Magmatic and tectonic evolution of the Chaval Granite at the end of the Neoproterozoic, northwestern border of the Borborema Province

The northwestern region of Borborema Province is represented by the Ceara Central and Northwest Ceara crustal blocks connected by an extensive transcurrent shear zone that represents the northern portion of the Transbrasiliano Lineament in a complex geological context, which brings together geological units of nature, origin, and ages of the Archean to the Paleozoic. In this scenario, there is a large amount of granitic bodies, with different natures, age and tectonic environment, but predominantly representing a more intense granitogenesis in the Paleozoic Neoproterozoic and early Paleozoic, with plutons emplaced in different stages of the Brazilian Orogeny. In this context, the Chaval Granite corresponds to an isolated body in the extreme northwest of Borborema Province, located near the Atlantic coast, in the northern states of Ceará and Piauí. It is an intrusive batholith housed in Siderian orthogneisses (Granja Complex) and in Neoproterozoic supracrustal rocks (Martinopole Group), but is partly covered by sedimentary rocks from the Parnaíba Paleozoic Basin (Serra Grande Group), and coastal Cenozoic deposits. Field data and petrographic studies highlight the porphyritic texture with microcline megacrystals involved in coarce matrix as a remarkable feature. The predominant petrographic types are granodiorites, with variations for monzogranites and tonalites. The predominant primary mineral constituents are pertitic microcline, oligoclase, and quartz; biotite and rarely hornblende as qualified minerals and additionally titanite, apatite, zircon, alanite, and opaque minerals. Another peculiar characteristic is the deformational features related to the installation of the Santa Rosa Transcurrent Shear Zone along its eastern flank. The effects of the transcurrent shear deformation led to the modification of the original magmatic fabrics in much of the eastern half of the batolith, generating various types of mylonites. Thus, the typically igneous textures preserved in the western half of the pluton were gradually replaced by tectonic fabrics, which initially evolved into proto-mylonites in the central portion of the body, grading to mylonites eastward, highlighting strongly stretching, comminution associated with dynamic recrystallization, highlighting the formation of microcline and plagioclase porphyroclasts in a mylonitic matrix, which are involved by mylonitic foliation. Geochemical studies reveal compositional similarities, compatible with petrographic classifications, in which they mostly present granodioritic composition, followed by monzogranites and tonalites, classified as I-type granites, peraluminous with compatible with the calcium-alkaline series. The geochemical signatures of the Chaval Granite indicate the character of the tectonic magmatic arc environment. U-Pb zircon analysis by Mass Spectrometry (LA-ICP-MS) indicates crystallization age of 633 Ma, placing it in the Neoproterozoic, late Cryogenic-Early Ediacaran period, being one of the oldest granitoids in northwestern Borborema Province, correlated to the granites of the Santa Quitéria Magmatic Arc in the Ceara Central Domain. Hf-TDM model ages (2.65 to 2.13 Ga) and εHf(t = 633 Ma) values from -9.6 to -18.1 suggest incorporation of neoarchean and paleoproterozoic crustal sources in their formation with a long crustal residence time. Similar Sm-Nd data in whole-rock indicate Nd-TDM model ages of 1.27, 1.72 and 2.04 Ga and negative εNd(t = 633 Ma) values of -2.64 to -9.13, indicating paleoproterozoic and mesoproterozoic sources, with considerable crustal residence time implying a more evolved nature.


INTRODUCTION
The Chaval Granite, the main object of the present study, outcrops near the Atlantic coast, north of Piauí and Ceará States, having as reference Chaval, Parnaíba, and Bom Princípio cities. It is a batholith of approximately 2,000 km 2 , inserted in the Northwestern Ceará Belt (NWCEB) , in the Northwestern Ceará Domain, on the northwest border of Borborema Province (Figs. 1 and 2).
The northwestern portion of the Borborema Province (BP), presents a wide variety of rocks from Archean to Paleozoic, with an emphasis on granite magmatism, highlighting bodies of varying sizes, natures, and ages, which are temporal markers of regional geological processes ( Figs. 1 and 2).
The literature presents several studies related to granitoids in this region (Sial 1989, Brito Neves et al. 2000, Fetter et al. 2000, 2003, Bizzi et al. 2003, Arthaud 2007, Ganade de Araujo et al. 2013. However, although cartographically well-identified, the knowledge of these granite bodies still lacks fundamental data for their comprehension and contextualization in the tectonic evolution of northwestern BP, such as structure and relationships with the surrounding rocks, petrography, geochemistry, typological characterization and isotopic and geochronology with more robust methods, which are fundamental to discuss correlations with better known of the granitogenesis events in the region. The granitogenesis in BP was divided into three main tectono-magmatic events recorded by Bizzi et al. (2003), approaching them as a succession of tectono-magmatic events related to the Brasiliano cycle, defined as follows: Supersuite I (early to syn-Brasiliano); Supersuite II (late-Brasiliano); and Supersuite III (post-Brasiliano).
In the case of Chaval Granite, considering the absence of detailed petrographic studies, geochemical and isotopic data, and previous discrepant geochronological data, makes it difficult to correlate it with other known granites.
The study developed here shows new field data, detailed petrographic analyses, isotopic and geochemical data, new geochronological analysis approach of this important magmatic unit, complementing the gaps of previous works and clarifying a wide range of questions from the magmatic and tectonic nature, and the process of emplacement and structuring of the Chaval Granite. With these new data, we favor studies of correlation with other events in the region, discussions and interpretations about the meaning of this body in the NW evolutionary context of BP.

