Structural Controls on Shallow Cenozoic Fluid Flow in the Otago Schist, New Zealand

Department of Geology, University of Otago, Dunedin 9054, New Zealand Department of Geological Sciences, University of Cape Town, Rondebosch 7700, South Africa Department of Geosciences and Natural Resources Management (Geology Section), University of Copenhagen, Copenhagen K, Denmark Department of Chemistry, University of Otago, Dunedin 9054, New Zealand Centre for Trace Element Analysis, University of Otago, Dunedin 9054, New Zealand


Introduction
Interactions between brittle faulting, fluid flow, alteration, and mineralization in the upper crust can strongly influence rock physical properties and strength [1][2][3], seismogenic potential and the distribution of earthquake sequences [4][5][6], and the evolution and geometry of mineralized zones. In the South Island of New Zealand, the timing and distribution of fluid flow along basement-hosted brittle-ductile shear zones controlled the formation of ore deposits, especially orogenic gold deposits [7][8][9][10][11]. However, relatively few studies have been performed with the aim of establishing a structural and geochemical framework for fluid flow and mineralization events that occurred at relatively shallow crustal levels in regionally extensive basement schists.
The Otago Schist ( Figure 1) contains well-studied examples of paleohydrothermal systems that developed within midcrustal faults and shear zones at various stages of regional metamorphism and exhumation [8][9][10][11][12][13]. However, there are also excellent examples of shallow paleohydrothermal systems that are relatively poorly understood. The purpose of this study is to determine the main structural and geochemical processes that influenced shallow fluid flow and mineralization within the Otago Schists. This will help to constrain the potential sources of fluids in shallow basement rocks, as well as the role of preexisting structures in controlling patterns of faulting and fluid flow. We characterise the structure and geochemistry of carbonate-bearing fault and vein networks and show that hydrothermal fluids were strongly channelized along brittle faults that developed in many cases by reactivation of preexisting exhumation joints. Whole-rock geochemistry, coupled with in situ mineral 87 Sr/ 86 Sr, δ 13 C, and δ 18 O analyses, enables the interpretation of fluid pathways and the main fluid-rock reactions that occurred during faulting.

