The thrust contact between the Canastra and Vazante groups in the Southern Brasília Belt : structural evolution , white mica crystallinity and implications for the Brasiliano orogeny

Manuscript ID: 20160052. Received in: 04/12/2016. Approved in: 06/20/2016. ABSTRACT: Two regional thrust-sheets of Neoproterozoic metasedimentary rocks occur in the Southern Brasília Belt, northwest Minas Gerais. The lower one comprises the Vazante Group, that is formed in the studied area, from base to top, by the Serra do Garrote (metapelites interlayered with carbonaceous phyllite), Serra do Poço Verde (beige to pink stromatolitic metadolomite with interlayered greenish slates), Morro do Calcário (gray stromatolitic metadolomite interlayered with gray slates) and Serra da Lapa (phyllite with dolarenitic lenses interlayered with slates) formations. The upper thrust sheet consists of the Canastra Group (Paracatu formation): laminated sericite phyllites and carbonaceous phyllites interlayered with quartzite. The Braziliano orogeny resulted in four phases of contractional deformation, associated with low-grade metamorphism. The first two (D1 and D2) are ductile, while the third and fourth ones (D3 and D4) are brittle-ductile. D1 developed a slaty S1 cleavage subparallel to the primary layering, with shallow to steep dips to NW. D2 developed a crenulation cleavage (S2) that dips moderately to NW and is associated with tight to isoclinal folds. D3 and D4 phases developed crenulations and open folds and kink bands. S3 dips steeply to NW, while S4 has moderate to steep dips to NE and SW. White mica crystallinity (Kübler index) measurements in metapelites indicate that both the Canastra and Vazante groups reached anchizone/epizone conditions, and metamorphic discontinuities along thrusts indicate that the peak of metamorphism is pre or syn-thrusting.

The thrust contact between the Canastra and Vazante groups in the Southern Brasília Belt: structural evolution, white mica crystallinity and implications for the Brasiliano orogeny

INTRODUCTION
Since the discovery of zinc deposits within the Vazante Group metasedimentary rocks, in the early 20 th century, several structural and petrological studies have been carried out in this external portion of the Southern Brasília Belt (Figs. 1A and 1B), located in northwest Minas Gerais State (Dardenne 2000, Valeriano et al. 2004, 2008).
The Vazante Mine -with presently total assets of 40-60 Mt to 20% Zn -is the world's largest deposit of hydrothermal nonsulfide zinc (willemite), and it is operated by Votorantim Metais (Baia 2013).The zinc ores are associated with a steeply dipping fault of NE-SW strike direction, the Vazante Fault, and are hosted in the metadolomitic rocks of the Vazante Group, which are in contact with the metapelitic rocks of the Canastra Group.(Monteiro et al. 2006), with location of the boreholes in Vazante, Ambrósio and Fagundes areas (red dots).
The Vazante deposit (Fig. 1C) is part of an important belt of mineral deposits hosted by low-grade metasedimentary rocks of the external Brasília Belt, which also includes the Morro Agudo, Ambrósio and Fagundes lead and phosphate deposits, and the Morro do Ouro gold mine (Pinho 1990, Monteiro 2002, Monteiro et al. 2006, Diniz-Oliveira 2013, Slezak et al. 2014) In this region (Fig. 1), the main geological feature is the thrust contact between the phyllites and quartzites of the Canastra Group and the underlying metapelites and dolomitic rocks of the Vazante Group (Dardenne 2000).Over the years, many proposals on the hierarchy of the deformation phases in the Southern Brasília Belt have been discussed (Campos Neto 1984a, Pinho et al. 1989, 1990, Pinho 1990, Pereira 1992, Pinho & Dardenne 1993, Rostirolla et al. 2002), and will be detailed further in this work.In addition, new knowledge (Campos et al. 2015) related to the metamorphic conditions was accepted by recent studies of X-ray diffraction (XRD) in the rocks from the Canastra Group, located in Distrito Federal and Goiás state (Fig. 1B).
Despite those studies, there still are many uncertainties about the geological history of stratigraphic and tectonic evolution of the host metasedimentary basin of the mineralization, especially the Canastra and Vazante groups.This study aimed to characterize in more detail the petrography and structural evolution of the important contact zone between the Canastra and Vazante groups surrounding the Vazante mine area.An area of 400 km 2 was mapped at the scale of 1:100,000 in conjunction with structural analysis and petrographic characterization, with the objective to compare the tectonic evolution of these two important lithostratigraphic units (Carvalho 2013, 2015, Carvalho et al. 2014, 2015, González et al. 2014).
White mica crystallinity determinations by XRD (Yang & Hesse 1991, Verdecchia et al. 2011) were carried out in metapelites (slates and phyllites) in order to better characterize the degree of regional metamorphism, and whether any of the mapped thrust surfaces constitute important metamorphic discontinuities.

