Journal of the Geological Survey of Brazil

The Juruena Terrain (Rondônia-Juruena Province) in the southeastern Amazonas State shows a NW- SE dextral shear zones system denominated Roosevelt-Guariba Transpressive Belt (RGTB). The RGTB was generated in response to intracontinental crustal reworking, juxtaposing Paleoproterozoic Juruena granitic-gneiss and chronocorrelated supracrustal associations. This granitic-gneiss basement shows high-K calc-alkaline (Teodósia Suite) to transitional I- to A-type (Igarapé das Lontras Suite) signatures, produced in a continental magmatic arc setting around 1760-1740 Ma (zircon, titanite; U-Pb SHRIMP, LA-ICP-MS). New geochronological data about of the deformation and metamorphic rocks in the RGTB were obtained from migmatite paragneisses, amphibolites, S-type leucogranite (Quatro Cachoeiras Complex and Itamaraty Suite; zircon U-Pb SHRIMP) and protomylonites and mylonites (Igarapé das Lontras and Teodosia protholiths; amphibole-muscovite-sericite Ar-Ar step heating). The results suggest that Southeastern Amazonas (northern Juruena Terrain) was metamorphised/deformed during 1530-1460 Ma under temperatures of 900 oC (zircon) to 580oC (hornblende) and 420oC (muscovite). The geochronological data show that the granite-gneiss basement (continental magmatic arc) and supracrustal rocks (foreland basin) were reworked by a regional event with age interval of 1530 Ma (high grade and anatexis) to 1460 Ma (medium grade). Finally, the Juruena Terrain is affected by a younger low-T event (1300 Ma, muscovite Ar-Ar step heating) with wide NE-trending structures (e.g. Buiuçu Shear Zone). This 1.3 Ga event suggests a continental reactivation caused by the pericratonic deformation related to Candeias/Sunsás Orogeny during the Columbia Supercontinent break-up, before of the Rodinia Supercontinent assembly. In summary, the Juruena Terrain in the southeast Amazonas shows a complex metamorphic and structural intracontinental evolution, involving polycyclic events since late Orosirian to Ectasian in a convergent tectonic setting. Therefore, the Juruena Terrain shows similar accretionary histories with others orogens and has apparent long-lived connections with Laurentia (Yavapai Province) and Baltica (Transscandinavian Igneous Belt), forming the core of the Columbia Supercontinent.

In the same region, Calymmian intrusions of subalkaline A-type and rapakivi granites (Serra da Providência Suite; 1.54-1.51 Ga) are associated with quartz monzonites and gabbronorites, including coeval (sub)volcanic rocks of the Serra do Gavião Group (Oliveira and Lira, 2017;Oliveira, 2016; Figure 2). Still in Mesoproterozoic times (Ectasian) there is evidence of reworking of the Rondônia-Juruena Province by thermotectonic event related to the Rondonian-San Inácio/Cachoeirinha Orogeny (1.50-1.30 Ga). This collisional event at 1.37-1.35 Ga (Teixeira et al., 1989;Bettencourt et al., 1999;Santos et al., 2003;Scandolara et al., 2011) shows also felsic intrusions, in this case related to the orogenic collapse and extensional phase (Alto Candeias, 1.34 Ga; São Lourenço-Caripunas, 1.31 Ga). In the southeast Amazonas State this collisional event was not recognized until now and the tectonothermal effects are not so well understood. However, structural geophysical analysis and multiscale study has suggested a crustal evolution model based on Paleoproterozoic accretion and intracontinental Mesoproterozoic tectonothermal events affecting the Juruena Terrain in this region (Oliveira and Almeida, 2021).  ; B) simplified geotectonic map of the Juruena Terrain according to Scandolara et al. (2016).