Regional Geology and Active Tectonics
New Zealand is composed of two main geological provinces, the Western and Eastern Provinces, which are intruded by the Median Batholith [14,15] (Figure 1(a)). Metasedimentary rocks in the Western Province define a series of tectonostratigraphic terranes that formed on the Cambrian to Ordovician Gondwana margin, which were subsequently intruded by plutonic rocks [16]. The Eastern Province, which contains the Otago Schists studied here, represents the forearc and accretionary prism to the Mesozoic Gondwana margin [16] (Figures 1(b) and 1(c)). Active tectonics in the South Island of New Zealand is dominated by the Alpine Fault system, which represents the present-day boundary between the Australian and Pacific Plates. Motion along the Alpine Fault is predominantly dextral strike-slip, but a significant component of dip-slip has caused formation of the Southern Alps mountain range and has resulted in te exhumation of the middle to upper crustal rocks at the surface (e.g., [17]).
Our study area on the coastline south of Dunedin City is in the Eastern Province Permian-Triassic Rakaia Terrane and Caples Terrane/Chrystalls Beach Complex (Figures 1(b) and 1(c)). These terranes were formed on the submarine convergent margin of Gondwana and are dominated by metaturbidites, although the Rakaia Terrane is slightly more SiO 2 rich than the Caples Terrane and is thought to have been derived from a more continental source [18]. The Chrystalls Beach Complex is a predominantly metasedimentary mélange that also contains rare metabasalts and metavolcanics and is interpreted as either an atypical part of the Caples Terrane or an intervening microterrane [19,20]. The continental source for the Rakaia Terrane is suggested by whole-rock 87 Sr/ 86 Sr isotope data (at 135 Ma) that show it to be more radiogenic ( 87 Sr/ 86 Sr ð135 MaÞ > 0:7065) than the Caples Terrane ( 87 Sr/ 86 Sr ð135 MaÞ < 0:7055) or the Chrystalls Beach Complex (0.7052 and 0.7064) [21][22][23][24][25].
The Rakaia-Caples/Chrystalls Beach rocks experienced metamorphism and deformation within the Mesozoic accretionary prism, which led to formation of an expansive schist belt termed the Otago Schist (Figure 1(c)). The Otago Schist was metamorphosed at prehnite-pumpellyite to upper greenschist facies conditions between~200 Ma and 135 Ma, with the metamorphic peak estimated to have been~140-135 Ma [22,[26][27][28]. Crustal xenoliths in intraplate basalts indicate that the lower Otago crust was affected by granulite to ultra-hightemperature metamorphic conditions at~92 Ma [29].
Progressive exhumation of the Mesozoic accretionary prism from the Early Cretaceous resulted in the formation of regionally extensive exhumation joints and associated fracture systems in the Otago Schist [28,30,31]. The orientation of these joints is mainly perpendicular to the metamorphic foliation and, in cases where a stretching lineation or metamorphic rodding is present, suborthogonal to the linear fabrics [31]. Joints are most abundant in greenschist facies rocks and less abundant at lower metamorphic grades (prehnite-pumpellyte facies) [31]. Following the development of the modern Alpine Fault plate boundary in the Early Miocene, much of the South Island of New Zealand experienced compressional inversion, which resulted in widespread reverse reactivation of normal faults that had initially formed in response to Late Cretaceous-Oligocene rifting and basin subsidence [32,33]. One of the major reactivated faults is the Akatore Fault, which strikes NE-SW and dips steeply (c. 60-70°) to the SE in the study area ( Figure 1(b)). The Akatore Fault is the easternmost onshore structure in the active Otago reverse fault province [34], which contains several active reverse faults striking NE-SW to NNE-SSW. The Akatore Fault hosted at least three M7.0 reversefault earthquakes between 13,317 B.C. and 1278 A.D [35].
Analysis of borehole breakouts and earthquake focal mechanisms indicates that the contemporary crustal stress field in the South Island is relatively homogenous and is characterized in most areas (including Otago) by a regional strike-slip stress regime (i.e., σ 2 is subvertical) and a maximum horizontal compressive stress axis (σ 1 ) between c. 110°and 120° [36][37][38][39][40][41][42]. This σ 1 orientation is broadly compatible with active reverse faulting along NE-NNE striking structures, although this would require σ 3 to be subvertical in a typical "Andersonian" faulting regime. Analysis of stress ratios throughout New Zealand shows that σ 2 is comparable in magnitude to σ 3 in the lower South Island, suggesting that switching between strike-slip and reverse-fault stress regimes may be possible [41]. A scenario in which σ 1 > σ vertical = σ 2~σ3 , with possible switching between stress regimes, was also suggested to explain the mixture of strikeslip and reverse fault ruptures observed during the 2010-2011 Canterbury earthquake sequence [40].  Map showing the distribution of metamorphic facies in the Otago Schist, metamorphic terranes, the Chrystalls Beach Complex, and the Akatore Fault, together with the field locations at Akatore Creek and Bruce Rocks. Stereoplot in the bottom-left corner illustrates the modern-day strike-slip stress field in Otago and Canterbury as reconstructed from earthquake focal mechanisms and borehole breakout data (after [39] and [41]). (c) Simplified cross-section through the Otago Schist showing the regional scale antiformal structure. Schematic relationship to the Mesozoic accretionary prism is also shown [43].

Analytical Methods
3 Geofluids comparison can be made between the reconstructed paleostress orientations and the contemporary stress field summarized in the previous section.

