Made available in DSpace on 2015-03-13T17:08:14Z (GMT). No. of bitstreams: 1 MariaFNB.pdf: 1315338 bytes, checksum: 0d0177ce82f07bd3aa4bb82fa98ec33d (MD5) Previous issue date: 2008-06-13 / Conselho Nacional de Desenvolvimento Cient?fico e Tecnol?gico / Crustal thickness and VP/VS estimates are essential to the studies of subsurface geological structures and also to the understanding of the regional tectonic evolution of a given area. In this dissertation, we use the Langston?s (1979) Receiver Function Method using teleseismic events reaching the seismographic station with angles close to the vertical. In this method, the information of the geologic structures close to the station is isolated so that effects related to the instrument response and source mechanics are not present. The resulting time series obtained after the deconvolution between horizontal components contains the larger amplitude referring to the P arrival, followed by smaller arrival caused by the reverberation and conversion of the P-wave at the base of the crust. We also used the HK-Stacking after Zhu & Kanamori (2000) to obtain crustal thickness and Vp/VS estimates. This method works stacking receiver functions so that the best estimates of crustal thickness and Vp/VS are found when the direct P, the Ps wave and the first multiple are coherently stacked. We used five broadband seismographic stations distributed over the Borborema Province, NE Brazil. Crustal thickness and Vp/VS estimates are consistent with the crust-mantle interface obtained using gravity data. We also identified crutal thickening in the NW portion of the province, close to Sobral/CE. Towards the center-north portion of the province, there is an evident crustal thinning which coincides with a geological feature consisting of an alignment of sedimentary basins known as the Cariris-Potiguar trend. Towards the NE portion of the province, in Sol?nea/PB and Agrestina/PE regions, occurs a crustal thickening and a systematic increase in the VP/VS values which suggest the presence of mafic rocks in the lower crust also consistent with the hypothesis of underplating in the region / A estimativa da espessura da crosta terrestre e raz?o VP/VS s?o essenciais para o detalhamento de estruturas e fei??es geol?gicas, al?m de corroborarem para o entendimento da evolu??o tect?nica regional. Neste trabalho, utiliza-se o m?todo da Fun??o do Receptor de Langston (1979) com eventos teless?smicos que incidem sob uma esta??o sismogr?fica com um ?ngulo pr?ximo da vertical. ? necess?rio o isolamento de informa??es das estruturas pr?ximas ao receptor, eliminando informa??es relacionadas ? resposta do instrumento, e ao mecanismo da fonte. O sismograma sint?tico obtido ap?s uma deconvolu??o entre as componentes horizontais possui um pico maior referente ? onda P, seguido por picos menores da onda Ps e m?ltiplas. A Onda Ps ? considerada como onda P convertida em onda S refratada na descontinuidade Moho. Para o c?lculo das estimativas de espessura crustal e raz?es Vp/VS utilizou-se o procedimento HK-Stacking de Zhu & Kanamori (2000). Esse m?todo trabalha com o empilhamento das fun??es do receptor. As melhores estimativas de espessura crustal e raz?o VP/VS s?o encontradas quando as tr?s fases P, Ps e primeira m?ltipla s?o empilhadas coerentemente. Foram utilizadas cinco esta??es sismogr?ficas banda-larga distribu?das estrategicamente pela Prov?ncia Borborema, nordeste do Brasil. As estimativas de espessura crustal e raz?o VP/VS s?o consistentes com o modelo atual da interface crosta-manto usados pela gravimetria. Foi identificado um espessamento crustal na por??o NW da prov?ncia, pr?ximo de Sobral/CE, na borda leste da Bacia do Parna?ba. Em dire??o a por??o centro-norte da Prov?ncia Borborema ? evidente um afinamento crustal, coincidente com a fei??o geol?gica que consiste de um alinhamento de bacias sedimentares conhecido como o trend Cariris-Potiguar. Na por??o NE, nas regi?es de Sol?nea/PB e Agrestina/PE, ocorre um espessamento crustal e aumento da raz?o VP/VS sugerindo presen?a de rochas mais m?ficas na crosta inferior, consistente com a hip?tese de underplating na regi?o

Made available in DSpace on 2015-03-13T17:50:33Z (GMT). No. of bitstreams: 1 RosanaMN_DISSERT.pdf: 3523232 bytes, checksum: 011fb01612f8bf7e79dd72d9c0642aae (MD5) Previous issue date: 2010-08-03 / The Borborema Province, Northeastern Brazil, had its internal structure investigated by different geophysical methods like gravity, magnetics and seismics. Additionally, many geological studies were also carried out to define the structural domains of this province. Despite the plethora of studies, there are still many important open aspects about its evolution. Here, we study the velocity structure of S-wave in the crust using dispersion of surface waves. The dispersion of surface waves allows an estimate of the average thickness of the crust across the region between the stations. The inversion of the velocity structure was carried out using the inter-station dispersion of surface waves of Rayleigh and Love types. The teleseismic events are mainly from the edges of the South and North American plates. The period of data collection occurred between 2007 and 2010 and we selected 7 events with magnitude above 5.0 MW and up to 40 km depth. The difference between the events back-azimuths and the interstation path was not greater than 10. We also know the depth of the Moho, results from Receiver Functions (Novo Barbosa, 2008), and use those as constrains in inversion. Even using different parameterizations of models for the inversion, our results were very similar the mean profiles velocity structure of S-wave. In pairs of stations located in the Cear?a Central Domain Borborema the province, there are ranges of depths for which the velocities of S are very close. Most of the results in the profile near the Moho complicate their interpretation at that depth, coinciding with the geology of the region, where there are many shear zones. In particular, the profile that have the route Potiguar Bacia in inter-station, had low velocities in the crust. We combine these results to the results of gravimetry and magnetometry (Oliveira, 2008) and receptor function (Novo Barbosa, 2008). We finally, the first results on the behavior of the velocity structure of S-wave with depth in the Province Borborema / A Prov?ncia Borborema, Nordeste do Brasil, tem sua estrutura interna investigada por diferentes m?todos geof?sicos: gravim?tricos, magn?ticos e s?smicos. Adicionalmente, muitos estudos geol?gicos foram levados a definir dom?nios estruturais para a prov?ncia; mas, ainda h? muitos aspectos em aberto sobre sua evolu??o. Neste trabalho, estudamos o comportamento da velocidade da onda S