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Aspectos lito-estruturais e evolução crustal da região centro-oeste de Goiás
(Universidade Federal do Pará, 1985-11-13) COSTA, João Batista Sena; VILLAS, Raimundo Netuno Nobre; http://lattes.cnpq.br/1406458719432983; HASUI, Yociteru; http://lattes.cnpq.br/3392176511494801
The study area is bounded by the cities Paraíso do Norte, Gurupi, and Dianópolis in north-central Goiás State. The area contains diverse lithostratigraphic units and various generations of structures related to distinct thermo-tectonic events. Based on the distribution and the petrographic and structural characteristics of the ancient rock assemblage, four litho-structural domains were defined and attributed to the Archean. Domain "1" includes the region of Almas-Dianópolis and is interpreted as part of granite-greenstone terrane. It includes a group of tonalitic gneisses with associated supracrustal rocks (Goiano Complex), a sequence of metavolcanic rocks and metasediments (Riachão do Ouro Group), and various tonalite bodies (Serra do Boqueirão Suite) intruded into the earlier units. The evolution of the domain includes three principal deformational events: a) Formation of the amphibolites and/or biotite gneisses and granitoids characterized by sub-vertical banding oriented N10ºE and accompanied by mineralogical changes under conditions of amphibolite facies; b) deposition of the Riachão do Ouro Group, followed by isoclinal folding oriented N10°E and consequent transformation to greenschist facies. The emplacement of the tonalitic diapirs of the Serra do Boqueirão Suite is related to this event; c) a foliation gently inclined to the SE resulting from a simple low-angle ductile-brittle shearing process which affected the west part of this domain, transforming the rocks of the Goiano Complex into mylonitic gneisses under amphibolite facies conditions. Domain 2 includes the counties of Porto Nacional, Brejinho de Nazaré, and Natividade in the east-central part of the area. It is characterized by granulitic gneisses (Porto Nacional Complex), by tonalitic gneisses with associated supracrustal rocks (Manoel Alves Complex), including metasediments and metavolcanics (Morro do Aquiles Formation), and by pegmatitic granites such as the Xobó Suite. The different lithologic units take the form of lenses or sub-horizontal concordant to sub-concordant bodies with strike N30°E. They show structural features produced by a low-angle ductile-brittle shearing process under amphibolite facies conditions. Superposed on the low-angle features are various zones of high-angle directional shear having different intensities of deformation, but all in greenschist facies conditions. Domain 3 is within the NW part of Paraiso do Norte county and is interpreted as a granite-greenstone terrane similar to that of Domain 1. This Domain includes the Colméia Complex, the Rio do Coco Group, and the alkaline gneisses of Monte Santo. Two principal deformational phases are responsible for the structures in this domain: a) folding (S) of the gneissic granitoids of the Colméia Complex into recumbent folds oriented E-W. The axial plane schistosity (S1) formed in medium to amphibolite facies conditions; b) deposition of the Rio do Coco Group, discordant with the Colméia Complex, followed by sub-vertical folding oriented E-W. The second generation of folds in the Colméia Complex is related to this deformational event. Domain 4, in the west-central part of the area, includes parts of Paraíso do Norte, Fatima, Gurupi, and Porto Nacional counties. This domain is composed of the Rio dos Mangues Complex, the Matança and Serrote Suites, and the alcaline gneisses of the Serra da Estrela, distributed in sub-concordant sheets oriented N30°E. Similarly to that observed in Domain 2, these rock assemblages show structural features related to low-and high-angle shearing events. The transition between Domains 1 and 2 and between Domains 3 and 4 is gradational, such that two ancient blocks of crust are defined (Domains 1+2 and 3+4] separated by a belt of granulitic rocks (Porto Nacional Complex). The zone of juxtaposition corresponda to a belt of low-angle ductile shearing developed by the overthrusting of the Brazilian block, on the east, onto the Araguacema block to the west. Similar geologic conditions have been well characterized in South Africa, in western Greenland, and in NW Scotland and are beginning to be described in various regions in Brazil, constituting a new way to understand the relations between Archean terranes. Granite bodies of the Lajeado Suite at the end of the Lower Proterozoic and ultrabasic bodies in the first half of the Middle Proterozoic were injected into this crustal segment stabilized at the end of the Archean. During this epoch the Transbrazilian Lineament became defined as a brittle shear zone. Basins were developed in the second half of the Middle Proterozoic, with deposition of the Baixo Araguaia Supergroup and the Natividade Group. These two are separated today by a block limited by the cities of Paraíso do Norte, Gurupi, and Porto Nacional. The Transbrazilian Lineament was reactivated in this period.At the end of the Middle Proterozoic an E-W regional compression produced the Araguaia and Uruaçu fold belts. The evolution of the Araguaia fold belt involved four stages of structural deformation. In the first stage, N-S recumbent folds were formed having axial plane schistosity (S1) developed in intermediate amphibolite facies to intermediate greenschist facies conditions. The intermediary stages involved folding and refolding of the S1. The last stage is related to the formation of domai structures resulting