Geochemical Analysis of Carbonate Veins and Fault Rock
Matrices. Major element compositions were determined in situ on single minerals using a JEOL JXA-8200 Superprobe at the University of Copenhagen, Denmark, and a Zeiss scanning electron microscope (SEM) at the University of Otago Micro and Nanoscale Imaging facility (OMNI). The Superprobe operated with an acceleration voltage of 15 kV, a beam current of 15 nA, and a spot size of 5 μm, whereas the SEM operated with an acceleration voltage of 15 kV and a beam current of 2.7 nA.
Whole-rock major and trace element compositions were determined by ALS Minerals in Brisbane, Australia, by inductively coupled plasma-atomic emission spectroscopy (ICP-AES) or by coupled plasma-atomic mass spectroscopy (ICP-MS). Loss on ignition (LOI) was measured by weighing one gram of sample powder, prior to and after experiencing 1000°C for one hour. 143 Nd/ 144 Nd and 87 Sr/ 86 Sr whole-rock isotope data were measured at the University of Cape Town on a NuPlasma HR in the MC-ICP-MS Facility. Samples were dissolved in HF : HNO 3 solution for 48 hours at 140°C and subsequently dried down and converted to nitrate followed by standard chemistry to separated Nd and Sr [45,46]. The reference standards were JNdi-1 for the Nd isotopes and NIST SRM987 for the Sr isotopes [47].
In situ trace element concentrations and Sr isotope data were measured using Laser Ablation Multiple Collector Inductively Coupled Plasma Mass Spectrometry (LA-MC-ICP-MS) in the Department of Chemistry, Centre for Trace Element Analysis, University of Otago. An Applied Spectra RESOlution 193 m laser ablation system with an M-50 laser ablation cell coupled to a Nu Plasma-HR MC-ICP-MS instrument collected data directly on thin sections. The instrument laser was operated with an on-sample fluence of 2.5 J/cm2 at a laser repetition rate at about 5 Hz with a stage propagation speed of 5-10 μm/s on a targeted area with data collected in time-resolved mode. The concentration of in situ trace elements was collected with a spot diameter of 50 μm, where the ablated material is ionised and measured by quadrupole ICP-MS. Reference materials were analysed repeatedly against NIST 610 glass and combined with measured Ca of carbonate mineral grains for corrections. In situ 87 Sr/ 86 Sr data were collected as line transects on thin sections at a propagation speed of 5-10 μm/s. A 2 Hz preablation run was programmed to clean the surface of the track before ablations, where He gas transferred the ablated material into the ICP-MS. Six collector chambers in the ICP-MS were set to collect material with atomic masses from 82 to 88, representing the masses of Sr, Rb, and Kr, and are used to correct the isotopic values measured, due to overlapping atomic masses between the isotopic element of Sr, Rb, and Kr. The Sr data were collected and reduced [48].
Target carbonate phases were microdrilled with a target weight up to 2000 μg ± 200 μg. δ 13 C (δ 13 C = 13C/ 12 C) and δ 18 O (δ 18 O = 18O/ 16 O) analyses were conducted on the Isotopic Ratio Mass Spectrometer (IRMS) with Thermo Delta Plus XP coupled to a trace GC ultra with a combi PAL autosampler at the Department of Chemistry, University of Otago. Samples were sealed and air was replaced by helium. Five drops of phosphoric acid were applied, followed by 100 μl aliquot of the evolved CO 2 -He gas which was later extracted and injected into the IRMS. The standards NBS-18, IRU-Marble, and NBS-19 were used to calibrate the instrument and along with laboratory standards IRU-Marble and Atlantis3 (marine carbonate) to determine the precision and accuracy.

Structural Geology of Akatore
Creek and Bruce Rocks. Akatore Creek and Bruce Rocks are located on the southern limb of a regional-scale antiform in the dominantly quartzofeldspathic Otago Schist ( Figure 1; [28,49]). The main protolith lithologies to the Otago Schist are mudstone and sandstone, which are overprinted by a metamorphic foliation in both field areas. The combination of quartz, albite, chlorite, and muscovite, together with minor epidote, titanite, and calcite at Bruce Rocks indicates greenschist facies conditions, whereas the occurrence of pumpellyite at Akatore Creek indicates prehnite-pumpellyite facies metamorphic conditions [49]. Whole rock Ar-Ar and Rb-Sr data indicate that the metamorphic assemblages in both areas formed in the Late Jurassic to Early Cretaceous [22,28,49].

Metamorphic Foliation and Exhumation
Joints. Foliation measurements in both field areas are tightly clustered. At Akatore Creek, the metamorphic foliation is shallowly east dipping, whereas at Bruce Rocks, the foliation dips moderately to the southwest (Figures 2(a) and 2(b)). The foliation in both areas is crosscut by pervasively developed sets of exhumation joints, interpreted to have formed during Early-Late Cretaceous exhumation due to release of residual elastic strain [31]. The joints commonly formed at large angles to the metamorphic foliation (Figures 2(c), 2(d), 3, 4(a), and 4(b)) and are relatively planar for distances of metres to tens of metres ( Figure 3). The spacing between adjacent joints varies from a few centimetres to a few metres (

