Emplacement of the Anta Granite from Rio de Janeiro State (SE, Brazil); determined by magnetic fabrics

Magnetic fabric and rock magnetism studies were performed on the three facies of the Anta granite (SE of Rio de Janeiro State, southern Brazil). This intrusion is roughly elliptical (~ 14 km2), NE-SW oriented and composed of granodiorite, monzodiorite, quartz-diorite, syenogranite, and monzogranite. It shows solid-state deformation and tectonic foliation at its borders and is apparently isotropic in the central part where the internal fabrics are impossible or very difficult to measure through classical techniques. Magnetic fabrics were determined by applying both anisotropy of low-field magnetic susceptibility (AMS) and anisotropy of anhysteretic remanent magnetization (AARM). The AMS and AARM fabrics are coaxial for all facies. The parallelism between AMS and AARM tensors excludes the presence of a single domain (SD) effect in the AMS fabric. Several rock-magnetism experiments performed on one specimen from each facies show that, for all units, magnetic susceptibility and fabrics are carried by magnetite grains. Most of the magnetic foliations are steeply dipping in all facies, and are roughly parallel or sub-parallel to the foliation measured in the field and in the country rocks. In contrast, the magnetic lineations present mostly low plunges for almost the whole pluton, except for one site where it is steep (> 60°). Thin section analysis show that rocks from the borders of the Anta pluton are solid-state deformed, indicating that the borders of the pluton were affected by the regional strain during its emplacement. On the other hand, the lack of solid-state deformation at outcrop scale and in thin sections precludes deformation in the central part of the pluton to be determined, where igneous textures are preserved. This evidence allows us to interpret the magnetic fabrics observed in this part of the pluton as primary in origin (magmatic) and acquired when the rocks were solidified as a result of magma flow, in which steeply plunging magnetic lineation suggests that a feeder zone could underlain this area. Our data suggest that the regional deformation partially affected the emplacement of the Anta granite.


INTRODUCTION
The highlands of the Rio de Janeiro State are composed of granitic gneiss, paragneiss, and granite that are part of the Ribeira Belt. The Ribeira Belt, or Ribeira Orogen, is a Brasiliano/ Pan-African orogenic belt located at the Mantiqueira Province (Almeida et al. 1981), with NE-SW structural trend, mostly controlled by NE high-angle strike-slip shear zones. This event was responsible for the generation of the voluminous granitic magmatism at Central Ribeira belt. The geodynamic evolution of the Ribeira belt took place during the amalgamation of the Western Gondwana, and was controlled by diachronic amalgamation of magmatic arcs, terranes, and cratons (Brito Neves et al. 1999, Campos Neto 2000, Trouw et al. 2000, Heilbron et al. 2004, Basei et al. 2010, Bento dos Santos et al. 2015. This belt represents a collisional orogen that has developed in several episodes of the convergence of the Brasiliana-Pan-African orogeny during the Neoproterozoic-Cambrian, with last stages occurring in the Lower Ordovician. Several studies on the Ribeira Belt suggest that its granitoids are part of a Tonian to Ordovician orogenic belt and were generated at distinct collisional stages of the Brasiliano/Pan-African orogenic cycle (Machado et al. 1996, Trouw et al. 2000, Heilbron and Machado 2003, Silva et al. 2003, 2005, Tupinambá et al. 2012, Heilbron et al. 2013. The Ribeira belt in Rio de Janeiro State was divided into four tectonic domains separated by ductile shear zones, whose direction is parallel to the regional structures with predominantly horizontal slip (Machado et al. 2016). From SE to NW, the domains are: Litorâneo, Serra dos Orgãos, Paraíba do Sul, and Juiz de Fora (Fig. 1A). Based on geochronological data (Rb-Sr and U-Pb), the granitic magmatism was divided into three main groups (Machado et al. 2000); pre-, syn-, and post-collisional with ages ranging from 590 to 570, 560 to 530, and 520 to 480 Ma, respectively (Fig. 1A). In all tectonic domains there are orogenic, pre-, syn-, and post-collisional granitoid plutons with calc-alkaline to alkaline affinities. They were emplaced and/or reworked during intense magmatic activity during the stages of the Brasiliano (Pan-African) orogeny.
The majority of syn-tectonic granite plutons in the Ribeira belt, as is the case of the Anta granite, have characteristic such as solid-state deformation and tectonic foliation at its borders, while the central part of the pluton have such weak internal fabrics that it is impossible or very difficult to measure them through classical techniques based on direct field observations, or in thin sections, and consequently these granites are often considered isotropic. On the other hand, it is important to understand the internal fabric of the granitic plutons, to investigate: • their relationship with the regional structure; • the magmatic flow; • solid-state deformation.
