Bacia Sedimentares brasileira - BRITO NEVES 2002

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Gondwana Research, 1.! 5, No. I , pp. 175-196. 
0 2002 International Association for Gondwana Research, Japan. 
ISSN: 1342-937X 
Main Stages of the Development of the Sedimentary Basins of 
South America and their Relationship with the Tectonics of 
Supercontinents 
Benjamim Bley de Brito Neves 
lnstituto de GeociFnczas-Universidade de SGo Paulo, Rua do Lago, 562.05508-900, SGo Paulo SP, Brazil, E-mail: bbleybn@usp.br 
(Maniusrript received December 20,2000; accrpted May 30,2003) 
Abstract 
Twelve main stages of sedimentary basms of the South American Platform have been identified as follows: one 
Neoarchean, seven Proterozoic and four Phanerozoic. Basin-forming tectonics are related to the accretionhsion and 
fission of the major continental landmasses of the Earth’s history, such as Atlantica, Nena, Rodinia, GondwandPannotia 
and Pangea. The first proposed stage of basin development precedes the formation of these major landmasses and was 
developed on Mesoarchean microcontinents. ‘The last stage succeeds the fission of Pangea and is still in progress. 
Key words: Supercontinent, fusion, fission, cratonic sequences, basin-forming tectonics. 
Introduction 
During specific stages in geological time continental 
masses drew close to each other, accreted and later 
separated, and today we are in an intermediate stage 
between the last accretion (Pangea) and the next future 
supercontinent. The South American platform contains 
sedimentary basins from the Neoarchaean to the present 
and is remarkable for the excellent preservation of the 
lithostratigraphic records of Paleoproterozoic and 
Mesoproterozoic basins. This paper analyses the 
approximately 12 major phases of sedimentary basin 
formation and deformational tectonics, as postulated by 
Kingston et al. (1983). Locations are shown in the index 
map (Fig. 1) and in the subsequent figures. 
Previous Work 
Studies of basin evolution have usually discussed 
paleogeography and tectonic development, but they are 
seldom related to the interaction of lithosphere plates on 
a global scale. Examples of good studies of the 
Precambrian are the works of Amaral (1974, 1984), 
Almeida and Hasui (1984), Costa and Hasui (1991) in 
the Amazonian region and Dominguez (1993, 1996) in 
the S5o Francisco cratonic region of central-eastern Brazil. 
For the Phanerozoic, the studies have leaned mostly towards 
the concept of sedimentary sequences (Almeida, 1967, 
1969; Soares et al., 1974, 1978; Sloss, 1988; Almeida et 
al., 2000). Most of these early studies were based on Rb/ 
Sr and WAr data, and they suffered from the lack of 
adequate geochronological information. Many correlations 
of Precambrian sequences now require extensive revision 
in the light of new data obtained by those more advanced 
methods (U/Pb and Pb/Pb in zircons, etc.). 
For the Phanerozoic there exists an impressive amount 
of data of a multi-disciplinary nature that has been 
objectively used in the more recent syntheses. The original 
sketches ofAlmeida (1969) and Soares et al. (1974,1978) 
were confirmed in essence and improved. Recent 
syntheses were published by Milani and Zalan (1999) for 
the large basins of the continental interior (‘IS’ or 
syneclises, Kingston et al., 1983) and by Cainelli and 
Mohriak (1999) for the coastal basins. 
For the evolution of continental masses, classical works 
include those by Gower et al. (1990), Sengor (1990), 
Hoffman (1991), Rogers (1996), Unrug (1996), Dalziel 
(1997) and others. 
Some Pr- and Necessary Observations 
The South American platform can be divided into the 
pre-Brasiliano Northern and Northwestern area (11, and 
Gondwana 
Research 
176 B.B. BRIT0 NEVES 
80"W 
- 40"s \ - 'a h l 6 0 " W 40"w Pata onia I I 
Fig. 1. General situation index map. Main of geographic features of South America. The main Brasiliano cratonic domains are shown in light gray: 
N-NW-Amazonian, N-NE-S. Luis, E-S. Francisco, SE-Lds Alves, S-Rio de La Plata. 
the Brasiliano Central and Central-Eastern area (2). The 
Brasiliano Orogenic Cycle (present in area 2) is as 
significant to South America as the Hercynian to Eurasia 
and the middle Paleoproterozoic orogenic cycles to North 
America. Brasiliano areas include Archaean, Paleoproterozoic 
and Mesoproterozoic rocks that have been variably 
reworked from moderate to deep levels, and the effects 
of previous events are masked in many areas. 
Pre-Brasiliano structures are the cratonic nuclei of the 
Brasiliano network. In their interior they show well- 
preserved lithostructural evidence of older orogenic cycles, 
although they contain local structures and isotope data 
caused by Brasiliano events. These nuclei preserve several 
Proterozoic basins, many of which have been partially 
transformed into mobile belts, whereas some others show 
only gentle to moderate deformation. 
Gondwana Research, V 5, No. 2,2002 
SEDIMENTARY BASINS OF SOUTH AMERICA IN RELATION TO SUPERCONTINENTS 177 
The best information about sedimentation and tectonics 
is generally available from the central-eastern region of 
the continent in the Sao Francisco Craton and adjacent 
areas. In the Amazonian region, Proterozoic sequences 
are known only at reconnaissance scale, although these 
pre-Brasiliano rocks cover a large area of the northern 
part of the continent. Especially in this Amazonian region 
there is a notable trend of Precambrian younging of the 
basement units, cover sequences and Proterozoic 
anorogenic granitic plutonism (1.88 Ga to 0.99 Ga) from 
northeast to the southwest (Brito Neves et al., 1984). 
Pre-Atlantica Stages 1 and 2 (Older than 
2.0 Ga) 
Neoarchaean Aguas CZaras basin (stage I) 
Formation and coalescence of microcontinental cells 
started at about 3.5 Ga, increasing in number and size 
and covering a large area of South America by the end of 
the Neoarchaean. This maximum of terrane formation 
and dockage at ca. 2.75 Ga is known as the 'Jequie Cycle' 
in Bahia and/or the 'Rio da Velhas Event' in Minas Gerais. 
During these early processes of lithosphere plate 
interaction, sedimentary basins developed in settings such 
51ow 
as fore arc, back arc and post-orqgenic collapse, all of 
which are today represented by Low-Grade Terranes (LGT) 
of the greenstone-belt type. 