Geofluids
In cases where joint tips overlapped, reactivation as smalldisplacement strike-slip faults resulted in the formation of rhombohedral-shaped dilational jogs filled by carbonatecemented mosaic or crackle breccias (Figures 4(c), 4(e), and 4(g)). Small faults with displacements of less than a few centimetres typically contain thin (<cm) layers of cohesive carbonate-cemented breccia ( Figure 4(d)) and/or thin (<mm) discontinuous carbonate veins. They can also be surrounded by orange-stained carbonate alteration zones up to a few centimetres wide. Faults that developed larger displacements contain layers of carbonate-cemented fault breccia up to a few tens of centimetres wide, which can be surrounded by orange-stained carbonate alteration zones up to a few metres wide (Figure 4 d)) are also present within the alteration zones; these often have siderite on the rim and calcite at the core (Figures 6(c) and 6(d)). Microscopic crosscutting relationships indicate that the syntaxial veins formed first, followed by the networks of fibrous calcite veins, which in turn were crosscut by the larger carbonate veins ( Figure 5(b)). Nearly all of the carbonate phases from both study areas lack deformation twins, with the exception of infrequent Type I deformation twins, develops in botryoidal calcite from Akatore Creek ( Figure 6(a); [50]).

Elemental Composition of Alteration Zones.
Samples for whole-rock major and trace element analyses were collected from an outcrop at Bruce Rocks composed of greyschist.   (a)

Geofluids
The outcrop is cut by a fault that contains a 1.5-meter-thick layer of carbonate-cemented breccia surrounded by a 0.1-1 m wide carbonate-bearing alteration zone (Figure 7(a)). Three samples represent the greyschist host rocks (samples 1, 2, and 3); two samples were collected from within the main alteration zone (sample 5 from the margin and sample 6 closer to the fault breccia); two samples were collected from within a subsidiary 20 cm-thick alteration zone surrounding a hydrothermal vein lying parallel to the foliation (samples 4A and 4B); and two samples were collected from the fault breccia (samples 7 and 8).
Whole-rock SiO 2 values of the greyschist range from 65 to 70 wt.%, with CaO, Fe 2 O 3 , and MgO between 1 and 4 wt.% ( Table 2). The greyschist in the alteration zone,  Published in-situ 87 Sr/ 86 Sr for epidote are plotted for comparison [11,24]. (b) Individual in situ 87 Sr/ 86 Sr isotope data of the different types of carbonate phases from Akatore Creek and Bruce Rocks. The grey boxes represent the weighted average Sr isotope ratio with errors from each group of samples.   Table 2). The fault breccia also has low SiO 2 (37-40 wt.%) and high CaO (18-22 wt.%) ( Table 2). Loss on ignition (LOI) and Sr are both low in the greyschist samples (LOI = 3-4 wt.%, Sr = 42:7-92.9 ppm; Table 2), but distinctly higher in the altered greyschist (LOI = 13-17 wt.%, Sr = 364-652) and the fault breccia (LOI = 18-22 wt.%, Sr = 296-350 ppm; Table 2). Mass balance calculations show losses and gains of major and trace elements during alteration (Figure 7(b)). Volume corrections were applied by calculating a correction factor (k) according to the abundances of TiO 2 , Zr, Nb, and Hf, which appear to have been immobile during alteration [11]. Each element from the altered samples was compared to the average of the unaltered greyschist (samples 1-3; Figure 7). Results suggest that during alteration there was enrichment in CaO, Fe 2 O 3 , MgO, MnO, Sr, and Y, as well as several REEs, with small losses in SiO 2 , Al 2 O 3 , and K 2 O (Figure 7).  Table 3).

