Properties of Impact-Related Pseudotachylite and Associated Shocked Zircon and Monazite in the Upper Levels of a Large Impact Basin: A Case Study from the Vredefort Impact Structure

: The Vredefort impact structure in South Africa is deeply eroded to its lowermost levels. However, granophyre (impact melt) dykes in such structures preserve clasts of supracrustal rocks, transported down from the uppermost levels of the initial structure. Studying these clasts is the only way to understand the properties of already eroded impactites. One such lithic clast from the Vredefort impact structure contains a thin pseudotachylite vein and is shown to be derived from the near-surface environment of the impact crater. Traditionally, impact pseudotachylites are referred to as in situ melt rocks with the same chemical and isotopic composition as their host rocks. The composition of the sampled pseudotachylite vein is not identical to its host rock, as shown by the micro-X-ray ﬂuorescence ( µ XRF) and energy-dispersive X-ray (EDX) spectrometry mapping. Mapping shows that the melt transfer and material mixing within pseudotachylites may have commonly occurred at the upper levels of the structure. The vein is spatially related to shocked zircon and monazite crystals in the sample. Granular zircons with small granules are concentrated within and around the vein (not farther than 6–7 mm from the vein). Zircons with planar fractures and shock microtwins occur farther from the vein (6–12 mm). Zircons with microtwins (65 ◦ / {112}) are also found inside the vein, and twinned monazite (180 ◦ / [101]) is found very close to the vein. These spatial relationships point to elevated shock pressure and shear stress, concentrated along the vein’s plane during impact.


Introduction
The Vredefort impact structure is amongst the largest impact basins known on Earth. Having been deeply eroded during 2020 My of its history, it allows investigation of the impactites at the lowest levels of this large impact structure [1][2][3][4][5]. For example, impact-related pseudotachylites, formed at 8-10 km below the original level of the Vredefort structure, have been investigated in detail; their geochemical, isotopic, and (micro)structural properties have been studied continuously for over a century [4,[6][7][8][9][10][11][12]. However, the properties of the impactites formed in Vredefort at the higher structural levels, closer to the original surface, are practically unknown, with the upper portions of the structure being eroded [13,14]. Two billion years of erosion made such studies difficult, but not completely impossible.
The Vredefort impact structure contains remnants of Vredefort granophyre dykes, considered to have been derived from above, from the Vredefort impact melt sheet [1,3,[15][16][17][18]. Impact melt was injected into the fractures, penetrating to 5.5-7.5 km below the crater floor [5]. On its way downwards, the granophyre melt incorporated various lithic clasts of the country rock, many preserved within the  [25]. (B) Field photograph of the sampled outcrop, after [20]. The granophyre matrix (brown) contains multiple lithic clasts (light-grey). The rectangle shows the sampled clast. (C) Thin section of the sampled clast with the pseudotachylite vein (dark grey) and its host meta-granite (light grey).
The central uplift of the structure consists of Archean basement granites in the core, with the overturned supracrustal sequence in the collar exposed in the NW. The collar consists of the Dominion Group and the Witwatersrand, Ventersdorp, and Transvaal Supergroups ( Figure 1A). The SE part of the structure is covered by the Karoo sedimentary and volcanic rocks [22].
Within the granitic core and along the core-collar boundary, nine granophyre dykes are exposed [3,7,15,22]. These dykes have a dacitic composition and contain numerous lithic clasts from the supracrustal sequence [1,3,18]. The dykes are believed to have been an impact melt, which was injected downwards [1,[15][16][17][18]. Recently, the core granophyre dyke on the farm Daskop was shown to have a very limited downwards extent (~3 m; [5]), providing additional evidence that the melt source was located above the present erosional level.
The sample discussed in this study was collected from the Daskop granophyre dyke (26 • 56 51.66 S 27 • 22 27.06 E). It is a small meta-granite clast with a sharply crosscutting vein ( Figure 1B). Preliminary petrological and geochemical analyses of this clast were presented in [20]. It was shown geochemically and petrographically that the vein has a granitic affinity, rather than being an offshoot of a granophyre within the inclusion [20].