GEOLOGICAL SETTING
The Brasília Belt (Fig. 1B) is one of the most important geotectonic domains of Central Brazil and it is a thrust-fault complex of Neoproterozoic passive margin metasedimentary successions that were thrusted eastward against the western margin of the São Francisco Craton (Dardenne 2000, Valeriano et al. 2004, 2008), during the Brasiliano Neoproterozoic orogenic collage of the Gondwana supercontinent (Almeida 1967, Almeida & Hasui 1984, Neves et al. 1990), with the convergence of the Amazon, São Francisco and Paranapanema paleocontinental blocks (Almeida 1977, 1981, Neves et al. 1999, Dardenne 2000, Valeriano et al. 2004, 2008).
The Southern Brasília Belt shows a general increase in deformation and metamorphism from the cratonic zone to west, ranging from anchimetamorphic sediments in the former area to granulite facies rocks in the uppermost allochthons.
Studies dealing with the tectonic evolution of the Southern Brasília Belt in the Passos Nappe segment, south of the study area, indicate an inverted metamorphic zonation caused by a deflection of isotherms in a subduction zone setting and continuous non-coaxial shear expulsion of high-pressure rocks towards shallow crustal levels (Simões 1995), on top of the external thrust-fold belt of low-metamorphic grade.Biotite-bearing phyllites and schists occur along the base of the Passos Nappe, whereas the metapelitic rocks of the underlying thrust-fold belt are slates and phyllites of lower-metamorphic grade indicated by quartz-chlorite-white mica assemblages (Simões 1995, Valeriano et al. 2000).
The metamorphic peak in the upper Passos Nappe is pre or syn D 2 and occurred about 630 Ma (Seer & Dardenne 2000), followed by a retrogressive metamorphic event during nappe exhumation at ~610 Ma (Valeriano et al. 2004).The youngest K-Ar cooling on white mica around 600 Ma in the Passos Nappe, and around 590 Ma in the external thrust-fold domain (Valeriano et al. 2000), provides a time limit for the thrust stacking in the Southern Brasília Belt.
The deformational evolution of the Brasília Belt is consensually polyphased, involving early sin-metamorphic low-angle nappe emplacement followed by later folding and faulting at shallower crustal levels.
Deformational evolution of the Araxá and Passos upper metamorphic nappes (Valeriano 1992, Simões 1995, associations indicate a late-D 2 retrogressive event associated by those authors as related to nappe exhumation. In the underlying low-metamorphic grade thrust-fold belt, geometric models for the deformational evolution of Ibiá, Canastra and Vazante groups vary among several previous studies, but generally with a similar overall history involving early thrusting and late folding and faulting.Campos Neto (1984a) distinguished between seven phases of deformation in the Canastra and Vazante group rocks, north of the study area: the first two are ductile and related to the orogenic paroxysmal period with SW folding; the following three are also ductile, but related to a late period, respectively, of thrust-sheets parallel to the principal structures, NW and NE folding; and the last two are brittle-ductile, involving E-W folding and transverse faulting.Pinho et al. (1989Pinho et al. ( , 1990)), Pereira (1992) and Pinho and Dardenne (1993) defined only two deformation phases in the Canastra Group near Coromandel town, south of the study area: a first one of regional character related to shear zones and thrust belts that were responsible for the formation of the main penetrative foliation parallel to subparallel to primary layering; and a second one limited to kink bands, tension gashes and crenulations.
Two previous studies were performed around the Vazante Fault, within the study area of Vazante Group rocks.Pinho (1990) differentiated between four phases of deformation: the first two related with heterogeneous, brittle-ductile simple shear zones in progressive ductile regime; a third compressional phase characterized by reverse faults in ductile-brittle regime; and a last, extensional phase.Rostirolla et al. (2002), however, reported five deformation phases: the first two formed by heterogeneous brittle-ductile simple shear in a progressive ductile regime, the third one producing a ductile-brittle sinistral transcurrent pattern, and the last two developed under an extensional regime, with development of tension gashes.
Both the Canastra and Vazante groups were deposited in the context of the Meso to Neoproterozoic passive margin basin along the southwestern margin of the São Francisco Craton, during the break-up of the São Francisco-Congo craton by west-directed subduction and consumption at 900-950 Ma (Neves et al. 1996).The main structural deformation and metamorphic grade occurred at 650-610 Ma, during the Brasiliano orogeny (Pimentel & Fuck 1992).
XRD studies by Campos et al. (2015) have shown that the rocks of the Canastra Group located in Distrito Federal and Goiás state (Fig. 1B) are composed of quartz and muscovite with Kübler Index (KI) Full Width Half Maximum (FWHM) values ranging from 0.09 to 0.14°Δ2θ for fractions of less than 2 µm, and from 0.30 to 0.37°Δ2θ for fractions of less than 0.2 µm.These values, although not corrected according to the methods proposed by Warr & Rice (1994), indicate epizone metamorphism, while underlying rocks from the Bambuí and Paranoá groups exhibit Kübler index values within the transition between diagenesis-anchizone and anchizone-epizone.There is no metamorphic data available from the Vazante Group, but, as for the Canastra Group, it is considered to be of very low-metamorphic grade.