from the intrusion of the granite bodies of the Santa Luzia Suite. As a result of this evolution, the Araguaia belt has an importent asymmetry characterized by intensification of deformation and mineralogical transformations from west to east. The Uruaçu fold belt is In general characterized by folds with variably-oriented axial planes and mineralogical changes tipical of greenschist facies. In the studied region, regular variations In deformational intensity and metamorphic degree were not found. The immature sediments of the Monte do Carmo Formation are the products of the last lithogenetic processes of the Middle Proterozoic in the area. During the evolution of the Araguaia and Uruaçu fold belts, the north part of the Goiano massif had a limited participation in such a way that it functioned as a rigid block with respect to the folding on either side. The final products related to the polycyclic evolution of this crustal segment during the Priecambrian are represented by directional fault systems oriented principally N40º -60ºE and N40º -50º W. The NE system of faults reflects a reactivation of the Transbrazilian Lineament in the Upper Proterozoic. Thick sedimentary sequences were deposited in the Phanerozoic and new movements on the Transbrazilian Lineament caused the development of important block faulting which is reflected in part by the present-day geomorphology of the area.
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Estratigrafia e evolução estrutural do segmento setentrional da faixa de desdobramentos Paraguai - Araguaia
(Universidade Federal do Pará, 1979-06-13) ABREU, Francisco de Assis Matos de; HASUI, Yociteru; http://lattes.cnpq.br/3392176511494801
The northern part of the Paraguai-Araguaia orogenic belt comprises a significant portion of the South American Platform. Here, the Brazilian geotectonic cycle (550-900 m.y), produced a mountain chain through a complex sequence of sedimentary metamorphic, magmatic, and structural events along the eastern margin of the Amazon craton. The lithologic sequence is designated stratigraphically as the Baixo Araguaia Supergroup which comprises the Estrondo Group and the overlying Tocantins Group. The basal formation in the Estrondo Group is the Morro do Campo Formation which consists of quartzites and subordinate schists and gneisses. The Xambioá overlies the Morro do Campo and includes several kinds of schists. The Tocantins Group is formed by Couto Magalhães Formation, represented by phyllites and intercalated quartzites and the overlying Pequizeiro Formation consiwts of pelitic sediments and Mg-rich igneous derivatives. The Estrondo and the Tocantins groups are intruded by ultramafic, mafic, and granitic rocks that are associated with late and post-tectonic igneous events. The Rio das Barreiras Formation, a sedimentary sequence represented by a polymictic conglomerate with carbonate matrix and sandy and silty interlayers, unconformably overlies the Pequizeiro Formation and may represent erosional remnants of a final phase of the Brazilian cycle. Primary lithologic structures in Baixo Araguaia Su pergroup are preserved as relict compositional stratification, inclined, parallel, and graded bedding in metasediments, and flow structures in the igneous rocks. Superposed penetrative planar and linear deformation structures are present in several generations. The regional N-S striking schistosity is of axial-plane type and is related to the intrafolial folds, with an easterly dip getting vergence to Amazon craton. The regional dip is 309 and decreases to abaut 159 adjacent to the Amazon craton. Gneissic banding parallels schistosity of overlying schists in the larger folds and they share a common mineral lineation. Polyphase deformation is recorded by a fold sequence which varies in scale from 1 cm to 30 km and is related to the differents structural levels within the crust. The lower structural level includes: a) similar-type intrafolial isoclinal folds which are contemporaneous with regional metamorphism; b) similar tight folds which involve the s.chistosity and transposed bedding; c) shear folds of crenulation developed near to the top of the level in the more plastic horizons. The intermediate level comprises; d) isolated regional flexures near the localities of Colméia, Xambioà-, Lontra, Muricizal; e) two generations of open and cross folds associated with the Iriri-Martírios lineament zone. N-S and NW-SE fracture and fault systems cut ali stratigraphi.c units of the Baixo Araguaia Supergroup. The faults consist of: 1) NW treding transcurrent fault with strike iengths of severa]. Kilometers; 2) thrust faults with N-S- strike such as those near Andorinhas and Muricizal mountains; 3) N-S striking normal faults developed at the edge of the Parnaíba basin and elsewhere. The mapped facies sequence ranges from incipient greenschist facies in the west to amphibolite facies in the east implying an Bastward increase in metamorphic grade. Sericite to garnet isograds are discernibles. Three magmatic events are distinguished. They comprises: a) pre-tectonic basic and ultrabasic plutonic-volcanic magmatism; b) late-tectonic granitic intrusion; c) post- tectonic unfoliated granitic intrusions. Eleven K-Ar mica dates from gneisses and schists of the orogenic belt yield values in the range of 516 ± 10 m.y to 358 ± 19 m.y. (Brazilian Cycle). Five Rb/Sr determinations from the gneissic core of the Colméia fold gives values around 2,000 m.y (Amazonic cycle). The geologic evolution of the northern Paraguai-Araguaia orogenic belt consists of three sequential stages: I) deposition of psammitic and pelitic sediments comprising the Estrondo and lower Tocantins