcareous rock has an inequigranular texture and displays a flat-lying flow banding-like structure. They are white to greyish in colour with lath-shaped grains of 2-5 mm in length. Skarn occurs as small, brown to dark brown fine-grained patches within the formation to the west of the Neusberg (Figure 3). Where fresh, the skarn contains lenses of quartzite and patches of epidote.
The calc-silicate-rich quartzites are fine-to medium-grained and show a parting at irregularly spaced intervals parallel to the bedding. Primary sedimentary structures, such as bedding planes, are observed and are similar to those in the overlying feldspathic mica-rich quartzite. No crossbedding has been identified in the Puntsit Formation in the area under consideration. There is a sharp contact between the Puntsit Formation and the overlying Goede Hoop Formation. The contacts between the calc-silicate-rich quartzite and the intercalated amphibole schist ( Figure 4A) are commonly gradational. The amphibole schist is fine-grained, brown in colour, with bands varying in thickness from a few millimetres to about 10 cm. The prominent northwest-southeast trending foliation is concordant with the regional northwest-southeast structural trend in the calc-silicaterich quartzites.

Goede Hoop Formation
The Goede Hoop Formation comprises feldspathic mica-rich quartzite as defined by [16,68]. It exhibits a granoblastic texture and underlies prominent ridges to the east of the Neusspruit Shear Zone ( Figure 3). It is the youngest and uppermost formation of the Korannaland Group. Primary sedimentary structures, such as crossbedding ( Figure 4B), the presence of pebbles ( Figure 4C), and graded bedding ( Figure 4D) are locally preserved. Cross-bedded structures show a younging direction to the northeast defined by upwards fining cycles ( Figure 4D). The feldspathic mica-rich quartzite is medium-to coarse-grained, and, in a similar fashion to the calc-silicate-rich quartzite, also shows a parting at variously spaced intervals parallel to the foliation. The intrusive contact with the Friersdale Charnockite is characterised by a contact zone comprising biotite gneiss, which is mapped for a total length of about 200 m ( Figure 3). The biotite gneiss is medium-to coarse-grained and contains lenses of mafic composition of about 4 to 7 cm in size.

Plutonic Rocks
The plutonic rocks crop out as hills or large continuous rocks in the study area. The absolute age relations of the plutonic rocks in the area under consideration are unclear at present so that careful assessment of contact relationships is, therefore, required. The plutonic rocks are represented by the Kakamas Suid Gneiss, the 1156 ± 8 Ma to 1151 ± 14 Ma Riemvasmaak Gneiss ( [43]; which correlates to the 1155 ± 7 Ma Rooipad Granite of [4]), the Warm Zand leucogneiss, and the 1080 ± 13 Ma Friersdale Charnockite of the Keimoes Suite [22] (Figure 3). In this paper, the term used for continuity purposes will be Riemvasmaak Gneiss, after [16].   The basement on which the supracrustal rocks of the various domains were deposited is one of the enigmas in the Namaqua Sector. It was demonstrated that the basement could be anything in the range of 1.8-2.0 Ga in age [3,13,33,38,48,69]. In the study area, the supracrustal rocks are represented by the Korannaland Group.
It was established that the enigmatic basement for the supracrustal rocks of the Namaqua Sector is early to middle Orange River Orogeny crust of~1.7 Ga age [5]. The Orange River Orogeny basement stretches from the Kaapvaal Craton westwards underneath the Kakamas Domain and the Bushmanland Subprovince and appears as migmatitic rocks of low-P granulite facies in the western Bushmanland Subprovince, e.g., [3,5]. Isotopic studies on the migmatites and crustal xenoliths in the western Bushmanland Subprovince yielded ages of 1.9-1.7 Ga [70,71] confirming an elusive Paleoproterozoic-aged basement in the Namaqua Sector [5,72].

Kakamas Suid Gneiss
The Kakamas Suid Gneiss is present west of the Neusberg Mountain ( Figure 3). This lithology has not received much attention in the literature. A previous study [25] added it with their Wolfkop Formation, while [41] described the Kakamas Suid Gneiss as grey gneiss, based on its slightly elevated biotite content [16]. It displays a brown weathered colour ( Figure 4E) and is grey when fresh. It consists of quartz, orthoclase, biotite, hornblende, microcline, and plagioclase. It is well-foliated, medium-to coarse-grained, and exhibits an inequigranular fabric displaying an augen texture. It contains flattened and stretched quartz-feldspar aggregates of 2 to 4 cm in size, which define augen structures ( Figure 4E). The foliation is defined by the alignment of mafic minerals and the intermediate axis of the augen. The long axes of the augen lie within the foliation plane. Strong anastomosing foliation is well-defined ( Figure 4F). The presence of K-feldspar-dominated augen suggests an intrusive origin.