Most of these areas are highly deformed basement older 
than sedimentary cover, but one relatively undeformed 
unit is still preserved in the central part of the Serra dos 
Carajas (southeastern Amazonia) (Fig. 2). This Bacia de 
Aguas Claras Formation consists of up to 1500 m of 
siliciclastic rocks that developed on a marine platform 
grading to littoral and fluvial deposits (Nogueira et al., 
1995). They rest discordantly on the Archaean Gr2o Par6 
and Igarapk Ipojuca Groups in horst-graben structures in 
the interior of a positive flower structure of the major 
regional shear zones. The lower member of this unit 
contains mostly pelitic beds (including manganese ores), 
siltstone and fine-grained sandstone units interpreted as 
having been deposited on a marine platform. The upper 
member consists of fine-grained and coarse-grained 
sandstone of intertidal and fluvial (braided) origin with 
well-developed facies variations (Nogueira et al., 1995). 
From field relationships and isotope data, Mougeot et al. 
(1992) suggested that this basin was older than 2700 Ma, 
making it the oldest well preserved sedimentary sequence 
deposited under stable conditions on the South American 
Platform. 
50"W 
50"W 
Fig. 2. The Aguas Claras Formation in the interior of Serra do Carajis Range. It corresponds to Stage 1 as the oldest (Archaean) sedimentary basin 
of South America. From Nogueira et al. (1995). 
Gondwana Research, V. 5, No. 1,2002 
178 B.B. BRIT0 NEVES 
Paleoproterozoic basins (stage 2) 
Development of sedimentary basins acceleratedfollowing the coalescence of the Neoarchaean 
microcontinental cells. Their stratigraphic position and 
zircon-bearing clasts dated at 2.15 Ga in some of the 
uppermost lithostratigraphic units show that they both 
preceded and followed global orogenic events, principally 
the Siderian (2.5-2.3 Ga), Rhyacian (2.3-2.05 Ga) and 
Orosirian (2.05-1.8 Ga). These basins developed during 
the first major continental (or supercontinental) collages, 
for example the Atlantica Supercontinent of Rogers 
(1996). 
Basins developed during this stage contain a 
predominance of fluvial siliciclastic shallow marine 
deposits with minor volcanism, with clasts derived 
from Archaean greenstone belt sequences, plutons and 
magmatic arcs. They also contain banded iron formation, 
carbonate beds, jaspilite associated with Fe-Mn and gold- 
and uranium-bearing conglomerate with occurrences of 
detrital pyrite. At Jacobina (central Bahia), the 
sedimentary pile attains a preserved thickness of 5000 m 
of very mature sediments. This continued deposition 
under stable shelf conditions coexisted side by side with 
distinct development of basins more typical of the 
Archean, such as volcano-sedimentary basins with 
‘greenstone belt’ suites (Serrinha in Bahia, Barama- 
Mazaruni/Vila Nova in the northeast of Amazonia, etc.). 
Only locally can it be shown that these platform basins 
discordantly overlie the Paleoproterozoic greenstone belt 
sequences (North Guyana Trough, the Orapu-Bonidoro 
Group, discordant over the Barama Mazaruni; Ledru 
et al., 1994). 
The tectonic environments of these basins varied from 
passive continental margin type (Minas Group, Marginal 
Syneclise, ‘MS’), foreland zones (Northern Guyana, 
Francevillian), interior rifts (Jacobina, Interior Fracture, 
‘IF’), continental interior syneclises (Colomi, ‘IS’), rifts 
developed over rising mantle plumes (Upper Contendas 
sequence) and pull-apart basins, etc. (A syneclise is a 
broad basin of deposition; ‘MS’, ‘IF’ and related terms are 
from the classification of Kingston et al., 1983.) The 
deformational tectonics also varied widely but were nearly 
always subsidiary to the accretionary, collisional, and 
transpressive orogens that led to continental assembly at 
the end of the Paleoproterozoic and were responsible for 
the general arrangement of the Atlantica Supercontinent. 
Deformation of the basins is generally very intense and 
locally consists of refolding and tectonic imbrication with 
the subjacent rock units (Archaean magmatic arcs and 
greenstone belts). Only very rarely was the deformation 
moderate and the general features of Proterozoic basins 
preserved. 
The Formation of Atlantica Supercontinent 
and Subsequent Processes (Prelude to 
Stage 3) 
The continental mass Atlantica consisted of blocks that 
now occur in South America and Africa (Ledru et al., 1994; 
Rogers, 1996). I t formed gradually during several 
Paleoproterozoic orogenic stages (2.35 Ga, 2.2-2.15 Ga, 
2.0 Ga, 1.95-1.80 Ga). 
The first event following accretion was widespread 
silicic magmatism and minor sediments of the Uatumii 
Group. Magmatism of the Uatumg Group (Supergroup, 
Association, etc.) is found in practically all countries in 
the northern part of the continent over an area 
> 1,500,000 km2 from eastern Colombia to Suriname. It 
consisted mostly of felsic volcanic rocks (Iricoum6- 
Surumu-Iriri, Cuchivero, Burro-Burro, Kuyuwini, etc.) and 
associated granitoid plutons. The Uatumii flows and 
pyroclastic rocks range from trachyte to andesite with 
minor basalt and show both calc-alkaline and alkaline 
trends. Pyroclastic rocks include tuff, breccia and 
agglomerate, ignimbrite, tuffaceous sandstone beds, 
microbreccia etc. 
The Uatumii event occurred during the Orosirian 
orogenies that affected most of the world (but with few 
representatives from South America). Their rock units 
are generally older than 1.8 Ga, with dates mostly between 
1.97 and 1.85 Ga (Tassinari and Macambira, 1999). They 
succeeded important orogenic events from 2.2 to 2.0 Ga 
(Maroni-Itacaiunas/Transamazonian) and were nearly 
coeval with orogenic protesses in the Ventuari-Tapaj6s Belt 
that completed the formation of Atlantica (Tassinari and 
Macambira, 1999). They occurred mostly in old and thick 
Archaean basement inliers that form the Pakaraima block 
(north of the Amazonas River) and the Xingu block (to 
the south, in the Xingu River, see Figs. 1, 3 and 4). 