Canastra Group
The Canastra Group succession is regarded as a regressive megacycle that grades from continental shelf facies dominated by currents, and shallow platform facies dominated by storms.The Canastra Group consists of alternations of quartzite and carbonaceous phyllite with lateral and vertical gradations (Pinho & Dardenne 1993) and subordinate carbonate facies.It is divided, from base to top, into the following formations (Freitas-Silva 1991, 1996, Campos Neto 1984b, Dardenne 2000): Serra do Landim (greenish calc-phyllite and calc-schist); Paracatu (carbonaceous phyllite rich in organic matter and pyrite interlayered with white quartzite); and Chapada dos Pilões (regular intercalations of phyllite rich in organic matter and pyrite and quartzite on base and top).

Vazante Group
The Vazante Group (Dardenne 2000, Valeriano et al. 2004, Babinski et al. 2005) extends about 250 km in the N-S direction, and is predominantly composed of carbonate rocks interlayered with metapelitic rocks.It is regarded as shallow platform facies dominated by tidal currents, represented, from base to top, by the following formations: Retiro/Santo Antônio do Bonito Formation -basal unit of white quartzite and conglomerates interlayered with pelitic levels; Rocinha Formation -rhythmic sandstones and slates; Lagamar Formation -psammo-pelitic carbonate unit with alternating conglomerates, quartzite, metasiltstone and slates; Serra do Garrote Formation -dark to greenish gray carbonaceous slates, sometimes rhythmic, interlayered with quartzite; Serra do Poço Verde Formation -gray to pink metadolomite interlayered with greenish metapelite and marble, subdivided into Morro do Pinheiro and Pamplona members; Morro do Calcário Formation -stromatolitic 570 Brazilian Journal of Geology, 46(4): 567-583, December 2016 The thrust contact between the Canastra and Vazante groups metadolomite associated with oolitic and oncolytic limestones; and Serra da Lapa Formation -consisting of carbonaceous phyllite with metasiltstones, metadolomite lenses and minor quartzite levels.