Riemvasmaak Gneiss
The Riemvasmaak Gneiss/Rooipad Granite ( [16] and [4], respectively) is identified by [16] as a variety of pink gneiss. The sharp contact with the Kakamas Suid Gneiss ( Figure 4G), the presence of xenoliths, and lit-par-lit contact relationships [6,16] suggest an intrusive origin. The pinkish Riemvasmaak Gneiss is medium-to coarse-grained, with a granoblastic texture, foliated, and contains alkali feldspar, quartz, biotite, hornblende, and plagioclase. Xenoliths with lenticular shape consist of fine-grained quartz, alkali feldspar, and biotite. The contacts with the surrounding gneisses are sharp and obscured in some places by Quaternary sand deposits. The contact with the calc-silicate-rich quartzite of the Puntsit Formation is sharp, which suggests it is younger than, and intrusive into, the supracrustal rocks. This then constrains the age of deposition of the Korannaland Group. An age of emplacement of 1151 ± 14 Ma was reported for the Riemvasmaak Gneiss [43], with the synonymous Rooipad Granite having an emplacement age of 1155 ± 7 Ma [4,6] further north of the study area in the Kakamas Domain.

Warm Zand Leucogneiss
The Warm Zand leucogneiss outcrops as a hill of exfoliated boulders ( Figure 4H) between the Neusberg and Vuurkop (Figure 3). A similar lithology was also identified in the Areachap Domain [72]. It has a brown weathered colour and is pink when fresh. It is fineto medium-grained, displays a granoblastic texture, and contains alkali feldspar, quartz, hornblende, and biotite in decreasing abundance. Foliation is faintly visible compared to the Kakamas Suid Gneiss due to this gneiss having a lower content of mafic minerals such as hornblende, biotite, and opaques. No mafic or felsic enclaves have been identified in the leucogneiss. The contacts with the other plutonic rocks and the supracrustal succession are covered by Quaternary sand deposits.

Friersdale Charnockite
The Friersdale Charnockite occurs as exfoliated boulders ( Figure 4I), and large and continuous outcrops in the northern, north-eastern, and eastern parts of the study area ( Figure 3). It intrudes the Puntsit and Goede Hoop Formations of the Korannaland Group in the study area. The weathered Friersdale Charnockite shows onion skin exfoliation. This lithology exhibits a grey to brown colour, is weakly foliated, and is medium-to coarsegrained displaying a granoblastic texture. It contains alkali feldspar, blue opalescent quartz, and biotite, along with lenses of felsic or mafic composition of about 3 to 10 cm in size ( Figure 4J). There is a sharp contact between the supracrustal rocks and the Friersdale Charnockite in the study area. In some places, the contact is delineated by a foliated biotite gneiss observed nowhere else in the area under consideration. The biotite gneiss has a granoblastic texture, which can be interpreted as a contact metamorphic effect. Mafic lenses in the biotite gneiss also occur in the Friersdale Charnockite but are not found in the supracrustal rocks. The foliation in the biotite gneiss and in the feldspathic mica-rich quartzite of the Goede Hoop Formation are concordant. The Friersdale Charnockite is emplaced at 1080 ± 13 Ma and classified as a late-to post-tectonic granite in the Kakamas Domain [22]. The presence of the Friersdale Charnockite as large and continuous outcrops and containing lenses of mafic and felsic composition suggest an intrusive origin.

Metamorphism
The metamorphic activity in the Kakamas Domain is a classic high-T and low-P type in the Namaqua Sector. The M 1 metamorphism is of granulite facies estimated at T = 800-900 • C and P =~5 kbar and occurred at 1220-1180 Ma [48]. Similar conditions were determined in the Riemvasmaak area [68] and also in the Central dome near Kakamas [25]. The M 2 metamorphic event occurred under slow cooling and heating episodes at near constant mid-crustal pressure conditions [48,59], associated with the emplacement of syn-tectonic granitoids between~1200 and 1150 Ma [38] in the Kakamas Domain [16]. The subsequent M 3 event occurred during the emplacement of voluminous post-tectonic granitoids of the Keimoes Suite between 1113-1080 Ma, e.g., [22,37,38] with estimated P-T conditions of T = 640-550 • C and P = 4.8 kbar [21,42,58] in the Kakamas Domain. The low-grade M 4 metamorphic event is expressed by the late growth of minerals such as epidote and muscovite, which occurred adjacent to the Neusspruit Shear Zone. Late-grown biotite at the expense of garnet was also identified by [25]. The metamorphic conditions were estimated at T =~350 • C and P =~2.5 kbar [25].