com a profundidade na crosta, usando a caracter?stica de dispers?o das ondas de superf?cie. No m?todo Inter-Esta??o, a dispers?o calculada em cada esta??o, nos ajuda a estimar a espessura m?dia da crosta na regi?o entre as duas esta??es. As invers?es das curvas de dispers~ao s~ao feitas usando a dispers?o inter-esta??o de ondas Rayleigh e Love. Os eventos teless??smicos selecionados s?o principalmente das bordas das placas Sul-Americana e Americana. O per?odo da coleta de dados ocorreu entre 2007 e 2010. Foram usados 7 eventos com magnitudes acima de 5.0 MW e at? 40 km de profundidade. A pequena quantidade de dados se justifica pelo fato dos eventos estarem a pelo menos 10_ do caminho de c?rculo m?ximo entre as esta?oes. Usamos tamb?em o conhecimento da profundidade da Moho, resultados de Fun??es do Receptor (Novo Barbosa, 2008) como v??nculos na invers?o. Mesmo usando diferentes parametriza??es de modelos para a invers~ao, nossos resultados foram de perfis m?edios de velocidade de onda S muito parecidos. Nos pares de estac? ~oes localizados no dom??nio Cear? Central da Prov??ncia Borborema, h? intervalos de profundidades, para os quais as velocidades de S s?o muito pr?ximas na regi?o inter-estac? ~ao desse dom??nio. Na maioria dos resultados, as varia??es da velocidade da onda S no perfil pr?oximas a Moho, dificultam a interpreta??o dos mesmos a essa profundidade e podem indicar forte varia??o lateral, coincidindo com a geologia da regi?o, onde existem muitas zonas de cisalhamento. Em particular, o perfil que possui a Bacia Potiguar no percurso inter-estac? ~ao, apresenta baixas velocidades na crosta. Integramos esses resultados aos resultados da gravimetria e magnetometria (Oliveira, 2008) e func? ~ao do receptor (Novo Barbosa, 2008). Assim, obtivemos os primeiros ind??cios sobre o comportamento da velocidade da onda S com a profundidade, na prov??ncia Borborema

Submitted by Automa??o e Estat?stica (sst@bczm.ufrn.br) on 2015-12-08T00:26:45Z No. of bitstreams: 1 MariaTatianyDuarteDeOliveira_DISSERT.pdf: 21145540 bytes, checksum: 89c0dc510ee92a8aeafd623a30df117c (MD5) / Approved for entry into archive by Arlan Eloi Leite Silva (eloihistoriador@yahoo.com.br) on 2015-12-10T22:56:19Z (GMT) No. of bitstreams: 1 MariaTatianyDuarteDeOliveira_DISSERT.pdf: 21145540 bytes, checksum: 89c0dc510ee92a8aeafd623a30df117c (MD5) / Made available in DSpace on 2015-12-10T22:56:19Z (GMT). No. of bitstreams: 1 MariaTatianyDuarteDeOliveira_DISSERT.pdf: 21145540 bytes, checksum: 89c0dc510ee92a8aeafd623a30df117c (MD5) Previous issue date: 2014-02-26 / A ?rea estudada situa-se, geograficamente, no extremo NE do Estado do Rio Grande do Norte situados nos munic?pios de Taipu e Po?o Branco e geologicamente inseridos no Terreno Cristalino S?o Jos? do Campestre pertencente ? Prov?ncia Borborema, onde observando rela??es de campo, dados petrogr?ficos e geoqu?micos, permitiram individualizar tr?s pl?tons denominados: Gameleira, Taipu e Pitombeira. O Pl?ton Gameleira ? composto por rochas granodior?ticas caracterizadas por fenocristais zonados de plagiocl?sios e tendo anfib?lio e biotita como m?ficos principais. Quimicamente, s?o rochas metaluminosas, de natureza c?lcio-alcalina e apresentam car?ter magnesiana. O Pl?ton Pitombeira ? composto por duas f?cies: (a) uma monzogran?tico ? sienogran?tica de textura grossa a porfir?tica caracterizada por fenocristais de K-feldspato e (b) uma de composi??o quartzo dior?tica a tonal?tica distinta por suas ripas de plagiocl?sio parcialmente zonadas e com borda de resfriamento. Quimicamente s?o rochas transicionais entre metaluminosas a peraluminosas, de natureza subalcalina (c?lcio-alcalina de alto K) e car?ter ferroso. Por fim, o Pl?ton Taipu ? formado por rochas monzogran?ticas a sienogran?ticas, contendo biotita como m?fico principal. S?o rochas peraluminosas, de natureza subalcalinas (c?lcio-alcalina de alto K) e car?ter ferroso. No que se refere ?s an?lises de elementos terras raras (ETR), pode-se inferir que os tr?s pl?tons estudados apresentam anomalias negativas de Eu e enriquecimento em ETR leves, com raz?es de LaN/YbN entre 9,38 a 16,20 ppm (Pl?ton Gameleira), 17,99 a 31,39 ppm (f?cies gran?tica do Pl?ton Pitombeira), 14,15 a 21,81 ppm (f?cies dior?tica do Pl?ton Pitombeira) e 15,17 a 175,41 ppm (Pl?ton Taipu). Analisando os dados qu?micos e os diagramas em conjunto ? poss?vel sugerir que os pl?tons estudados pertencem a um ambiente tect?nico tardi a p?s-colisional. Abstract The studied area is geographically situated in the extreme northeastern of Rio Grande do Norte State located in the municipalities of Taipu and Po?o Branco and geologically entered in the Crystalline Land S?o Jos? do Campestre which belongs to Borborema Province, where by observing the field relations, petrographic and geochemical datas, has allowed to individualize three plutons named: Gameleira, Taipu and Pitombeira. The Gameleira Pluton consists in granodioritic rocks characterized by phenocrysts zoned plagioclase having amphibole and biotite as the main mafic. Which are Chemically, metaluminous rocks, naturally from calc-alkaline and present magnesian character. The Pitombeira Pluton consists in two facies: (a) one monzogranite-syenogranite to coarse texture and to the porphyritic characterized by K-feldspar phenocrysts and (b) quartz dioric-tonalitic composition to a distinct for its laths of plagioclase partially zoned and also with cooling edges. Chemically are transitional rocks between metaluminous to peraluminous, naturally from subalkaline (high-K calc-alkaline) and ferrous character. Thus, the Taipu pluton is formed by monzagranitic-sienogranitic rocks, containing biotite as its main mafic. They are peraluminous rocks, naturally subalkaline (high-K calc-alkaline) and ferrous character. As regards to the rare earth elements analysis (REE), which can be inferred that the three studied plutons exhibit negative anomalies of Eu and REE slight enrichment, with ratios of LaN / YbN between 9.38 to 16.20 ppm (Gameleira Pluton) 17.99 to 31.39 ppm (Pluton Pitombeira granitic facies), from 14.15 to 21.81 ppm (Pluton Pitombeira dioritic facies) and from 15.17 to 175.41 ppm (Pluton Taipu). Analyzing the chemical and diagrams datas to one another, it?s allowed to suggest that the studied plutons belong to a late tectonic environment to a post-collisional. / The studied area is situated in the northeastern extremity of the Rio Grande do Norte State, between the municipalities of Taipu and Po?o Branco, and is geologically inserted into the S?o Jos? do Campestre Crystalline Terrain within the Borborema Province, where the analysis of field relationships, petrographic and geochemical data allowed the distinction of three plutons named: Gameleira, Taipu and