The Uatumii Event shows a close relationship (‘the day 
after’) to the formation of the Atlantica Supercontinent 
and is an important precursor to the subsequent tectono- 
sedimentary development of the Amazonian block in Late 
Paleoproterozoic times (stage 3). It may have resulted 
from sublithosphere events (activated mantle, 
underplating, plumes, etc.) or passive events (activated 
lithosphere) related to plate interaction elsewhere. The 
former may have occurred as a consequence of thickening 
and crustal growth associated with the oldest (Maroni- 
Itacaiunas) Paleoproterozoic orogenic events. The latter 
may be attributed to accretionary orogeny in adjacent 
regions, as exemplified by the rocks of the Ventuari-Tapaj6s 
region that occur along a NNW-SSE-trending belt about 
2200 km long in the central-western part of the Central 
Amazonian Block. A phase of extensional tectonics 
Gondwana Research, V. 5, No. 1,2002 
SEDIMENTARY BASINS OF SOUTH AMERICA IN RELATION TO SUPERCONTINENTS 179 
associated with these events was suggested by Montalviio 
and Bezerra (1980) and Costa et al. (1991), the latter 
estimating values up to 2.5 for the 'beta' factor for crustal 
extension. 
Late Paleoproterozoic and Mesoproterozoic 
(Stages 3 to 6) 
Roraima stage (Urupi-Gorotire-Beneficente, stage 3) 
The Uatumii Event was immediately followed by the 
development of intracratonic sedimentary basins with 
local thicknesses up to 3,000 m. They formed from the 
upper Orosirian (ca. 2.0 Ga) to the Statherian (ca. 1.8 
Ga) during thermal relaxation and isostatic adjustments 
continuing from Uatumii time. Reis and Carvalho (1996) 
estimated a minimum period of 100 Ma for the deposition 
of the whole sequence. On the Guyana Shield (Fig. 31, 
these sediments cover a nearly continuous area of about 
73,000 km2, with remnants in Venezuela (Neblina, Duida, 
Paru, Sipapo, Roraima), Amazonas (Ufaranda, Surucucus, 
68' 64" 
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Tepequem, Urutamin, UrupVPittinga, etc.) and Suriname 
(Tafelberg). On the Central Brazil Shield, equivalent 
sediments are erosional remnants of a former basin in 
the Rio Xingu area as well as in the Alto Tapajos Basin 
(Teles Pires-Juruena and Aripuang rivers; Fig. 4). 
Deposits consist mainly of continental clastic rocks, 
subordinate shallow marine sediments and some volcanic 
rocks at a few stratigraphic levels. Sediments overlie the 
Uatum5 volcanics and contain Uatumii clasts both at the 
base and at several other stratigraphic levels. Basic intrusive 
rocks (Avanavero/Pedras, Pretas/Crepori) commonly formed 
at the end of sedimentation, indicating the beginning of 
new tectonics of the Statherian period (stage 4). 
The Roraima Supergroup is one of the best known suites 
and probably formed in several different basins (Reis and 
Carvalho, 1996). The main areas of exposure contain a 
sequence of continental clastic sediments (Arai Fm.) that 
were followed by two transgressive-regressive episodes 
(Suapi Group), passing upward to shallow marine 
sediments with some continental volcanic rocks, and 
terminated by continental and intertidal deposits. 
60' 56' 
Amazonas 
_ _ _ _ . .---- 
64" 60' 56" 
Fig. 3. Roraima (s.1) and Urupi occurrences in the Guyana Shield, north of the Amazonian Craton (light gray). In black is the Avanavero/Pedras 
Pretas Suite (Statherian mafic magmatism). After Reis and Carvalho (1996).Gondwana Research, V 5, No. 1,2002 
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Gondwana Research, K 5, No. 1,2002 
B.B. BRIT0 NEVES 
SEDIMENTARY BASINS OF SOUTH AMERICA IN RELATION TO SUPERCONTINENTS 181 
Both the Roraima Supergroup and other units of this 
tectonic stage formed during positive to moderate 
inversion of the preceding (Uatum6) extensional phase. 
Deposits formed in rifts (local fault zones), syneclises 
(open folds) and horizontal tablelands (‘dalas’, Montalvgo 
and Bezerra, 1980). Deformation occurred only along 
linear fault zones that delimit the blocks and contain 
cataclastic rocks. No compressional shortening occurred 
even where intrusive rocks cut or are adjacent to the 
sediments. These intrusions are Statherian or younger 
and consist of granitic, basic, and alkaline rocks formed 
mainly in an anorogenic environment with the exception 
of a few orogenic intrusives on the easternmost margin 
of the Rio Negro-Juruena Belt. 
Accentuated dips in some areas developed in the upper 
middle part of the Mesoproterozoic, during the so-called 
‘K mudku Episode’ (‘Nickerian’ or ‘Orinoquense’) . This 
deformation may have been caused by 1.3-1.1-Ga 
Grenville orogenies (sensu lato) in the southwestern 
region of Amazonia. According to Fraga et al. (1994) 
this late tectonic activity (with E-W to WNW-ESE trends) 
may locally have been strong enough to cause 
metamorphic foliation and lineation in the Roraima 
Supergroup and its substrate in addition to some tectonic 
imbrication south of the Roraima area. 
The stratigraphic succession, field relationships and 
tectonics of the Urupi Formation (Fig 3) are very similar 
to those of the Roraima Supergroup (Daoud and Fuck, 
1987). The Urupi Formation contains a larger amount of 
immature clastic sediments and pyroclastics than the 
Roraima Supergroup, and the unconformity with the 
underlying Uatum6 suite may represent a longer period 
of erosion. 
Rocks similar to the Urupi Formation occur farther 
south along the tributaries of the Xingu, Iriri and Tapaj6s 
rivers (Fig. 4), where tablelands of the Gorotire Group 
are exposed as remnants of box-folds. They consist of 
subaerial rocks in sequences less than 800 m thick that 
rest discordantly on Uatum6 and older suites. These 
sediments were formed mostly in unstable cratonic 
environments, and throughout the sequence they consist 
mainly of quartzo-feldspathic sandstone beds containing 
rock fragments, poorly sorted sandstones and abundant 
oligomictic and polymictic conglomerates. Shale and fine- 
grained clastic sediments are rare. The sediments are 
intruded by basic magmas of the Statherian Crepori 
Formation (‘Avanavero’ magmatism) and are locally 
overlain discordantly by sandstone beds of the 
Cubencranquem Formation. 
The Beneficiente Group (Fig. 4) in the Alto Tapajos 
Basin (Juruena and Teles Pires rivers) is considered to be 
the stratigraphic and structural equivalent of the Gorotire 
Group although it contains a thicker marine sequence 
(Schobbenhaus et al., 1984). It consists of white quartz- 
sandstone and light-grey to dark-grey siltstone, with minor 
beds of argillite, limestone and dolomite in a section more 
than 750 m thick. It occurs along a NNW-SSE trend, 
parallel to the Rio Negro-Juruena accretionary system and 
may have been deposited in an extensional back-arc basin 
(Tassinari and Macambira, 1999). The basin is outlined 
by fault lines and contains domal structures resulting from 
the emplacement of granite and alkaline plutons in the 
Upper Proterozoic and Mesoproterozoic. The Beneficiente 
Group is overlain locally by Upper Paleozoic sedimentary 
remnants (reason for the name ‘Alto Tapajos Basin’). 