Groups. Basic and ultrabasic igneous activity in late Tocantins time result in the deposition of mixture of pelitic sediments and Mg-rich igneous material which comprise the Pequizeiro Formation. II) polyphase deformation, metamorphism, magmatism, and orogenic uplift followed. These events are subdivided as follows: 1) F1 - deformation and regional metamorphism (Ma) in which So (original bedding) was transposed by isoclinal folding to S1 (regional schistosity) and progressive metamorphism produced sericite and garnet map zunes; 2) F2 - deformation produced tight folds in the schistosity (S1) resulting an axial plane surface (S2); well-marked mineral lineation (L2); 3) F3 deformation developed crenulation folds and a second phase of transposition (S3); e) F4 - deformation produced large folds accopanied by migmatization and late-tectonic granitic intrusions; 5) F5 - deformation formed small-scale plastic folds in cataclastic zones along the Iriri-Martírios lineament. III) The post-metamorphic Rio das Barreiras Formation was then deposited unconformably over this structural sequente and the final deformation event produced fault movements (transcurrent, thrust and normal), established joints, and permitted the rise of post-tectonic granitic plutons. This stage marks a transition from an environment of compressional stress to one of tensional stress on the regional scale. Subsequent to stageIII, consolidation of the South American platform occurred. Related erosional, sedimentary, magmatic, and'tectonic processes affedted this ares at numerous times throughout post-Brazilian cycle time.
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Evolução geológica da região de Colméia
(Universidade Federal do Pará, 1980-09-03) COSTA, João Batista Sena; HASUI, Yociteru; http://lattes.cnpq.br/3392176511494801
A geological mapping of the Colmeia region, in northern Goiás, has been carried out on a 1:100.000 scale. Semi-detailed geological observations coupled with stratigraphic, structural and petrological data are integrated aiming at the geological evolution of that region. The oldest recognized unit, the Archean Colmeia Complex, is represented by gneisses, granites and migmatites with associated schists, quartzites and amphibolites, and forms the central core of the Colmeia brachyanticline. Two main deformation periods have affected these rocks at the end of the Archean: the earliest period, F1deformed the rock banding surfaces into folds with E-W orlented axes and originated a well-defined axial-plane schistosity; the other one, F2, caused the refolding of the banding surfaces and folded the schistosity planes as to produce folds also with E-W oriented axes. Furthermbre, two migmatization phases were recognized: the first phase was contemporaneous with F1 and formed quartz-feldspar-rich neossomes in which minerais show a preferred orientation; the second phase predates F2 but post-dates F1, and is characterized by neossomes consisting essentially of non-oriented quartz and feldspar minerals. In the Middle Proterozoic, the Amazon Craton was regenerated leading to the accumulation of a thick volcano-sedimentary pile known as the Baixo Araguaia Super Group (Abreu, 1978). The lower unit of this pile is represented by the Estrondo Group which consists, from bottom to top of the Morro do Campo Formation (quartzites with schist intercalations), the Xambioá Formation (schists of various lithologies) and the Canto da Vazante Formation (feldspathic schists with biotite schist intercalations). The upper unit constitutes the Tocantins Group which is represented in the Colmeia region by the chlorite-quartz schists of the Pequizeiro Formation. Metamorphosed mafic and ultramafic rocks are associated with both the Estrondo and the Tocantins Group. In the Colmeia region, the Baixo Araguaia Super Group had a poliphasic evolution throughout the Middle Proterozoic. Its rocles recorded three major deformation periods: the first one is represented by intrafolial folding of the So surfaces and by the formation of an axial-plane schistosity; the second deformation event disturbed the schistosity surfaces generatinÉ folds with inclined axial planes and N-S oriented axes; the third deformation period is characterized by crenulation of the schistosity. The resulting folds have milimetric to kilometric dimensione and their axes parallel. NW-SE directions. Where the schistosity was completely transposed, crenulation cleavage was developed and biotite and chlorite recrystallizations took place on the transposition planes. The planar structures of the Baixo Araguaia basement were bent in response to shearing. Regional metamorphism of greenschist and amphibolite facies is concomitant with the first deformation episode while the second event affected the underlying Colmeia Complex superirnposing a similar folding style; at the same time contemporaneous migmatization originated N-S oriented quartz-feldspathic neossomes. Subsequent remobilization of the Colmeia Complex and the emplacement of intrusive granitic bodies gave rise to the Colmeia brachyanticline with which minor N-S oriented folds are associated. Radial faults were developed cutting both the basement and the metasedimentary cover. Other major discontinuities are also related to this event. The sedimentation of the Rio das Barreiras Formation marks the final act of the evolutionary history of the Colmeia region. Such an evolution included lithogenetic processes of the Archean and Middle Proterozoic as well as thermo-tectonic phenomena related to the Jequié and Uruaçuano cycles. K-Ar and Rb-Sr radiometric dating indicates reheating associated with the Transamazonic and Brazilian cycles.