Structural Controls on the Shallow Hydrothermal Fluid
System. We interpret the paleohydrothermal systems exposed at Akatore Creek and Bruce Rocks to have developed within the Otago Schist under low-temperature and lowpressure conditions (Figure 10). The presence of infrequent thin (type 1) deformation twins in calcite suggests temperatures below 170°C [50,52,53]. Additionally, the range of δ 13 C and δ 18 O values overlaps with other datasets obtained from shallow (<5 km depth; [10]) cavity-filling hydrothermal vein calcite in the Southern Alps of New Zealand [10] (Figures 9 and 10). This field of δ 13 C and δ 18 O has previously been interpreted to represent remobilisation of metamorphic calcite and reprecipitation at low temperatures (200-300°C; [10]). Primary metamorphic calcite in the Otago Schist makes up c. 5% of the modal mineralogy, and has a restricted carbon and oxygen stable isotope range, where relatively low δ 13 C likely reflects metamorphism of primary organic matter ( Figure 9, [10,54,55]). Breakdown of metamorphic carbonate and liberation of CO 2 into a relatively shallow hydrothermal system will result in fluid precipitation at a lower temperature, and therefore a shift towards higher δ 18 O values while maintaining an overlap in δ 13 C values (Figure 9, [10]). Overall, the carbon and oxygen isotope ratios from both study areas are clustered and overlap with published data collected from carbonates that were precipitated in shallow hydrothermal systems in the Southern Alps [10,11].
Structural observations suggest that on a macroscale (metres to decametres) fluid flow was strongly channelized along foliation surfaces and Cretaceous exhumation joints that were reactivated as small-displacement strike-slip faults. This formed breccia-and vein-bearing fault networks with orientations that were strongly controlled by the orientations of the preexisting joint sets (Figure 10(a)). On a more local scale, fluid diffusion from the faults into the surrounding wall rocks was controlled mainly by the permeability of the schist wall rocks, which favoured fluid penetration along foliation surfaces and grain boundaries (Figure 10(b)). Additionally, large volumes of fluid appear to have been channelled within dilational jogs connecting overlapping fault segments, a geometry that was likely inherited from overlapping joints (Figures 4(c), 4(e), and 4(g)). Since the fault networks (and associated breccias and veins) are the youngest tectonic structures observed in the field areas, this supports the interpretation that faulting and associated hydrothermal fluid flow occurred under relatively lowtemperature conditions, since the exhumation joints are thought to have formed mainly above the ductile-tobrittle transition at <250°C [31].
The calculated paleostress tensor for the strike-slip fault networks at Akatore Creek is characterised by a σ 1 azimuth of 094°and a subvertical σ 2 , representing an Andersonian strike-slip stress regime (Figure 2(g)). The modern-day stress tensor in the Otago and Canterbury regions contains a subhorizontal σ 1 with an azimuth of 115°± 5° [39,40] similar to the paleo-σ 1 derived from the strike-slip faults in the study areas. The contemporary stress field is thought to have initiated in the Early Miocene, when the South Island of New Zealand experienced a transition from dominantly extensional tectonics to dominantly compressional and strike-slip tectonics, controlled by the development of the Alpine Fault as the modern-day plate boundary [39]. During compressional inversion, previously formed Cretaceous-Oligocene basin-bounding normal fault systems -including the Akatore Fault in the study area-were reactivated as high-angle reverse faults that continue to be active to the present day [56]. Our interpretation is that the vein-and breccia-bearing strike-slip fault networks exposed at Akatore Creek and Bruce Rocks (Figures 2-4) represent shallowly formed, post-Early Miocene structures that formed in a stress field similar to the contemporary stress field. If this is correct, the fault networks broadly overlap in age with reverse movements on the nearby Akatore Fault, which has accumulated several hundreds of metres of reverse displacement at the surface since the Miocene [35][36][37][38][39][40][41][42][44][45][46][47][48][49][50][51][52][53][54][55][56][57]. The fault networks exposed along the coast may therefore represent the 21 Geofluids manifestation of broadly distributed, upper-crustal deformation within the "damage zones" of regional-scale reverse faults such as the Akatore Fault. The broadly synchronous activity of steep, NE-SW striking reverse faults (e.g., Akatore Fault) and conjugate sets of strike-slip faults, is a deformation pattern similar to that recognized in recent earthquake sequences in Otago and Canterbury. For example, the 2010-2011 Canterbury earthquake sequence involved activation of steeply-dipping, NE-SW striking reverse faults and conjugate sets of E-W (dextral) and NW-SE (sinistral) trending strikeslip to oblique-slip faults, with orientations comparable to those documented in this paper [40]. Analysis of stress ratios in Otago and Canterbury suggest that the magnitude of σ 3 is similar to the magnitude of σ 2 , meaning that switching between "strike-slip" and "reverse" Andersonian stress regimes is possible [40,41]. One possibility is that the fault networks described here represent distributed deformation associated with rupture on the Akatore Fault, in which case the carbonate-cemented breccias and carbonate veins may reflect channelized fluid flow associated with permeability increases within coseismic fracture zones.