GEOLOGICAL CONTEXT OF THE NORTHWESTERN BORBOREMA PROVINCE
The BP is a large and important crustal compartment in the Northeast region of Brazil, with correspondence in the northwestern portion of the African continent, especially the orogenic systems of the Brasiliano-Pan-African cycle (Brito Neves et al. 2001). It represents a complex polycyclic evolution, recording ages from the Archean to the Neoproterozoic, with a marked influence of the Brasiliano/Pan-African cycle, which was responsible for the end of the amalgamation of the Gondwana Continent, between 660 and 570 Ma (Brito Neves et al. 2000).
The north-northwest portion of Borborema Province is divided into six major structural domains called Northwestern Ceará (NWCED), Central Ceará (CECD), Orós-Jaguaribe, Rio Piranhas-Seridó, São José do Campestre and Zona Transversal (Brito Neves et al. 2000, 2001, Arthaud 2007, Gomes et al. 2019 (Fig. 1). These domains are delimited by mega-transcurrent shear zones evolved at the end of the Neoproterozoic.  bodies, more precisely in the NWCED and CECD of nature, age and tectonic environments, which are important markers of tectonic events and magmatic evolution.
The study area is located in the NWCED, which is delimited by the Sobral-Pedro II Lineament that is part of the Transbrasiliano Lineament to the north (Fig. 2). The NWCED consists of Paleoproterozoic basement (Siderian period), dated 2.35 Ga (Fetter et al. 2003), represented by the Granja Complex, constituted by tonalitic and granodioritic orthogneisses, amphibolites, sillimanite-garnet gneiss, migmatites, and granulites.

GRANITOGENESIS OF THE NORTHWESTERN BORBOREMA PROVINCE
The Neoproterozoic in the northern Borborema Province is marked by the building of orogens related to the Brasiliano Cycle with intense magmatic activity, diversified granitogenesis, development of extensive shear zones, and formation of metamorphic supracrustal successions that have reached metamorphic conditions of high-amphibolite to granulite facies (Brito Neves et al. 2000, Almeida et al. 2002, Cavalcante et al. 2003, Arthaud 2007, Ganade de Araujo et al. 2014, Amaral et al. 2015.
At the northwestern edge of the Borborema Province, other granitoids in isolated plutons present deformational effects such as the Pedra do Sal, Chaval, and Tucunduba granites, which are cut by transcurrent shear zones , Gorayeb & Lima 2014 and are certainly correlated to older events as discussed above.

Granitoids of the Tamboril-Santa Quitéria Complex (Magmatic Arc)
The Tamboril-Santa Quitéria Complex (TSQC) include a group of the granitoids from northwestern of BP, which are the oldest granitic rocks of the Neoproterozoic rocks of CECD and are distributed over approximately 40,000 km 2 with NE-SW structural trends (Fig. 2). It is a granitic-gnaissic-migmatite complex whose main characteristic is the intense migmatization associated with a large volume of anatectic granites. Fetter et al. (2003) reported age of 665 ± 5 Ma (U-Pb in zircon) for the volcanic rocks flanking the batholith in the TSQC. The more deformed granitic plutons revealed ages dated between 637 ± 6 and 624 ± 1 Ma, with possible magmatism continuation until 591 Ma. These authors also stated that this magmatism is related to plutonism in a continental magmatic arc (Santa Quitéria Magmatic Arc) whose intense deformation and anatexis resulting from the Brasiliano/Pan-African collision hinders the reconstruction of the arc geometry. In addition, it is suggested that the granitic plutonism represents the last stages of the arc evolution, with a progressive increase of the crustal participation, especially by remelting of the earlier magmatic material.
Still, Fetter et al. (2003) divided the granitoids into four main groups, which represent the evolution phases of the magmatic arc, described below: • Group 1: comprises pre-collisional granitoids, consisting of diorites to granodiorites, with high Mg and low K that represent the most primitive phase of the arc's continental magmatism. Gray granodiorites, sometimes deformed and metamorphosed, that were partially removed in the later stages of arc development predominate. They are associated and mixed with schists, gneisses with different migmatization degrees. Mafic types with irregular distribution and dimensions, such as amphibolites, are also observed. In contrast, there are heterogeneous, more felsic migmatite complexes that host extensive mafic bodies regionally, but also occur around newer plutons with megacrystals; • Group 2: includes more evolved pink and gray granites associated with nebulite migmatites, represented by quartzrich rocks, from granodiorite to granite composition. They represent higher degrees of pre-collisional diorite removal; • Group 3: it is represented by porphyritic granodiorites and monzogranites, with feldspar megacrysts, weakly deformed. Locally, these rocks contain varying amounts of rounded or irregular diorite enclaves, with no major signs of magma interaction, representing phases of non-plutonic dikes. This association is interpreted as representing the emplacement of the granites related to the regional phase of tension during arc development. This group is significantly less abundant than the other igneous associations of the TSQC; • Group 4: represents the final phase of the magmatic arc development that is characterized by the emplacement of granitoids with high K and low Ca, predominantly monzogranitic composition with feldspar megacrysts. They include calcium-alkali and alkali-calcium plutons. This group represents the progressive gradual participation of the crustal materials, mainly with remelting of the first two groups, suggesting the existence of several magmatic pulses in the final stages of arc development.
These first two lithological groups are characteristic of the early arc magmatism in terms of composition, structure, and evolution.