Field and petrographic studies
The field studies involved detailed geological mapping of an area of 400 km 2 with characterization of the lithostratigraphic units of the thrust-contact between the Canastra and Vazante groups, and the geometry and superposition of deformational phases.This characterization was associated with petrographic examination of thin sections of selected samples of both units.

White mica crystallinity studies by X-ray diffraction analysis
Whole-rock white mica crystallinity by XRD analyses were carried out in the Centro de Investigaciones de Minerales Arcillosos (CIMAr) of the Universidad Nacional del Comahue, Argentina, for the measurement of KI of metapelites of the Canastra and Vazante groups.
Whole rock and clay minerals were identified using a Rigaku DMAX-2D diffractometer, employing Cu radiation, with a step size of 0.05º2θ and scanning speed of 0.01º/ min, at 40 kV and 20 mA.The preparations of the total rocks were scanned from 3º a 65º2θ, and the clay minerals (< 2 μm) were scanned from 40º2θ a 2º2θ.Clay-size fraction (< 2 μm) samples for XRD analysis were prepared following the recommendations of Moore and Reynolds (1997).A < 2 μm fraction, assumed to be representative of the neo-formed and transformed phases and conventionally used for main crystallographic index measurements, was separated from 10 metapelite samples.Clay-mineral composition was established by the comparison of orientated aggregates that were air-dried (AD), ethylene-glycol solvated (EG; 24 hours), and heated at 500ºC (H500; 4 hours).
The XRD reflections were evaluated with the Rigaku software.Quantitative analyzes of the clays were performed following the mineral intensity factor method described by Moore and Reynolds (1997).For quantitative estimation of phyllosilicate, the NEWMOD III program was used.The KI (Kübler 1968, Kish 1991) was measured in the white mica (001 crystallographic plane) reflection by the FWHM parameter of program, in AD oriented clay mineral aggregates.
The interpretation of KI for diagenesis and metamorphism is using the following boundaries for 0.25 and 0.42ºΔ2θ: more than 0.42º is diagenetic zone; between 0.25º and 0.42º the anchizone; and below 0.25º the epizone (Campos et al. 2015).

Lithostratigraphic units
The geologic map of the study area (Fig. 2) shows that the Canastra and Vazante Group rocks are in thrust contact, and therefore represent two tectonic terranes with distinct lithological and deformational characteristics.The Canastra Group, within the studied area, is represented only by the Paracatu formation quartzites and phyllites, thrusted over the carbonatic-pelitic rocks of the Vazante Group, represented by four units (from base to top): Serra do Garrote, Serra do Poço Verde, Morro do Calcário and Serra da Lapa formations (Figs. 2 and 3).

Canastra group
The local apparent thickness of the Canastra Group is 800 m, of which 600 m are quartz-sericite phyllite interlayered with carbonaceous quartzite and 200 m are laminated slates (Fig. 3).
The quartz-sericite phyllite is a fine grained carbonaceous rock of gray color, with millimeter-thick quartzite lenses.The mineralogy consists of quartz, plagioclase, K-feldspar, white mica, chlorite and anhedral opaque minerals, and detrital zircon and tourmaline (Fig. 4A).
Pure or impure quartzites displays white color, medium to coarse grained quartz and subordinate plagioclase, white mica, chlorite and opaque minerals (pyrite and magnetite).Metamorphic textures show evidence of dynamic recrystallization (Figs.4B and 4C) locally with polygonal grains.
The laminated slates exhibit very fine to fine grain size, with green and gray or purple color with some carbonaceous material, containing fine to medium-grained impure muscovitic quartzite lenses.

Vazante group
The local apparent thickness of the Vazante Group (Fig. 3) is 3,400 m, represented by the Serra do Garrote formation (1,000 m), Serra do Poço Verde formation (800 m), Morro do Calcário formation (700 m) and Serra da Lapa formation (900 m).These units are briefly described ahead, from bottom to top.