Pitombeira. The Gamaleira Pluton is composed of granodioritic rocks characterized by zoned plagioclase phenocrysts, with amphibole and biotite as the main mafic phases. Geochemically, these are metaluminous rocks of calc-alkaline nature and magnesian character. The Pitombeira Pluton encompasses two facies: (a) a coarse-grained to porphyritic monzo- to syenogranitic facies marked by K-feldspar phenocrysts; and (b) a quartz dioritic to tonalitic facies with partially zoned plagioclase laths showing chilled rims. Geochemically, rocks of the monzo- to syenogranitic facies are transitional between metaluminous and peraluminous, display a subalkaline nature (high K calc-alkaline) and a ferroan character, whereas rocks of the quartz dioritic to tonalitic facies are metaluminous, with shoshonitic affinity and ferroan character. Lastly, the Taipu Pluton is made of monzoto syenogranitic rocks with biotite as the chief mafic mineral. They are peraluminous rocks of subalkaline nature (high-K calc-alkaline) and ferroan character. Regarding the rare-earth elements (REE), it is possible to conclude that the three studied plutons display negative Eu anomalies and a relative enrichment of LREE over HREE, with LaN/YbN ratios between 9.39 to 16.20 (Gameleira Pluton), 17.99 to 31.39 (granitic facies of the Pitombeira Pluton), 14.15 to 21.81 (dioritic facies of the Pitombeira Pluton) and 15.17 to 175.41 (Taipu Pluton). Based on the combined investigation of geochemical data and discrimination tectonic diagrams, a late- to post-collisional tectonic environment is suggested for the plutons here studied

Submitted by Automa??o e Estat?stica (sst@bczm.ufrn.br) on 2016-03-02T23:01:37Z No. of bitstreams: 1 JoseGedsonFernandesDaSilva_DISSERT.pdf: 27021892 bytes, checksum: 7b5f5e3fe5ef57651e7226b69f4eea85 (MD5) / Approved for entry into archive by Arlan Eloi Leite Silva (eloihistoriador@yahoo.com.br) on 2016-03-04T21:31:17Z (GMT) No. of bitstreams: 1 JoseGedsonFernandesDaSilva_DISSERT.pdf: 27021892 bytes, checksum: 7b5f5e3fe5ef57651e7226b69f4eea85 (MD5) / Made available in DSpace on 2016-03-04T21:31:17Z (GMT). No. of bitstreams: 1 JoseGedsonFernandesDaSilva_DISSERT.pdf: 27021892 bytes, checksum: 7b5f5e3fe5ef57651e7226b69f4eea85 (MD5) Previous issue date: 2014-07-25 / Petr?leo Brasileiro S.A. - PETROBRAS / A an?lise estratigr?fica de subsuperf?cie de estratos devonianos da Bacia do Rio do Peixe, rec?m-datados por palinologia, resultou na classifica??o de duas novas unidades litoestratigr?ficas reunidas no Grupo Santa Helena. A Forma??o Pil?es (unidade inferior), na qual predominam pelitos escuros e arenitos m?dios a muito finos, associados a conglomerados e brechas. A Forma??o Triunfo (unidade superior) composta por arenitos cinza-esbranqui?ados, grossos a conglomer?ticos, caul?nicos, com estratifica??es cruzadas, conglomerados, pelitos e arenitos finos intercalados. Estas unidades foram caracterizadas com o apoio de testemunhos, amostras laterais e de calha, perfis geof?sicos convencionais e de imagem, de tr?s po?os perfurados pela PETROBRAS, e s?smica 3D. Na Forma??o Pil?es predominam f?cies prodeltaicas, com f?cies de t?lus e debritos subaquosos e de lobos turbid?ticos arenosos intercalados, na parte distal de sistemas de leques deltaicos e f?cies de barras do sistema fluviodeltaico entrela?ado (braided) da Forma??o Triunfo. O Grupo Santa Helena corresponde ? tectonossequ?ncia devoniana inferior, cuja espessura m?xima conhecida ? de 343 metros (is?cora) no po?o 1-PIL-1-PB (Pil?es n?1), depositada durante um ciclo transgressivo-regressivo em um graben, com eixo deposicional controlado por um segmento NO-SE da Zona de Cisalhamento Patos. O limite inferior desta tectonossequ?ncia ? n?o-conforme e o superior ? discordante com a tectonossequ?ncia cret?cea inferior (Grupo Rio do Peixe), com um hiato de aproximadamente 265 milh?es de anos. Ignimbritos e brechas coignimbr?ticas (brecha vulc?nica Po?o da Jurema), relacionadas a um evento vulc?nico pirocl?stico ainda desconhecido, foram reconhecidas na margem norte do Semigraben de Sousa. H? evid?ncia, a partir de dados de subsuperf?cie, de que este evento ? contempor?neo ao preeenchimento do graben devoniano. Os resultados deste estudo indicam que a evolu??o tectonovulcanossedimentar da bacia ? poli-hist?rica. Esta atualiza??o litoestratigr?fica abre novas perspectivas de pesquisas geol?gicas na Bacia do Rio do Peixe e em outras bacias interiores do Nordeste do Brasil. Os resultados da pesquisa tamb?m contribuem para o melhor conhecimento da evolu??o da Prov?ncia Borborema e da paleogeografia do Gonduana ocidental durante o Eodevoniano. / Subsurface stratigraphic analysis of Devonian strata from the Rio do Peixe Basin, newly recognized by palynological studies, has resulted in the identification of two new lithostratigraphic units assembled in the Santa Helena Group. The Pil?es Formation, the lower unit, is composed mainly of dark mudstones and medium-tovery fine-grained sandstones, with minor conglomerates and breccias. The Triunfo Formation, the upper unit, comprises whitish grey, kaolinitic, coarse-grained to conglomeratic, cross stratified sandstones and conglomerates, with interbedded mudstones and fine-grained sandstones. These units were characterized using cores, sidewall and cuttings samples, conventional logs and image log, from three wells drilled by PETROBRAS, and 3D seismic data. The Pil?es Formation is interpreted as prodeltaic facies, with lesser associated subaqueous talus, debrite and sandy turbidite lobe facies, distal part of fandelta and braided fluviodeltaic facies of Triunfo Formation. The Santa Helena Group corresponds to the Lower Devonian tectono-sequence deposited in a NW-SE-trending graben during a transgressiveregressive cycle. With 343 meters of thickness (isochore) in well 1-PIL-1-PB (Pil?es 1), this sequence has a non-conformity at the lower boundary and its upper boundary is an unconformity with the Lower Cretaceous tectono-sequence (Rio do Peixe Group), that represents a hiatus of about 265 million years. Ignimbrites and coignimbrite breccias (Po?o da Jurema volcanic breccia), related to an unknown pyroclastic volcanic event, were recognized at the northern margin of the Sousa halfgraben. Evidence from well data suggests that this event is coeval with the Devonian graben filling. The present study indicates a polyhistorical tectono-volcanosedimentary evolution of the basin. This lithostratigraphic update brings new perspectives for geological research in the Rio do Peixe Basin, as well as in other inland basins of the Northeastern of Brazil. The results of the research also contribute to the kwnoledge of the Borborema Province and western Gondwana paleogeography during the Early Devonian.