In such cases, magnetic methods, especially the anisotropy of low-field magnetic susceptibility (AMS), have been widely used to determine the internal fabric of the plutons (e.g., Bouchez 1997). Magnetic anisotropy techniques are a powerful petrophysical tool that has been employed to determine planar (bedding, cleavage, and/or foliation) and linear (mineral lineations) structural elements in sedimentary, metamorphic, and igneous rocks (for a review, see Tarling and Hrouda 1993, Borradaile and Henry 1997, Martín-Hernández et al. 2004, Herro-Bervera 2006, Martín-Hernández et al. 2009and Almqvist et al. 2014). AMS is well suited for mapping magmatic foliations and lineations in igneous intrusions (e.g., Bouchez 1997, Archanjo et al. 1998, Archanjo et al. 2002, Trindade et al. 1999, Mamtani 2014, Sheibi and Majidi 2015. The method can be applied even in rocks that are visually isotropic (Bouchez 1997). One of the distinct advantages of AMS measurements in granites is the ability to determine the lineation direction which is rarely observed in granites. The magnetic lineation is often inferred to indicate the stretching direction imposed by magma flow in igneous rocks (Tarling and Hrouda 1993, Borradaile and Henry 1997, Raposo et al. 2012Bhatt et al. 2017, among many others). Numerous studies of AMS in granitoids have demonstrated a strong correlation between visible foliation and lineation and equivalent magnetic fabrics (Román-Berdiel et al. 1995, Archanjo et al. 1998, Esmaeily et al. 2007, Raeisi et al. 2019.
Magnetic fabric can also be determined using anisotropy of anhysteretic remanent magnetization (AARM), which is not so popular in studies of granites as well in sedimentary rocks (Raposo et al. 2006, Oliva-Urcia et al. 2009, Raposo et al. 2014. This anisotropy isolates the contribution of remanence-bearing minerals from that of the paramagnetic and/or diamagnetic matrix. Since the ferromagnetic particles, which define the AARM tensor, and the paramagnetic and/or diamagnetic minerals may crystallize at different times with different orientations, the determination of the AARM allows an investigation of possibly overprinted fabrics. To understand magmatic processes in plutons is one of the key problems because of the complexity of the geometric patterns and physical causes of magma flow. In many cases, the direct field evidence for large-scale flow has been erased from rock record (Trubač et al. 2009). The flow patterns may be inferred from the preserved mesoscopic fabrics acquired late in the magma chamber history along migrating crystallization fronts and easily reset by regional tectonic deformation (Benn et al. 1994, Paterson et al. 1998. The inference on the large-scale flow patterns within a pluton is difficult because of the poor strain memory of magmatic fabrics (Paterson et al. 1998). Late deformation makes new fabrics which may appear locally on large bodies, or can be more pervasive on smaller ones. These fabrics may modify or erase the earlier (primary) fabric depending on temperature and strain intensity. Indeed, granite pluton emplacement and deformation during the regional tectonic events is a hard study task, since granitic rocks do not always develop mesoscopic scale deformation fabrics. In syn-tectonic intrusions, the distinction between primary and secondary fabrics using microstructural observations may not be possible, considering that the emplacement of magmas is mostly controlled by the regional strain. In such a scenario, magmatic structures may have the same orientation of country rocks, even if a solid-state foliation is not strongly developed.
We have applied both AMS and AARM techniques to the Anta granite to determine the internal fabrics mainly of its central part, since it is visually isotropic, to provide information on its emplacement, and to verify whether the whole body was affected by the regional strain. This granite has not been studied for any aspect, even geochemically, as show in this paper. In addition, it is the first granite from Rio de Janeiro State studied by magnetic methods. To better understand the magnetic fabrics we have also performed an extensive rock magnetism study.

GEOLOGICAL SETTING
The Anta granite is located in the border of the Paraiba do Sul shear zone, in the southwestern region of the state of Rio de Janeiro. This shear zone is one of the most important structures in the Central part of the Ribeira belt, which has been classically considered as a dextral shear zone developed in response to a transpressive regime which produced wide mylonitic zones (Corrêa Neto et al. 1993, Machado andEndo 1993). Stress directions determined from plagioclase fabrics has confirmed the kinematics of this deformation regime (Egydio- Silva and Mainprice 1999). After the magnetic fabrics determined in this paper, the Anta granite can now be associated to the group of granites of the Ribeira belt, which are smaller massifs, such as stocks or small tabular or elongated batholiths associated with regional high-angle ductile shear zones (Nummer 2001, Nummer et al. 2007). The plutons are foliated, with solid-state deformation at the borders and igneous flow structures in the central part. Contacts are often tectonically deformed and transposed to be concordant with host rock structures. I-type granites or granodiorites are predominant, although S-type granites are also found (Nummer et al. 2007).