Taken as a whole, rocks of this stage represent 
a widespread first stage of sedimentary and 
volcanosedimentary covers of Atlantica, well recorded in 
this part of the Amazonian pre-Brasiliano domain. It 
continued into, and may have overlapped, deposition of 
similar suites in other regions of Atlantica. 
Statherian Taphrogenesis (Pre-Nena), fission of Atlantica 
(stage 4) 
Ubiquitous Statherian taphrogenesis (1.8-1.6 Ga; Brito 
Neves et al., 1995a; Magini et al., 1999) followed the 
fission of Atlantica and preceded the formation of NENA 
(Northern Europe-North America supercontinent; Gower 
et al., 1990). It is particularly well recorded in South 
America and represents a transition from accumulation 
of Roraima-type sediments in platforms and extensional 
troughs to the development of younger Mesoproterozoic 
basins. It delimited, and was responsible for, development 
of most of the Mesoproterozoic basins, and by fracturing 
the Archean and Paleoproterozoic basement it set the lines 
along which the Neoproterozoic cratons and mobile belts 
subsequently developed. 
Statherian extension is well shown by magmatism. 
Mafic intrusives (dyke swarms and sills) occur from 
northern Venezuela (Avanavero, Roraima Intrusive Suite, 
Crepori, Pedra Preta) southward to northern Uruguay 
(Florida) and Argentina (Tandil) and westward from 
Atlantic coastal areas (Salvador, Rio Pardo) to the interior 
of Bolivia (Fig. 5, Fig. 6). It includes mafic-ultramafic 
bodies, anorogenic granite plutons (Amazonian region, 
Minas Gerais, Bahia, Rio de la Plata craton) and volcanic 
(trap) rocks. 
Although mostly extensional, Statherian activity 
included some local deformation of Roraima-age basins 
in the Amazonian region. It had an important role in basin- 
forming tectonics in the Amazonian region, in Bahia and 
Minas Gerais (Espinhaqo range), in the Borbsrema 
Province (Western Potiguar and Jaguaribeano fold belts) 
and in many other regions in South America and parts of 
Gondwana Research, V. 5, No. 1,2002 
182 B.B. BRIT0 NEVES 
Fig. 5. 'The Statherian Taphrogenesis in the South American continent, a general overview. The Statherian occurrences include mafic dyke-swarms, 
felsic volcanic traps, volcano-sedimentary rifts (and locally some rapakivi granites). See text. 
Africa and North America. Some Statherian and slightly 
younger supracrustal rocks were later folded in the 
Mesoproterozoic and Neoproterozoic (Mantiqueira 
Setentrional and Central, Jaguaribeano, Eastern 
Tocantins, etc.), where they occur in the interior of the 
Brasiliano mobile belts (underling Neoproterozoic rock 
units). 
Accretionary orogenic processes may have been 
synchronous with Statherian extension in the Rio Negro- 
Juruena belt (westwards of the Alto Tapajos Basin), in 
the Jauru area (Mato Grosso, southwestern Amazonia), 
and other areas. Some mafic rocks in the Espinhaqo range 
(Serro, Minas Gerais) may be remnants of a Statherian 
oceanic crust. 
Post-Nena Mesoproterozoic basins. (stage 5). 
Poorly known lower to middle parts of Mesoproterozoic 
basins containintracratonic clastic and locally 
volcanoclastic sequences that overlie the areas affected 
by Statherian extension and orogeny in the northern part 
of South America, the southern part of North America 
and Fennoscandia. In the central-eastern part of South 
America they occur in Statherian rifts locally expanded 
to form syneclises (GoiAs-Tocantins, Arai and Natividade 
groups) and in Bahia and Minas Gerais (Espinhaqo, 
Chapada Diamantina) (see Fig. 6). A well preserved 
lithostratigraphy shows increasing occurrence of 
epicontinental marine invasions upward in the sequences. 
Gondwana Research, V. 5, No. 1,2002 
SEDIMENTARY BASINS OF SOUTH AMERICA IN RELATION TO SUPERCONTINENTS 183 
0 150 300km - 
Fig. 6. Paleoproterozoic (to 
Mesoproterozoic) rifts in 
the central-eastern part 
of Brazil. The outline of 
the S6o Francisco 
Craton (Neoproterozoic 
in age) is shown only for 
reference. 
Exact ages can only be inferred but are probably in the 
time interval 1.6/1.55 Ga to > 1.2 Ga. In Amazonia (Fig. 
4) the centers of subsidence and sedimentation migrated 
progressively westward (west of Alto Tapaj6s Basin) 
toward domains of younger thermal age (1.8-1.6 Ga) in 
the Rio Negro-Juruena orogen. 
Local volcanoclastic rocks and sub-greywacke contain 
fragments of volcanic rocks and chert. At least two zones 
of alkaline basalt (Arinos Formation) are intercalated with 
arkosic sandstone in the Caiabis Graben. Gabbro and 
diabase intrusions have poorly defined WAr ages of 1.4 
Ga (lowest level) and 1.2 Ga (Ectasian age). In the WNW- 
Central-western region of Amazonia 
Mesoproterozoic deposits in the central and western 
part of Amazonia (Fig. 4) extend from the right margin 
of the Rio Madeira, along the upper course of the Rio 
Juruena (tablelands of Dardanelos and Caiabis) through 
the northern part of the Amazonas Basin to the confluence 
of the Branco river with the Negro river. They display a 
NNW-SSE trend following the Rio Negro-Juruena 
accretionary belt that forms the regional basement 
Sections thicker than 1000 m occur in the Prosperanqa/ 
Acari and Prainha units (Caputo, 1971). 
On the Caiabis and Dardanelos tablelands, clastic 
sediments are mainly arkosic, medium to coarse-grained, 
and micaceous, with thin beds of polymictic conglomerate. 
ESE-striking Juruena-Teles Pires structural high, 
preliminary Rb/Sr data suggest that small subcircular 
intrusives of alkali-syenite, trachyte, and quartz-syenite 
(Canamg) are the same age. 