Optical and Scanning Electron Microscopy (SEM) Images
Four polished thin sections were prepared from the sampled clast ( Figure 1C) and were investigated by optical microscopy and scanning electron microscopy (SEM) at the Department of Geology, University of the Free State, South Africa. Optical transmitted light images were acquired using an Olympus BX51 optical microscope equipped with an Olympus 162 U-TVO.63XC camera (Olympus Corporation, Tokyo, Japan). Backscattered electron (BSE) images and qualitative energy-dispersive X-ray (EDX) spectrometry maps were obtained using a JEOL JSM-6610 SEM (JEOL Ltd., Tokyo, Japan) equipped with a LaB 6 electron gun and a Thermo Scientific Ultradry EDX detector (Thermo Fisher Scientific, Waltham, MA, USA). The EDX detector was used to identify mineral phases and to collect semi-quantitative chemical maps of the areas of interest. Zircon and monazite crystals were located using BSE imaging. The analytical conditions for collecting the BSE images and chemical maps were 15 kV accelerating voltage, 8 nA probe current, and 10 mm working distance.

Energy-Dispersive Micro-X-Ray Fluorescence Spectrometry (ED-µXRF)
One of the thin sections was mapped semi-quantitatively for distribution of elements using a Bruker M4 Tornado, an energy-dispersive micro-X-ray fluorescence spectrometer (ED-µXRF; Bruker Corporation, Billerica, MA, USA) at the Stoneman Laboratory, University of Pretoria, Pretoria, South Africa. The instrument is configured with a Rhodium tube, which was operated at 50 kV, 500 µA, and 30 W. The polychromatic beam (0-50 keV) is focused using a polycapillary lens to a spot size of ca. 25 µm, with the incident beam and take-off angles at 51 • . The instrument is equipped with two silicon drift detectors with an energy resolution of 145 eV for Mn Kα, which face each other at a 180 • angle and 90 • to the tube with respect to the sample surface. The sample chamber was evacuated to <20 Mbar to enable light elements such as Na to be measured. A step size of 25 µm and an integration time per pixel of 50 ms was used for a larger area, with the step size reduced to 5 µm for a smaller area. The distribution of the following 20 elements was qualitatively mapped: Si, Ti, Al, Fe, Ca, Mg, Mn, Na, K, Ba, Co, Cr, Cu, Ni, P, Rb, S, Sr, V, and Zn.

Electron Backscatter Diffraction (EBSD) Analyses
The thin sections were chemo-mechanically polished and carbon-coated with a thin carbon layer (5-10 nm). Deformation microstructures in zircon were analyzed in situ with forescatter electron (FSE) and electron backscatter diffraction (EBSD) in a field emission gun scanning electron microscope (FEG-SEM). These analyses were performed at the Laboratory for scanning electron microscopy and focused ion beam applications, Faculty of Earth Sciences, Geography and Astronomy, University of Vienna, Austria. Orientation contrast images were produced using an FSE detector mounted on the EBSD-tube of an FEI Quanta 3D FEG-SEM (Field Electron and Ion Company, Hillsboro, OR, USA), which is equipped with a Schottky field emission electron source, an EDAX Pegasus Apex 4 system consisting of a Digiview IV EBSD camera, and an Apollo XV silicon drift detector for EDX analysis (AMETEK, Inc., Berwyn, PA, USA). Electron beam conditions for analyses were 15 kV accelerating voltage, 4 nA probe current using the analytic mode. Stage settings were at 70 • tilt and 14 mm working distance. After potentially deformed crystals of zircon and monazite were identified based on BSE and orientation contrast images, EBSD crystallographic orientation mapping was applied to selected grains. An EBSD camera binning of 4 × 4 was used to index single frame data at 49 ms exposure time, reaching indexing rates of ca. 20 points per second. The Kikuchi pattern contrast was improved by applying both static and dynamic background subtraction and intensity histogram normalization. Hough transformation settings were 120 × 120 pixels binned pattern size and 1 • Theta step size, while the Rho fraction was limited to the inner 88% of the Kikuchi pattern. A 9 × 9 convolution mask was applied to index 3-15 peaks with a minimum peak distance of 8 pixels in Hough space. The following zircon lattice parameters were used for reference: di-tetragonal, Laue group 4/mmm, a = b = 6.612 Å, c = 5.983 Å, α = β = γ = 90 • [26]. The following monazite parameters were used for a reference: monoclinic prismatic, Laue group 2/m, a = 6.79 Å, b = 7.02 Å, c = 6.467 Å, α = γ = 90 • , β = 103.38 • [27]. Map data were collected in hexagonal grid mode using step sizes of 80 to 90 nm (specified for each map in figure captions). EDX intensities and EBSD data were collected simultaneously using the OIM v7.3 Data Collection software.
The EBSD data were re-indexed with the EDAX OIM v7.3 Analysis software. Data re-indexing was assisted by assigning data points to phases based on selected EDX intensity ranges in EDX energy regions of interest. Crystal orientation maps were cleaned using the Confidence Index Standardization (CIS) procedure, which unifies the confidence index of equally oriented points within a grain (presuming a minimum grain size of 3 pixels in more than one row and a tolerance angle of 5 • ). The Confidence Index (CI) represents the difference in the number of triangles (found between three bands each) between the first and second orientation solution, divided by the total number of identified triangles. No orientation data were changed during cleanup. The data were filtered for CI > 0.1 to exclude single, statistically poor data points, which do not belong to a "grain." EBSD data were visualized with the EDAX OIM v7.3 Analysis software and the MTEX v5.1.1. toolbox for MATLAB [28].