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Evolução geológica da região de Tucuruí - Pará
(Universidade Federal do Pará, 1982-05-27) MATTA, Milton Antonio da Silva; HASUI, Yociteru; http://lattes.cnpq.br/3392176511494801
The northern part of the Araguaia Belt is exposed in the Tucuruí region and their stratigraphic, structural, metamorphic and magmatic features had been studied aiming at contributing for the understanding of the geological evolution of the area. The oldest stratigraphic unit of the area is represented by the Xingu Complex, composed by gneisses and granitos and subordinated schists and anphibolites. These rocks show evidence of a polycyclic metamorphic and structural history. Over this unit, during the niddle Proterozoic, the Tucuruí Group was developed. The bottom of this unit is composed by a sequence of tholeiitic basal-tic flows which were hera enclosed in the Caripé Formation. The Morrote Formation, is made up of graywackes, and constitutes the upper part of the Tucurui Group. The geossinclinal evolution of the Araguaia Belt took place during the Uruaçuano Cycle. This geotectonic unit is represented in the studied area by the Couto Magalhães Formation (Tocantins Group) which comprises pelitic and psamitic metasediments. These rocks show a greenshist facies metamorphism and structures generated by two phases of deformation in conditions of lower structures level. After the metamorphism of the Araguaia Belt, the Couto Magalhães Formation acted as the place of mafic and ultramafic intrusion and, lately, the Tucuruí Fault thrusted the metamorphic rocks of the Tocantins Group over the Tucuruí Group lithotypes. This faulting, besides generating a. series of structural features in the both groups as well as in the later migmatites, has also induced a dynamic metamorphic event into the rocks under green-schist facies conditions. Through the statistic treatment of structural data from the denso fault population which cuts the area, it was possible to deduce the shertening and the eterlding directiors related to the progressivo deformation induced by the thrust faulting had acted from E to W. Post-faulting mafic dykes represent the last magmatic event related to the Mesozoic Era. During the Cenozoic the area was a place of Tertiary sedimentation (Barreiras Formation), with sand, clays and conglomeratic levels. A final reactivation was responsible for the fracturing and faulting showed by the Barreiras Formation lithotypes Quatérnaty deposits mostly alluvial sediments, are the final units of the area.