The occurrence of a significant volume of granitic magmatism in the orogenic belt in Rio de Janeiro state can be explained by three geodynamic models (Nummer 2001): • magmatic arc models associated with oceanic lithosphere subduction, which are described as the model formation of the Rio Negro Magmatic Suite in the Ribeira belt (Tupinambá 1999); • island-arch/continent collision models, which are a case of extensive Brasiliana granitogenesis in the Proterozoic belt of the Mantiqueira Province, or continent-continent; • intraplate models, where the predominant regime is crustal extension.

The Anta Granite and sampling
Anta granite is a small body with dimensions around 2 × 7 km (~14 km 2 ) and is elongated with major axis in the NE-SW direction (Fig. 1B) parallel with the preferential trend of the Paraíba do Sul shear zone. It is intrusive in the paraderivated sequences of the Paraíba do Sul Complex and Rio Turvo suite described by Tupinambá (2012aTupinambá ( , 2012b. The pluton is located near the region of the Sapucaia city, Rio de Janeiro State, approximately 1km from the eastern margin of the main axis of the Paraíba do Sul shear zone. It has features such as "sugarloaf mountain shape", which is typical of the granitoids from the Ribeira belt. The pluton was initially described by Pinto (1980) and Corrêa Neto et al. (1993), who considered it as clearly conditioned by the Paraíba do Sul shear zone and was classified as collisional (Corrêa Neto et al. 1994). However, some authors have classified the body as post-tectonic (Silva et al. 2000). Anta granite was not included in the classification of Neoproterozoic granitoids from the Ribeira belt in Rio de Janeiro State, in pre-, syn-, and post-tectonics proposed by Machado and Demange (1994) due to the lack of knowledge on its emplacement since the central portion of the body, apparently macroscopically isotropic, which is not true, as will be shown by magnetic fabrics.
Three distinct facies were identified in the Anta pluton ( Fig. 1B). They are: • more mafic facies composed of hornblende-biotite granodiorite partially foliated to quartz diorite in the eastern portion (SE-NE) of the body; • an undeformed facies in the center of the pluton (represented here by sites located to SW, AT-10 to AT-14, Fig. 1B) composed of monzogranite and syenogranite; • a more felsic facies composed of syenogranite to alkali-granite with megacrystal of elongated microcline in the western portion (NW-SW) of the body.
The pluton is deformed at the edges with ENE-WSWoriented foliation. Lithologically, it is composed of granodiorite, monzodiorite, quartz-diorite, syenogranite, and monzogranite. The different lithologies show different shades of gray and present medium to coarse grains. They have feldspathic porphyroclasts and fractured feldspathic grain lenses, constituting 25 to 75% of the volume, in incipient or advanced recrystallization granoblastic matrix, whose tabular and/or prismatic mafic minerals are oriented according to cataclastic foliation. Petrographic analyses (Fig. 2) show that the essential mineralogy of granite consists of microcline, orthoclase, quartz, plagioclase, biotite, and hornblende; oxides (mainly titanomagnetites), alanite, and epidote appear as accessories.
In the thin sections ( Fig. 2), typical igneous structures are preserved for the lithotypes of the central facies of the Anta granite ( Fig. 1B) were observed, such as granoblastic texture and polygonal contacts, slightly deformed at the grain edges ( Figs. 2A and 2D). The southwest and west (Fig. 1B, western) facies of the granite show porphyritic texture with microcline megacrystals, sometimes quartz and subordinate plagioclase (Figs. 2B and 2E) that represent relic igneous structures of intergrowth and were formed by processes of static crystallization from a liquid whose original shape may have been modified by deformation. These phenocrysts exhibit undulating extinction levels, brittle/ductile state deformation, and sometimes recrystallized edges surrounded by the mylonitic/ protomylonitic matrix. The facies of the northeast border ( Fig. 1B, eastern) are composed of predominantly mesocratic quartz, plagioclase, pyroxene, biotite, and hornblende, and were classified as granodiorite and monzodiorite. In this portion of the pluton, mafic bands commonly occur as fine-grained quartz-diorite. This facies presents a higher degree of deformation (Figs. 2C and 2F), with a mylonitic texture, where quartz grains are anhedral and rotate with ribbons formation. The average particle size of the matrix ranges from 0.5 to 5 mm and sub-grain clusters reach up to 15 mm, forming polygonized contacts with plagioclase crystals, suggesting static recrystallization under high-temperature conditions. The plagioclase of these rocks presents an anhedral to subeuhedral shape ranging from medium to coarse granulation (3 to 7 mm), with corroded contacts between the Pl: plagioclase; Qtz: quartz; Bt: biotite; Mc: microcline. grains. Biotite has fine to medium granulation and is abundant in the matrix. The rocks of this facies, which have the highest deformation, generally have undulating extinction, grain edge migration, subgrains formation, and even maclas deformation, indicating temperatures between 650-700°C for quartz deformation (Stipp et al. 2002).