Submitted by Automa??o e Estat?stica (sst@bczm.ufrn.br) on 2016-03-02T23:01:37Z No. of bitstreams: 1 RafaelaCarreiroDias_DISSERT.pdf: 7493649 bytes, checksum: 18d66dcedc96371bd5f40830e9aec1ba (MD5) / Approved for entry into archive by Arlan Eloi Leite Silva (eloihistoriador@yahoo.com.br) on 2016-03-04T21:54:12Z (GMT) No. of bitstreams: 1 RafaelaCarreiroDias_DISSERT.pdf: 7493649 bytes, checksum: 18d66dcedc96371bd5f40830e9aec1ba (MD5) / Made available in DSpace on 2016-03-04T21:54:12Z (GMT). No. of bitstreams: 1 RafaelaCarreiroDias_DISSERT.pdf: 7493649 bytes, checksum: 18d66dcedc96371bd5f40830e9aec1ba (MD5) Previous issue date: 2014-03-06 / Conselho Nacional de Desenvolvimento Cient?fico e Tecnol?gico - CNPq / O ru?do s?smico tem sido tradicionalmente considerado como uma perturba??o n?o desejada do ambiente que ?contamina? a aquisi??o de dados de terremotos. Mas ao longo da ?ltima d?cada tem sido mostrado que informa??es coerentes sobre a estrutura do subsolo podem ser extra?das a partir de correla??es cruzadas do ru?do s?smico de ambiente. Neste contexto, as regras s?o reversas, sendo os terremotos o que necessitamos excluir dos dados. Os principais causadores do ru?do s?smico de ambiente s?o os microssismos oce?nicos e perturba??es atmosf?ricas. A per?odos menores que 30 s, o espectro do ru?do s?smico de ambiente ? dominado por energia micross?smica. O microssismo ? o sinal s?smico mais cont?nuo da Terra e pode ser classificado como prim?rio (observado na faixa 10-20 s) e secund?rio (observado na faixa 5-10 s). A fun??o de Green do meio de propaga??o entre dois receptores pode ser reconstru?da atrav?s da correla??o cruzada do ru?do s?smico de ambiente registrado simultaneamente nesses dois receptores. A reconstru??o da fun??o de Green ? geralmente proporcional ? por??o de ondas de superf?cie do campo de onda s?smico, j? que a energia micross?smica viaja principalmente como ondas de superf?cie. Neste trabalho, s?o apresentadas 194 fun??es de Green obtidas a partir de correla??es cruzadas de 1 m?s de registro da componente vertical do ru?do s?smico de ambiente para diferentes pares de esta??es s?smicas do Nordeste do Brasil. As correla??es cruzadas di?rias foram empilhadas utilizando a t?cnica n?o linear tf-PWS que real?a sinais coerentes fracos atrav?s da redu??o de ru?do incoerente. As correla??es cruzadas mostram que o sinal emergido ? dominado por ondas Rayleigh nas componentes verticais e que as velocidades de dispers?o podem ser medidas confiavelmente para uma faixa de per?odos entre 5 e 20 s. O estudo inclui tanto esta??es permanentes para monitoramento s?smico, quanto esta??es tempor?rias de experimentos passivos na regi?o, formando uma rede combinada de 33 esta??es separadas por dist?ncias entre 60 e 1311 km, aproximadamente. Estas medidas de velocidades de dispers?o de ondas Rayleigh em seguida s?o usadas na elabora??o de imagens tomogr?ficas da Prov?ncia Borborema do Nordeste do Brasil. As tomografias de ru?do s?smico obtidas aqui permitem mapear satisfatoriamente fei??es estruturais existentes na regi?o. As imagens tomogr?ficas de per?odos mais curtos (~5 s) mostram a estrutura crustal rasa e claramente definem as bacias sedimentares marginais e intracontinentais, bem como as partes de zonas de cisalhamento importantes que atravessam a Prov?ncia Borborema. As imagens tomogr?ficas de per?odos mais longos (10 - 20 s) atingem profundidades da crosta superior e a maior parte das anomalias desaparece. Algumas delas localizada no interior da Prov?ncia Borborema, no entanto, persistem. A evolu??o Cenoz?ica da Prov?ncia Borborema foi marcada por epis?dios de vulcanismo Cenoz?ico e eleva??o, mas nenhuma correla??o ? observada com estas caracter?sticas Cenoz?icas e as anomalias profundas. As anomalias n?o se correlacionam com mapas dispon?veis de fluxo de calor superficial na Prov?nica Borborema, e a origem das anomalias profundas permanece enigm?tica. / Ambient seismic noise has traditionally been considered as an unwanted perturbation in seismic data acquisition that "contaminates" the clean recording of earthquakes. Over the last decade, however, it has been demonstrated that consistent information about the subsurface structure can be extracted from cross-correlation of ambient seismic noise. In this context, the rules are reversed: the ambient seismic noise becomes the desired seismic signal, while earthquakes become the unwanted perturbation that needs to be removed. At periods lower than 30 s, the spectrum of ambient seismic noise is dominated by microseism, which originates from distant atmospheric perturbations over the oceans. The microsseism is the most continuous seismic signal and can be classified as primary ? when observed in the range 10-20 s ? and secondary ? when observed in the range 5-10 s. The Green?s function of the propagating medium between two receivers (seismic stations) can be reconstructed by cross-correlating seismic noise simultaneously recorded at the receivers. The reconstruction of the Green?s function is generally proportional to the surface-wave portion of the seismic wavefield, as microsseismic energy travels mostly as surface-waves. In this work, 194 Green?s functions obtained from stacking of one month of daily cross-correlations of ambient seismic noise recorded in the vertical component of several pairs of broadband seismic stations in Northeast Brazil are presented. The daily cross-correlations were stacked using a timefrequency, phase-weighted scheme that enhances weak coherent signals by reducing incoherent noise. The cross-correlations show that, as expected, the emerged signal is dominated by Rayleigh waves, with dispersion velocities being reliably measured for periods ranging between 5 and 20 s. Both permanent stations from a monitoring seismic network and temporary stations from past passive experiments in the region are considered, resulting in a combined network of 33 stations separated by distances between 60 and 1311 km, approximately. The Rayleigh-wave, dispersion velocity measurements are then used to develop tomographic images of group velocity variation for the Borborema Province of Northeast Brazil. The tomographic maps allow to satisfactorily map buried structural features in the region. At short periods (~5 s) the images reflect shallow crustal structure, clearly delineating intra-continental and marginal sedimentary basins, as well as portions of important shear zones traversing the Borborema Province. At longer periods (10 ? 20 s) the images are sensitive to deeper structure in the upper crust, and most of the shallower anomalies fade away. Interestingly, some of them do persist. The deep anomalies do not correlate with either the location of Cenozoic volcanism and uplift - which marked the evolution of the Borborema Province in the Cenozoic - or available maps of surface heat-flow, and the origin of the deep anomalies remains enigmatic.