Ganade de Araujo et al. (2014) also provided data supporting the idea that the granitoids of the TSQC represent different phases of a magmatic arc, dividing it into three main phases, as follows: • Juvenile arc magmatism (880 to 800 Ma): this phase is basically represented by granodiorites and tonalities of the Tamboril and Lagoa Caiçara units, and originates in an early subduction zone in extensional environment with great contribution of juvenile magma attributed to the consumption of the Goiás-Pharusian Ocean. This phase still accounts for the continuation of the subduction, development of extensional basins of retro-arc with magmatism associated and supracrustals derived from both the arc and the continent (crustal); • Magmatism related to mature arc of the Andean type (660 to 630 Ma): it represents younger granitoids of the Santa Quitéria and Boi units, and a set of gneisses and granitoids from the Lagoa Caiçara unit. At this stage, the magmatism sources are both mantelic and crustal, with characteristics of a more mature stage related to subduction environment; • Reworking of arc rocks in the event of crustal anatexis (620 to 610 Ma): this phase is basically represented by granitic neosome, grouped in the Tamboril unit, resulting from the refusion of the surrounding protolith, mainly intermediate composition orthogneisses of the Lagoa Caicara and Santa Quiteria units and small portions of metasedimentary rocks of the Ceará Complex. The isotopic composition of neosome reflects an early source of crustal components. This phase represents the end of the collision with two subductions of the continental crust to the west and east of the Santa Quitéria Magmatic Arc (back-arc basin).

Post-orogenic granitoids
A wide range of granite plutons is distributed along and near the main axis of the Sobral-Pedro II Lineament (TBL). They represent post-orogenic bodies intrusive in the volcano-sedimentary successions of the Ubajara and Jaibaras groups, as well as in the basement gneisses. They are bodies housed in shallow depth, at higher crustal level, developing an expressive aureole of thermal metamorphism in larger bodies, that reached maximum conditions in pyroxene-hornfels facies (Danni 1972, Gorayeb & Coimbra 1995. This magmatism is related to the extensional tectonic event that generated horst and grabens, such as Jaibaras Graben, in the interface between the CECD and NWCED of the Neoproterozoic-Paleozoic boundary. They were grouped in the Meruoca Granitic Suite constituted by the Meruoca, Mucambo, Serra da Barriga, Anil and Pajé granitic plutons, and the Aroeiras dike swarm and other smaller bodies (Costa et al. 1979, Gorayeb & Abreu 1991, Gorayeb et al. 1993, Gorayeb & Soares 1994, Nascimento 2012, Gorayeb et al. 2014a, 2014b. To the southwest of the city of Chaval, a peralkaline pluton (Brejinho Nepheline Syenite) is also correlated to this extensional tectonics (Gorayeb et al. 2011).

GEOLOGY OF THE AREA
The Chaval Granite is located at the northwestern edge of the Borborema Province, in the Northwest Ceará Belt , Gorayeb & Lima 2014. The principal geological units in the region comprise Paleoproterozoic orthogneisses (Granja Complex), Neoproterozoic supracrustal rocks (Martinópole Group), Paleozoic sedimentary rocks of the Parnaíba Basin and recent coastal sedimentary cover (Figs. 3 and 4).
The Chaval Granite stands out as an expressive body of batholitic dimensions in the northwest end of the area, bordered by the Santa Rosa Transcurrent Shear Zone (SRTSZ) to the east, disappearing under sedimentary deposits to the south and west (Figs. 3 and 4C).
An alkaline pluton named Brejinho Nepheline Syenite (Gorayeb et al. 2011) is a small alkaline body located southwest of the studied area, showing intrusive relationships in orthogneisses of the Granja Complex and sectioning the SRTSZ. Rb-Sr dates in whole-rock indicate age of 554 ± 11 Ma (Gorayeb et al. 2011). This small pluton is considered an important representative of post-tectonic magmatic phases related to the extensional tectonics of the early Paleozoic, which formed the Jaibaras grabens system (Gorayeb et al. 1993).
In the southwestern part of the area, Paleozoic sedimentary rocks of the Serra Grande Group, consisting of thick sub-horizontal layers of conglomerate and sandstones representing the basal unit of the Parnaíba Basin, are placed on non-conformities in the units described above (Fig. 4D).

FIELD ASPECTS AND PETROGRAPHY OF CHAVAL GRANITE
Initially named "Chaval-type granitoid" in the Jaibaras Project (CPRM) by Costa et al. (1979), the Chaval Granite defines a batholith of approximately 2,000 km 2 that outcrops near the Atlantic coast between the states of Piauí and Ceará, having as reference the cities of Bom Princípio, Parnaíba (PI) and Chaval (CE). Although a large part of the body is covered by sedimentary rocks from the Parnaíba Basin, to the southeast, and by Cenozoic sediments from different coastal environments, such as wind, alluvial, and mangrove deposits, large rock exposures of Chaval Granite occur along the drainages and in hills and boulders with bulging tops, without major relief highlights. On the eastern side of the study area, the granitoid presents an intrusive relationship with the orthogneisses of the Granja Complex, which are difficult to recognize due to the deformation imposed by the SRTSZ, demarcating a tectonic contact.
The petrographic analysis of 36 samples representing the varied petrographic facies of the Chaval Granite was performed using conventional optical microscopy, for mineralogical characterization and quantification, and textural/microstructural analysis. Modal mineralogical analysis of nine representative samples was performed using SWIFT Automatic Point Counter from the Petrology Laboratory of the Graduate Program of Geochemistry and Petrology/Geosciences Institute/Federal University of Pará (LAPETRO/PPGG/IG/UFPA), with 1,200 or 1,500 counts according to sample grain variation. The petrographic classification was based on Streckeisen (1976), Le Maitre (2002), Fettes andDesmons (2008), andPaschier &Trouw (1998), and the modal results were plotted as Q-A-P and Q (A + P)-M' diagrams.