Optical Imaging
The clast is massive, and we consider it to be a meta-granite ( Figure 1C), with irregularly shaped fractured quartz grains up to 600 µm in diameter, interstitial fine-grained quartz, and interstitial altered biotite (Figure 2A,B; see also [20]). The clast is shocked and thermally reworked within impact melt; therefore, there is also a possibility that it could be a fragment of meta-sedimentary rock with granitic composition, such as sandstone cemented by clay (dark pockets between the quartz grains). As the clast has granitic composition [20], for convenience, we will call it "granite" or "meta-granite" hereafter in the text. Locally, close to the clast edges, granophyre pockets with characteristic orthopyroxene needles and fine-grained matrix are observed ( Figure 2C). Closer to the PT vein, in the center of the clast, the texture is foliated and consists of fine-grained polycrystalline quartz interlayered with thin veinlets of optically dark material ( Figure 2D-F). The PT vein is brown to black and contains fine-grained, plastically deformed, and partially molten quartz aggregates ( Figures 1C and 3A,B, upper part). The PT vein's matrix is cryptocrystalline, inhomogeneous in color, with dark clustered spherules up to 50 µm in diameter ( Figure 3C, arrow), and dark ring textures up to 300 µm in diameter ( Figure 3D

µXRF Mapping
Chemical (µXRF) mapping of the clast's edge, where the meta-granite is resorbed by granophyre, shows the chemical contrast between granophyre and clast ( Figure 4). The granophyre is enriched in Ca, Fe, Mg, Mn, Cr, Ti, and S, of which Fe, Mg, Mn, and Cr are concentrated in the orthopyroxene needles (e.g., Figure 4E), and Ca and Ti are enriched in the matrix ( Figure 4D,F). On the other hand, meta-granite contains more Si ( Figure 4B), Zn, Sr, and Rb. The elements K, Al, Na, and V concentrations are roughly equal in both rock phases (e.g., Figure 4C). These chemical relationships reflect literature data for basement granite and granophyre (see overview in [20]), except Sr and Rb, of which Sr should be enriched in granophyre. In contrast, Rb should be approximately equal in both rock phases.  The µXRF mapping of the central part of the clast, where the PT vein is in contact with the foliated granite, shows that the PT vein differs in composition from the host meta-granite. The PT vein is relatively enriched in Fe, Mg, Mn, Ti, Al, Cr, and V (e.g., Figure 5A,B,D), and depleted in Si, Zn, Rb, and Sr ( Figure 5A) with respect to the host granite. The PT vein is locally enriched in S and Cu, including patches in the surrounding foliated granite ("melt pockets," Figure 5E). The elements K ( Figure 5C) and Na are roughly the same in granite and the PT vein but are depleted in the foliated zone around the PT vein, whereas Ca was not detected ( Figure 5F). The PT vein matrix is inhomogeneous and displays a patchy distribution of Fe, and Mg ( Figure 5B,C), as well as Mn, K, and Na.