variation of edge-core transition, in a fractional crystallization system, including rocks of the central portion of the pluton with incipient zonation to the facies recrystallized by metamorphism, as in the eastern portion of the body, with predominance of mafic minerals such as biotite, hornblende, and magnetite, indicating crystallization in medium to deep crust (Fig. 3B). In terms of tectonic environments, the analyzed samples are predominantly distributed in the field of syn-collisional granites; however, some of them fall into the field of late-collisional granites (Fig. 3C).
Oriented samples from 21 sites widely distributed throughout the Anta granite (Fig. 1B) were collected along road cuts and farms in and around Sapucaia city from outcrops, which are certainly in situ. Unfortunately, it was not possible to obtain the same site numbers for each facies of equal distributions of the pluton due to the lack of the good outcrop exposure. In some places, large outcrops do occur; however, they are either not in situ boulders or are weathered. In addition, we have problems with the access to the higher outcrops, since the Anta granite has "sugarloaf mountain shape." In spite of this, a significant portion of the Anta pluton could be sampled. Sample orientations were determined using both magnetic and sun compasses, whenever possible. At least 10-13 cores, using a gasoline-powered rock drill, were collected from each site for magnetic measurements, and at least 3 specimens (2.5 × 2.2 cm) were cut from each core.

Anisotropy of low-field magnetic susceptibility
The AMS describes the variation of magnetic susceptibility (K) with direction within a rock and represents the contribution of all the rock-forming minerals (i.e., dia-, para-, and ferromagnetic). Its use is not restricted to iron oxide bearing rocks. For anisotropic rocks, K is a symmetrical second-rank tensor which relates the intensity of the applied field (H) to the acquired induced magnetization (M) of a material (Tarling and Hrouda 1993). The tensor is expressed by its principal eigenvalues and eigenvectors K max > K int > K min representing the maximum, intermediate, and minimum axes of susceptibility, respectively. K max axis represents the magnetic lineation while K min is the pole of the magnetic foliation (the plane formed by K max and K int axes). If K AMS is carried by either Fe-bearing silicate paramagnetic matrix minerals or (titano) hematite or pyrrhotite, the AMS, their anisotropy, is due to the preferred mineral crystallographic orientations (magnetocrystalline anisotropy). Otherwise, if K AMS is carried by cubic ferrimagnetic minerals such as titanomagnetite or magnetite, AMS anisotropy is due to the grain shape (shape-anisotropy), in which K max is parallel to the long axis of the particle (for MD grains), and to the magnetic grain interaction or distribution within a rock. Cañón-Tapia (2001) and Gaillot et al. (2006) showed that the AMS might still be dominated by the shape effect, despite the occurrence of magnetic grain interaction or distribution anisotropy in the rock.
AMS data have been used to study a wide variety of geological processes that give a fabric to a rock unit (for reviews, see Borradaile and Henry 1997, Martín-Hernández et al. 2004, Herro-Bervera 2006, Martín-Hernández et al. 2009and Almqvist et al. 2014). In granite rocks, AMS became widely used, since it is not restrict to remanence-bearing minerals and it can be determined even in rocks with predominant paramagnetic minerals (see the reviews, and Bouchez 1997).

Rock magnetism properties
K-T curves from low-temperature (from about -195°C to room temperature) susceptibility were recorded using a CS3-L apparatus coupled to a Kappabridge (KLY-4S) instrument (Agico, Czech Republic). Specimens were cooled in the Ni N 2 liquid temperature and heated up to room temperature. Corresponding high K-T curves were carried out in an Ar atmosphere using a CS-3 apparatus coupled to the KLY-4S. Specimens were progressively heated up to 700°C and subsequently cooled to room temperature. These experiments were performed on at least one sample from each facies of the granite.
The behavior of NRM was studied by alternate field (AF) tumbling demagnetization in steps of 5 or 10 mT up to 100 mT, this experiment was performed in 12 samples from the distinct facies. All remanences were measured with a JR5A magnetometer (Agico, Czech Republic).