Serra do Garrote formation
This unit is predominantly composed of black carbonaceous laminated slates of fine to medium grain size with quartz, feldspar (submillimeter plagioclase with sericitization and chloritization), white mica and anhedral opaque minerals.The metamorphic texture is lepidoblastic, and primary layering is still locally preserved as differences in grain size and composition, with two distinct lithofacies: laminated metasiltstones and laminated metamudstone, containing millimeter-to centimeter-thick levels of metasandstones and metasiltstones.

Serra do Poço Verde Formation
The Serra do Poço Verde formation consists of a metadolomitic sequence formed by: stromatolitic intensely recrystallized gray metadolomites; beige to pink metadolomites with barite nodules interlayered with greenish metapelites, locally with mudcracks, and stromatolitic beige metadolomites.The lamination is locally preserved as microbial/algal mats (Figs.4D and 4E) and bird's eyes, oncolytic marble, metasandstone lenses and intraclastic breccia intercalations occur in all of these rocks.

Morro do Calcário formation
The metadolomites of the Morro do Calcário formation display bluish-gray colors and coarse grain size, with silicification features represented by chert.Algal mat structure is locally preserved, which reveals the primary layering of the rock.They are interpreted as dolostone with carbonate cementation or boundstones involving aggregation of ooids and peloids (Fig. 4F).
The gray slate intercalations have bluish-gray color, slaty texture with presence of impure fine metasandstones lenses.The particle size is fine with angular and rounded clasts, locally tectonically stretched.Mineralogy is given by sub-milimetric quartz, white mica (sericite) and chlorite, as well as anhedral opaque minerals.The thrust contact between the Canastra and Vazante groups

Serra da Lapa formation
The top unit of the local Vazante group is the Serra da Lapa formation, represented by metarhythmites and sericite phyllites with carbonaceous quartzite lenses.

Deformational evolution of the Canastra and Vazante groups
The dominant structural style of the external zones of the Southern Brasília Belt is characterized by complex structures related to regional ductile tectonics developed under low-grade metamorphism, generated by thrust-faults with general eastward tectonic transport direction.In the study area, one of these major thrust zones resulted in the juxtaposition of the Canastra Group rocks over those of the Vazante Group.The existence of this thrust is supported in the present work by detailed mapping of the Barrocão Synform area (Fig. 2), where the basal contact of Canastra Group rocks truncates underlying contacts within Vazante Group rocks.
Based on geometric style, orientation and superimposition of folds and associated (or absence of ) foliations and lineations, four deformation phases were recognized (Figs. 6 and 7), two pre-or syn-metamorphic phases with development of penetrative foliations, and two post-metamorphic phases with the development of crenulation cleavages superimposed over the previous two.
The structural analysis allows for the differentiation of four phases of superimposed contractional deformation: D 1 and D 2 occurred in the ductile regime with penetrative foliations associated with folding during the emplacement of a low-angle Nappe system with the development of a thrust fault, while D 3 and D 4 are brittle-ductile with crenulation cleavages associated with post-metamorphic peak shortening.In most cases, the thrusting accompanied the original sedimentary layering between Canastra and Vazante units with the development of cleavages with stretching lineation showing the same eastern direction as the thrust.
The four documented deformation phases in the studied area (Fig. 7) are a S 1 slaty cleavage, which is difficult to differentiate from the primary bedding (S 0 ); a S 2 crenulation cleavage, with associated L 2 intersection and stretching ■ D 1 : the first (D 1 ) deformation phase is essentially observed as a penetrative slaty cleavage (S 1 ), marked by the preferential orientation of phyllosilicates.As described by previous studies related to the Brasília Belt units, the S 1 cleavage in the study area is only clearly identified in S 2 fold hinges, where S 1 parallel to the primary layering (S 0 ) is cross-cut by the S 2 foliation (Figs.7A, 7B and 7C).
The S 1 (// S 0 ) foliation generally dips gently to WNW direction with maximum attitude of 290/22, and with a secondary concentration that dips to the opposite direction (Fig. 6).No lineation was noticed associated with S 1 foliation, possibly due to the strong overprint by the D 2 main deformation phase; ■ D 2 : the second (D 2 ) deformation phase was responsible for the development of intense tight to isoclinal folding and the main penetrative axial planar S 2 foliation, and associated stretching and intersection (S 2 x S 1 // S 0 ) L 2 lineations.The S 2 foliation predominantly dips moderately to NW (Fig. 6).Under the microscope, S 2 is generally observed as a crenulation cleavage near D 2 fold hinge zones or as an oblique foliation with respect to S 0 //S 1 in fold limbs.In thin sections (Figs.7B, 7C and 7D), the S 2 foliation is conspicuous in almost all rock types, except in the metadolomites, and is defined by preferred orientation of phyllosilicates, quartz, and platy opaque grains (Figs.7D and 7E).D 2 deformation is commonly associated with undulose extinction of quartz grains, and dynamic recrystallization textures with polycrystalline quartz with irregular serrate boundaries.Sericite and chlorite recrystallization and growth were also observed.An intersection (L 2 ) lineation, representing the axes of D 2 folds, shows a large dispersal of orientation, but with predominant low to intermediate plunges to the NW.An L 2 stretching lineation follows the same range of orientation Although the Vazante Fault was not studied here, this structure is important because it hosts the largest silicate zinclead deposit in the world, related to tectonic-hydrothermal activity near the contact between lower Pamplona and upper Morro do Pinheiro members, metadolomites of the Serra do Poço Verde formation, Vazante Group (Dardenne 2000, Appold & Monteiro 2009).It dips ~60-70º NW with N40-50E strike, parallel to regional geologic contacts.The Vazante fault is considered as an extensional structure by most authors, but with still unclear relationships with the timing of orogeny (Pinho 1990, Diniz-Oliveira 2013, Slezak et al. 2014).
One of the main D 3 structures in the studied area, named in this work as the Barrocão synform (Fig. 5), is a sub-vertical synformal fold with NW-trending axis that occurs in approximately 30 km 2 of the total mapped area.The orientation of this structure, which also folds several thrust surfaces, is coincident with the average orientation of D 3 crenulation lineation (Fig. 6), and is related to post-thrusting shortening.

