Brusque Transect From Atlantic Coast to Bolivian Border, Southern Brazil

Mantovani, Marta Sílvia Maria; Vasconcellos, A. C. B. C.; Shukowsky, Wladimir; Milani, Édison J.; Basel, M. A. S.; Hurter, Suzanne; Freitas, Sílvio Rogério Correia de

doi:10.1029/gt004

Cited by 5 publications

(7 citation statements)

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“…7), enquanto as feições regionais permaneceram semelhantes àquelas apresen- Figure 6 -Relief on the Moho (depth in km), given the topographic load shown in figure 5, an effective elastic lithospheric thickness of 20 km, and an original Moho at 35 km. Edge effects do not affect the study área tadas em estudos anteriores (Mantovani et al 1989, Shukowsky et al 1991, Ussami et al 1993.…”

Section: Figura 5 -Topografia (Contornos a Cada 200 M) Os Dados São mentioning

confidence: 89%

“…Essa anomalia não pode ser explicada apenas pelo volume dos diques, mas deve ser provavelmente associada a intrusões básicas profundas (como sugerido por Mantovani et al 1991e Ussami et al 1993; na área costeira de Florianópolis, observa-se um gradiente marcante, que não pode mais ser relacionado com o armamento crustal da margem continental, pois esse efeito foi compensado pela remoção das anomalias isostáticas.…”

Section: Figura 6 -Relevo Da Moho (Profundidade Em Km) Calculado Em unclassified

“…A proposta existência, ou não, do Cinturão Ribeira (a nordeste do Complexo Luis Alves) no Escudo Sul-Rio-Grandense (Fragoso César 1991) e a continuação do Cinturão Dom Feliciano entre as duas áreas (Fragoso César 1980, Fragoso César et al 1987, Basei 1985 ainda estão em aberto. Interpretando dados gravimétricos, Shukowsky et al (1991) sugeriram a continuação do Cinturão Dom Feliciano e a continuidade entre o Complexo Luis Alves e o Craton Rio de La Plata, mas não aquela do Cinturão Ribeira, preferindo correlacionar as rochas ocidentais do Escudo Sul-Rio-Grandense com o Maciço de Curitiba. Neste trabalho, os dados gravimétricos são reavaliados em vista de (1) adição de mais de 800 novas estações gravimétricas medidas em 1992, (2) eliminação de anomalias devido ao relevo isostático na Moho, destacando-se as anomalias ligadas às estruturas crustais, (3) avaliação preliminar de dados magnetométricos e (4) estudos sobre a es- pessura litosférica efetiva da área meridional . Embora as interpretações de dados gravimétricos não sejam unívocas, podem ser utilizadas para discriminar modelos geológicos conflitantes, abundantes para essa região.…”

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“…GEOLOGIA REGIONAL O mapa geológico da margem costeira de parte dos Estados de São Paulo, Paraná e Santa Catarina (Fig. 2) foi compilado de Awdziesj et al (1986), Basei (1985), Basei et al (1991), Biondi et al (1989), Janasi & Ulbrich (1991 e Mantovani et al (1989Mantovani et al ( , 1991, e aquele das porções do Uruguai e do Rio Grande do Sul (Fig. 3) por Dália Salda et al (1988), Preciozzi et al (1980), Bossi e Campal (1991), Santos et al (1989), Fragoso César (1980, Fragoso César et al (1987) e Fernandes et al (1990Fernandes et al ( , 1992.…”

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Estrutura Do Escudo Sul-Brasileiro: Uma Revisão Através De Dados Gravimétricos E Magnetométricos