Neusberg Macrofold
The regions on the map marked as various sub-areas enclose the essential structural feature of that sub-area ( Figure 5). Each sub-area highlights a reasonable continuity of individual structure to distinguish the various stages of deformation that took place. Observations and related interpretations of structural patterns within each sub-area are compared and correlated in order to produce a common and comprehensive deformational history for the entire structure in the study area.

Structural Fabrics and Related Metamorphic Grade
Pervasive foliation was developed in the intrusive rocks and most of the supracrustal rocks. The planar fabric in the pre-tectonic plutons (S 1 ) is defined by a compositional banding, which is co-planar to the lithological foliation. The S 1 foliation is mainly defined by the transposition of the primary bedding (S 0 ) forming early F 1 isoclinal folding, which may be a tectonically produced surface (S 1 ) [6,25,62]. The S 1 foliation is identified as a shearrelated fabric in the supracrustal and intrusive rocks, and co-planar to the XY-plane of the strain ellipsoid, e.g., [73,74]. The L-fabric (L 2 ) is defined by elongated pebbles, sigmoidal quartz-feldspar grains, and mineral lineations. The pervasive penetrative foliation (S 2 ) is described as the axial planar fabric, with the implication that S 2 is also parallel to the co-planar S 0 /S 1 fabric ( Figure 6). The F 2 structure is an inclined plunging fold closure characterised by alternating lithologies along strike of the axial trace. D 1 and D 2 are therefore co-planar.   [16,25,48,59], highlighting a significant time span during which the crust reached its thermal peak related to the emplacement of syn-to posttectonic granites in the Kakamas Domain [38]. The S 2 fabric is regionally sub-horizontal except for the area where it undergoes rotation from sub-horizontal to vertical and is deformed by the later northwest-trending shear zone.

Sub-Area 1
Sub-area 1 is characterised by a closure ( Figure 7A) with its hinge closing towards the southeast with limbs dipping mostly towards the northeast ( Figure 7B). The stereonet of foliation S 1 /S 2 shows only one cluster of the poles to the planes ( Figure 8A, black solid dots) so that the limbs of the fold in sub-area 1 are parallel to each other, and the structure is described as an isoclinal fold. The main foliation plane dips 53 • towards 038 • ( Figure 8A, black great circle) describing a moderately inclined fold. The axial plane trends NW-SE, with the fold axis plunging 37 • towards 055 • ( Figure 8A, blue solid dot) describing a gently northeast plunging fold. The mesoscopic fold in the closure trends towards the southeast ( Figure 7E). The stretching lineations (L 2 ) plunge to the northeast ( Figure 8A, green dots) probably indicating layer parallel slip during folding. The younging direction of strata of the Korannaland Group in sub-area 1 is top-normal defining the southern closure of the Neusberg as a syncline ( Figure 7A,B).

Sub-Area 2
Sub-area 2 is characterised by a closure (Figure 7C,D) in the calc-silicate rocks of the Puntsit Formation closing towards the northwest ( Figure 7D). Similar to sub-area 1, the stereographic plot shows the main foliation plane dipping 40 • towards 043 • ( Figure 8B, pink great circle) describing a moderately inclined fold. Like in sub-area 1, the limbs of the fold in this sub-area are initially parallel to each other describing an isoclinal fold. The axial plane trens NW-SE and dips NE, with the fold axis in sub-area 2 plunging 45 • towards 060 • ( Figure 7B,E, red dot) describing a gently northeast plunging fold. The axial trace of the parasitic fold trends towards the northwest ( Figure 7F). The stretching lineations plunge to the northeast ( Figure 8B, brown dots). The younging of the strata of the Korannaland Group is also top-normal defining the structure in sub-area 2 as an anticline ( Figure 7F).