White mica crystallinity studies by X-ray diffraction analysis
Ten samples (Tab. 1) from three drill holes in Vazante, Paracatu and Fagundes (Minas Gerais) areas (Fig. 1C) were collected for white mica crystallinity studies by XRD analysis (Gonzalez et al. 2014), aiming to detect a difference in metamorphic grade between the Canastra and Vazante thrust-sheets.
Eight samples from the Vazante Group consist of carbonaceous phyllites from the Serra da Lapa (three samples) and Serra do Garrote (three samples) formations and two samples of metadolomites from the Morro do Calcário formation.Two slate samples from the Serra do Landim formation, Canastra Group, were also analyzed.
The white mica crystallinity results (Tab. 1 and Fig. 8) show that in all samples the dominant phyllosilicate is illite, with subordinate chlorite.Percentages of illite and chlorite in the samples vary, respectively, from 60 to 100% and from 4 to 40%.The whole-rock results confirm the presence of abundant quartz and traces of 578 Brazilian Journal of Geology, 46(4): 567-583, December 2016 The thrust contact between the Canastra and Vazante groups plagioclase, K-feldspar and carbonate, as observed in thin sections.
The FWHM KI for white mica varies from 0.15 to 0.21 Δº2θ, and the KI CIS varies from 0.23 to 0.29 Δº2θ (Fig. 9).Values between 0.23 and 0.29 ∆º2θ suggest temperatures between 250 and 300ºC.In an average continental geothermal gradient of 30ºC/km, they would result in calculated depths of about 10 km.The measured KI results indicate a very low-grade metamorphism, in high anchizone to lower epizone conditions.
Only one episode of clay mineral growth in the rocks analyzed from Canastra and Vazante groups were reported by the white mica crystallinity data, which is coincident, respectively, with the phyllosilicates crystallization on the S 2 foliation.