Submitted by Automa??o e Estat?stica (sst@bczm.ufrn.br) on 2016-03-22T00:29:29Z No. of bitstreams: 1 RosanaMariaDoNascimento_TESE.pdf: 79491407 bytes, checksum: 65543c87c5a9f10fd3119a3ddf108730 (MD5) / Approved for entry into archive by Arlan Eloi Leite Silva (eloihistoriador@yahoo.com.br) on 2016-03-22T23:55:31Z (GMT) No. of bitstreams: 1 RosanaMariaDoNascimento_TESE.pdf: 79491407 bytes, checksum: 65543c87c5a9f10fd3119a3ddf108730 (MD5) / Made available in DSpace on 2016-03-22T23:55:31Z (GMT). No. of bitstreams: 1 RosanaMariaDoNascimento_TESE.pdf: 79491407 bytes, checksum: 65543c87c5a9f10fd3119a3ddf108730 (MD5) Previous issue date: 2015-01-29 / Coordena??o de Aperfei?oamento de Pessoal de N?vel Superior - CAPES / Conselho Nacional de Desenvolvimento Cient?fico e Tecnol?gico - CNPq / A Prov?ncia Borborema, localizada no nordeste do Brasil, possui um embasamento de idade Pr?-cambriana e um arcabou?o tect?nico estruturado no Neoproteroz?ico (740-560 Ma). Ap?s a separa??o dos continentes Sul-Americano e Africano, durante o Mesoz?ico formou-se um sistema de riftes no nordeste brasileiro, o qual deu origem ?s bacias marginais e interiores localizadas na Prov?ncia. Depois da separa??o continental, eventos de vulcanismos e epirogenia ocorreram na Prov?ncia, tais como o soerguimento do Planalto da Borborema e o magmatismo ao longo da linha Macau-Queimadas (AMQ), marcando assim a evolu??o da Prov?ncia. As causas do soerguimento do Planalto poderiam estar associadas a um underplating magm?tico (material m?fico preso na base da crosta), talvez relacionado com a gera??o de plugs continentais jovens (45-7 Ma) ao longo do AMQ devido a um mecanismo de convec??o em pequena escala na borda do continente. O objetivo deste trabalho ? investigar as causas do soerguimento intra-placa e sua poss?vel rela??o com o vulcanismo AMQ utilizando sismologia de banda larga, tendo em conta a correla??o de nossos resultados com estudos geof?sicos e geol?gicos realizados na Prov?ncia Borborema. As metodologias de banda larga para investigar a estrutura profunda na Prov?ncia incluem as fun??es do receptor e velocidade de dispers?o das ondas de superf?cie. Tanto as fun??es de receptor quanto a tomografia de dispers?o de ondas superficiais s?o m?todos que utilizam eventos teless?smicos e permitem obter estimativas de par?metros estruturais como espessura crustal, raz?o Vp/Vs e velocidade de onda S. Os sismogramas utilizados neste trabalho para as fun??es do receptor foram obtidas de 52 esta??es localizadas no Nordeste do Brasil: 16 esta??es de banda larga da rede RSISNE (Rede Sismogr?fica do Nordeste do Brasil), 21 esta??es de per?odo curto da rede INCT-ET (Instituto Nacional de Ci?ncia e Tecnologia ? Estudos Tect?nicos) e 6 esta??es de banda larga. Estes resultados acrescentam significativamente dados anteriores coletados em esta??es isoladas como a esta??o RCBR, da rede global GSN, as esta??es banda v larga CAUB e AGBL do projeto BLSP (Brazilian Lithosphere Seismic Project IAG/USP) e de 6 esta??es banda larga do projeto Mil?nio (Estudos geof?sicos e tect?nicos na Prov?ncia Borborema - CNPq). Para dispers?o de ondas de superf?cie foram usados sismogramas de 22 esta??es: 16 esta??es de banda larga da rede RSISNE, bem como das 6 esta??es banda larga do projeto Mil?nio. Neste trabalho foram desenvolvidas: (i) estimativas de espessura crustal e raz?o Vp/Vs para cada esta??o usando as fun??es do receptor, (ii) novas medidas de velocidade de grupo de ondas de superf?cie, que foram integradas com os percursos usados em uma tomografia da Am?rica do Sul, j? desenvolvida, para ampliar a resolu??o no Nordeste Brasileiro e (iii) modelos de velocidades de onda S (1D) para v?rios locais na Prov?ncia Borborema usando a invers?o simult?nea de fun??es do receptor com velocidades de dispers?o. Os resultados descrevem velocidades de onda S para a base da crosta que s?o consistentes com a presen?a de uma camada m?fica de 5-7.5 km de espessura. Foi observada a camada m?fica em apenas uma por??o da regi?o do planalto (parte sul) e aus?ncia da mesma na parte norte. Outra observa??o importante e que corrobora estudos de fun??es do receptor e refra??o s?smica s?o as diferentes espessuras crustais, tamb?m dividindo o planalto em uma parte de crosta fina (parte norte) e outra parte de crosta espessa (parte sul). Os modelos existentes para evidenciar a epirogenia n?o conseguem explicar todas essas observa??es. Sendo assim, prop?e-se que durante a orogenia Brasiliana, uma camada de material m?fico pr?-existente foi delaminada, total ou parcialmente, da crosta. A delamina??o parcial teria acontecido na parte sul do planalto, onde estudos independentes evidenciaram uma reologia mais resistente ? deforma??o. Ap?s isso, durante o Mesoz?ico e consequente processo de rifteamento houve afinamento da crosta da regi?o costeira e depress?o sertaneja, incluindo a parte norte do planalto. J? no Cenoz?ico, o soerguimento da parte norte do planalto teria ocorrido e o resultado seria uma parte norte sem material m?fico na base da crosta e parte sul com camada m?fica parcialmente delaminada,mas ambos com topografia elevada at? os dias atuais. / The Borborema Province, located in northeastern Brazil, has a basement of Precambrian age and a tectonic framework structured at the Neoproterozoic (740-560 Ma). After separation between South America and Africa during the Mesozoic, a rift system was formed, giving rise to a number of marginal and inland basins in the Province. After continental breakup, episodes of volcanism and uplift characterized the evolution of the Province. Plateau uplift was initially related to magmatic underplating of mafic material at the base of the crust, perhaps related to the generation of young continental plugs (45-7 Ma) along the Macau-Queimadas Alignment (MQA), due to a small-scale convection at the continental edge. The goal of this study is to investigate the causes of intra-plate uplift and its relationship to MQA volcanism, by using broadband seismology and integrating our results with independent