Sub-Area 3
Sub-area 3 is located between the Neusberg to the west and Vuurkop to the east. The parasitic folds in this sub-area indicate that the axial plane trends NW-SE ( Figure 7G), which is confirmed with data plotted on the stereogram ( Figure 8C). The stereographic plot shows two clusters with an interlimb angle of 105 • defining an open fold in sub-area 3 ( Figure 8C). The best fit girdle is illustrated by the ruby great circle. The axial plane dips 88 • towards 045 • and is trending 317-137 • ( Figure 8C, purple dashed great circle) describing an upright fold. The fold axis plunges 59 • towards 318 • ( Figure 8C, olive green dot) describing a gently northwest-plunging fold. Stretching lineations (L 2 ) were not observed in this sub-area. The structure between the NM and VM is a synformal structure.

Thrusting
Thrusting is developed along the Neusberg Thrust (Figure 8). This fault is a northwestsoutheast-striking structure dipping between 25 • and 75 • in a north-easterly direction. The Neusberg Thrust extends for approximately 3.5 km in length in the study area and has a footwall composed of calc-silicate and feldspathic mica-rich quartzites. The fault rock is comprised of breccias and defines a well-demarcated thrust zone ( Figure 9A). These cataclastic fault rocks contain angular clasts of metasedimentary rocks. The change of the dip orientation from the overall northeast-dipping to upright layers of feldspathic mica-rich quartzite ( Figure 9B) is interpreted to be the result of a thrust-fold developed in the hanging wall ramp. Along the Neusberg Thrust, the fault rock assemblage varies in thickness and can reach several meters along this fault. There is no complete thrust front preserved in the study area, but only the southwest-dipping overturned layers of the feldspathic mica-rich quartzite remained on the west side of a well-demarcated valley ( Figure 9C).

Shearing
The portion of the Neusspruit Shear Zone investigated in this study is over 10 km in length and obscured further south by aeolian and river sand deposits. Its trace is defined by a steep northeast-dipping, 1.2 to 1.8 km wide zone in the study area. This prominent northwest-striking structure is traced further south and north of the study area describing a gently undulating, but regionally consistent northwest-southeast trend. The Neusspruit Shear Zone forms the eastern limit of regional migmatisation and probably marks the western boundary of the Keimoes Suite granites [16], of which the Friersdale Charnockite, classified as a post-tectonic granite ( [37] and references therein), intruded the highly deformed supracrustal rocks. Under high-grade conditions, the ductile behaviour of the shear zone is shown by both quartz and feldspar that are deformed as elongate single crystals or aggregates of recrystallised grains ( Figure 10C). Horizontal displacement has amounted to between 8.3 km and 16.5 km dextrally [25,75]. Some normal dip-slip movement has also been reported to have occurred by [75]. This is confirmed by kinematic analysis (Section 4.5.2).

Shear Sense Indicators
Shear sense indicators are illustrated by small-scale structures that are used to determine the shear sense movement in the Neusspruit Shear Zone. They are meso-and microscopic structures from which the sense of relative displacement can be inferred in the shear zone. Such structures include shear bands, the progressive inflexion of the foliation, lozenge-shaped sigmoidal, asymmetric boudins, and isolated asymmetric objects. These shear sense indicators are observed in the XZ-planes perpendicular to the XY-plane and parallel to the mineral stretching lineations. The shear bands are identified in the Kakamas Suid Gneiss, with short and closely spaced mm-scale C shear bands developed obliquely with respect to the shear boundary ( Figure 10A). S-C fabrics in the Kakamas Suid Gneiss indicate a dextral shear sense of movement along the Neusspruit Shear Zone. Kinematic indicators, such as progressive dextral inflexion of the foliation at the contact with the shear bands also indicate dextral shear movement ( Figure 10B). The photomicrograph of the Kakamas Suid Gneiss shows a lozenge-shaped sigmoid containing recrystallised grains of quartz and feldspar ( Figure 10C). The mixture of fine-grained (40-200 µm) aggregates ( Figure 10C; top right side) is similar to a mortar texture, comprising tightly interlocking fine-to medium-grained crystals formed by crushing and recrystallisation of a pre-existing coarser grained rock, which is suggested as evidence of a high strain rate along the Neusspruit Shear Zone, and indicative of dynamic recrystallization in response to ductile deformation as described by [76].
The top and bottom parts of asymmetric boudins in the calc-silicate-rich quartzite ( Figure 10D) are subvertical with long axis plunging in the XY-plane indicating a subvertical sense of shearing along the Neusspruit Shear Zone. Isolated asymmetric objects occur in the calc-silicate-rich quartzite as mantled epidotised and/or chloritised plagioclase porphyroclasts ( Figure 10E). The core-object geometry shows recrystallization and rotation similar to that of delta (δ)-type mantled objects [76,77]. The plagioclase porphyroclast indicates a dextral shear sense of movement ( Figure 10E).