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Evolução geotectônica do pré-cambriano da região meio norte do Brasil e sua correlação com a África Ocidental
(Universidade Federal do Pará, 1990-12-04) ABREU, Francisco de Assis Matos de; HASUI, Yociteru; http://lattes.cnpq.br/3392176511494801
This study presente a proposal for the geotectonic evolution for the pre-Cambrian portion of mid north region of Brazil and its correlation with western Africa based on the Integration of multldisciplinary geologic Information. Two types of geotectonic units are recognized: estabilized areas at the lower Proterozoic/early mid-Proterozoic (cratonic nuclei) and adjacent areas whose tectonic instability continued until the Phanerozoic (mobile belts). In the first case, one finds the Amazonian craton, not analysed in this work, and the Western African Craton/São Luis. The second case, assesses the vast reglon known In Brazil as Araguaia Belt and northwest of the Borborema Province that along with the southwest portion of the Tentugai Belt provide south continuity to the Parnaíba basin emergence. On the African side, the easternmost part of the West African Craton corresponding to the Pharusian, Daomeinian and to the west side of the Rocklides and Mauritanides belts, this last one with configurated evolution until the Hercynian Orogeny. In the cratonic nuclei one finds preserved geometric aspects which are fundamental for the past relationship between the more ancient sialitic crust where one visualizes the presence of globular batholiths, incrusted in high degree gneiss highly deformed and its cover often represented by sequences of the "greenstone belt type". The formation of this continental crust would have ocurred initlally by underplating being increased horizontaliy afterwards by primary cratonic nuclei. In the areas where tectonic Instability continued, continental Ilthosphere was extremely modified providing conditions for the establishment of sedimentary basins by colapse of the superstructure, generating magma simultaneously with plastic deformation that established complex relationships between gneiss and the roots of these basins, generating high degree terrain, low dip follations and migmatization zones. In the studied region, mostly on the Brazilian portion, these areas, where the Instability continued, involves a NE-SW macro shear beit, extending Itself from Africa, crossing the northwest of Ceará and continuing south under the sediment of the Parnaiba basin. These directions modify to E-W as they approach the African border at Sierra Leone and Ivory Coast at the border of the Amazonian. Craton reaching a NW-SE direction In the Guiana Shield. Basically, they encompass the northwest of Ceará In the NE-SW direction and the NE-SW strong gravimetric references. The high and medium degree rocks of this region are replaced in the northwest direction by low to medium degree rocks of the São Luis Craton and by the birrimian complex of volcano-sedimentary basins: the NW-SE Tentugai Belt establishes itself discontinually in relation to the NE-SW structures of the northwest belt of Ceará. Area of less expressive width with these same directions are found west of the Amazonlan Craton. There, it would have occurred a wide range of phenomena In terms of deformation processes that reached an expressive granitogenesis and cratonization with Rb/Sr ages with range of 1900-2000 Ma determining, therefore, the period in which these pheneomena ocurred in the Arquean and eariy Proterozoic. Plane and linear elements define geometrically in the various segments analyzed the special positions of the main axis of the ellipsoid of deformation. The general movement along the NE-SW and E-W segmente was dextral, with NW-SE and ENW-SSE secondary sinistrai directions of shear. The prevalling metamorphlc conditions in this period mark the presence of stabilized groups of minerais with inciplent to medium degree in the cratonic domaln, while at the beit the conditions of high degree and anatexia might have occurred for large areas. Such geotectonic matrix has conditioned geologic phenomena occurred in the region. The tectonic stability occurred was followed by the emergent of conditions for the deposition of important platform sequences with start around 1600-1700 Ma (Tarkwaiano, Gorotire, Guelb at Hadid etc.). The unstable conditions reappearred around 800-1000 Ma on a more restricted fashion in terms of their area of influence, and it resulted In the formation of an extensive crusta) mobility zone contouring stabilized cratonic areas in the early Proterozoic responsible by the development of the Farausian, Daomenian, northwest of Ceará, Tentugal, Rockelian, Mauritian and Araguaia belts. The distention processes were more important In the Faruslan Beit with the formation of an ocean crust (Bou Azzer ofiolites - Marrocos) and a continental crust strongiy percolated at the Araguaia Belt. In other areas the distention processes were lesa important. Large scale crustal reworking with total or partial rehomonization of rocke occurs in this region as well as granitogenesis with age around 500-600 Ma. Tardl-kinematic effects expressed through tectonic movements among the narrow linear zones and restrict molasses may have followed all these processes and are represented by the Jalbaras Group, Piriá Formation, Rio das Barreiras Formation, among others, In the early Eon Phanerozoic.
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Metamorfismo das rochas pelíticas do segmento setentrional da faixa Paraguai-Araguaia
(Universidade Federal do Pará, 1980-03-20) SILVA, José Maurício Rangel da; HASUI, Yociteru; http://lattes.cnpq.br/3392176511494801
Petrographic, petrochemical and microstructural data were used in the study of the metamorphism. In keeping with the work's scalé, the data .are regionally consistent. The metamorphism acted on sedimentary parent rocks, chemically similar to shales and greywacke admixtures. Relict sedimentary structures point to a sedimentary origin. The mineral assembrages distribution in Baixo Araguaia Group shows, from west to east, a regional metamorphic zoning with sericite, chlorite and biotite. Around megastructures (with supposed basement nucleus) a garnet zone has been recognized. The baric type is medium-pressure and corraspodds to Northern Appalachians and Scottish Highlands. Metamorphism and tectonic events are correlativa. The intensity of metamorphism, correspondingly to staurolite and kyanite crystallization, outlasts the deformation F2. The cooling of the meta sedimentary sequence brought out the biotite and muscovite crystallization. The metamorphism is referable to a polyphase cycle. The final manifestations .of the metamorphism belong to the Brasiliano Cycle.