The study area in the southeast Amazonas State ( Figure  2) encompasses the northern part of the Juruena Terrain (Scandolara et al., 1999), mainly in the Aripuanã, Roosevelt and Guariba River basins. In this paper we present new U-Pb SHRIMP geochronological data (zircon and titanite) of calc-alkaline basement (Teodósia Suite, Juruena Complex), supracrustal rocks (Quatro Cachoeiras Complex), twomica granite (Itamarati Suite), and new Ar-Ar step heating ages (muscovite and hornblende) of granites and sheared subvolcanic rocks (Colíder Group, Teodósia Suite and Igarapé das Lontras Suite). The aim is to show how Mesoproterozoic events affected the Paleoproterozoic basement of this region, seeking to shed light on the discussion about the magmatic events and the tectonothermal effects in the Rondônia-Juruena Province. With this, the article intends to contribute also to the discussions about the configurations of supercontinent assemblies/break-ups in the southern region of the Amazon Craton and the involvement of the Juruena Terrain in the Columbia Supercontinet formation. In the Supercontinent cycle, separeted blocks of continental crust can collide and merge, forming new and larger continents, triggering the tectonic framework of several orogenic belts, such Roosevelt-Guariba Transpressive Belt in the Juruena Terrain.
The understanding of the crustal growth/reworking may also help to us to better define the crust architecture using isotopic mapping, constraining the distribution of mineral deposits. For example, in general sense, BIF-hosted Fe deposits are spatially related to juvenile or reworked crustal domains and orogenic Au deposits are associated with juvenile crustal domains. In the specific case of the Juruena Terrain, the crust architecture is important to understand the chemical fertility and main structural footprints of the Au-(Cu) magmatic-hydrothermal deposits.  Reis et al., 2006;Oliveira et al., 2014;Almeida et al., 2016;Meloni et al. 2021). Conventions: ATB -Alto Tapajós Basin; SD -Sucunduri Dome; MS -Machadinho Synclinal; JS -Jatuarana Synclinal; Au -gold occurrence.
Two main models have been proposed for the geodynamic evolution of the Juruena Terrain: i) accretionary evolution based on continental (e.g. Scandolara et al., 2016; or island (Assis et al., 2017) magmatic arc systems; or ii) extensional within-plate or continental rifting settings (e.g. Neder et al., 2002;Barros et al., 2009;Rizzotto et al., 2019a,b). Alternative evolutionary models propose the alternation between compressive and extensional tectonic phases, responsible for crustal thickening and crustal thinning, respectively (Trevisan et al., 2021 and references therein). Trevisan et al. (2021) identified three main magmatic events related to the crustal thickening and crustal thinning tectonic regimes in the Juruena Terrain, in response to flat and slab-rollback subduction, respectively. These magmatic events were defined by Alves et al. (2020)  In most evolutionary models, the geology and macrostructures of southeastern Amazonas are considered as being extensions of northeastern Rondônia and northern Mato Grosso (e.g. Trevisan et al., 2021 and references therein). However, recent works show that Northern Juruena Terrain (NJT) characteristics are contrasting with those existing in Rondônia and Mato Grosso, pointing to predominance of Sthaterian (volcano)sedimentary sucessions, younger and well-preserved, overlying an Orosirian basement with crust Tapajós-Parima age (Simões et al., 2020). Furthermore, the RGTB in southeastern Amazonas is oblique in relationship to the regional WNW-ESE structures of the Juruena Complex in northern Mato Grosso (Ribeiro and Duarte, 2010). From multiscale regional studies and structural analysis, Oliveira and Almeida (2021) proposes a tectonic compartmentalization for the NJT controlled by the RGTB. The RGTB is a high-T NW-SE-trend shear zone system with 60 km in width, cross-cutting the regional WNW-ESE structures of the Juruena Complex to south. According to this compartmentalization, three petrotectonic associations are individualized: pre-Juruena, Juruena and post-Juruena ( Figure 2).