DISCUSSION
Four phases of superimposed compressive deformation are geometrically characterized in the study area.The first two (D 1 and D 2 ) occurred in the ductile regime with the development of penetrative foliations associated with folds generated during the development of low-angle thrust-faults that affected the Canastra Group rocks.This contractional event, related to the peak activity of the Brasiliano orogeny, was also responsible for the low-grade metamorphism that originated phyllites and slates with growth of sericite and chlorite, also with quartz recrystallization.The third and fourth (D 3 and D 4 ) phases occurred under brittle-ductile regimes, with heterogeneous deformation involving folds, associated crenulations and kink bands, locally with faults and fractures  along axial planes.No mineral growth was observed associated with D 3 and D 4 structures, an indication that a shortening took place after the metamorphic peak.
Tentative correlation of the four deformation phases defined in this work can be made with those of previous studies of Vazante and Canastra groups, as follows (Tab.2): D 1 and D 2 correspond to the regional compressional shear zones and thrust-faults responsible for the main structures in the belt (penetrative cleavage parallel and sub-parallel to the primary layering), as defined by Pereira (1992) and Pinho and Dardenne (1993), and to the heterogeneous brittle-ductile simple shear in progressive ductile regime of Pinho (1990) and Rostirolla et al. (2002).D 3 and D 4 may be correlated with the pure shear brittle-ductile regime with kink bands, tension gashes and crenulation cleavages of Pereira et al. (1994) and of Pinho and Dardenne (1993), and with the sinistral brittle-ductile directional and brittle extensional phases of Rostirolla et al. (2002).A broader evolutionary model can be proposed from comparison of these local evolutionary schemes with similar studies in other segments of the Southern Brasília Belt, south of the study area.As proposed by Valeriano (1992), Simões (1995) and Seer and Dardenne (2000), all four deformation phases are compatible with a broad E-W orogenic compression, but in progressively shallower environments.D 1 and D 2 phases are related to thrust tectonics resulting in folds and thrusts with movement towards the São Francisco Craton.In the southern most segments of the Brasília Belt, the aforementioned authors relate D 3 folds with WNWtrending sinistral transcurrent shear zones which displaced the main thrust surfaces.D 4 folds, with predominantly NS-oriented axes, are related to final E-W shortening in a pure shear regime.
White mica crystallinity data show only one episode of clay mineral growth in the rocks analyzed from Canastra and Vazante groups, which are related to the second phase of deformation (D 2 ), contemporary with the regional  metamorphic peak (Rostirolla et al. 2002), which was also responsible for the development of penetrative S 2 cleavage in lower epizone conditions.Campos et al. (2015) recently measured KI values of samples from the Canastra, Paranoá and Bambuí groups in the Distrito Federal and adjoining areas in Goiás state.Although those values are in KI FWHM without correction, as indicated by Warr and Rice (1994) standardization's parameters, they conclude that the Canastra Group rocks reached epizone conditions, while the Paranoá and Bambuí samples, from underlying thrust sheet, reached only anchizone conditions.These results are consistent with the new results in this work, with both the Canastra and Vazante thrust sheet having reached high anchizone to epizone conditions, especially in the rocks above the thrust-fault contact.
As represented in Figure 9, a similar metamorphic degree is observed between the Canastra and the Vazante groups in the studied area.However, metamorphic discontinuities along thrust planes within the Vazante Group rocks suggest that metamorphism pre-dated thrusting, which is compatible with observations in other areas of the Southern Brasília Belt (Simões 1995, Valeriano et al. 2000).