Kinematic Analysis
Shear zones play a major role in the deformation of the crust at a variety of scales, as expressions of strain localization during orogeny and rifting, and as reactivated structures [78]. An important characteristic of ductile shear zones is that the wall rocks are moved parallel to the shear zone boundary and that the magnitude of the movement exceeds any stretching or shortening within the wall rocks, e.g., [77]. In this study, the Neusspruit Shear Zone is bounded by deformed supracrustal wall rocks with laterally uniform fabrics. The Kakamas Suid Gneiss in the shear zone is intensely deformed and affected by vortical flow characterised by a vorticity vector ( Figure 10G). The XZ-plane, in which the vorticity indicators are observed, is normal to the vorticity vector and known also as the Vorticity Profile Plane (VPP) [79,80]. With deformed wall rock along the shear zone, the flow is described as simple shear [73], and the Vorticity Profile Plane is normal to the XY-plane (defined by the mylonitic foliation S M ; Figure 10F,G) and parallel to the stretching lineation (L M ) characteristics of monoclinic flow symmetry in the Neusspruit Shear Zone. Previous research [77] outlines the application of such characteristics for monoclinic flow symmetry for both undeformed and deformed wall rock in high-grade rocks.
Kinematic analysis using stereographic projections ( Figure 8F) displays the main mylonitic foliation S M ( Figure 8F; black great circle) dipping 73 • towards 050 • describing a steeply inclined structure. The main mylonitic foliation S M shows an approximately similar orientation to that of the main foliation plane in the isoclinal folds in the Neusberg Mountain and is steeply inclined as compared to the moderately inclined supracrustal rocks in the Neusberg. The main foliation on the XZ-plane ( Figure 8F; orange great circle) dips 74 • towards 140 • in the Neusspruit Shear Zone, and its interception with the main mylonitic foliation, S M , is illustrated by the small red triangle ( Figure 8F) plunging east, indicative of the shear direction of the shear zone, and therefore the direction of motion of crustal blocks along the shear zone. The stretching lineations, L M , in the shear zone plunge east ( Figure 8F, olive green dots) differently to the northeast-plunging stretching lineations ( Figure 8A,B, green and brown dots, respectively) in the Neusberg Mountain, indicative of reactivation.

Basement/Cover Stratigraphy
The basement in the Namaqua Sector is of Palaeoproterozoic age (1.8-1.7 Ga) and emplaced during the Orange River Orogeny [5,72], but has not been encountered in the study area. The ages of emplacement of the stratigraphically oldest rocks in the study area, such as the Kakamas Suid Gneiss and Warm Zand leucogneiss, have not yet been investigated. Only the timing of emplacement of the Riemvasmaak Gneiss and Friersdale Charnockite in the Kakamas Domain were investigated by [43] and [22], respectively, using the U-Pb zircon age method. The latter is classified as post-tectonic in the Namaqua Sector [16,22,37]. The other intrusive rocks in the study area show a strong pervasive fabric, implying that they must be at least pre-to syn-tectonic, which constrains their time of emplacement.
The timing of deposition of the metasedimentary rocks also remains speculative. They also have a pervasive S 2 fabric so their age of deposition must be constrained to be prior to the main deformation event implying that they were deposited during pre-to syn-tectonic times. The calc-silicate-rich quartzite of the Puntsit Formation is overlain by the feldspathic mica-rich quartzite of the Goede Hoop Formation, which is classified as the youngest metasedimentary formation. No cross-bedded structures were observed in the calc-silicate-rich quartzite but were identified in the feldspathic mica-rich quartzite ( Figure 4B). The younging of strata in the Goede Hoop Formation is defined by upwards fining cycles ( Figure 4D) with the younging direction towards the northeast of the isoclinal fold. The protolith for the calc-silicate-rich quartzite, with intercalations of amphibole schist, is likely to be of psammitic and calcareous composition, with intercalations of likely basaltic material. The feldspathic mica-rich quartzite is considered to have had a fluviatile type of material as a sedimentary precursor. The metasedimentary rocks were subsequently intensely metamorphosed and deformed during the Namaqua Orogeny.