The Juruena Association is subdivided in two domains, the first (Supracrustal Domain) is located to the east, enclosing calc-alkaline to alkali-calcic volcanic rocks (I-type Colíder Group and A-type Pedro Sara Formation, 1820-1745 Ma; , Simões et al., 2020 and volcanosedimentary sucessions (Camaiú Formation and Vila do Carmo Group, older than 1740 Ma). The tectonic setting is related to intracontinental rift, similar to the other Sthatherian taphrogenetic systems observed in the Amazon, São Francisco-Congo and North China cratons, attributed to prebreak up conditions of the Columbia Supercontinent (e.g. Reis et al., 2013;Simões et al., 2020). These supracrustal rocks show well-preserved subhorizontal primary structures, with the vertical tectonic exposing locally the basement through hostgraben systems. This basement (pre-Juruena Association) is represented by the metavolcanosedimentary sucession with low metamorphic grade of the Abacaxis Formation (Meloni et al., 2021), intruded by the Arraiá and Chuim granites (Matupi Suites, 1850-1835Meloni et al. 2019).
According to Almeida et al. (2016) and Oliveira and Lira (2019), the second domain (Granite-Gneiss Domain) is formed by a high-temperature mylonitic belt (RGTB) showing igneous A-type to high-K calc-alkaline protholiths (Teodósia and Igarapé das Lontras Suites). Locally are describe paragneisses, amphibolites and migmatites (metavolcanosedimentary sucession of Quatro Cachoeiras Complex) and metavolcanic rocks (deformed rocks of Colíder Group), metamorphosed under high-temperature upper amphibolite facies conditions and moderate pressure (Oliveira, 2016, Lisboa, 2019. The Supracrustal and Granite-Gneiss domains were tectonically juxtaposed as the consequence of the evolution of the RGTB (Oliveira and Almeida, 2021). In southwest contact with the RGTB occurs a bimodal magmatism represented by A2-type subalkaline rocks of the Serra da Providência Suite and Serra do Gavião Group, in association with tholeiitic gabbros and diabases, related to the Post-Juruena Association. This southwest sector is characterized by a wide bimodal intracontinental post-orogenic magmatism (Scandolara et al. 2013) that locally intrudes the Granite-Gneiss and Supracrustal domains of the Juruena Association (e.g. Almeida et al., 2016;Meloni et al., 2021;Oliveira and Lira, 2019).
Lastly this terrain was recover by younger and wide intracratonic sedimentary sequences of the Manicoré, Prainha and Palmeiral formations, showing maximum sedimentation age around 1330-1100 Ma. According to Reis et al. (2013) this period represents the cratonization stage of the Juruena Terrain. These sedimentary sequences are delimited by normal faults produced from later reactivations of the RGTB, generating rollover structures and tilted blocks, as observed for example in the Jatuarana and Machadinho synclines (e.g. Almeida et al., 2016;Oliveira and Lira, 2019).