The samples analyzed were widely distributed in the outcropping areas of the granitic body (Fig. 3). Despite its batholitic dimensions, it presents relatively homogeneous mineralogy but with significant textural/microstructural variation that changes from typically magmatic features to mylonitic structures, reflecting the SRTSZ movement at the eastern interface of the pluton with the gneiss and schists country rocks.
The Chaval Granite has two fabric domains with very distinct characteristics, mainly from the structural point of view. The first domain comprises typically plutonic rocks with preserved magmatic features, represented by porphyritic granites occupying the central and western portions of the body (Figs. 5 and 6). The second domain consists of mylonitic granites with striking records of shear deformation and gradually varying intensity, distributed since central until eastern portions of the body, and resulted from the establishment of SRTSZ (Figs. 3 and 6). Lenticular and irregular enclaves or schllieren sheets (concentration of biotite) are oriented according to the magmatic flow (Figs. 5D and 5F). Some with irregular shapes, fine granulation, and intermediate composition with xenocrysts are also observed (Figs. 5D and 5E). Its origin can be related to magma mixing. Schllieren types concentrated in biotite can be explained as residues from the fusion of the original sources of the magma (restites).
Small intrusive bodies, hololeucocratic pegmatitic and aplitic veins and dikes, rich in alkali-feldspar and quartz, are observed sectioning the main rocks. They sometimes present small laccoliths or inverted funnel-shape, which represent the most evolved phases of the evolutionary magmatic process of the Chaval Granite (Fig. 5C).
The plutonic-type textures are located in the central portion to the west of the body. On the opposite side, from the central portion to the east, the records are typical of shear deformation with progressive transformations, with greater deformation intensity toward the SRTSZ. The main petrographic types within the domains will be described below.

Porphyritic granites
Low to non-deformed domain of the granite occurs in the western portion of the batholith close to the cities of Buruti dos Lopes, Parnaíba, and Bom Princípio, where magmatic characteristics are preserved with little or no record of ductile deformation. They are porphyritic granites, composed of megacrysts of alkali-feldspar (up to 10 cm), with remarkable oscillatory zoning, in coarse grain size phaneritic matrix. The granites are leucocratic, equigranular (in their matrix), with mineral association consisting of microcline, plagioclase, quartz and titanite in varying amounts, followed by biotite, as well as allanite, zircon, apatite, and opaque minerals as accessory phases.
The most striking structures are magmatic flow layering, defined by the preferential alignment of tabular microcline phenocrystals (Fig. 5A).
The accumulation of microcline megacrystals in concentration between 60 and 90% in relation to the matrix is common (cumulus microcline megacrystals with intercumulus), characterizing cumulatic syenitic or quartz syenitic rocks (Fig. 5B). This is related to the magmatic differentiation process in an important phase of granitic pluton evolution (Gill 2010).
The modal analysis data of undeformed granite samples (Tab. 1) reveal only small variation in the mineralogical content, so that in the Streckeisen diagram (Le Maitre 2002) the samples plot predominantly in monzogranite and granodiorite fields, except for a sample that plots in the tonalite field Stratified sandstones of the Serra Grande Group exposed in a section on BR-343. (Fig. 7). In this diagram, the samples show a slight alignment comparable to the calcium-alkaline trend of granite series of Lameyre and Bowden (1982).
Microscopic observation shows that tabular euhedral phenocrysts are mainly perthitic microcline (rarely plagioclase), displaying Carlsbad twinning, usually zoned concentrically whose crystal growth zones are demarcated by the inclusion of biotite lamellae in aligned trails. The megacrystals are supported by a coarse-grained matrix with a hypidiomorphic granular texture, consisting predominantly of well-developed crystals of plagioclase, microcline, quartz, and biotite (Fig. 8).

Deformed granites
The fabric observed in the deformed granite is related to the SRTSZ activity. While maintaining the porphyroid aspect, with deformational fabric show gradually increasing inf deformation from west to east, in the eastern portion of the batholith, overlapping the original igneous fabric. This domain corresponds to what Gorayeb and Lima (2014) defined in their structural map as Domain B (subdomains B1 and B2), with representative outcrops in the city of Chaval and surrounding areas (Fig. 3). Figure 9A shows an extensive outcrop where deformed granitoids occur. . Note local accumulation of microcline megacrystals preferably aligned, denoting magmatic flow in channels and conduits within the residual magma; (B) Porphyritic granite with magmatic flow structure with subvertically aligned microcline tabular megacrystals in the lower half of the photo; and in the upper portion, accumulation of these crystals generating sienitic cumulates (magmatic differentiation) by gravitational rise in the residual liquid; (C) Small intrusive leucogranites bodies in the form of inverted funnelshape (F) and laccolith (L) with flow upward in small conduits, representing late phase of the magmatic differentiation process (see red arrows); (D) Several mafic enclaves encased in porphyritic granite, forming hybride microdiorite with flow magmatic structure, denoting magma mixing process; (E) Small mafic-microdioritic enclaves with irregular contacts and shapes and xenocrysts, enclosed by granite with cumulated megacrystals aligned (magmatic layering) related to magma mixing; (F) Schlieren-type enclaves (biotite concentrates) oriented according to the magmatic flow.