The eastern part of the Amazonian region contains 
erosional remnants of the Cubencranqukm Group in box 
folds along the upper courses of the Iriri and Xingu rivers 
(Fig. 4). Sequences are not more than 300 m thick over a 
wide area underlain by older sedimentary cover, volcanic 
traps and high-grade rocks of the regional basement. 
At one place the Cubencranqugm sequence overlies a 
1.64-Ga anorogenic granite, and the basal unit consists 
of beds of polymictic conglomerate with pebbles of 
Uatumii volcanic rocks and sandstone (possibly Gorotire). 
Most of the rocks are reddish arkosic sandstones with 
Gondwana Research, V. 5, No. 2,2002 
184 B.B. BRIT0 NEVES 
immature medium-grained sediments intercalated with 
siltstone and subordinate argillite. Some lithic greywacke, 
volcanic breccia and ash-tuff occurs in the middle part of 
the sequence. The open folds of the Cubencranqukm are 
discordant with the deformed Gorotire suite beneath it. 
The Prosperanqa-Acari Formation crosses the Amazonas 
River along an inverted Proterozoic syneclise that evolved 
into the Paleozoic Purus Arch (see also Fig. 11) between 
the Solim6es and Mkdio Amazonas basins. The deposits 
lie discordantly over the sedimentary and volcanic 
sequences of the previous stages (Caputo, 1971). The 
Prosperanqa suite consists mostly of brown to reddish beds 
of micaceous, medium to fine-grained, arkosic sandstone 
with clay fragments that are massive or display 
crossbedding or parallel stratification. Subordinate beds 
are siltstone, shale and oligomictic conglomerate with 
pebbles of quartzite and rhyolite. Prosperanqa sediments 
grade upward to fine-grained clastic units, calcareous 
siltstones and carbonate of the Acari Formation. deposited 
in fluvial (braided) to coastal marine environments. Some 
beds were intruded by the Bacaba Diabase (1290 Ma; 
Teixeira, 1983) during the Ectasian (Iwanuch, 1999), but 
some of the diabase is Upper Paleozoic 
The complete extent of Mesoproterozoic sedimentation 
and volcanism is unclear. Mesoproterozoic (Caliminian, 
Ectasian) suites are well preserved only on the interior of 
lithosphere segments that acted as cratonic domains 
during the Brasiliano, and they are commonly deformed 
within the Neoproterozoic Brasiliano belts. Thus it is 
possible that Mesoproterozoic suites extended farther to 
WESTERN ----.--------(- 
MARGINAL ZONE 
the west in Rondonia and Mato Grosso, where several 
rock units were involved in the Guapork and Aguapei 
orogenies. Sedimentation may also have occurred farther 
to the south, covered by the large Cenozoic sedimentary 
basin of the upper course of the Juruena river (Fig. 4). In 
central Brazil, west of the large mafic-ultramafic massifs 
of GoiAs-Tocantins, there is evidence for rifting informally 
referred to as the Ectasian taphrogenesis (preliminary 
studies by Correia and Pinho, 2000). Also, farther to the 
south and southeast, Ectasian volcano-sedimentary rocks 
have been reported in the central part of the Mantiqueira 
Province (Juliani et al., 2000), which is now in the interior 
of a Brasiliano fold belt. 
Bahia and Minas Gerais 
Mesoproterozoic basins in Bahia and Minas Gerais 
contain well exposed sequences generally thicker than 
3000 m that cover an area of 150,000 km (Fig. 6). They 
follow Statherian tectonic trends (and lithostratigraphic 
precursors) and are best exposed in Brasiliano cratonic 
domains. The oldest sediments are Caliminian, but no 
dates are available for end of sedimentation. Rock 
assemblages grade upward from eolian and fluvial 
sediments, through transitional environments (Paraguaqu, 
Galho do Miguel groups), to carbonate shelf and tidal 
deposits (Dominguez, 1993; Martins-Neto, 1998). The 
basins connected with the sea and show periodic 
incursions of fluvial sediments in incised valleys and 
estuarine deposits (Chapada Diamantina/Gentio and 
Conselheiro Mata groups). The sediments also connect 
CENTRALZONE + t-------. EASTERN 
MARGINAL ZONE 
@ 
Fig. 7. Cross-section of the Aguapei aulacogen, Brazil and Bolivia. After Saes (1999) 
Gondwana Research, V. 5, No. 1,2002 
SEDIMENTARY BASINS OF SOUTH AMERICA IN RELATION TO SUPERCONTINENTS 185 
in the subsurface with basins in Goias (Romero Silva and 
Zalhn, 2000). Suites in Bahia show a moderate degree of 
deformation by convergence of the basement blocks 
(‘oroaulacogen’), which caused development of N-S axial 
plane foliation in pelite beds, but it is not known whether 
this is an overprint of older deformation (‘Espinhaqo 
Orogeny’) or a consequence of the Brasiliano cycle. 
Pre-Rodinia Stage (Stage 6) 
Westward growth of the Amazonian Block and the 
development of Proterozoic cover left a well-preserved 
record along the Brazil-Bolivia border (Figs. 7 and 8). 
Rifts developed during the lowest part of the Stenian (1.20 
to 1.1 Ga) over the Proterozoic orogenic belts, which were 
divided by Van Schmus et al. (1998) into the Jauru, 
Araputanga, Cabacal belts (ca. 1.75 Ga), Santa Helena 
90 
13‘ 
65‘ 
belt (ca. 1.45 Ga) and Santo Ignacio belt (ca. 1.36 Ga). 
Greater extension in the north created an oceanic basin 
(Nova BrasilAndia-Guapore; Scandolara, 1999; Fig. 8). 
Although most suites were deformed during the upper 
part of the Stenian (Sunsas-Grenville), a few scattered 
areas in the southwestern part.of theAmazon region were 
only moderately folded. 
In Rondonia a continental margin developed after the 
rift stage, evolving to open-ocean deposition of terrigenous 
psammo-pelitic turbidite beds with subordinate plutonic 
and volcanic tholeiitic rocks. Subsequent transpression 
of these rocks at ca. 1.15-1.0 Ga developed the Guapore 
fold belt containing mesozonal metamorphites cut by 
intrusive rocks and discordantly covered by sediments of 
Stage 7 (Scandolara, 1999; Rizzotto et al., 1999). 