Juruena Terrain: synthesis of previous geochronology data
The southeastern Amazonas is known for the scarcity of previous geochronological and isotopic data. The available data was mostly obtained during the seventies (Leal et al., 1978) using Rb/Sr and K/Ar methods (isochrone ages). Only recently, some new U-Pb and Sm-Nd data were published (e.g. Almeida et al., 2009;Reis et al., 2013). In contrast, the Rondônia-Juruena Province in the northeast Rondônia and northern Mato Grosso is better documented for geochronological data (e.g. Scandolara, 2006Scandolara, , 2014Scandolara, , 2016Duarte et al., 2012. Abundant U-Pb zircon ages are available for widespread Paleoproterozoic calc-alkaline plutonism (Juruena Accretionary Belt; Scandolara et al., 2016) in northern Mato Grosso (e.g. Pinho et al. 2003, Souza et al., 2005, Silva and Abram, 2008, Ribeiro and Dutra, 2010 and northeastern Rondônia (e.g. Scandolara, 2006;Scandolara et al., 2014, Quadros et al., 2011. The main magmatic associations are represented by Paranaíta, Vitória, Vespor, São Pedro, São Romão suites, and Juruena Complex and orthoderived rocks of the Jamari Complex (Table 1 The same is true for the U-Pb zircon ages of the corresponding volcanic rocks (Colíder Group and Pedro Sara Formation) of this magmatism in the Juruena Accretionary Belt. In northern Mato Grosso and southeastern Amazonas, the ages of the Colíder Group are for example as old as 1800 Ma (e.g. Pinho et al. 2003, Ribeiro and Dutra, 2010, Dutra et al., 2012, Almeida and Oliveira, 2016Meloni et al., 2021), with at least ~60 Ma of duration (1820-1760 Ma; Table 1) and outcropping preferably around the Alto Tapajós Basin (Figure 2). Also in northern Mato Grosso, some metavolcanic rocks (Roosevelt Group; Table 1) generated in an intermountain basin setting (rhyolites interbedded with clastic/chemical sediments) yielded a 1770-1740 interval age (e.g. Ribeiro and Dutra, 2010;Néder et al., 2000;Santos et al., 2000). The Roosevelt Group, correlated with Vila do Carmo Basin located in southeastern Amazonas (Reis et al., 2013)  . The metavolcano-sedimentary rocks (Quatro Cachoeiras Complex; Table 1) in northeastern Rondônia were dated by Payolla et al. (2002Payolla et al. ( , 2003a and Quadros et al. The two older populations are probably related to the Tapajós-Parima crust sources (2040( -1860Santos et al., 2000), while the main population shows strong relationships with source areas of the Juruena Accretionary Belt (1850-1730 Ma; Scandolara et al., 2016). The younger age population coincides with similar source areas of rocks of the Ouro Preto Orogeny (1670-1630 Ma; Santos et al., 2003). According to Payolla et al. (2002) the deposition of the Quatro Cachoeiras Basin had taken place between 1660 Ma and 1590 Ma (Table  1).

Analytical procedures
In situ zircon U-Pb LA-ICP-MS (RB-16A sample, figure  3A; Table 2) analyze was carried out in the Laboratório de Estudos Geocronológicos, Geodinâmicos e Ambientais of the Universidade de Brasília (UnB), Brasília, Brazil, following all procedures described in Bühn et al. (2009). Concentrates of zircon were obtained by crushing the rock and then sieving and panning. Zircon crystals ranging 0.177 mm (80#) to 0.074 mm (200#) were hand-picked under a binocular microscope, mounted in epoxy resin, and polished with diamond paste. The analyses were performed with a Thermo Finnigan Neptune multicollector inductively coupled plasma mass spectrometer with an attached New Wave 213μm Nd-YAG solid state laser, using a standard-sample bracketing technique with four sample analyses between a blank and a GJ-1 zircon standard. The accuracy was controlled using the zircon standard 91500. Ablation time and spot diameters were, respectively, 40 s and 30 mm for the U-Pb analyses. Raw data were reduced using an in-house program and corrections were done for background, instrumental mass-bias drift and common Pb, as described in Bühn et al. (2009). Analyses were preceded by backscattered electron (BSE) imagery also done at UnB using a Scanning Electron Microscope FEI Quanta 450.
Data was reduced using the SQUID© 1.03 software (Ludwig, 2001) and the ages calculated using Isoplot© 3.0 (Ludwig, 2003). One determination on the standard was obtained for each three analyses of unknowns. Each spot size is typically 20-30 mm in diameter. The presented ages are mean average 207Pb/206Pb ages calculated at 2σ level, whereas the individual analyses are quoted at 1σ level.