HALLINAN¹,

Mantovani²,

SHUKOWSKY³

et al. 1993

RBG

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STRUCTURE OF S-BRAZILIAN SHIELD: A REVISION FROM GRAVITY AND MAGNETIC DATA. New gravity data in southern Brazil are combined with previous data in Brazil and Uruguay, permitting detailed analysis of the basement structure. The Brasiliano cycle tectonic frameworks suggested by previous geological and geophysical studies are tested. Pre-Brasilianp structure (Transamazonian cycle), however, is an importam and hitherto unstated source of lateral density contrast responsible for distinctive gravity discontinuities. Gravity anomalies associated with Mesozoic magmatism are also discordant within the Brasiliano structure, and can also be distinguished by strong accompanying magnetic anomalies. Individual blocks within the Rio de La Plata craton are recognised and a new block, the Paso de los Toros Block, is defmed. The continuation of the Rio de La Plata Craton into Brazil is challenged. The possibly related pre-Brasiliano Nico Perez Terrane (strongly reworked during the Brasiliano) forms the basement to the Rio Grande do Sul Shield, at least to the west of the Pelotas Batholith. Residual isostatic gravity anomalies suggest the continuation of the Ribeira Belt from Paraná State to Rio Grande do Sul. The Curitiba Massif, however, does not. The Luis Alves Complex does continue at least partially towards the south, but its presence beneath the Rio Grande do Sul shield cannot be demonstrated by gravimetric data. The Internai Domain of the Santa Catarina part of the Dom Feliciano Belt can be traced to the Costeiro Granitoid Belt to the north, and is tentatively proposed to lie off the eastern seaboard in Rio Grande do Sul and Uruguay, but is no longer thought to correlate with the Pelotas Batholith. In this scenario, could the Brusque Group metasediments be linked to the Rocha Group?

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Section: Figura 5 -Topografia (Contornos a Cada 200 M) Os Dados São mentioning

confidence: 89%

Section: Figura 6 -Relevo Da Moho (Profundidade Em Km) Calculado Em unclassified

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Estrutura Do Escudo Sul-Brasileiro: Uma Revisão Através De Dados Gravimétricos E Magnetométricos

HALLINAN¹,

Mantovani²,

SHUKOWSKY³

et al. 1993

RBG

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“…Although in that region the basement is covered by thick sedimentary sequences, Mantovani et al (1991), relying on geophysical evidence, suggest that the volcanic field has been emplaced at the contact between the Rio de La Plata-Luis Alves craton and the Dom Feliciano Proterozoic mobile belt. K/Ar data indicate a Late Cretaceous age ranging from 68 Ma (Amaral et al 1967, Sonoki andGarda 1988) to 76 Ma (Gibson et al 1999).…”

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The Lages diatremes: mineral composition and petrological implications

Barabino

Gomes

Traversa

2007

An. Acad. Bras. Ciênc.

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Chemical data of heavy minerals from Lages diatremes in southern Brazil have been studied with the aim of characterizing the sample source(s). Three groups of minerals are recognized: I) aluminian-chromian pyroxene, pyrope garnet and chromian spinel, which represent disaggregated fragments of spinel, spinel+garnet and garnet facies peridotite; II) low-Cr aluminian pyroxene that occurs as megacrysts are high pressure phases (7-12 kb) being crystallized from an alkaline-like evolving magma; III) low-Cr aluminian diopside of crustal origin. Evidence of carbonatitic cryptic metasomatic enrichment is shown by clinopyroxenes of Groups I and II. The data do not support a kimberlitic affinity as it has been suggested for the diatremes. Rather, they are interpreted as vents related to the alkaline magmatism affecting the area in Late Cretaceous. The alkaline parental magma of the pyroxene megacrysts was generated from a metasomatized mantle at garnet facies that incorporated fragments of the surrounding still fertile mantle. Presumably at spinel-facies level the magma began to fractionate the megacrysts, whose crystallization proceeded over a large range of falling pressure and temperature. The chemical similarities between Group III clinopyroxenes and those from the differentiated lithotypes indicate that the magma carried this mineral phase on its evolution, at crustal conditions, towards a more evolved alkaline composition. Still, a non-cognate origin for the Group III clinopyroxenes cannot be discarded.

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