Coercivity remanent spectra from partial anhysteretic remanent magnetization (pARM, Jackson et al. 1989) were determined in the same specimens submitted to AF of NRM. They were determined using a Molspin alternating field demagnetizer as the source of the AF field; superimposition of a steady field (DC field) was attained by a small coil (home-made) inside and coaxial to the demagnetizer and it was controlled by a Molspin apparatus. The pARM acquisition consists of applying a steady field (DC field) in between two chosen values (AF window, H 1 and H 2, H 1 < H 2 ) of a decaying AF peak (H) while the rest of the assemblage is demagnetized from a peak field H > H 2 . Then, specimens were exposed to an AF peak of 100 mT and DC field of 0.16 mT with an AF window width of 10 mT. Tumbling AF demagnetization at 130 mT was applied after each pARM acquisition.
After AF tumbling demagnetization of the last pARM acquisition, the specimens were subjected to isothermal remanent magnetization (IRM) in progressively increasing magnetizing fields using a pulse magnetometer (MMPM9, Magnetic Measurements).
Hysteresis measurements at room temperature were performed using a vibrating sample magnetometer (VSM-Nuvo, Molspin, Newcastle-upon-Tyne, UK) in fields up to 1 T.
All magnetic measurements were performed at the Laboratory of Magnetic Anisotropies and Rock Magnetism of the Geosciences Institute of the University of São Paulo.

Anisotropy of anhysteretic remanent magnetization
The anisotropy of remanent magnetization isolates the contribution of remanence-bearing minerals from that of paramagnetic and/or diamagnetic matrix (see Jackson 1991 for a review). This anisotropy is determined from the intensity of an artificial magnetic remanence acquired when a magnetic field is applied along different directions (positions) through the sample. This has distinct advantages because it precludes the effect of inverse AMS fabric due to single domain (SD) titanomagnetite or magnetite (Stephenson et al. 1986), since the magnetization occurs always parallel to the long axis of the magnetic grains ( Jackson 1991). Among the artificial remanences that can be used to calculate the anisotropy of remanent magnetization tensors, the anhysteretic remanence (AARM) is the most used one, being preferable due to its being acquired in a weak field, which guarantees that the magnetization is linearly related to the inducing field and the AARM tensors are of second-rank. The AARM tensor, as well as AMS, is a symmetrical second-rank tensor expressed by its main eigenvectors AARM max > AARM int > AARM min representing the maximum, intermediate, and minimum axes of anhysteretic remanence intensity, respectively, in which AARM max corresponds to the magnetic lineation and the AARM min is the magnetic foliation pole (normal to AARM max -AARM int plane). Even though less used, the AARM technique has been employed for a wide range of applications in geosciences, such as petrofabric determinations (Trindade et al. 1999, Borradaile and Gauthier 2003, Raposo and Gastal 2009, Raposo et al. 2012, among others).
The AARM was determined in five sites of the different facies of the Anta granite, in seven positions measurement scheme. The procedure consists of cycles of anhysteretic remanence acquisition, measurement, and demagnetization along different positions for each specimen. The AARM tensor was determined by iteratively magnetizing the specimen in an AF peak of 60 mT (this field was chosen based on the coercivity remanent spectra) with a DC field of 0.16 mT in the desired orientation, measuring the resulting remanence, and AF tumble-demagnetizing in 120 mT before proceeding to the next step. Before AARM determinations, the samples were demagnetized by AF tumbling at 200 mT to establish the base level. The best-fit AARM tensors were calculated by the least-squares method, which showed root-mean-squares of less than 5%, indicating that the ellipsoids are well-resolved ( Jackson 1991).

MAGNETIC MEASUREMENTS: RESULTS
Anisotropy of low-field magnetic susceptibility directional and scalar data AMS measurements were performed on 2.5 × 2.2 cm cylindrical specimens that were cut from the cores collected from 22 sites of the Anta pluton, using a Kappabridge instrument (KLY-4S, Agico, Czech Republic). The mean AMS eigenvectors (K max , K int , K min ) and the 95% confidence regions for each site were calculated using the ANISOFT 4.2 (Agico, Czech Republic). Scalar and directional AMS data are presented in Table 2.
The eigenvectors within the sites are generally well grouped with low values and small angles for the 95% confidence regions (Tab. 2) as observed in the representative examples of the Figure 4. For the majority of the sites, the magnetic lineation (K max ) is NE/SW oriented (Figs. 4A and 4D) with a slight variation to E/W (Figs. 4B, 4C and 4F), the plunges range from horizontal (< 20°, Figs. 4A and 4D) to inclined moderate inclination (between 20 and 40°), the most inclined plunge (> 60°) was found only in one site AT-11 (Fig. 4E, Tab. 2). The magnetic foliations (K max -K int plane) are preferably NE/SW oriented with dips from horizontal to vertical (Fig. 4). Both magnetic lineations and foliations are, in part, similar to the lineations and foliations measured in the Paraiba do Sul shear zone.