Four samples (Table 2) of the Juruena Terrain are dated using U-Th-Pb SHRIMP (Sensitive High Resolution Ion MicroProbe): mylonitic biotite granite (GH-03A, figure 3E), migmatitic paragneiss (AA-22B, figure 3G), amphibolite (AA-32, figura 3H) and two-mica granodiorite (GH-12A, figura 3F). Approximately 0.5 kg of each sample was collected and subsequently crushed, milled and sieved. The 60-200 mesh fractions were washed and dried to be processed using heavy liquids (LST-Lithium-Sodium-Tungstate and TBE-Tetra-Bromo-Ethane), which produced two fractions (lighter than 2.95 and heavier than 2.95). The heavy fraction was submitted to hand magnet to remove fraction M1 (essentially magnetite and ilmenite). The fraction without magnetite was processed in a Frantz LB1 Isodynamic magnetic separator in two steps using an inclination of 18o. First, using 0.5 Ampère and 10o of lateral inclination and secondly using 1 ampere and 5 degrees of lateral inclination. This last step results in fractions M3 (where titanite was concentrated) and NM (where zircon was concentrated). Table 2. Simplified description and location of the dated samples, including summary of ages and methods. Abbreviations according Siivola and Schmid (2007).
About 100 crystals of zircon were picked from the least magnetic fraction (NM) and -when present -about 20 crystals of titanite were picked from fraction M3. The selected grains were placed on double-sided tape together with fragments of standards. A cylinder measuring 25mm in its internal diameter was placed on the double-sided tape and a liquid epoxy mixture was poured into it. The resulting epoxy disc was dried and polished using sand paper and diamond paste of 1 micrometer. Each mount was initially carbon-coated to obtain backscattered electrons (BSE) images using a TESCAN-VEGA3 scanning electron microscope (SEM) at the Centre for Microscopy, Characterization, and Analysis, in the University of Western Australia. Images (BSE) were acquired under accelerating voltage of 20 kV, current of 10 nA, and a working distance of 15 mm. For the SHRIMP analyses the mounts were lightly repolished and gold-coated. The isotopic U-Pb analyses were obtained at the SHRIMP II facilities of the Curtin University of Technology in Perth, Western Australia, following the procedures described by Compston et al. (1984Compston et al. ( , 1992 and the operational routine described by Smith et al. (1998)

High-K calc-alkaline (I type to transitional I/A--type) deformed granitoids (Igarapé das Lontras and Teodósia Suites)
The isotopic dataset of the the Almeida et al. (2009) was revised, considering the hornblende-biotite augen gneiss (RB-16A sample) located in the Roosevelt River (Table 2; Figures 2 and 3A). These authors obtained previously a crystallization age of 1758.2 ± 4.7 Ma, interpreted as that of the protholith of the São Romão Suite (I-type Andean-type magmatism). However, Almeida et al. (2016) point to an A-type chemical signature for this sample, contrasting with a calc-alkaline trend.
A more detailed review of this isotopic data shows at least four age populations with low Th/U ratios (0.4-0.2, locally 0.7-0.6), despite some age overlaps occurring within analytical error (Table 3; Figure 4A): i) 1877 ± 44 Ma; ii) 1807 ± 47 Ma; iii) 1764 ± 13 Ma; and iv) 1736 ± 29 Ma. The older age (1877 Ma) was obtained from two inherited crystals (upper intercept), attributed to rocks with Silicic Large Igneous Province (SLIP) Uatumã age (Tapajós-Parima crust; see Klein et al., 2012). Two other crystals yielded an age of 1807 ± 47 Ma (upper intercept), probably related to the early stages of the Accretionary Juruena Belt. However, within error margin, these apparent two populations may be only one, recording, togheter, the origin of the Accretionary Juruena Belt.
The main population (15 crystals) yielded an age of 1764 ± 13 Ma (antecrystals in the sense of Miller et al., 2007), corresponding to grains generated within the earlier magmatic pulses, which the zircon crystals are normally greater (100-370 μm) and brighter in BSE images, showing also welldefined magmatic zoning ( Figure 5A, e.g. Z9, Z13, Z17, Z19 and Z22 crystals). In turn, these antecrysts are incorporated by later pulses, represented by the younger population of 1736 ± 29 Ma (concordia age), interpreted as crystallization age of the protholith. Thus, both zircon populations were generated in the same magmatic event and the protholith is a granitoid rock of the Igarapé das Lontras Suite, correlated in age to the Jamari Complex (1.76-1.73 Ga; Table 1, Figure 1).