geophysical and geological studies in the Borborema Province. The investigation of the deep structure of the Province with broadband seismic data includes receiver functions and surface-wave dispersion tomography. Both the receiver functions and surface-wave dispersion tomography are methods that use teleseismic events and allow to develop estimates of crustal parameters such as crustal thickness, Vp/Vs ratio, and S-velocity structure. The seismograms used for the receiver function work were obtained from 52 stations in Northeast Brazil: 16 broadband stations from the RSISNE network (Rede Sismogr?fica do Nordeste do Brasil), and 21 short-period and 6 broadband stations from the INCT-ET network (Instituto Nacional de Ci?ncia e Tecnologia ? Estudos Tect?nicos). These results add signifi- cantly to previous datasets collected at individual stations in the Province, which include station RCBR (GSN - Global Seismic Network), stations CAUB and AGBL (Brazilian Lithosphere Seismic Project IAG/USP), and 6 other broadband stations that were part of the Projeto Mil?nio - Estudos geof?sicos e tect?nicos na Prov?ncia Borborema/CNPq. For the surface-wave vii tomography, seismograms recorde at 22 broadband stations were utilized: 16 broadband stations from the RSISNE network and 6 broadband stations from the Mil?nio project. The new constraints developed in this work include: (i) estimates of crustal thickness and bulk Vp/Vs ratio for each station using receiver functions; (ii) new measurements of surfassewave group velocity, which were integrated to existing measurementes from a continental-scale tomography for South America, and (iii) S-wave velocity models (1D) at various locations in the Borborema Province, developed through the simultaneous inversion of receiver functions and surface-wave dispersion velocities. The results display S-wave velocity structure down to the base of the crust that are consistent with the presence of a 5-7.5 km thick mafic layer. The mafic layer was observed only in the southern portion of the Plateau and absent in its northern portion. Another important observation is that our models divide the plateau into a region of thin crust (northern Plateau) and a region of thick crust (southern Plateau), confirming results from independent refraction surveys and receiver function analyses. Existing models of plateau uplift, nonetheless, cannot explain all the new observations. It is proposed that during the Brazilian orogeny a layer of preexisting mafic material was delaminated, as a whole or in part, from the original Brasiliano crust. Partial delamination would have happened in the southern portion of the plateau, where independent studies found evidence of a more resistant rheology. During Mesozoic rifting, thinning of the crust around the southern Plateau would have formed the marginal basins and the Sertaneja depression, which would have included the northern part of the Plateau. In the Cenozoic, uplift of the northern Plateau would have occurred, resulting in a northern Plateau without mafic material at the base of the crust and a southern Plateau with partially delaminated mafic layer.

Submitted by Automa??o e Estat?stica (sst@bczm.ufrn.br) on 2016-07-25T19:35:27Z No. of bitstreams: 1 AlanPereiraDaCosta_DISSERT.pdf: 24726684 bytes, checksum: 6b4523ea74314d3a8b4944c8fbeef8ad (MD5) / Approved for entry into archive by Arlan Eloi Leite Silva (eloihistoriador@yahoo.com.br) on 2016-07-28T21:11:34Z (GMT) No. of bitstreams: 1 AlanPereiraDaCosta_DISSERT.pdf: 24726684 bytes, checksum: 6b4523ea74314d3a8b4944c8fbeef8ad (MD5) / Made available in DSpace on 2016-07-28T21:11:35Z (GMT). No. of bitstreams: 1 AlanPereiraDaCosta_DISSERT.pdf: 24726684 bytes, checksum: 6b4523ea74314d3a8b4944c8fbeef8ad (MD5) Previous issue date: 2015-04-23 / A atividade plut?nica ediacarana, relacionada a orog?nese Brasiliana/Pan-Africana, constitui uma das mais importantes fei??es geol?gicas na Prov?ncia Borborema, representada em sua extens?o por in?meros bat?litos, stocks e diques. O Pl?ton Gran?tico Serra da Rajada (PGSR), principal objeto desse estudo, situado na por??o central do Dom?nio Rio Piranhas-Serid? representa um exemplo dessa atividade, sendo objeto de estudos cartogr?fico, petrogr?fico, litogeoqu?mico e geocronol?gico. Suas rochas s?o individualizadas em duas f?cies, sendo a f?cies gran?tica descrita como monzogranitos constitu?dos por K-feldspato, plagiocl?sio (oligocl?sico-An23-24%), quartzo e biotita (m?fico principal), tendo como minerais acess?rios opacos, titanita, allanita, apatita e zirc?o. Clorita, mica branca e carbonato s?o minerais de altera??o. A f?cies dior?tica compreende rochas formadas por quartzo diorito contendo plagiocl?sio (fase mineral dominante), quartzo e K-feldspato. Biotita e anfib?lio s?o os minerais m?ficos dominantes, e titanita, minerais opacos, allanita, zirc?o e apatita s?o os acess?rios. Contudo, os trabalhos de cartografia geol?gica tamb?m identificaram na regi?o a presen?a de outras unidades litoestratigr?ficas, descritas como gnaisses e migmatitos indiferenciados com lentes de anfibolitos relacionados ao Complexo Caic? (Paleoproterozoica) e rochas metassedimentares do Grupo Serid? (Neoproterozoico) compostos por paragnaisses com lentes de calciossilic?ticas, muscovita quartzitos e biotita xistos (respectivamente forma??es Jucurutu, Equador e Serid?), os quais s?o as encaixantes para as rochas do PGSR. Ainda foram identificados diques de leucomicrogranito e de pegmatitos, ambos relacionados ao final do magmatismo Ediacarano, bem como dep?sitos col?vio-eluviais e aluvionares relacionados ao Ne?geno e Quatern?rio, respectivamente. Dados litogeoqu?micos, na f?cies gran?tica do PGSR, evidenciam rochas bastante evolu?das (SiO2 69% a 75%), rica em ?lcalis (Na2O+K2O ? 8,0%), empobrecidas em MgO (? 0,45%), CaO (? 1,42%) e TiO2 (? 