Comparison of Sub-Areas
The regional crustal stacking due to the northeast-directed indentation of the eastern margin of the Namaqua Sector towards the Kaapvaal Craton, e.g., [27,81], became locked so that no further convergence could take place, resulting in a strike-slip motion along various northwest-southeast-trending shear zones and faults dissecting the Namaqua Sector into different structural domains (Figures 1 and 2). The structural features in the area under consideration are folding, a pervasive northeast-dipping foliation, a northwesterly trending shear zone, and a north-westerly trending thrust fault with vergence to the southwest. The north-easterly plunging moderately inclined isoclinal folds, which define a syncline in sub-area 1 (Figure 7A,B) and an anticline in sub-area 2 ( Figure 7C,D), respectively, define the Neusberg macrofold. Investigations by [25] and [6] also described the southern closure of the Neusberg Mountain as an inclined isoclinal fold. The Neusberg and Vuurkop Mountains are separated by a gently north-northwest plunging, and upright open fold defining a synformal structure in sub-area 3. The northwest-southeast orientation of the axial trace of the mesofold ( Figure 7E,F) from subareas 1 and 2, respectively, is similar to, but differs from, the north-south to northwest-southeast-oriented axial trace identified in the parasitic folds ( Figure 7G) of sub-area 3. The stretching lineations (L 1 ) are particularly well developed in sub-areas 1 and 2 and plunge north-easterly in the Neusberg macrofold but are non-existent in sub-area 3. The axial traces of the isoclinal folds in sub-areas 1 and 2 in the Neusberg macrofold are aligned with the Neusspruit Shear Zone due to further compression and crustal shortening. The stereoplot of the axial planes of sub-areas 1 and 2 shows approximately the same north-easterly oriented dip direction in the Neusberg macrofold with the axial plane in sub-area 3 marginally more NNE-oriented, with the fold axis plunging toward the NW as opposed to the NE for the folds in sub-areas 1 and 2 ( Figure 8D). The change of the orientation of the axial plane from the northeast in sub-areas 1 and 2 to marginally more north-northwest, as well as a change in the orientation of the fold axis in sub-area 3 ( Figure 8D) is possibly related to the emplacement of the Friersdale Charnockite of the Keimoes Suite within the supracrustal rocks. The isoclinal nature of the folds in sub-areas 1 and 2 suggests a greater degree of strain compared to the open fold in sub-area 3, probably related to the proximity to the Neusspruit Shear Zone, which may have acted as some sort of barrier to deformation.

Metamorphism and Deformation
The study area is characterised by high-T, low-P granulite facies metamorphic conditions in the Kakamas Domain [25]. Similar metamorphic conditions were recognised in other areas and associated with clockwise P-T paths recorded by means of mineral equilibria, e.g., [21,48,58,59]. According to [25], there were three main metamorphic and deformation events that occurred in the Kakamas Domain (Table 2). In this study, we reinterpret the polyphase metamorphic and deformation events in this part of the Domain, of which four main events were recognised ( Table 2).

M 1 and D 1 Events
The M 1 peak metamorphic event in the Kakamas Domain is characterised by granulite facies conditions estimated at T =~800 • C and P = 5.5 kbar [25] (Table 2). Similar metamorphic conditions were determined north of Pofadder (800-900 • C and~5 kbar [48,49], and dated 1220-1180 Ma [38,48]. The peak metamorphic paragenesis is reflected by garnetcordierite-orthoclase-spinel-quartz in spinel + quartz-bearing metapelites [48]. The D 1a deformation event is described as the early event related to oceanic basin closure in the eastern Namaqua Sector [1,5,6,60]. The timing of basin closure was determined as occurring at 1197 ± 5 Ma based on metamorphic overgrowths on detrital zircons [20]. The D 1a event is characterised by the development of the Hartbees River Thrust recognised as an inter-domain structure between the Kakamas Domain and Bushmanland Subprovince [4][5][6]. The D 1b deformation event is characterised by compression recognised in all the rocks below the Goede Hoop Formation. Some relic intrafolial folds have been observed in the S 1 foliation in the Puntsit Formation, confirming the penetrative transposition of S 0 into S 1 .