Other two other samples belonging to the Juruena Accretionary Belt were also analysed. The LB-31A sample ( Table 2; Figures 2 and 3B) comes from the type-area of the Teodósia Suite, Aripuanã River, representing a rare undeformed granitic rock. Ten zircon crystals yielded a Concordia age of 1754 ± 8 Ma (Table 3; Figure 4B), in accordance with Almeida et al. (2009) original results (Table 2), showing high Th/U ratios (1.1-0.6). The zircon crystal are fractured, showing corroded edges, apatite inclusions and slight magmatic zoning ( Figure  5B,C). In the Guariba River (Figure 1), a well-foliated (NWtrending) mylonitic biotite granite (GH-03A;  Figure 4C) from seven zircons and three titanites, interpreted as the crystallization age of the protolith. The colorless to pale yellow zircon crystals are euhedral, bypiramidal and show magmatic zoning and high Th/U ratios (1.6-1.0), with no inherited cores and inclusions. Titanites are also typically igneous ( Figure 5D) showing 0.9-0.8 Th/U ratios.    Figure 4D). These rocks were correlated to the Quatro Cachoeiras Complex, described in the northeastern of Rondônia (Quadros et al., 2011), located about 100 km to the west of studied area.

Analytical procedures
The four selected samples (RB-16A, UP-25C, UP-27A and FS-66; Table 1) were first examined under a petrological microscope to assess the level of alteration of the phase to be analyzed (0.5 to 1.0 mm diameter amphibole and muscovite). These single amphibole and muscovite grains were 40Ar/39Ar step-heated with a Synrad® CO2 continuous laser and isotopic analyses of the five evolved argon isotopes were performed on a MAP215® noble gas mass spectrometer at Geosciences Rennes. All isotopic measurements are corrected for mass discrimination and atmospheric argon contamination. following Lee et al. (2006) and Mark et al. (2011), as well as K, Ca and Cl isotopic interferences. Decay constants used are from Renne et al. (2011). Samples and standards (Amphibole Hb3gr; age: 1081.0 ± 0.11% Ma; Renne et al., 2011) were co-irradiated with Cd-shielding for 298 hours at the McMaster reactor (Hamilton. Canada. location 8E) with a J/h of 5.86 x 10-6 h-1. Further analytical details are outlined by Ruffet et al. (1991Ruffet et al. ( , 1995. Apparent age errors are plotted at the 1σ level and do not include the errors on the 40Ar*/39ArK ratio and age of the monitor and decay constant. Plateau ages were calculated if 70% or more of the 39ArK was released in at least three or more contiguous steps. the apparent ages of which agreeing to within 1σ of the integrated age of the plateau segment. The errors on the 40Ar*/39ArK ratio and age of the monitor and decay constant are included in the final calculation of the error margins on the pseudo-plateau age or on apparent ages individually cited. The 40Ar/39Ar age spectra are shown in Figure 6.
Muscovite and sericite from two phyllonites of the Roosevelt River (Figure 2) were also analyzed. These rocks are represented by muscovite-quartz-biotite-schist and sericitequartz schist, which protoliths corresponds to fine do mediumgrained sheared granites (Igarapé das Lontras Suite). Both phyllonites are also associated to regional NW-trending shear zones of the Roosevelt-Guariba Deformation Belt (RGDB). The UP-25C (muscovite) and UP-27A (sericite) samples yielded plateau ages respectively of 1466.5 ± 1.4 Ma (1s) and 1467.6 ± 0.8 Ma (1s) (Figures 3C,D and 6B,C), corresponding to a maximum cooling age for the tectonothermal event of 420o-510oC, according to the estimate blocking temperature for the white micas in the Ar-Ar isotopic system (Kirschner et al., 1996a.b).