Evolution of Fluid Composition and Wall-Rock
Interaction. Paleohydrothermal fluid flow was associated with enrichments in CaO, Fe 2 O 3 , MgO, CO 2 , and MnO, and losses in SiO 2 , Al 2 O 3 , and K 2 O during alteration of the schist wall rocks ( Figure 10). This mobilisation correlates with precipitation of calcite, ankerite, and siderite as the main carbonate phases. Petrographic observations of syntaxial veins showing a distinct compositional difference between the core (calcite) and rims (siderite) suggests that there was a change in fluid composition from early Fe-rich fluids to later Ca-rich (and Fe-depleted) fluids. One possible reason for this could be the late precipitation of hydrothermal pyrite that would result in the removal of Fe in the system.
Strontium is a useful trace element in hydrothermal carbonate minerals because it has a similar charge and ionic radius to Ca, which means a substitution can readily occur. Potassium, which is substituted easily by Rb, is not compatible in carbonate phases due to a much larger ionic radius than Ca, and so the carbonate Sr isotope ratio is not affected by overdecay of 87 Rb. Any variation of Sr isotopic compositions in hydrothermal carbonates will therefore reflect

Geofluids
fluid-rock interaction. The majority of in-situ Sr isotope data from the hydrothermal carbonate phases varies between 87 Sr/ 86 Sr = 0:70577 and 0.70646 and shows no significant difference between the different types of carbonate texture ( Figure 8, Table 4). The high Sr concentration in mica-rich layers within fibrous foliation-parallel veins is also coupled to the most radiogenic Sr isotope ratio of 0:70641 ± 0:00008 (n = 2). The value is lower than age-corrected (20 Ma) bulk Otago Schist ( 87 Sr/ 86 Sr (20 Ma) of 0.70890-0.71791) (Figure 8(a), Table 4). Therefore, the hydrothermal carbonates require interaction between a moderately unradiogenic component and a relatively radiogenic component. The radiogenic component could be derived from breakdown of mica grains, which are hosted within the hydrothermal fault breccias and altered greyschist and have interacted with the hydrothermal carbonates. The origin of an unradiogenic Sr component requires breakdown of mineral phases that have low Rb/Sr. Metamorphic epidote is a minor component in the greyschist but has 87 Sr/ 86 Sr of 0.70343-0.70519 [11,25] that is less radiogenic than the hydrothermal carbonates  Table 2). Since metamorphic epidote takes up no Rb, it is representative of the initial greyschist Sr isotope ratio at the time of Otago Schist metamorphism (150-135 Ma-Late Jurassic-Early Cretaceous; [28]). Other possibilities for nonradiogenic fluid components are metamorphic plagioclase and metamorphic calcite, both of which have low Rb/Sr and therefore should have the same initial metamorphic value as the epidote. Age correction of the Otago Schist bulk rocks gives a similar value to the metamorphic epidote. A key point is that the CO 2 -rich nature of the fluids that fluxed through Bruce Rocks and Akatore Creek suggests that metamorphic carbonate was probably mobilised in the fluid source. Since the hydrothermal fault breccias have higher fluid: rock ratios than the surrounding wall-rock, this may explain why whole-rock Sr isotope data of the hydrothermal breccias are more radiogenic than the altered greyschist. Another reason could be that the hydrothermal fault breccias have a higher concentration of hydrothermal carbonate compared to the altered greyschist.

Conclusions
The vein-and breccia-bearing fault networks exposed at Akatore Creek and Bruce Rocks are interpreted to represent a post-Early Miocene hydrothermal system that formed at shallow depths in the Otago Schist. The orientation and geometry of the fault networks and the associated channelized fluid flow were strongly influenced by the metamorphic foliation and by reactivation of preexisting Cretaceous exhumation joints. Paleostress analysis suggests that the small-displacement strike-slip fault networks developed in a paleostress field containing a maximum principal stress (σ 1 ) oriented at c. 094°, which is similar to the modern-day σ 1 orientation in Canterbury and Otago. The δ 18 O values of vein carbonates in the field areas overlap with shallow hydrothermal calcite elsewhere in the South Island. Stable isotope data coupled with the presence of thin type 1 twins in calcite implies vein precipitation under low-temperature conditions (<200°C). Sr isotope data indicate that the carbonate Sr isotope signature is inherited from mixing between an unradiogenic and a radiogenic source. The unradiogenic source may be metamorphic epidote and calcite, while the radiogenic source is likely to be muscovite from the host greyschists, although meteoric water and seawater cannot be ruled out. The brittle fault networks and associated hydrothermal systems are interpreted to have formed after the onset of Early Miocene compression, and may represent fracturing and fluid flow associated with reverse reactivation of regional-scale faults such as the nearby Akatore Fault.

Data Availability
The collected geochemical data used to support the findings of this study are included within the article.

Conflicts of Interest
The authors declare that there is no conflict of interest regarding the publication of this paper.