CONCLUSIONS
In this work, we present a geological and structural map of an area of approximately 400 km 2 that shows that the psammo-pelitic metasedimentary rocks of the Canastra Group and pelitic-carbonatic metasedimentary rocks of the Vazante Group are separated by a regional thrust-fault, supported by detailed mapping of Barrocão synform area, where the Canastra Group thrust fault truncates contacts between Vazante Group strata in the footwall.The deformation in the Canastra Group rocks was more intense than in the Vazante Group rocks, with generally tighter main phase (D 2 ) folds in a similar style with thicker hinges and thinner limbs.Furthermore, metapelites of the Canastra Group are phyllites, in contrast with slates from the underlying Vazante Group.
Four deformation phases were defined in the study area.The first one (D 1 ) occurred in a ductile contractional regime and is represented by a slaty cleavage generally subparallel to bedding.The second phase of deformation (D 2 ) is also of ductile contractional nature and is represented by a crenulation cleavage associated with tight to isoclinal folds.The orientation of the L 2 stretching lineation, plunging predominantly to NW, supports tectonic transport to SE during D 2 .
The third and fourth phases of deformation (D 3 and D 4 ) are related to post-thrust stacking and developed gentle to open folds and associated kink bands and crenulations, but without the development of penetrative foliations.The third phase of deformation was responsible for the Barrocão Synform, an expressive map-scale structure mapped in this work.
XRD data on white mica crystallinity indicate that rocks below and above the thrust-fault contact between the Canastra and Vazante groups reached similar anchizone/epizone conditions, typical of lower greenschist facies.The Canastra Group rocks show only one episode of clay mineral growth related to chlorite crystallization on the S 2 foliation in syn-thrusting regime.In the Vazante Group, metamorphic discontinuities along thrust planes indicate that the peak of metamorphism probably pre-dated thrusting.

Figure 1 .
Figure 1.Geological location of the study area.(A) Tectonic provinces of the South American platform (Dardenne 2000) with the Brasília Belt in black; (B) Southern Brasília Belt with location of the Paracatu-Vazante zone, of the study area (red rectangle) and of samples analyzed by Campos et al. (2015) in red circles; (C) geological map of the Vazante Group (Monteiro et al. 2006), with location of the boreholes in Vazante, Ambrósio and Fagundes areas (red dots).

S 3 Figure 2
Figure 2. (A) Lithostratigraphic units and their structural relationship in the studied area; (B) geological section A-B from Carvalho et al. (2014).

Figure 6 .Figure 7 .
Figure 6.Comparative geometric characteristics of the observed deformational phases.Stereographic projections are equal-area using the lower hemisphere, with contours of poles to S 1 // S 0 , S 2 , S 3 and S 4 (black dots) and red circles representing either L 2 , L 3 or L 4 lineations, as indicated in each diagram.
(Figs. 7A, 7F, 7G and 7H); ■ D 3 and D 4 deformation phases: they are responsible for the development of open folding, generally without the development of any pervasive axial plane foliation.These structures heterogeneously overprinted the previous D 1 and D 2 structures (Figs.7D, 7E, 7F and 7G).D 3 and D 4 folds are both characteristically concentric, frequently with angular style, associated with small scale kink bands.D 3 and D 4 are only differentiated by orientation, since many outcrops display the overprint of both fold generation.D 3 folds have gently plunging axes (and L 3 crenulation lineation) with NW-SE direction.D 4 folds and crenulations also show gently plunging axes (and L 4 crenulation lineation), but with predominant NE-SW orientation.Folds of both deformation phases display steep to sub-vertical axial planes (Figs.7D, 7E, 7F and 7G).Fractures, tabular quartz veins and tension gashes are verified with the same direction of the D 3 and D 4 folds axial planes, locally closely spaced.Some normal faults were also observed with the same direction of the D 3 axial planes, generally dipping 60º-75º to NE, SE or SW.

Figure 8 .
Figure 8. Representative white mica crystallinity studies by X-ray diffraction (XRD) diagrams of Vazante/Canastra Group samples showing illite (I) and chlorite (Cl) peaks.Normal in red and glycollated in blue.

Figure 9 .
Figure 9. Kübler index diagram showing similar metamorphic grade between the Canastra and Vazante groups in the studied area.Metamorphic discontinuities along thrust planes in the Vazante Group rocks indicate that thrusting post-dated metamorphic peak.KI: Kübler index; FWHM: full width half maximum.

Table 1 .
X-Ray diffraction results for analyzed samples from the Vazante and Canastra groups.

Table 2 .
Comparison between deformation phases in this work and selected previous works.Here is presented a correlation based in the description of each structural geometry literature data.