In the Juruena Terrain the intensity of regional EW deformation (D1 event) decreases from southwest to northeast (Oliveira and Almeida, 2021)   The 1480-1460 Ma Ar-Ar ages are related to the NWtrending shear zones generation, responsible for the installation of the Roosevelt-Guariba Deformational Belt (RGDB) according to Oliveira (2016) and Oliveira and Almeida (2021). For other hand, the 1300 Ma Ar-Ar age, related to the NE-trending shear zones (Buiuçu Fault), may be interpreted as hinterland reflex of the Sunsás Orogeny  or Rondonian-San Inácio Orogeny (Bettencourt et al., 2010), at the northeasternmost point of Rondônia-Juruena Province. Only in the westernmost area (Jamari Domain; Scandolara, 2006) are observed magmatic rocks with 1315-1310 Ma (São Lourenço-Caripunas Suite), generated in the late stages of this orogeny .   Table 3). The closure temperatures (minerals/methods) are in agreement with Grove andHarrison (1996), Kamber et al. (1995) and Purdy and Jäger (1976).
Finally, the Beneficent and Palmeiral Basins (Figures  7 and 8) played important play role in the cratonization of the Juruena Terrain, developed between 1.40 Ga and 1.00 Ga (Oliveira and Almeida, 2021;Reis et al., 2013). Younger structures are related to the crustal reactivations (Oliveira and Almeida, 2021), controlling the gold mineralizations in the region (D3) or as NW-SE late normal faults (D4) associated mainly to the Paleozoic basins (Toczeck et al., 2019).
According to Oliveira (2016) and Oliveira and Almeida (2021) the geotectonic framework of Juruena Terrain in the southeastern Amazonas is compatible with an evolution based on foreland basin, developed over the Tapajós-Parima basement during the Juruena Orogen (1.82-1.74 Ga). Thick/ wide supracrustal sucessions and older weakness zones are also associated with development of this foreland basin, which in turn is preserved of from late Statherian (1.67-1.63 Ga) regional metamorphism and deformation (D1, E-W structures).

The Juruena Terrain and the evolution of the Columbia Supercontinent
Considering the Supercontinent cycles and available paleomagnetic data, the Juruena Accretionary Belt (1.85-1.73 Ga) probably was involved in the final amalgamation stages of the Paleoproterozoic Columbia supercontinent (e.g. Bispo- Santos et al., 2008), showing apparent long-lived connections with Laurentia (Yavapai Province) and Baltica (Transscandinavian Belt). Some paleomagnetic data (e.g. Bispo- Santos et al. 2008Santos et al. , 2014D´Agrella-Filho et al. 2016) favors the idea that the Amazon Craton joined the Columbia supercontinent at ~1790 Ma ago, in a similar scenario of the South America and Baltica configuration (SAMBA), acordding Johansson (2009) and Bispo- Santos et al. (2008Santos et al. ( , 2014. Based on these paleomagnetic data, Baltica, Laurentia and Amazonia remained quasi-stationary for a long time (from 1780 Ma to 1540 Ma), generating a large continental mass (core of Columbia) in Paleo-Mesoproterozoic times ( Figure 10). Belt in this sense shows also the same westward younging growth, similarly the NW Amazon Craton (e.g. Almeida et al., 2022) and the Transscandinavian Igneous Belt (e.g. Högdahl et al., 2004).