Based on the deformational aspects, two subgroups were identified. The first subgroup (B1) is represented by partially deformed rocks, exhibiting evidence of deformation, but preserving the original magmatic (plutonic) features, characterizing the beginning of the mylonitic deformation, affecting especially quartz crystals of the matrix (Fig. 6). The microcline megacrysts are not significantly modified, maintaining the original shapes only with microfractures and crystal segmentation (Figs. 6A and 6C). On the other hand, the reduction of the matrix granulation (comminution) from coarse to medium-or fine-grained is already observed. This process developed a spaced foliation defined by the stretching and preferential orientation of quartz crystals and biotite lamellae, characterizing the ductile deformation (Figs. 9B-9F). With these limited modifications of primary fabric, the rocks are classified as protomylonites based on the mylonite classifications of Bell and Etheridge (1973) and Sibson (1977).
In the B2 subgroup, the igneous textures appeared more modified, showing the higher intensity of the shear processes, with typical mylonitic features, as indicated by Passchier and Trouw (1998) and Trouw et al. (2010) (Fig. 10). They include strong foliation transposition and mineral stretching, tectonic banding, sub-grain, recrystallized polygonal grain aggregates, and mylonitic anastomosed foliation (Figs. 10A-10F). Microcline porphyroclasts (originally phenocrysts) are present as stretched almond shape, sometimes acquiring a sigmoidal shape (Figs. 10B-10D), immersed in the mylonite matrix represented by ribbon quartz crystals and strongly oriented   biotite lamellae and fine quartz-feldspathic aggregates (Figs. 6F, 10C, 10D and 10F). The occurrence of S-C fabric is common (Fig. 6E). In this case, the fine or medium-grained rocks are a product of intense comminution by dynamic recrystallization. Based on the classification proposal by Trouw et al. (2010) can be classified as medium-grade mylonites.
The loss on ignition (LOI) (mainly H 2 O) was determined using thermogravimetric techniques, in which a predetermined sample amount is dried at 105ºC to remove moisture, followed by burning at 1,000ºC. The samples presented total values close to 100%, indicating low fire loss values and good analytical quality. To calculate the parameters and use in the geochemical diagrams, the concentrations of the major elements were recalculated using the conversion factor for volatile correction, according to the procedures by Rollinson (1993), Wilson (1989) and Gill (2010).
The discriminant diagrams of element variation and correlation with the obtained geochemical data were performed using the GCDKit 3.0 software. The purpose was to define the nature of the magmatism and the tectonic environment of body emplacement, providing knowledge on the processes that influenced the Chaval Granite formation.
The data in Tables 2A and B show small differences in the contents of the major elements in the studied samples, reflecting the original composition of the petrographic types.
In the Harker diagrams (Fig. 11), the compositional homogeneity of litotypes is better observed, therefore, the TiO 2 , CaO, P 2 O 5 , MgO, and Fe 2 O 3 (t) diagrams present incipient negative correlation with increased SiO 2 , and positive with Na 2 O for more evolved rocks. The trace elements show lesser compositional difference between the petrographic non-deformed types show that Rb and Ba behave compatibly since the contents decrease as silica increases, although they do not present continuous trends. The Sr content was directly proportional to the silica increase, in more evolved rocks, even with discontinuous trends. Y has a negative trend, decreasing for more developed rocks. Ga levels, on the other hand, show discontinuous trends that decreased in more evolved rocks. The Nb content displayed a discontinuous trend, decreasing with increasing silica, which is, decreasing in more evolved rocks. The discriminant geochemical diagrams such as the R1-R2 classification (La Roche et al. 1980) show that most samples are located in the granodiorite field, whereas two samples (2011/CHA-29 and 2011/CHA-35) are in the tonalite field (Fig. 12). These geochemical behaviors are compatible with the petrographic classifications.
In the Shand alumina-saturation diagram (Fig. 13), most samples are observed in the peraluminous field grading to the metaluminous field, which is in agreement with the petrographic data in the presence of biotite, alkali-feldspar, and plagioclase.
In the AFM diagram, the samples lie below the dividing curve and clearly define a compositional trend compatible with the calcium-alkaline series (Fig. 14).
In the multi-element diagram normalized to the Thompson (1982) primitive mantle the samples show similar geochemical signatures, indicating co-geneticity with large ion light element (LILE) enrichment compared to the light rare earth elements (LREE) and high-field-strength elements (HFS), and negative Ba, Nb, P, and Ti anomalies, also reflecting the compositional variations (Fig. 15).
The behavior of rare earth elements (REE) also demonstrates this similarity by highlighting a slightly inclined pattern with enrichment of LREE compared to heavy rare earth elements (HREE), with moderate to high fractionation, with La/ Yb ratio between 4.5 and 27, and moderate negative europium anomalies [(Eu/Eu*) N = 0.26 to 0.9] (Fig. 16).
In the granite typology diagrams of Whalen et al. (1987), the geochemical data are mostly in the field of I and S granites type, with some samples at the edge of this field (Fig. 17).
In the tectonic environment classification diagram by Pearce et al. (1984), the samples of the Chaval Granite plot in the field of granite magmatic arc, and according to Brown et al. (1984) are comparable to the Normal Continental Arc granites (Fig. 18). This allows linking the Chaval Granite emplacement to an orogenic environment related to the continental collision according to concepts of Pitcher (1993) and Barbarin (1999), and sin-collisional (Pearce et al., 1984, Maniar andPiccoli, 1989).