BSE Imaging and EDX Mapping
BSE images at the edge of the clast show fractured quartz grains with interstitial altered biotite, as well as pockets filled with granophyre ( Figure 6A). According to the EDX mapping, granophyre is enriched in Al, Ca, Mg, Fe, and Ti, whereas granite is enriched in Si ( Figure 6). The PT vein in contact with foliated granite displays fine-grained BSE-bright skeletal phases (acicular crystals of ilmenite, isometric and elongated grains of sulphides, and poikilitic/skeletal spinel), which are surrounded by K-feldspar or quartz-rich matrix, with tabular crystals and needles of plagioclase ( Figures 7A, 8A and 9A). The PT vein's matrix is depleted in Si with respect to the host foliated granite but enriched in Al, Mg, Fe, Ti, and Mn. Vein shows lobate contacts and chemically inhomogeneous matrix, where Al, Mg, Fe, K, and Na display a patchy distribution (Figures 7C,D and 8B-E). K and Na are depleted in domains with Fe-and Mg-enrichment, and vice versa ( Figure 8C-E), whereas the distribution of Al does not spatially correlate with other elements (Figures 7C and 8B). Mg-and Fe-enriched domains are up to 300 µm in diameter, corresponding to the spherules/ring textures shown in Figure 3D.

EBSD Mapping Data
Out of 67 zircon grains analyzed with the BSE and orientation contrast imaging, 20 (ca. 30%) display a granular texture; 8 (ca. 12%) exhibit planar fractures, of those, one revealed microtwins; 30 (ca. 45%) were found fractured or fragmented, of those, two have microtwins, and one has planar deformation bands (PDBs); 9 (ca. 13%) are only slightly deformed with crystal-plastic deformation or undeformed, of those, one has microtwins. Besides, we have examined five monazite grains, three of which are fractured, one is twinned, and one is undeformed (see below).
Zircon grains with shock microtwins (four in total) were found within the PT vein and at a distance of 6 and 7.5 mm from the PT vein. Within the PT vein and in the foliated granite around the vein, granular zircons are present, being spatially associated with the PT vein in thin sections (see also [19]). Farther away from the PT vein, at a distance greater than 3-6 mm, granular zircon is not found, but zircon with planar fractures (PFs) is abundant. At a distance greater than 12 mm, no distinct shock deformation features in zircon are observed [19].
In the PT vein's matrix, fragmented zircon grains with shock microtwins were documented [29]. One of the grains with microtwins ( Figure 9, Grain 01-11) is fragmented, with the fragments separated by up to~50 µm within the PT matrix ( Figure 9A). Two larger fragments contain an equivalent microtwin set ( Figure 9B,C), showing that the grain was fractured across the length of a microtwin lamella. Shock microtwins typically form thin lamellae, which are rotated at 65 • about the [110] axis of the host grain and occupy the {112} plane in the host grain [30]. Pole figures reveal accordingly that the [001] of the microtwin lamellae is rotated at about 65 • with respect to the [001] axis of the host, and one of the <110> axes and two of the <011> axes coincide between the lamellae and the host ( Figure 9D).
Grain 01-19 is located at a distance of ca. 2 mm from the PT vein and is composed of granules from <0.5 to 1 µm in size ( Figure 10A-C). The grain is located within a fine-grained matrix and is resorbed at the edges ( Figure 10A). The EBSD map ( Figure 10C  Grain 01-14 is located~7.5 mm from the PT vein and is severely fractured. In the BSE image, at least three sets of PFs are observed ( Figure 11A). In the EBSD map, two domains in the bottom right have different orientations than the host (color-coded orange and green). The orange domain is only slightly misaligned with respect to the main orientation of the grain and is consistent with the effects of moderate crystal-plastic deformation. The green domain has a characteristic orientation for shock microtwin lamellae, i.e., displays the rotation of [001] at about 65 • with respect to the parent grain, one coincident <110> axis, and two coincident <011> axes ( Figure 11D). The domain with microtwin-type orientation (color-coded green in Figure 11C) appears to be crosscut by PFs. White areas visible inside the grain in the EBSD map correspond to open fractures and the BSE-dark rim with the poor EBSD quality pattern (along the left margin and the top and bottom margins). This dark rim reflects the growth zoning of the grain. Monazite grains are less abundant but also occur in the studied sample. Grains 01-16a and 01-16b are located at 0.5 mm from the PT vein; both grains have pores. The equidimensional euhedral grain 01-16b is undeformed, as visible in the orientation contract image ( Figure 12A). Elongated subhedral grain 01-16a, located next to 01-16b, is deformed, exhibiting both subgrains and planar lamellae ( Figure 12B,C). Three main orientation domains are distinguished from the EBSD maps and pole figures (Figure 12B-D). Domains 1 and 2 appear crystal-plastically deformed with internal misorientation/mosaic texture and moderate dispersion of crystallographic axes ("asterism"). Besides, domains 1 and 2 form mutually alternating planar lamellae, likely microtwins, which are sharply cut by domain 3. Domain 3 is undeformed, shows no dispersion of crystallographic axes ( Figure 12D), and has an irregular shape. All three domains have a coincident orientation of their [010] axes, whereas domains 1 and 2 have the following twin relationships: 180 • /[101].