The mean magnetic susceptibility, expressed by the arithmetic average of K m = (K max + K int + K min )/3 in SI units, is generally high for all facies (Tab. 2), ranging from 0.25 × 10 -3 (AT-14) to 96.07 × 10 -3 (AT-4) with an average of 26.19 × 10 -3 . High and low values of K m are found in the borders and central part of the pluton.
The mean of the degree of anisotropy, given by the arithmetic average of P = K max /K min , ranging from 1.08 (8%, AT-19) to 2.22 (122%, AT-8, Tab. 2) with an average of 1.40 (40%). Even though P values are variables between the lithological units, the highest values are in the borders of the pluton, mainly in the deformed mafic units (granodiorite to monzodiorite) In general, there is no clear relation between K m and P parameters for the Anta granite facies (Fig. 5A). The Jelinek's (1981) shape parameter of the ellipsoid expressed by T = [2ln( K int / K min )/ln(K max /K min )]-1 is oblate (T > 0) and triaxial (T ~ 0) for the majority of sites (Tab. 2, Fig. 5B); however, for few sites, it is prolate (T < 0, Fig. 5B).

Rock magnetism properties
Representative examples of K-T curves are shown in Fig. 6A for different facies of the Anta granite. In all analyzed specimens, a well-defined peak was observed around -150°C, which indicates the Verwey transition, characteristic of almost pure magnetite. The correspondent high K-T curves show a small Hopkinson peak, and all of them display a decrease in the intensity of susceptibility around 580°C (Fig. 6A), indicating the presence of Ti-poor titanomagnetite or magnetite. The cooling and heating curves are reversible.
Examples of acquisition of remanent coercivity spectra determined from AF demagnetization of natural remanent magnetization (NRM) are shown in Figure 6B. The remanent coercivity is generally low, with medium destructive field < 20 mT, characteristic of multi-domain magnetite grains.
Results from the pARM curves are presented in Figure 6C, which show that all samples are of low coercivity, indicating that magnetite grains are relatively large around 2-5 μm, since coercivity is linked to grain size ( Jackson et al. 1989).
The IRM pattern is shown in Figure 6D, which displays that more than 95% of the magnetization reaches the total saturated isothermal remanent magnetization (SIRM) in fields < 150 mT, except for two samples (AT-17 and AT-18) whose total saturation is reached in fields < 200-250 mT (Fig. 6D). The IRM curves indicate the presence of fully saturated, coarse Table 2. Anisotropy of low-field magnetic susceptibility (AMS) data for Anta granite.
Unit: the lithological facies; ogn: orthogneiss (countryrock); mgt: monzogranite; gdt: granodiorite; sgp: syenogranite; N: the number of specimens included in the AMS means; K m : the mean magnetic susceptibility (SI units); P: the degree of anisotropy; T: the Jelinek's shape parameter ( Jelinek 1981); K max , K int and K min : mean AMS eigenvectors which represent the maximum, intermediate and minimum susceptibility intensities, respectively; Dec: declination in degrees; Inc: inclination in degrees; e/z: the semi angles of the major and minor axes of the 95% confidence ellipse, respectively, calculated by the Jelinek (1981)  and fine magnetite grains, which is in agreement with the pARM spectra (Fig. 6C).
Some typical hysteresis curves from the analyzed facies are illustrated in Figure 7. For all units, the shape of the hysteresis curves reveals that ferromagnetic grains carry bulk susceptibility. However, for some specimens, hysteresis loops show that there is a significant contribution (> 80%, Figs. 7B, 7C and 7D) of paramagnetic minerals to the bulk magnetic susceptibility, as can be observed in the high-field part of the hysteresis curves. In general, hysteresis curves for the majority of the specimens (Fig. 7) are narrowing waisted, typical of low-coercivity ferromagnetic grains since the loops are totally closed at 0.2 T. In addition, most samples fall into MD domain state on the Dunlop's (2002) plot (Fig. 7E), which is coherent  and high temperatures obtained in argon atmosphere) (B) Remanent coercivity spectra determined from AF tumbling demagnetization of natural remanent magnetization (NRM). Remanence intensities are normalized to the first measurement; (C) Remanent coercivity spectra derived from partial anhysteretic remanence (pARM) acquisition in an AF peak demagnetization at 100 mT with AF window width of 10 mT during DC field application of 0.16 mT. Remanence intensities are normalized to the highest value of partial remanence acquisition; (D) Isothermal remanence magnetization (IRM) acquisition curves, intensities of remanences are normalized to saturation of IRM (SIRM) versus field strength. AT-5 and AT-8 are from granodiorite to monzodiorite facies, AT-12 and AT-18 are from monzo-to syenogranite facies, and AT-17 is from porphyritic syenogranite facies.
with other experiments such as the IRM and pARM acquisition curves (Figs. 6C and 6D).