South of the Guapore mobile belt the Aguapei-Sunsas 
branching rifts (in Mato Grosso) showed variable rates of 
62’ 
Paleo-Mesozoic cover 
Meso-Neoproterozoic basins 
Younger granites of Rondonia 
Nova Brasilandia belt 
Undifferentiated basement 
SL = S%o LourenGo 
PN = Pacads Novos 
UP = Uopione 
I 100krn I 
Fig. 8. Guapork-Nova Brasildiidia fold 
belt (late Mesoproterozoic in 
age) and the system of rifts of 
Rondbnia, southwest Amazonian 
Craton. Modified after Scandolara 
and Amorim (1999). 
Gondwana Research, V. 5, No. 1,2002 
186 B.B. BRIT0 NEVES 
~ ~~~ 
extension insufficient to develop an ocean. Saes (1999) 
grouped sedimentation into three depositional phases in 
a deep central zone from S2o Vicente to Santo Corazon 
and two marginal shallow rift zones (Fig. 7). The rift 
phase consists of psammite and psephite deposited only 
in the depocenters. The subsequent syneclise phase 
covered the maximum area of subsidence with fine- 
grained clastic sediments deposited on coastal plains and 
low-energy shallow-marine environments. Fluvial and 
eolian sediments predominate in the uppermost phase of 
tectonic inversion. Deformation and greenschist-facies 
metamorphism is significant only in the central zones of 
tight folds and decreases toward external zones, which 
contain subhorizontal or gently folded suites that form 
tablelands. Local subhorizontal displacement of tabular 
quartzitic masses overlying the basement occurs in the 
southernmost part of the system of rifts. 
At present Stenian cover is well known only on the 
Amazonian Craton, but it may also include undated suites 
in central Brazil (Parano6 and similar units) and in the 
central-eastern region of Brazil (upper units of the 
Chapada Diamantina). It may also have been developed 
in the Borborema Province of northeastern Brazil, but any 
vestiges have been destroyed by the intense Cariris Velhos 
orogeny at ca. 0.96 Ga, which left rocks mainly at 
mesozonal levels, and by Neoproterozoic tectonic- 
magmatic events. 
Post-Rodinia Palmeiral Stage (Stage 7) 
Palmeiral deposits constitute the best record of 
sedimentation immediately after the incorporation of 
South American area in Rodinia. They may have been 
deposited in part of a very broad Mesoproterozoic/ 
Neoproterozoic syneclise formed by post-orogenic thermal 
contraction of the Guapor6 belt (Scandolara and Amorim, 
1999; Pedreira and Bahia, 2000). Their subsequent 
segmentation into rift-type compartments (inversion of 
regimes) may have been part of the worldwide ‘Tonian’ 
taphrogenetic event that led to the break-up of Rodinia. 
Generalized extension with adjustments along previous 
lines of structural weakness followed the Guaporb/Nova 
Brasilindia orogeny in the Neo-Estenian. It formed 
graben-like structures that now preserve erosional 
remnants of the formerly widespread Palmeiral Formation 
The Sao Lourenco Graben (Fig. 8) has oligomictic 
conglomerate near the base of the sequence but consists 
mostly of fine-grained orthoquartzitic to feldspathic 
sandstone beds with light colors, parallel lamination, and 
intercalations of siltstone and argillite. The sequence is 
similar in the Pacaas Novos Graben, with many more beds 
of arkosic sandstone and evidence of crossbedding. The 
Uopianes Graben contains immature sediments, with 
several conglomeratic zones intercalated with arkosic 
sandstone in addition to volcanoclastic rocks with ash- 
tuff and crystal-tuff. Smaller grabens in the surrounding 
areas contain similar sequences. A major part of this stage 
of sedimentation may be overlain by the sediments of the 
Solimdes Syneclise and/or by the ‘Dala Cisandina’ (the 
Cenozoic plains of the eastern side of the Andean Chain). 
Magmatism can be attributed to the same extensional 
regime at the end of the Mesoproterozoic and the 
beginning of the Neoproterozoic. Granitic suites studied 
by Bettencourt et al. (1999) include Santa Clara (ca. 
1081+ 50 Ma), Costa Marques and the Younger Granites 
of Rondonia (ca. 998-991 Ma). The Nova Floresta Suite 
(in Paca6s Novos graben, Fig. 8) of gabbro, troctolite and 
diabase intrudes the Palmeiral Formation plus alkaline 
basalt flows. There are some K-Ar ages from 1098 Ma to 
967 Ma for the diabases. 
Diachronic Dispersion (Fission) of Rodinia 
The break-up of Rodinia was responsible for the 
development of widespread Neoproterozoic sedimentary 
and volcanosedimentary domains, many of which have 
since been transformed into mobile belts. In South 
America it appears to have occurred in three phases 
between 1.1 Ga and 0.63 Ga. The first phase at the 
beginning of the Tonian (ca. 1050 to ca. 900 Ma) is shown 
mostly by basic magmatism (dyke swarms, basalt flows) 
in the Amazonian region (Nova Floresta and other areas), 
in the central eastern region of Brazil, along the Atlantic 
coast and sparsely in Africa. Granitic and alkaline 
anorogenic magmatism also occurred in western 
Amazonia. 
Subduction in the central-western region of Brazil 
(Mara Rosa Arc, ca. 930 Ma) and possibly in the south of 
Brazil (Passinho Event, ca. 850 Ma) are the oldest evidence 
for Neoproterozoic oceanic domains after the breakup of 
Rodinia and plate interactions, these being the first stages 
of the Brasiliano collage. 
The second phase of taphrogenesis in South America 
appears to have been widespread during the middle of 
the Neoproterozoic (ca. 800-700 Ma; early part of stage 
8). Local rifting varied from one province to another and 
ended with the formation of large continental and oceanic 
basins. This phase was initially accompanied by glaciation 
commonly correlated with worldwide Sturtian events, and 
a number of interior basins and rift basins have basal 
diamictite beds grading laterally to shelf (QPC = quartzite, 
pelite and carbonate) and turbidite sequences, as well as 
other units of deeper marine environments. This 
widespread phase of opening was contemporaneous with 
Gondwana Research, K 5, No. 1,2002 
SEDIMENTARY BASINS OF SOUTH AMERICA IN RELATION TO SUPERCONTINENTS 187 
Neoproterozoic oceanic and related environments 
A/D= RokelidelGoianides; B=Pharusian; C=Peri-franciscan 
E = Adamastor; F = Arabian-Nubian(ANEKT) 
Neoproterozoic continental lithospheric segments 
~ a (The sons of Rodinia) 
Areas with different geological problems 
(Sedimentary cover, deep crustal reworking, etc) 
convergence in other areas, such as the formation of arcs 
in southern Brazil (Mantiqueira Province) and collision 
in the central-western region of Brazil (Tocantins 
Province). 