U-Pb GEOCHRONOLOGY
The ages of the Chaval Granite were determined by the U-Pb zircon dating technique, using the Thermo Finnigan Neptune Multi-collector mass spectrometer (ICP-MS-LA) in the Isotopic Geology Laboratory of the Geosciences Institute of the Federal University of Pará (Pará-Iso/IG, UFPA). The zircon grains were previously concentrated using conventional techniques, which included manual sifting in two fractions (250-180 and 180-125 μm), magnetic separation with neodymium magnet and Frantz Isodynamic apparatus, and gravimetric separation using the panning technique and micro-panning with 96º alcohol. The analytical procedures followed the recommendations of Ludwig (2003), Bühn et al. (2009), Chemale Jr. et al. (2012), and Milhomem Neto et al. (2017b. Cathodoluminescence images of the zircons were obtained using the scanning electron microscope (SEM) in the Microanalysis Laboratory of IG/UFPA.
The zircon grains were selected and fixed on cylindrical mounts in epoxy resin and later, polished to obtain a smooth surface. Subsequently, they were analyzed with a laser [New Wave UP 213 Nd: YAG (λ = 213 nm)] coupled to a mass spectrometer (ICP-MS) at 10 Hz frequency, approximately 100 mJ/cm 2 energy and beam size between 15 and 30 μm. The instrumental mass differences were corrected using the GJ-1 standard zircon analysis ( Jackson et al. 2004). The age calculations and the U-Pb data points were plotted in the Wetherill diagram using the ISOPLOT/EX 3.0 software (Ludwig 2003).
For the geochronological studies, four samples of the Chaval Granite were selected and treated, two from the preserved magmatic portion (2016-CHA-02 and 2016-CHA-05) and two from the deformed portion (2016-CHA-03 and 2016-CHA-12); however, only the two samples 2016-CHA-02 and 2016-CHA-05 produced satisfactory results.
The geochronological analysis results are displayed in Tables 3 and 4. Initially, the data show Th/U ratios between 0.15 and 1.0 for the majority analyzed zircon crystals, compatible with the magmatic zircon values (Th/U > 0.1) reported by Hoskin & Black (2000) and Rubatto (2002).
Thirty-three crystals from the 2016-CHA-02 sample were analyzed, and the isotopic data allowed calculating the discord line that resulted in a superior intercept age of 669 ± 68 Ma with MSWD = 0.11. However, only 18 zircon crystals defined a more accurate concordia age of 632.9 ± 8.3 Ma with MSWD = 1.5 (Fig. 21A), with a high degree of concordance and high analytical reliability. Thus, the age of 633 Ma is interpreted as representing the crystallization age of Chaval Granite.
Twenty-six crystal from the 2016/CHA-05 sample were analyzed, and the isotopic data allowed calculating the discord line that resulted in a superior intercept age of 528 ± 59 Ma with MSWD = 0.79. However, only 9 zircon crystals defined a more accurate concordia age of 633 ± 11 Ma with MSWD = 0.00014 (Fig. 21B). These data are similar to the other results and are interpreted as the age of crystallization for Chaval Granite.

Whole-rock Sm-Nd geochronology
Besides the crystallization age of the Chaval Granite, an isotopic study with the Sm-Nd -Model Age (T DM ) system was performed to determine the age of mantle separation/ segregation from the original magma during the formation of the studied granite.
The Sm-Nd isotopic analyses were performed in Pará-Iso Laboratory of Geoscience Institute/UFPA, following the analytical procedures of Gioia & Pimentel (2000) and Oliveira et al. (2008). Approximately 100 mg of pulverized rock was mixed with 100 mg of a 149 Sm-150 Nd Spike solution, which was dissolved in a Savillex vessel, using HNO 3 , HF, and HCl. The elements were extracted by two-stage ion-exchange chromatography on Teflon columns using the Eichron Ln resin for separation of Sm and Nd.
To correct mass discrepancies, the 143 Nd/ 144 Nd ratio was normalized to 143 Nd/ 144 Nd = 0.7219, using the exponential law (Russel et al. 1978). The accuracy and reproducibility of the results were controlled based on the reference materials BCR-1, 143 Nd/ 144 Nd, with a mean value (n = 7) of 0.512649 ± 12 (2σ) and La Jolla 143 Nd/ 144 Nd with a mean value (n = 7) of 0.511853 ± 5 (2σ). The decay constant used was 6.54 × 10 -12 a -1 according to Lugmair and Marti (1978) and the Nd model age (T DM ) was calculated according to the evolutionary mantle model of DePaolo (1981). During the Sm and Nd procedures, the chemical blanks were less than 0.1% of the concentrated element and were considered insignificant.
Whole-rock Sm-Nd data are listed in Table 5 and plotted in an ε Nd (t) versus Age (Ma) evolution diagram (Fig. 22). The obtained values are acceptable for ratios 147 Sm/ 144 Nd    Thompson (1982), for the Chaval Granite. (0.10202 to 0.12685) and degree of fractionation (-0.355 to -0.481), according to Sato and Tassinari (1997). The ε Nd (t) values calculated according to the crystallization age obtained in this work (t = 633 Ma), indicate negative values of -2.64, -8.06, and -9.13 and the calculated model ages (T DM ) indicate values of 1.27, 1.72, and 2.04 Ga.