0,36%) e teores moderados de Fe2O3t (2,16 a 3,53%). Apresentam natureza transicional entre metaluminosa e peraluminosa (predom?nio do ?ltimo) e possuem afinidade subalcalina/monzon?tica (c?lcio-alcalina de alto K). Diagramas de Harker mostram correla??es negativas em Fe2O3t, MgO e CaO, indicando fracionamento de m?ficos e plagiocl?sio. O espectro de ETR mostra enriquecimento dos ETR leves com rela??o aos ETR pesados (LaN/YbN = 23,70 a 0,23), com anomalia negativa no Eu (Eu/Eu* = 0,70 a 0,23), sugerindo fracionamento ou acumula??o na fonte de feldspatos (plagiocl?sio). A integra??o dos dados permite correlacionar ?s rochas do PGSR ?quelas referidas na literatura como Su?te C?lcio-Alcalina de Alto K Equigranular. Considera??es sobre as condi??es de cristaliza??o para as rochas do PGSR foram obtidas a partir da integra??o de dados petrogr?ficos e litogeoqu?micos, os quais indicaram atua??o de condi??es moderadas a elevadas de ?O2 (parag?nese mineral titanita + magnetita + quartzo), magma progenitor saturado em H2O (cristaliza??o precoce das biotitas), atua??o de processos tardi-magm?ticos de fluidos ricos em ?CO2, H2O e O2 causando altera??es em parte da assembleia mineral (carbonata??o e saussuritiza??o dos plagiocl?sio, cloritiza??o das biotitas e esfenitiza??o dos opacos). Condi??es de termobarom?tricas foram estimadas com base em par?metros geoqu?micos (Zr e P2O5), bem como por minerais normativos CIPW, com resultados mostrando temperatura m?nima de liquidus da ordem de 800?C e temperatura de solidus da ordem de 700?C. As press?es final/m?nima de cristaliza??o sugerem ser da ordem de 3 a 5 Kbar. A presen?a de minerais zonados (plagiocl?sio e allanita) associadas a dados litogeoqu?micos diagramas bi-log para Rb vs Ba e Rb vs Sr sugerem a atua??o da cristaliza??o fracionada como processo dominante na evolu??o magm?tica do PGSR. Estudos geocronol?gicos U-Pb e isot?picos Sm-Nd indicam, respectivamente, que o biotita monzogranito possui idade de cristaliza??o de 557?13 Ma, com idade modelo TDM de 2,36 Ga, tendo valor de eNd para a idade de cristaliza??o de -20,10, permitindo inferir fonte crustal paleoproterozoica para o magma. / The ediacaran plutonic activity related to the Brasilian/Pan-African orogeny is one of the most important geological features in the Borborema Province, represented along its extension by numerous batholiths, stocks, and dikes.The object of this study, the Serra Rajada Granitic Pluton (SRGP), located in the central portion of the Piranhas-Serid? River Domain is an example of this activity. This pluton has been the subject of cartographic, petrographic, geochronological and lithogeochemical studies and its rocks were characterized by two facies. First, the granitic facies were described as monzogranites consisting of K-feldspar, plagioclase (oligoclase - An23-24%), quartz and biotite (main mafic) and opaque minerals such as titanite, allanite, apatite, and zircon as accessories. Alteration minerals are chlorite, white mica and carbonate. Second, the dioritic facies consist of rocks formed by quartz diorite containing plagioclase (dominant mineral phase), quartz and K-feldspar. Biotite and amphibole are the dominant mafic minerals; and titanite, opaque minerals, allanite, zircon and apatite are the accessories. However, previous geological mapping work in the region also identified the presence of other lithostratigraphic units. These were described as gneisses and migmatites with undifferentiated amphibolite lenses related to the Caic? Complex (Paleoproterozoic) and metasedimentary rocks of the Serid? Group (Neoproterozoic) composed of paragneiss with calc-silicate lenses, muscovite quartzite and biotite schist (respectively, the Jucurutu formations, Equador and Serid?), the host rocks for the SRGP rocks. Leucomicrogranite and pegmatite dikes have also been identified, both related to the end of the Ediacaran magmatism and colluvial- eluvial and alluvial deposits related to Neogene and Quaternary, respectively. Lithogeochemical data on the SRGP granite facies, highlighted quite evolved rocks (SiO2 69% to 75%), rich in alkalis (Na2O+K2O ? 8.0%), depleted of MgO (? 0.45%), CaO (? 1.42%) and TiO2 (? 0.36%) and moderate levels of Fe2O3t (2.16 to 3.53%). They display transitional nature between metaluminous and peraluminous (predominance of the latter) with sub-alkaline/monzonitic (High K calcium-alkali) affinity. Harker diagrams show negative correlations for Fe2O3t, MgO, and CaO, indicating mafic and plagioclase fractionation. REE spectrum shows enrichment of LREE relative to heavy REE (LaN/YbN = 23.70 to 10.13), with negative anomaly in the Eu (Eu/Eu* = 0.70 to 0.23), suggesting fractionation or accumulation in the feldspars source (plagioclase). Data integration allows to correlate the SRGP rocks with those described as Calcium-Alkaline Suite of equigranular High K. The crystallization conditions of the SRGP rocks were determined from the integration of petrographic and lithogeochemical data. These data indicated intermediate to high conditions of ?O2 (mineral paragenesis titanite + magnetite + quartz), parent magma saturated in H2O (early biotite crystallization), tardi-magmatic processes of fluids rich in ?CO2, H2O and O2 causing part of the mineral assembly to change (plagioclase carbonation and saussuritization, biotite chloritization and opaques Sphenitization). Thermobarometrical conditions were estimated based on geochemical parameters (Zr and P2O5) and CIPW normative minerals, with results showing the liquidus minimum temperature of about800?C and the solidus temperature of approximately 700?C. The final/minimum crystallization pressure are suggested to be between 3 and 5 Kbar. The presence of zoned minerals (plagioclase and allanite) associated with lithogeochemical data in bi-log diagrams for Rb vs. Ba and Rb vs. Sr suggest the role of fractional crystallization as the dominant process in the magmatic evolution of SRGP. U-Pb Geochronological and Sm-Nd isotope studies indicated, respectively, the crystallization age of biotite monzogranite as 557 ? 13 Ma, with TDM model age of 2.36 Ga, and ?Nd value of -20.10 to the crystallization age, allowing to infer paleoproterozoic crustal source for the magma.