M 2 and D 2 Events
The M 2 metamorphic event is ascribed to slow cooling and heating episodes at near constant mid-crustal pressure conditions [48]. The peak metamorphism was followed by isobaric cooling to at least 700-660 • C, e.g., [48] during M 2 ( Table 2). The paragenesis during the M 2 event is defined by cordierite-garnet-orthoclase-hornblende-biotite-sillimanite in the kinzingites [25]. Previous research [48] confirmed that the presence of biotite and sillimanite is related to isobaric cooling of peak metamorphic cordierite and garnet. The M 2 metamorphic event is associated with the emplacement of the Riemvasmaak Gneiss dated at 1151 ± 14 Ma [43]. A similar age was established for the Rooipad Granite at 1155 ± 7 Ma [4]. In the study area, contact rocks, such as the skarn and wollastonitebearing calcareous rocks (Figure 3), occur as spotty rocks in the supracrustal rocks as the result of a fluid-induced compositional change due to the episodic emplacement of syn-tectonic granitoids. The paragenesis is defined by locally occurring wollastonite, as well as skarn within the calc-silicate-rich quartzite (Figure 3). The timing of emplacement of the syn-tectonic granites places the D 2 event between 1151 ± 14 Ma and~1105 Ma based on the timing of intrusion of late-to post-tectonic Keimoes Suite granitoids relative to the pre-to syn-tectonic granitic gneisses [37]. The D 2 event is characterised by co-planar S 0 /S 1 fabric and S 2 axial planar fabric defining northwest-southeast-striking F 2 folds in the Neusberg macrofold. The stretching lineations (L 2 ) trend northeast parallel to the fold axes of isoclinal folds in the Neusberg Mountain. The lineations plunge towards the northeast indicative of layer parallel slip during folding. Towards the end of the D 2 event, it is envisaged that the Neusberg thrust developed because of continued shortening, causing some stacking in the Goede Hoop Formation.

M 3 and D 3 Events
The M 3 metamorphic event is characterised by T =~640-550 • C and P = 4.8 kbar [21] ( Table 2) and is associated with magmatism between 1113 and 1080 Ma classified as posttectonic [22,35,37,43] (Table 2) in the Kakamas Domain. The intrusion of the supracrustal rocks by the Friersdale Charnockite is illustrated by a contact rock, in places identified as the biotite gneiss ( Figure 3). The D 3 event is characterised by a weakly defined fabric in the Friersdale Charnockite.

Tectonic Evolution
The tectonic evolution of the Kakamas Domain in the eastern Namaqua Sector is characterised by the southwest vergence and thrusting of this domain onto the Bushmanland Subprovince along the Hartbees River Thrust Zone [5]. This nappe trends mostly northwest-southeast and dips towards the northeast at about 20-75 • with stretching lineations that plunge towards the northeast. The metamorphism affecting the nappe is of granulite facies characterised by clockwise P-T-t-paths, established by the aid of mineral equilibria [21,58,59]. The peak metamorphic conditions have been estimated at T =~800 • C and P = 5.5 kbar [25,48,49] and dated between 1220-1100 Ma [38,48] during the Namaqua Orogeny. This metamorphic gradient is understood to be caused by early thrusting and thickening of the crust owing to tectonic stacking, associated with advective heat transfer related to large volumes of intrusive rocks, e.g., [5]. This interpretation is supported by [38,48,49] confirming the granulite facies conditions experienced by the Kakamas Domain. In this study, the general map pattern (Figures 6 and 8) indicates not only extensional tectonics, as established by [38,48,49] that occurred in the Kakamas Domain during deposition of the Korannaland Group, but also compressional tectonics, leading to tectonic stacking and magmatic accretion, as well as thickening of the crust. Previous research [5] confirm both extensional and compressional tectonics in the central, eastern, and northern parts of the Namaqua Sector. The Palaeoproterozoic basement emplaced at about 1.8-1.7 Ga during the Orange River Orogeny [5,72] was potentially reworked and mixed with juvenile Mesoproterozoic material in the Namaqua Sector during the Namaquan Orogeny, e.g., [3,33,37,38,48,72,82].
Based on available ages and field relationships, the granitic gneisses, such as the Riemvasmaak and Kakamas Suid Gneisses, are pre-to syn-tectonic due to their deformed nature, whereas the Friersdale Charnockite is post-tectonic because it is undeformed. The overall thickness of the metasedimentary rocks, which varies between 140 m and 200 m in the Goede Hoop Formation, and about 30 m to 80 m in the Puntsit Formation, excluding any repetition due to isoclinal folding as demonstrated in the Neusberg Mountain, suggests a restricted and narrow basin with limited sedimentary input. The protoliths to the calcsilicate and feldspathic mica-rich quartzites were likely carbonates and/or immature marls, and sandstones, respectively. The occurrence of the amphibole schist as intercalations in the calc-silicate-rich quartzite is suggestive of varying pulses of deposition of both clastic continental and volcanic materials in the Kakamas Domain.
Continued shortening led to thrusting, of which the overturned ramp dips southwesterly as opposed to the prominent north-easterly dipping foliation planes in the Neusberg. The timing of early compressional events is related to the early Namaquan Orogeny, as recognised by [43] elsewhere in the Kakamas Domain. The occurrence of isoclinal folds in the Neusberg suggests that a considerable amount of stress was applied during the D 2 event ( [25] and this study), associated with the emplacement of the granite gneisses between 1151 Ma [43] and~1125 Ma [35,37] in the Kakamas Domain. Previous research [37] reported similar ages across the boundary in the Areachap Domain where the well-foliated Louisvale Tonalite was emplaced at~1125 Ma, providing the maximum age for the main D 2 Namaquan deformation. The minimum age for the D 2 Namaquan deformation in the eastern Namaqua Sector is constrained by the post-tectonic Keimoes Suite for which the oldest reliably dated member, the weakly foliated Keboes Granite, has been dated at 1105 Ma [37].
Subsequent intrusion is related to the D 3 event and is characterised by the emplacement of the voluminous post-tectonic Friersdale Charnockite of the Keimoes Suite (at~1080 Ma) [22]. A late transcurrent northwest-southeast-trending shear zone occurred by reactivation of the D 1b structure into a steeply inclined and deeply rooted intra-domain shear zone between 1040 Ma and 1020 Ma defining the Neusspruit Shear Zone [25,26]. The Neusspruit Shear Zone has a dextral sense of movement, and its extension further north of the Orange River [5,6,25,26,31,75] constitutes a regional discontinuity in the Kakamas Domain.