Younger magmatic events with Calymmian age are present in the Juruena Acrettionary Belt, represented by two main types: a) abundant bimodal association with A-type rapakivi granite dominat (Serra da Providência Suite, 1.57-1.50 ga) and b) local S-type granites (Itamaraty Suite, 1.55-1.52 Ga) in association with high-grade paragneisses (Quatro Cachoeira Complex), suggesting minor crustal reworking and anatexis. This 1.55-1.52 Ga high-grade event is probably related to the early stages of the Rondonian-San Inácio/ Cachoeirinha Orogeny (1.54-1.46 Ga), most commom in the western margin of the SW Amazon Craton, producing distal orogenic processes responsible for the broad Calymmian granitic magmatism observed in the Juruena Terrain (Oliveira and Almeida, 2021). In the Grenville Province, the Pinwarian Orogeny is also characterized by abundant Calymmian granitoids (1526( -1466igneous zircon, Tucker andGower 1994, Heaman et al. 2004) and locally migmatized paragneiss (1640 ± 7 Ma, detrital zircon, Tucker and Gower 1994). The K-granites and AMCG associations (inboard magmatic arc) are dominant, but no crustal-derived granites are described (i.e. S-type granites).

Conclusions
The proposed model for the Juruena Terrain in the southeastern of Amazonas (Oliveira and Almeida, 2021) is reinforced by the new and previous geochronological data. The Sthaterian arc-related rocks (ortho and paraderived) are deformed by several events under different temperatures during Calymmian and Ectasian times, which shaped the architecture of the Roosevelt-Guariba Transpressive Belt (NW-trending): 1. Quatro Cachoeiras Complex is interpreted as an arcrelated basin (foreland) developed in the extensional setting in the final stages of the Juruena Acrettionary Belt evolution, showing only one 1.75 Ga detritic zircon population (arc basement provenance). In the type-area (northeast Rondônia) these migmatitic paragneisses show variable provenances, suggesting basement rock contributions from the Tapajós-Parima Province (1.92 Ga and 1.87-1.84 Ga) and Ouro Preto Orogeny rocks (1.67-1.63 Ma; Santos et al., 2003).
4. Based on Ar-Ar (amphibole, muscovite, sericite) and U-Pb (zircon, titanite) geochronological data, the estimated cooling rates range from 8.0oC/m.y. to 6.5oC/m.y. (1520-1470 Ma), suggesting high to moderate exhumation rates (4-5 km) and fast uplift of Juruena Terrain in Sthaterian-Calymmian times during Roosevelt-Guariba Transpressive Belt intracratonic evolution (Figure 9). This high cooling rates, and probably sharp exhumation, allowed intense denudation of the deepest crust formed by orthogneisses and metagranitoids, with only a restricted nucleus of paraderived migmatites and rare metavolcanic rocks were preserved. Thus, the 1.48-1.47 Ga interval age is probably representative of the NW-trending of the RGTB in the Northern Juruena Terrain; 5. The later tectonothermal event (1300 Ma), recorded in the Buiuçu Shear Zone (NE-trending). shows temperatures of 510o-420oC (Ar-Ar, muscovite). This event is interpreted as reactivation of older fault zones (infracrustal older basement according to Oliveira, 2016), probably related to final stages of the Candeias/Sunsás Orogeny (1.37-1.32 Ga).

Table1 (Continuation)
A c c e p t e d m a n u s c r i p t -U n c o r r e c t e d p r e -p r o o f

Table1 (Continuation)
A c c e p t e d m a n u s c r i p t -U n c o r r e c t e d p r e -p r o o f

Table1 (Continuation)
A c c e p t e d m a n u s c r i p t -U n c o r r e c t e d p r e -p r o o f  Miller et al. (2007): 1. Antecrysts: zircon grains that crystallized from earlier pulses (a crystal from an earlier pulse of magma which is incorporated by later pulses); 2. Autocrysts: grains generated within the youngest intrusive pulse (spatially and temporally associated with a distinct pulse or increment of magma); 3. Xenocrysts: grains assimilated from host rocks sufficiently older (at least several million years), being considered unrelated to the magma system; 4. Inherited: grain that comes from the melt source.

Table1 (Continuation)
A c c e p t e d m a n u s c r i p t -U n c o r r e c t e d p r e -p r o o f