Origin of the PT Vein
In previous studies [20,21], concern was raised regarding the origin of the PT melt vein within the granitic clast. The presence of granular (polycrystalline) zircon grains and grains with shock microtwins and PFs, which have consistent spatial relationships with the PT melt vein, point to the impact-related origin of the PT vein. Granular neoblastic zircon with the systematic orientation of granules ( Figure 10) has only been reported from shock metamorphism environments [31][32][33]. Zircon grains with PFs may occur in seismic zones [34,35] and under high crustal pressures [36] but are rather rare and more often reported from impactites [37][38][39][40][41]. Finally, zircons with polysynthetic microtwins have only been reported in nature from impact-related deposits [30,41,42].
The resorbed zircon with microtwin lamellae found in detached fragments, enclosed in the matrix of the PT vein, shows that the vein crystallized after the zircon was twinned and fragmented. Our data confirm the shock-related origin of the PT vein, with the following order of events, closely spaced in time: (1) The zircon was twinned (due to high shear stress during propagation of the rarefaction wave [43]); (2) The PT melt vein was formed (propagation of the rarefaction pressure wave or immediately after the propagation of the main pressure waves); (3) The zircon was fragmented, and fragments are separated within the PT melt (decompressionpropagation of the rarefaction pressure wave or immediately after the propagation of the main pressure waves [44]); (4) The PT vein crystallized (post-impact with reduction of pressure and temperature); (5) The host granite was fragmented, and the fragments were incorporated into the impact melt (post-impact crater modification); (6) The impact melt was injected downwards, carrying the granite fragment, and formed the granophyre dyke (opening the deep fractures in the crust below the crater due to post-impact relaxation within the crust [15,45]).
Of these, (1) and (2) could be coincident with each other; however, the formation of the PT vein could have taken longer. This order of events, based on the crosscutting relationships, clearly points at the impact origin of the PT melt vein.