Conclusions
1. The central part of the Namaqua Sector was subjected to intense deformation under high-grade metamorphic conditions correlated to granulite facies, but also shows greenschist facies overprints denoting the metamorphic nature during the 1.2-1.0 Ga Namaquan Orogeny. The compressional orogenic phase is associated with D 1 and D 2 events during which northeast-southwest-directed shortening resulted in southwest-directed thrusting illustrated by a late intra-domain thrust and southwest verging isoclinal folds in the Neusberg of the Kakamas Domain. The post-tectonic Friersdale Charnockite of the Keimoes Suite is emplaced during the D 3 deformation event in the study area. The Neusspruit Shear Zone is of a monoclinic nature and is described as a deeply rooted structure with shear direction towards the east.
2. The findings obtained have provided indications of the processes that occurred at the western margin of the Archean Kaapvaal Craton, and contributed to the understanding of the tectonic evolution of the Kakamas Domain within the Namaqua Sector. In this detailed study of a rather small area, the presence of a structure that forms part of the regional-scale structural pattern in the Kakamas Domain, together with the Neusspruit Shear Zone, and the Neusberg Thrust Fault, a presumed regional-scale thrust, were recognised to form part of an intensely flattened narrow basin in the eastern Namaqua Sector.
3. The general flattened pattern of the Neusberg Range associated with isoclinal folding represents a bulk of strain along with a monoclinic symmetry in the Neusspruit Shear Zone. The strain and vorticity indices suggest a transpressional shearing across the Neusspruit Shear Zone and adjacent regions.
4. The~1.2 to 1.8 km-wide, northwest-southeast-striking dextral-dominated Neusspruit Shear Zone constitutes a western regional boundary for the Korannaland Group. The Neusspruit Shear Zone is composed of steep, narrow zones of relatively high strain, such as high-grade gneiss, characterised by ductile deformation and penetrative strain. Although this study does not investigate strain analysis, further study on a regional scale based on finite strain and kinematic vorticity values are essential to describe the ductile flow type across the Neusspruit Shear Zone and adjacent regions.
5. New zircon SHRIMP U-Pb age, LA-ICP-MS, and isotopic analyses are required for both the magmatic and supracrustal rocks in the Kakamas Domain and constitute further studies. This will significantly contribute to the understanding of the petrogenetic processes, the timing of emplacement of the granitic gneisses, and the timing of deposition of the supracrustal rocks, respectively, as well as the approximate timing of occurrence of the shear zone. In addition, geochemical analyses should be applied to help constraint the tectonic setting and geodynamic role of the Kakamas Domain in the eastern Namaqua Sector during the 1.2-1.0 Ga Namaqua Orogeny.