The third phase of the break-up of Rodinia began in 
South America at the start of Neoproterozoic 111 (later 
part of stage 8; pre- to syn-Vendian; 640 to 620 Ma; 
Boggiani, 1997). The main stratigraphic records of this 
last phase are present in the Paraguai (base of the 
Fig. 9. Sketch diagram for the main 
Neoproterozoic oceanic basins (and 
connected realms) of western 
Gondwana (A, B, C, D, E, F). Main 
continental segments in gray: 
AM-Amazonian, SL-WA-S. Luis-West 
Africa, PR-Parnaiba, SFCKA-S. 
Francisco-Congo-Angola, KH-Kalahari, 
PP- Paranapanema, LA-Luis Alves, 
RP-Rio de la Plata, PA-Pampia; 
AA-Arequipa. 
Corumbd, Urucum, and Jacadigo groups) and Western 
Pampean belts (Puncoviscan rift). Varangerian glaciation 
is well preserved in the ParaguaiBelt (Puga and Jangada 
formations). This final phase was contemporaneous 
with the main phases of the Brasiliano/Pan-African 
orogeny, with the development of magmatic arcs and 
collisional belts in most of the structural provinces of South 
America (between 640 and 610 Ma). This synchrony 
shows that the break-up of one supercontinent (Rodinia) 
Gondzuana Reseauch, V. 5, No. 1,2002 
188 B.B. BRIT0 NEVES 
overlapped the amalgamation of another (Gondwand 
Pannotia). 
Dispersion in South America (and western part of 
Gondwana) created at least four main domains/systems 
that led to the development of continental margins and 
oceanic realms: the Goianides-Rokelides, Pharusian, 
circum-Siio Francisco-Congo and Adamastor (Fig. 9; Brito 
Neves et al., 1999). They formed a complex network of 
oceanic basins, gulfs and small oceanic basins, and they 
were connected by continental basins (rifts, rift systems 
and aulacogens). 
Pre-Gondwana-Pannotia Stage (Stage 8) 
The first (Tonian) phase of taphrogenesis during the 
breakup of Rodinia is known only (up to now) by the 
presence of magmatic rocks. The sediments formed during 
the succeeding two phases are described here as Stage 8. 
Events during initial accretion of Gondwana/Pannotia are 
discussed below as Stage 9. 
The second and third stages are here described in terms 
of four rock suites. They include: ‘QPC’- Quartzite, Pelite, 
carbonate; ‘BVAC’- Bimodal Volcanic Rocks, Arkose, 
Conglomerate; ‘Greenstones’ - tholeiitic volcanics 
predominating over sediments and ophiolitic remnants 
of oceanic environments (see ‘Proterozoic Rock 
Association’ in Condie, 1989) The fourth rock suite is 
formed by volcanic and plutonic suites of magmatic arcs. 
The QPC sequences are found along nearly all margins 
of large lithosphere segments formed by the break-up of 
Rodinia (Amazonia, Siio Francisco-Congo, West Africa, 
Paranapanema, Curitiba-Luis Alves, etc.; Fig. 9). These 
continental, coastal and shelf sequences can be described 
as ‘marginal’ or ‘proximal’ belts. They are commonly 
underlain by diarnictite, varvite and other glacial 
sediments deposited mainly, but not exclusively, in the 
Cryogenian Period (Sturtian). They occur in Marginal 
Syneclises (MS), on carbonate shelves, in aulacogens, and 
in large syneclises of the continental interior. The QPC 
sequences grade laterally to turbidite beds and deep-water 
sediments in several mobile belts, some of which include 
dismembered ophiolitic sequences. Lateral variations to 
BVAC suites have been interpreted as transitions to 
continental rift systems. The proportions of volcanic rocks 
and their composition (calc-alkaline, tholeiitic) are very 
variable, and their environments remain open to 
discussion. 
The glaciations that preceded the QPC sequences were 
widespread, and their erosion of the interior of the 
continental landmasses facilitated subsequent marine 
invasions after 750 Ma both in South America and Africa. 
In South America, these rock suites occur overlying the 
Amazonic craton (Alto Paraguai Group) and in the SZio 
Francisco Peninsula/craton (Siio Francisco Supergroup), 
and in the Rio de La Plata Block (Tandilia). In the S2o 
Francisco peninsula, the Neoproterozoic rocks were 
responsible for almost complete submersion, with only a 
few Paleoproterozoic and Mesoproterozoic basement 
islands exposed. In Africa these marine invasions are 
recorded in many basins, such as Taoudeni in West Africa, 
Lindian, West Congo, Damaran and Kundelungu in the 
southern part of the Congo Craton. 
Brasiliano distal basins contain only a poorly 
understood record of magmatic arcs and oceanic rocks, 
including submarine basalts, mid-ocean ridge volcanics 
and accretionary prisms. Fragments of oceanic suites are 
present in all structural Brasiliano provinces of South 
America, but no complete ophiolitic sequence has been 
found. Magmatic arcs began at ca. 930 Ma (Arenopolis/ 
Mara Rosa, Tocantins Province) and continued at later 
times during the Neoproterozoic and Cambrian (ca. 880 
Ma, ca. 750-700 Ma, 640-600 Ma, 580-550 Ma, 
533-520 Ma, 520-500 Ma.). 
Neoproterozoic deformation was responsible for the 
closure of oceanic basins and connected paleogeographic 
systems worldwide, reaching its climax in the accretion 
of Gondwana-Pannotia. In South America, the Brasiliano 
collage completed the assembly and divided the continent 
into two areas: 1) an area of pre-Brasiliano structures 
mainly in the northern-northwest of South America and 
along the Andean substrate and 2) an area containing 
four Brasiliano structural provinces in the eastern half of 
the continent (Almeida et al., 198l) , as previously 
mentioned. Brasiliano tectonogenesis was strong and 
widespread (affecting the fold belts and their basement) 
and these processes affected many areas so intensely that 
it is locally difficult to discriminate between Brasiliano 
and pre-Brasiliano terranes. Brasiliano processes were 
specifically most intense in basement (fold belts) with 
Mesoproterozoic thermal ages than in older rocks. 
Marginal belts with QPC sequences in both South 
America and Africa show decreasing structural 
deformation and degree of metamorphism toward the 
interior of the cratons. This process is well shown in the 
S2o Francisco Peninsula, where the stratigraphic suites 
and structures around the pear-shaped periphery of the 
craton show orthogonal trends in different segments. 