Based on all magnetic experiments, therefore, we conclude that coarse magnetite, which was also observed in thin sections, carry NRM and IRM magnetizations and are responsible for magnetic susceptibility, with few or significant contribution (> 80%) of the paramagnetic matrix minerals of the Anta pluton.
Unit: the lithological facies; N: the number of measured specimens; P: the degree of anisotropy; T: the Jelinek's shape parameter ( Jelinek 1981); AARM max , AARM int and AARM min : mean AARM eigenvectors which represent the maximum, intermediate and minimum remanent magnetization intensities, respectively; Dec: declination in degrees; Inc: inclination in degrees; e/z: the semi angles of the major and minor axes of the 95% confidence ellipse, respectively, calculated by the Jelinek (1981) Figure 8. This means that if fine SD magnetite grains are present, they did not affect the AMS fabrics. Therefore, the AMS fabrics of the Anta granite are normal ones, i.e., the magnetic fabric is similar to the petrofrabric. In addition, both magnetite grains and paramagnetic matrix minerals of the Anta pluton have the same orientation.

DISCUSSION
The magnetic fabric patterns in the Anta pluton are presented in Figures 9 (foliations) and 10 (lineations). Magnetic foliations (normal to K min , Fig. 9) are roughly parallel to the foliation measured in the field in the country rocks in a regional scale (inset, Fig. 9). They are predominantly NE-SW oriented with steeply dipping or vertical in all units ( Fig. 9) for the majority of sites. It is worth noting that the sites with the highest foliation dips are located in the borders portion of the pluton (Fig. 9), where the pluton is solid-state deformed (Fig. 2).
Magnetic lineations, K max (Fig. 10), are mainly ENE oriented and present mostly low plunges (< 30°) in approximately 85% of the sites, again most of them located at the border portion of the pluton; however, in some sites, K max is also ESE oriented (Fig. 10, Tab. 2). Seven sites display magnetic lineation plunges between 30 and 60°, and in one site, the plunges are > 60°, located at central facies of the granite (AT-11, Figs. 1B and 10) where foliation is not observed in the field, and also no solid state deformation was observed even in the thin section ( Figs. 2A and 2D), in which the primary magmatic structures are preserved. In general, the pattern of magnetic lineations is roughly measured in the field in the country rocks in a regional scale (inset, Fig. 10).
Fabrics in plutons are regarded either as related to magma emplacement or resulting from tectonic strain after or syn-tectonic. Therefore, fabric patterns in plutons can result from internal magma chamber processes such as magma pulses, convection, magma surges, dike injections, and crystal settling, or even be related to regional deformation, or involve a combination of these two processes (Paterson et al. 1998), which is characteristic of syn-tectonic regimes. However, this combination can be simultaneous, if a compressive component predominates during intrusion; or subsequent, considering that an intimate association of extension and compression is commonly observed along shear zones. In such a case, an originally vertical lineation may be obliterated by the shearing process. Indeed, fabrics related to emplacement such as the presence of magmatic microstructures and steep lineations are rarely preserved, since they are easily overprinted by minor ductile strain during or after cooling of the magma (Clemens et al. 1997). These overprinted fabrics may be observed in the whole pluton, or in some places, which is more common.
Comparing oriented structures from country rocks with internal magnetic and deformational fabrics in plutons allows determining whether pluton fabrics reflect the effect of regional tectonic strain. On the other hand, if foliations and lineations in country rocks and pluton are different, structures in the pluton will preferentially be considered as the result of internal processes in the pluton.