Geochemical Properties of Pseudotachylite
Although  semi-quantitatively demonstrated the general granitic affinity of the PT vein, most of the mapped elements display similar behavior within the vein and granophyre with respect to granite. Fe, Mg, Mn, Ti, Cr, S are enriched in both melt rocks compared to granite, whereas Si, Zn, Rb, Sr are enriched in granite compared to both granophyre and PT matrix. K and Na are equally distributed in all three rock phases.
Pronounced differences in composition between granite and granophyre are expected, as granophyre represents a fraction of the impact melt, formed as a result of the mixing of different target rocks, such as shale, quartzite, granite, lamprophyre, mafic lava, carbonate, etc., in various possible proportions [3,46]. On the other hand, the pseudotachylitic melt is advocated to form strictly in situ and correspond geochemically to its host rock [4,11]. Some pseudotachylites in granites were found to be slightly more mafic (i.e., enriched in Mg and Fe) than their host rocks [7,8] due to the initial melting of mafic and hydrous phases with lower fracture toughness in non-equilibrium conditions [47,48]. During the "flash" melting of granitic rocks, an excess of silica could survive as refractory quartz grains. In our sample, the occurrence of partially molten quartz aggregates ( Figure 3A,B) is consistent with their leftover refractory character after partial melting.
In the present sample, pseudotachylite indeed appears to be more mafic than its host, which might be due to the initial preferential melting of mafic phases (e.g., dark micro-veins around the main PT vein are formed from mafic phases, Figure 2E-F). On the other hand, similar behavior of most mapped elements within the PT vein and granophyre with respect to granite could point to a contaminated/mixed composition of the PT vein. In the upper levels of the impact crater, elevated shock pressures could lead to more violent and chaotic processes than is observed at the lower levels exposed today. Melt-forming processes could be different in the upper levels of the impact structure than those observed deep below the eroded crater floor. For example, the formation of pseudotachylite may involve compositional mixing. Melt/clast transport to some distances and/or between different lithologies might have occurred [48].
Such melt mixing and migration can be greatly facilitated at the upper structural levels by the inevitable and large-scale movements of the rock blocks during the rarefaction pressure wave propagation, crater settling, post-shock seismic activity, etс. [44,49,50]. Such high-energy movements would be somewhat restricted at a depth of 8-10 km of the current erosional level due to the lithostatic pressure from the overlying masses of rock. Nevertheless, a degree of material mixing was observed even at the current erosional level [48]. A higher degree of melt mixing and melt transport at the upper levels might result in certain similarities between the impact melt (granophyre) and "in situ" melt (pseudotachylite), somewhat opposite to what was previously believed.
The possible similarity of the PT melt and granophyre is also supported by a "spherulitic" character of the PT vein's matrix (Figures 7, 8 and 9A), similar to that of granophyre [1]. In granophyre, Mg-and Fe-rich crystals (orthopyroxene) are embedded in the Na-and K-rich matrix (spherules of feldspars). Similar patterns are observed within the matrix of the reported PT vein: Mg-and Fe-rich "spherules" are embedded in the K-and Na-rich matrix of the PT vein ( Figures 3C,D and 8).