In situ zircon Lu-Hf isotopes
Sample zircons (2016/CHA-02) were analyzed for Lu-Hf isotopes in domains with the same or similar internal structure to those analyzed for U-Pb dating. In this study, all the Hf isotopic measurements were performed on zircons with more than 95% of concordance on U-Pb ages. Initial 176 Hf/ 177 Hf ratios and ε Hf (t) values were calculated for the respective U-Pb ages of the granitoids, using t = 633 Ma. The procedure of Hf analysis (Milhomem Neto et al. 2017a) was developed using a Neptune Thermo Finnigan multi-collector MC-ICP-MS coupled with an Nd:YAG 213 nm LSX-213 G2 CETAC laser microprobe. The laser spot used was 50 μm in diameter, with an ablation time of 60 s, a repetition rate of 10 Hz, and He used as the carrier gas. Mass bias corrections of Lu-Hf isotopic ratios were done by applying the variations of GJ-1 standard. The raw data were processed in Microsoft Excel worksheets to calculate the 176 Hf/ 177 Hf and 176 Lu/ 177 Hf ratios, the Hf model-age and ε Hf (t) parameter for each analyzed point. The results are presented in Table 6. ε Hf (t = 633 Ma) has been calculated using current chondritic uniform reservoir (CHUR)  values of 176 Hf/ 177 Hf = 0.282785 and 176 Lu/ 177 Hf = 0.0336 by Bouvier et al. (2008). 176 Lu/ 177 Hf = 0.0388 and 176 Hf/ 177 Hf = 0.28325 were used for depleted mantle (Andersen et al. 2009). 176 Lu/ 177 Hf = 0.015 were used as the mean value of the continental crust to calculate the two-stage crustal Hf model age (Griffin et al. 2002, Belousova et al. 2009. Nine representative zircons of sample CHA-02 were analyzed. The results show variable ε Hf (t = 633 Ma) values ranging from -9.6 to -18.1 and Hf crustal model ages from 2,131 to 2,653 Ma with an average age of ~2.32 Ga (Tab. 6, Fig. 23).

DISCUSSION AND FINAL CONSIDERATIONS
Field geological, geochronological and geochemical data allow us to conclude that the Chaval Granite occupies a vast outcrop area, featuring a batholith of more than 60 km wide, representing the most important magmatic body of the Northwest Ceará Domain. Its magmatic evolution with housing in plutonic conditions at medium crustal level may be related to a magmatic arc environment at the end of Neoproterozoic, whose southwest continuity hides under sedimentary cover (Parnaíba Block) (Brito Neves et al. 1984, Daly et al. 2014. The results bring important advances to the geological knowledge of the region since it presents petrographic data associated to geochemical and isotopic data of U-Pb-Hf in zircon and Sm-Nd (T DM ) in whole-rock, previously unpublished in the literature.
The Chaval Granite is an atypical geological unit in the Northwest Ceará Domain, the northwestern edge of the Borborema Province, where it appears as an isolated body amidst the gneissic and supracrustal terrains of the Granja Complex and the Martinópole Group, respectively.
The petrographic characteristics of plutonic nature and the deformational fabric imposed by the tectonics of the Santa Rosa Transcurrent Shear Zone are unique in the granitoids within this crustal domain and coincide with the data from Gorayeb & Lima (2014). On the other hand, there are similar and chrono-correlated granites in Ceará Central Domain, such as the granitoids of the Santa Quiteria Magmatic Arc.
The Chaval Granite has a predominantly monzogranitic and granodiorite composition, with tonalitic and syenitic variations. However, despite its great extension, it is formed by very similar rocks, containing relatively homogeneous mineralogical associations (Mc, Pl, Qtz, and Bt). Structural, textural and microstructural aspects vary greatly throughout the body, defining a domain with preserved magmatic features to the northwestern portion of the body and other characterized by the presence of mylonitic features that are progressively more developed toward the eastern edge of the body, related to the edification of Santa Rosa Transcurrent Shear Zone.
The petrographic analysis, field data, petrography and literature suggest that the geological evolution of the Chaval Granite involved the accommodation of granite magma in orthogneisses of the Paleoproterozoic (Granja Complex) at middle crustal levels. This is suggested by the absence of thermal metamorphism, xenoliths, and chilled margins at the edges of the pluton, implying a low-temperature gradient between the magma and the country-rocks, as well as the ductile shear deformation conditions that affected the east flank of the body.
The evolution of Chaval Granite involved two main events. The first one comprises an important phase of the pluton emplacement involving magmatic differentiation that led to the formation of the main rocks of the body (porphyritic monzogranites and granodiorites) in an important magmatic crystallization phase that generated the microcline megacrystals. In another phase, it involved the accumulation of microcline megacrystals (cumulatic syenites), the formation of microdiorites by magma mixing, and late-stage aplites, leuco-alkaligranites, and pegmatites representing more advanced phases. The initial phase is represented by the crystallization of plagioclase, biotite, and zircon, and then by alkali-feldspar (microcline megacrysts) under low nucleation and high growth rate  conditions, under low subcooling from the magma with significant hydration of the system (Paterson et al. 2005, Vernon 2008). This process was marked by successive stages of feldspar growth, as evidenced by the concentric zoning of the phenocrysts, which together with biotite represent an important phase of crystallization of the Chaval Granite, highlighted by the porphyritic texture with microcline megacrysts that continued with the oligoclase growth along with the microcline and, subsequently, the crystallization of quartz. Megacrystals accumulation and magmatic layering flow structures are related to the process of magmatic differentiation and magma convection. Under these conditions, the phenocrysts tended to fluctuate in the residual magma in the magmatic chamber. A remarkable characteristic of Chaval Granite is the presence of K-feldspar megacrystals, whose maximum dimensions reach 12 cm. The features indicate that these are crystals of magmatic origin, such as their euhedral forms, presence of simple twinning (Carlsbad), oscillatory normal zoning, plagioclase and biotite inclusions that delineate internal mineral growth zones and mixing of megacrysts into microdiorites enclaves.