Field and petrographic evidence (Fig. 2) show that rocks from the Anta pluton were affected by the regional strain during and after emplacement, since magmatic foliation evolves to solid-state deformation higher in the oriental eastern border (e.g., AT-7 and AT-8, Fig. 2C) than the occidental western border (AT-17) of the pluton (Fig. 2B). Magnetic foliations for these rocks are steeply dipping and parallel to foliation measured in the field (inset, Fig. 9). The lineations are mostly subhorizontal. This indicates that magnetic fabrics in these portions of the pluton record this strain which is related to the dextral Paraiba do Sul shear zone (Fig. 1A), which controlled, in parts, the Anta emplacement. On the other hand, no deformation is observed in rocks from central facies of the pluton (e.g., AT-10, AT-11, AT-12, AT-13, and AT-14, Figs. 1B), the thin section (e.g. Figs. 2A and 2D) shows that primary magmatic structures were preserved. In fact, even magmatic foliation observed in the field in these sites and magnetic foliations are not parallel either to magnetic foliations from the eastern and Figure 8. Examples of magnetic fabrics determined from both anisotropy of low-field magnetic susceptibility (AMS) and anisotropy of anhysteretic remanent magnetization (AARM). All magnetic fabrics are coaxial. Squares are maximum susceptibility (K max ) and maximum remanence (AARM max ); triangles are intermediate susceptibility (K int ) and intermediate remanence (AARM int ) and circles are minimum susceptibility (K min ) and minimum remanence (AARM mim ). Dashed line ellipses = 95% confidence ellipses. Data plotted in the lower hemisphere stereonets. AT-9 is granodiorito to monzodiorito, AT-10 and AT-12 are monzo-to syenogranite.
western part of the pluton or to the regional deformation pattern (Fig. 9). Also, the magnetic lineation (Fig. 10) plunges from moderately to steeply. This indicates that the central portion of the Anta pluton was not affected by any tectonic deformation either during or after the emplacement, and magnetic fabric in this part of the pluton is probably primary (magmatic) in origin, acquired when the rocks were solidified reflecting magma flow. Therefore, the highest plunge lineation (AT-11, Figs. 2A and 10) could be linked to a magma feeder zone (magma chamber).  Since the borders -mainly the eastern one -of the pluton was affected by regional deformation, a question arises on whether the subhorizontal lineation represents an overprint of an initially steep lineation, reworked by shearing during or after emplacement. The AARM results clearly show that there is not a fabric overprint (i.e., AMS and AARM tensors are coaxial, Fig. 8). Two hypotheses can be evoked: • considering the syn-tectonic character of Anta granite, this regime affected only the borders of the pluton, which means that the magnetic fabric would be tectonic in origin, and the central section would represent an area of extension and, therefore, a preferential place for the ascension of magmas, as has been suggested by Raposo et al. (2012) for Piracaia pluton. Due to the dynamics of the Paraiba do Sul shear zone, the magma would be affected by strain and flow toward the borders, acquiring a magmatic foliation which evolved to solid state upon cooling; • considering that the highest plunge of magnetic lineation points toward south (in the central part of the pluton, AT-11, Fig. 10), it can be reasonably argued that the sites from the western border (which is less deformed) were strained by the shear zone. Low lineation plunges would be showing that these sites were fed by the source in the central portion (SW) of the pluton, in which high lineation plunges are found.
The latter hypothesis is corroborated by other undeformed sites from the central part. If this hypothesis is right, then the magma ascent started from the source in the SW part of the pluton and migrated to the borders, concomitantly with the movement of Paraiba do Sul shear zone that affected (syn-tectonically) this portion of the pluton. Therefore, the emplacement of Anta granite probably occurred during a local transpression due to a weak zone generated by Paraiba do Sul shear zone, in the syn-magmatism orogenetic phase that generated the transcurrent and transpressive opening that enabled diapirism with magmatic shortening, enabling the emplacement of the pluton. This weak zone was generated by thrust faults of orogenic eastern blocks over cratonic western blocks and refolded by Brazilian-Pan African orogeny recorded before to the syn-late magmatism (Heilbron and Machado 2003, Heilbron et al. 2013, Machado 2000. After that, the magmatic chamber housed in a transpressive regime, with a distensive component, was crystallized with a fractionated zoning (Fig. 11) similar to a model proposed by Bhatt et al. (2017), but in our case, with dextral movement.

SUMMARY AND CONCLUSION
The Anta pluton is composed of five petrographic units. Rock-magnetism determinations have allowed the characterization of magnetic properties and determine the internal fabric of the pluton. No SD effect was found in the AMS fabrics, as showed by rock-magnetism and AARM. The main magnetic mineral are magnetite grains, which are certainly responsible by magnetic susceptibility and AARM and probably by AMS fabric. No SD effect was found in the AMS fabrics, as showed by rock-magnetism, AARM and Dunlop's (2002) plot. The main magnetic mineral are magnetite grains, which are certainly responsible by magnetic susceptibility and AARM and probably by AMS fabric. Therefore, the AMS and AARM in the studied rocks are mainly due to the shape preferred orientation of magnetite grains. Both AMS and AARM tensors are coaxial and partially related to regional strain in the borders of the pluton, whereas they are related to magma flow in the central part (SW) of the pluton, where high lineation plunge suggests that this place could be linked to a magma feeder zone. Our data suggest that the regional strain did not affect the whole pluton.