Association of the PT Vein with Shocked Accessory Minerals
In the present sample, shocked granular zircon within and around pseudotachylitic vein in a lithic clast in granophyre is observed [19]. The only granular zircon grain with fine granules (≤3 µm) reported from Vredefort (besides the zircons from a present sample) was found in heavy mineral separates from granophyre [39]. However, at that time, crystallographic orientations of granules were not confirmed due to the absence of a suitable technique. Zircons with comparatively large (~10-100 µm) granules from Vredefort were found in alluvial deposits of the Vaal River [42] and in the foliated norite (an impact-generated mafic melt found in the geographical center of the structure) [30]. There are no systematic crystallographic relationships observed between the large zircon granules, and their formation mechanism remains to be explained.
Thus, we report a rare occurrence of granular zircon with fine granules (≤3 µm) and systematic orientation of granules from the Vredefort impact structure. Moreover, the pseudotachylites formed close to the impacted surface reveal their spatial association with the granular neoblastic zircon grains and with zircon grains with planar fractures. This association is likely related to the inhomogeneous distribution of shock pressure, which is elevated along porous zones, mechanical discontinuities, fractures, or lithological boundaries [51,52] and is responsible for the shock recrystallization of zircon, at the same time facilitating the formation of in situ melts [9,10].
Zircon with PFs is also associated with the PT vein, occurring at a distance of 6-12 mm from the PT vein, where no granular zircon is found [19]. Zircon with polysynthetic microtwins occurs both within the PT vein (Figure 9; [29]), as well as at a distance of 6 and 7.5 mm from the PT vein, in the zone of zircon with PFs ( Figure 11). There are only four grains with microtwins documented in two thin sections, and they appear to be spatially associated with the PT vein. The spatial association of zircon with PFs and microtwins with the melt veins was documented before and related to the high shear stress in the vicinity of the PT vein [52]. High shear stress after the shock wave propagation is suggested to initiate shock microtwins formation in zircon [43]. Moreover, micro-twinning in zircon occurred prior to the formation of PFs (Figure 11), which suggests that the shear stress necessary for mechanical twinning should be comparatively higher than that for planar fracturing.
In one of the previous studies, spatial relationships of shocked zircon and apatite grains with impact melt were observed [53]. Grains of these accessory minerals located closer to the impact melt were shown to be subject to higher shock levels of deformation/recrystallization, and thus they exhibit a high degree of isotopic age resetting, as opposed to grains that are located at a greater distance from impact melt [53]. In our sample, in contrast, shock effects in accessory minerals do not seem to spatially correlate with the proximity to the impact melt (i.e., to the granite clast margins), but are related to the PT vein. In our sample, zircon closer to the PT vein experienced a higher degree of shock recrystallization (i.e., acquired granular textures). We expect that the isotopic ages will also be reset in zircon grains located close to or within the PT vein, although further investigations are necessary.
Shocked monazite is also found in the vicinity of the PT melt vein and is composed of the twinned area (domains 1 and 2) and the re-crystallized area (domain 3). Impact-related mechanical twinning in monazite is not uncommon, with at least 12 distinct orientations of shock microtwins documented previously [54,55], with likely more twin orientations that are possible [48]. The twin orientation 180 • /[101] is among the previously documented orientations [55]. The twinned area is crystal-plastically deformed, whereas the recrystallized area is undeformed and hence postdates plastic deformation. Thus, monazite grain 01-16a experienced post-shock crystal-plastic deformation in domains 1 and 2 and recrystallization in domain 3. Whereas post-shock crystal-plastic deformation of microtwin lamellae was observed in zircon as well [52], recrystallization of twinned domains in zircon has not been documented in Vredefort [30,42,52]. Thus, the recrystallization of twinned areas in monazite ( Figure 12) demonstrates that monazite is less durable than zircon and may not retain shock deformation features throughout the geological history like zircon does [24,30].
The formation, deformation of polysynthetic microtwins, and subsequent recrystallization to strain-free neoblasts have been previously documented in titanite grains from a foliated pseudotachylite, Sudbury impact structure, and Archaean meta-granite from the core of the Vredefort impact structure [56]. The deformation of twins in titanite and their crystallization to strain-free neoblasts was explained by the effects of crater modification and heating due to the post-impact metamorphic evolution within large impact structures [56]. Post-shock heating could also explain crystal-plastic deformation and recrystallization to neoblasts observed in monazite from our sample. The post-shock heating of the studied clast was related to its involvement in the superheated impact melt [19].

Conclusions
We have studied the textural and compositional properties of a pseudotachylite vein hosted by a granite clast, which was transported from the uppermost levels of the Vredefort impact structure by a granophyre melt injected into the crater floor. The transport and preservation of such clasts facilitates the investigation of the eroded rocks and of the shock-related processes that occurred close to the impacted surface. With the help of crosscutting relationships, we have again confirmed the previously debated impact origin of the PT melt vein. The unknown properties of such "upper level" pseudotachylites have been suggested: (1) Possible contaminated/mixed composition of the pseudotachylites from the upper levels of the impact structure, which can be caused by the different mechanisms of pseudotachylite formation and development; (2) Spatial association of the shocked zircon with the PT vein, pointing at the elevated shock pressures/temperatures and high shear stresses in the vicinity of the PT melt vein (or vein's formation site). Future studies should demonstrate the effect of the PT vein's proximity on the isotopic age in zircon and monazite.
These properties might help in determining the origin of other pseudotachylite veins with unclear context and possibly in the identification of new impact structures. In the broader context, knowledge of the mechanisms and processes occurring at the upper levels of large impact basins might improve our understanding of impact processes and planetary evolution of the Earth, Moon, and other rocky bodies of the solar system.