Accumulations of K-feldspar megacrystals are frequent and prominent in the western pluton domain (region of Bom Princípio-PI), with much greater modal proportions (80 to 90%) in the coarse granitic matrix (residual magma). Normally, cumulates crystals are aligned denoting magmatic layering, with indicative of magma flows. Paterson et al. (2005) report a similar case in the Tuolumne Batholith of Sierra Nevada (California) where during K-feldspar growth, local mechanical instabilities in the magma were common and resulted in the physical accumulation of megacrysts in schlieren tubes, channels, irregular clusters, dike-like, and small diapirs. All of these features are identical to those reported in Chaval Granite.
In the later stages of tectonic evolution, after emplacement, an important deformational phase related to the SRTSZ formation, affecting all the east flank of the Chaval Granite and the ortogneisses country rocks. The rich and didactic collection of tectonic structures present in the eastern half of the pluton records the implantation of this shear zone with dextral kinematics, similar to those of the northern Borborema Province featuring a late Neoproterozoic transcurrent tectonic system (Arthaud & Torquato 1989), generated different mylonitic rocks (protomylonites, mylonites and ultramylonites).
The shearing process is related to the final stages of a continental collision formed in the final increments of the deformation    of an oblique collisional system that built the Northwest Ceará Shear Belt, leading to lateral extrusion of crustal masses in ductile flux at the end of the Brasiliano Orogeny in the northwest of the Borborema Province (Abreu et al. 1989, Arthaud & Torquato 1989, Ganade de Araujo et al. 2013. During deformation, the primary mineral phases were transformed or re-equilibrated to the new P-T parameters, which in the general context indicate that there is a gradation of dynamic metamorphism, increasing from west to east, since non-metamorphosed and undeformed granitic rocks (location Bom Princípio), followed by low-grade areas (paragenesis Qtz-Sc-Ep-Chl) and finally, at the eastern end, with stabilization of the Kfs-Pl-Bt-Qtz paragenesis that reaches the maximum conditions of dynamic metamorphism in amphibolite facies, as described by Gorayeb & Lima (2014).
The varied types of mylonitic rocks formed and the structural/microstructural features identified are classic and similar to those described by Sibson (1977), White et al. (1980), Lister & Snoke (1984, Trouw (1998), andTrouw et al. (2010). Based on the proposed classification of mylonites by Trouw et al. (2010) we can fit into the type of mid-grade mylonite.
The geochemical data reveal a systematic compositional variation, defining trends related to magmatic differentiation, with varying granodiorites, monzogranites, and tonalites, and of I-type and peraluminous to metaluminous character, compatible with the calcium-alkaline series. All these characteristics and the data in the discriminant diagrams of the tectonic environment reveal that the Chaval Granite is compatible with a normal type magmatic arc environment.
The geochronological studies in the literature pointed ages U-Pb on monazite crystals of 591 ± 10 Ma (Fetter 1999); and Pb evaporation in zircon 630 ± 19 Ma (Lima 1997) and 633 ± 3 Ma (Nogueira et al. 2013). The geochronological results of the U-Pb zircon systematic (U-Pb/LA-ICP-MS) indicate a crystallization age of 633 Ma for the Chaval Granite. This value is much more representative than other existing data in the literature and coincides with the preliminary dates obtained by Pb evaporation, indicating that the Chaval Granite emplacement occurred at the end of the Neoproterozoic, during the Cryogenic-Ediacaran period. Similar ages, between 624 and 666 Ma, have been determined in granitoids that integrate the Tamboril-Santa Quiteria Complex (Santa Quitéria Magmatic Arc) in the north region of the Borborema Province (Cavalcante et al. 2003, Fetter et al. 2003, Ganade de Araujo et al. 2013 (Fig. 24). Correlating with the evolutionary framework of Ganade de Araujo et al. (2013) the Chaval Granite fits into the tectonic context of syn-tardi collisional granite.
The 633 Ma Chaval Granite show Hf crustal model ages of 2.65 to 2.13 Ga. This indicates that the Chaval Granite incorporated Neoarchean and Paleoproterozoic crustal components during their genesis. The ε Hf (t) values ranging from -9.6 to -18.1 suggest a long crustal residence time. These strongly negative values of ε Hf (t) highlight the character of rocks associated with the partial melting of Neoarchean to Paleoproterozoic continental crust.
Whole-rock ID-Tims Sm-Nd isotopic study, shows significantly smaller data, though similar, to Lu-Hf data, T  model ages of 2.04, 1.72 and 1.27 Ga, with negative ε Nd (t) values (-2.64 to -9.13), indicating contributions from paleoproterozoic and mesoproterozoic sources, with a considerable time of crustal residence that implies a more advanced (or mature) nature.
These ages are recognized in the literature as related to a succession of emplacement pulses that make up the Santa Quitéria Magmatic Arc (SQMA). The fact that Chaval Granite can be correlated to SQMA, indicates that its most distal portion is over 100 km NW from this arc. In the region, only granitoids related to the Tamboril-Santa Quitéria Complex have similar values, ranging from 637 to 624 Ma and 638 Ma for porphyritic monzogranites of the Santa Quitéria unit.