Made available in DSpace on 2015-02-24T19:48:38Z (GMT). No. of bitstreams: 1 VladimirCM_ate_Cap2.pdf: 2326830 bytes, checksum: b58da6e64643f0b1b300b813b8340f81 (MD5) Previous issue date: 2004-11-30 / Companhia de Pesquisa de Recursos Minerais / This thesis aims to advance in the geological knowledge of the region comprising the Pianc?-Alto Br?gida (TPAB) and Alto paje? (TAP) terranes, in the Transversal Zone Domain (Borborema Province, NE Brazil), with the main objective of understanding the geodynamic evolution and the structural framework of these units. To reach this objective, and besides field work and interpretation of traditional aerial photographs, other tools were employed like of remote sensing products (Landsat 7 ETM+, aeroradiometrics, aeromagnetics and topographical images), lithogeochemical (whole rock) analyses and geochronological dating (U-Pb in zircon), besides integration with literature data. In the area, several precambrian geological units outcrop, represented in the TAP by the paleoproterozoic Serra Talhada and Afogados da Ingazeira complexes, Riacho Gravat? Complex (metavolcano-sedimentary sequence of Stenian-Tonian age) and Cariris Velhos orthogneisses (of Tonian age). The TPAB comprises the Santana do Garrote (lower unit) and Serra do Olho d'?gua (upper unit) formations of the Cachoeirinha Group (Neoproterozoic III), besides the Pianc? orthogneisses and Bom Jesus paragneisses; the latter correspond to an older (basement ?) block and a possible high grade equivalent of the Cachoeirinha Group (or Serid? Group ?), respectively. Several Brasiliano-age plutons occur in both terranes.The aeromagnetic data show the continuity, at depth, of the main shear zones mapped in the region. The Patos, Pernambuco, Boqueir?o dos Cochos, Serra do Caboclo, Afogados da Ingazeira/Jabitac? and Congo-Cruzeiro do Nordeste shear zones reach depths greater than to 6-16 km. The aeromagnetic signature of other shear zones, like the Juru one, suggests that these structures correspond to shallower crustal features. The satellite images (Landsat 7 ETM+) and aerogamaspectrometric images discriminate different geological units, contributing to the mapping of the structural framework of the region. The Serra do Caboclo Shear Zone was characterized as the boundary/suture between the TPAB and TAP. This structure is an outstanding, pervasive feature that separates contrasting geological units, such as the Neoproterozoic III Cachoeirinha Group in the TPAB and the Riacho Gravat? Complex and the Cariris Velhos metaplutonics, of Stenian-Tonian age, in the TAP. Occupying different blocks, these units are not found in authoctonous relations, like unconformities and intrusive contacts. Concerning the Cariris Velhos (ca. 1,0 Ga old) event is recorded by radiometric ages of the Riacho Gravat? Complex metavolcanics and intrusive augen and orthogneisses, all of them displaying geochemical affinities of arc or collisional settings. A structural signature of this event was not recorded in the region, possibly due to its low grade/low strain style, obliterated by the overprinting of younger, higher grade/high strain Brasiliano-age fabrics.The first tectonic event (D1) observed in the Cariris Velhos lithotypes presents contractional kinematics with transport to the NW. Neoproterozoic III geochronologic dates, obtained in late-D1 granitoids, imply a Brasiliano age (ca. 610-600 Ma) for this deformation event. The second tectonic event (D2) characterized in the region corresponds to the Brasiliano transcurrent kinematics of the outstanding shear zones and associated granitoid plutons. The geochronological (U-Pb in zircon) data obtained during this thesis also confirms the occurrence of the Cariris Velhos magmatic suite in the TAP, as well as the Neoproterozoic III age to the Cachoeirinha Group in the TPAB. The TAP (Riacho Gravat? Complex, augen and orthogneisses) is interpreted as a continental arc possibly accreted to a microcontinent during the Cariris Velhos (Stenian-Tonian) event. Later on, this terrane collided with the TPAB at the beginning of the Brasiliano orogeny (D1 contractional deformation), and both domins were reworked by the transcurrent shear deformation of the D2 event / A presente tese procurou avan?ar no conhecimento geol?gico da regi?o que abrange os terrenos Pianc?-Alto Br?gida (TPAB) e Alto paje? (TAP) , no Dom?nio da Zona Transversal (Prov?ncia Borborema, NE do Brasil), com o intuito principal de compreender a evolu??o geodin?mica e o condicionamento estrutural destas unidades. Para atingir este objetivo, al?m do trabalho de campo e da interpreta??o de fotografias a?reas tradicionais, foram utilizados outros produtos de sensoriamento remoto (imagens Landsat 7 ETM+, aeroradiom?tricas, aeromagn?ticas e topogr?ficas), an?lises litogeoqu?micas (rocha total) e data??es geocronol?gicas (U-Pb em zirc?o), al?m da integra??o com dados da literatura. Na regi?o afloram v?rias unidades geol?gicas precambrianas, representadas no T AP pelos complexos paleoproteroz?icos de Serra Talhada e Afogados da Ingazeira, Complexo Riacho Gravat? (seq??ncia metavulcanossedimentar de idade Esteniana-Toniana) e ortognaisses Cariris Velhos (Tonianos). No TPAB ocorrem as forma??es Santana do Garrote (unidade inferior) e Serra do Olho d'?gua (unidade superior) do Grupo Cachoeirinha (Neoproteroz?ico III), al?m dos ortognaisses de Pianc? e paragnaisses de Bom Jesus, estes dois ?ltimos podendo constituir um bloco mais antigo (embasamento ?) e um equivalente de alto grau do Grupo Cachoeirinha (ou Grupo Serid? ?), respectivamente. Em ambos os terrenos ainda ocorrem v?rios corpos degranit?ides brasilianos. Os dados aeromagn?ticos permitiram estimar a continuidade, em profundidade, das principais zonas de cisalhamento cartografadas na regi?o. As zonas de cisalhamento de Patos, Pernambuco, Boqueir?o dos Cochos, Serra do Caboclo, Afogados da Ingazeira/Jabitac? e Congo-Cruzeiro do Nordeste atingem profundidades . superiores a 6-16 km. A assinatura aeromagn?tica de outras zonas de cisalhamento, tais como a de Juru, sugere que tais estruturas correspondem a fei??es crustais mais rasas. As imagens de sat?lite (Landsat 7 ETM+) e aerogamaespectrom?tricas permitiram individualizar unidades geol?gicas distintas, bem como esbo?ar a trama estrutural da regi?o.A Zona de Cisalhamento Serra do Caboclo foi caracterizada como o limite/sutura entre o TPAB e TAP, tendo em vista ser uma estrutura marcante/penetrativa que separa unidades geol?gicas contrastantes, como o Grupo Cachoeirinha (Neoproteroz?ico III) no TPAB e o Complexo Riacho Gravat? (Esteniano-Toniano) e as metaplut?nicas Cariris Velhos, do TAP. Embora mais jovem, o Grupo Cachoeirinha n?o exibe contatos em n?o conformidade sobre o Complexo Riacho Gravat? ou ortognaisses Cariris Velhos, indicando que aquelas unidades estavam distanciadas quando da sua deposi??o. Com rela??o ao evento Cariris Velhos (ca. 1,0 Ga), a presen?a do mesmo ? indicada pelas metavulc?nicas do Complexo Riacho Gravat?, augen gnaisses e ortognaisses intrusivos, todos com afinidade geoqu?mica de contextos de arco ou colisional. Todavia, o registro estrutural associado a este evento n?o foi identificado, o que foi interpretado em fun??o de sua oblitera??o (constitu?am estruturas de baixo grau/baixo strain) pelos eventos subseq?entes. O primeiro evento tect?nico (01) observado nos litotipos de idade Cariris Velhos apresenta cinem?tica contracional com transporte para NW. Uma data??o do Neoproteroz?ico III, obtida em granit?ide tardi-D1, permite atribuir uma idade do in?cio do brasiliano para este eventodeformacional. O segundo evento (D2) caracterizado na regi?o corresponde ? tect?nica transcorrente Brasiliana, a qual ? materializada por marcantes zonas de cisalhamento e corpos gran?ticos associados. Os dados geocronol?gicos obtidos (U-Pb em zirc?o) confirmaram a presen?a do magmatismo Cariris Velhos no ?mbito do TAP, bem como a idade Neoproteroz?ica III para o Grupo Cachoeinha (TPAB) e para o evento tect?nico D1. O TAP (Complexo Riacho Gravat?, augen gnaisses e ortognaisses) deve constituir um arco continental (provavelmente acrescido a um microcontinente) formado durante o evento Cariris Velhos (Esteniano-Toniano). Este terreno colidiu com o TPAB no inicio da orog?nese brasiliana (deforma??o tangencial D1), sendo ambos os blocos afetados por retrabalhamento/cisalhamentos transcorrentes (evento D2) at? o final do Ciclo Brasiliano