Late Brasiliano Transition (Stage 9) 
A wide variety of basin-forming tectonics occurred 
during late Brasiliano time from the north (NW of the 
State of Cear6) to Uruguay in the south. The interiors of 
Brasiliano belts contain intradeeps, successor basins and 
Gondwana Research, V. 5, No. 1, 2002 
SEDIMENTARY BASINS OF SOUTH AMERICA IN RELATION TO SUPERCONTINENTS 189 
"Transition stage" 
accu rren ce s 
Paran3 syneclise 
Dam Feliciano is)/ 
Ribeira belt (ld) 
LUIS Pdves 
cratonrc block 
Major faults 
MC 
1 
300 km 
Fig. 10a. Early Paleozoic basins/occurrences (late Brasiliano) of southern Brazil- Mantiqueira Province. MG - Minas Gerais, SP - SHo Paulo, 
PR - ParanA, SC - Santa Catarina, RS - Rio Grande do Sul, 1 - Eleuterio, 2 - Pouso Alegre, 3 - Pic0 do Itapeva, 4 - Cajamar, 5 - Salto de 
Pirapora, 6 - Pirapora do Bom Jesus, 7 - Samambaia, 8 - Quatis, 9 - Castro, 10 - Camarinha, 11 - Ervalzinho, 12 - Guaratubinha, 
13 - Campo Alegre/Corupa, 14 - Itajai, 15 - CamaquH. Modified from Moro (2000) 
transitional environments. Marginal zones at the 
peripheries of the Neoproterozoic plates contain foreland 
and backland domains, and the far interiors of these plates 
contain impactogenic basins and intracontinental wrench 
basins. 
Despite this difference in environments, remnants of 
late Brasiliano basins contain very similar sedimentary 
and volcanosedimentary rocks and structures. In most 
basins the area of preserved rocks is much smaller than 
the original area of deposition, and today the only 
remnants are those preserved in troughs or protected from 
erosion by local tectonics and by Paleozoic covers. For 
this reason the more extensive occurrences lie on the 
basement of Proterozoic syneclises (see Fig. 10a and 
l o b ) along depositional sites that later became 
depocenters throughout the Paleozoic. 
Numerous widely spaced remnants of Stage 9 occur 
on the shield areas of Borborema (Brito Neves et al., 
1995b), Mantiqueira, and a few in Tocantins Province. 
The exposures are commonly too small to determine the 
original type of basin, and although the simple designation 
'molasse' basins is frequently applied, the term is 
inadequate because the rocks clearly formed in most of 
the tectonic varieties of basins described above. Because 
of their lithological similarities, their association with the 
final phases of the Brasilianoorogeny, and the overlying 
Ordovician and Siluro-Devonian cover, Almeida (1969) 
used these suites to define a 'transition stage' between 
Gondwana Research, V. 5, No. 1,2002 
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Gondwana Research, K 5, No. 1,2002 
B.B. BRIT0 NEVES 
SEDIMENTARY BASINS OF SOUTH AMERICA IN RELATION TO SUPERCONTINENTS 191 
the Brasiliano orogenies (unstable stage) and the 
subsequent phase of platform cover (post-Ordovician 
stable stage). Soares et al. (1978) suggested that these 
units represent the first (alpha) cratonic sequence (sensu 
Sloss, 1988) of the platform cover. 
Basin formation follows the diachrony of the orogenic 
events discussed above. Most of the rocks have isotopic 
ages concentrated around the Proterozoic-Cambrian 
boundary (ca. 540 Ma), but they range from 
Neoproterozoic I11 (605 Ma; Guaratubinha Rhyolite; Basei 
et al., 1998) up to the beginning of the Ordovician (ca. 
480 Ma; Pimentel et al., 1996). 
Contemporaneous with these stages of basin-forming 
tectonics are many extensional events over all of South 
America. They include mafic and ultramafic magmatism 
along the axis of the Amazonian Syneclise, mafic dyke 
swarms in the central-southern region of Amazonia and 
in the northern part of the S2o Francisco Craton, plus 
many occurrences of felsic dykes, hydrothermal veins and 
pegmatites. 
Sediments of QPC assemblages predominate in the 
foredeeps (Alto Paraguai, Lagarto-Palmares, Itajai, 
Camaquii; see Figs. 10a and lob), where some of the 
lowest stratigraphic units are coeval with those of the 
marginal fold belt. Over these QPC sediments are coarse- 
grained fluvial-clastic units derived from the erosion of 
the fold belts, grading to siltstone and beds of lacustrine 
pelite. 
Many of the basins of this transition stage are associated 
with widely spaced transcurrent faults, indicating the 
importance of escape tectonics in all structural provinces. 
Some basins in southern Brasil (Guaratubinha, Campo 
Alegre, Corupa; Fig. 10a) contain variegated coarse- 
grained clastic sediments and felsic volcanic rocks 
associated with late-orogenic alkaline plutons. Similar 
sedimentary rocks without associated magmatic rocks are 
present in intradeep basins bounded by fault lines and in 
grabens associated with extension and collapse in the 
interior of fold belts such as Ju6, Serra do C6gado in the 
Sergipano Belt of the Borborema Province, and the Apiai 
belt (Camarinha basin). Outcrop thicknesses are up to 
about 3000 m, but thicker sequences probably occur in 
those parts of the basins underlying syneclises. 
At the same time (ca. 590 Ma) a diversified 
sedimentary-volcanic-plutonic association along the ‘Serra 
do Mar’ range (southeastern Brazil) may have resulted 
from impactogenic tectonics caused by collisions and 
microcollisions of Brasiliano terranes and arcs in 
southeastern Brazil, from Santa Catarina to S2o Paulo 
( e g , Curitiba and Luis Alves blocks, Paranagud and Pien 
arcs, etc., Citroni, 1998; Basei et al., 1998). Other basins 
on the periphery of mobile belts, such as Castro (Parana) 
and Camaquz (Rio Grande do Sul), in southern Brazil, 
have commonly been described as foredeeps, but other 
authors have attributed their origin to rifting caused by 
(late-Brailiano) thermal contraction. 
Paleozoic Gondwanan Syneclises (Stage 10) 
The sedimentary cover developed on Western 
Gondwana covers an area exceeding 3,200,000 km z. In 
South America it is mainly preserved in six large syneclises 
(Acre, Solimdes, Amazonas, Parnaiba, ParanB and Chaco- 
Parana; Fig. 1 l), but smaller deposits occur in Mesozoic 
rifts of the continental interior and coastal regions as well 
as in Patagonia and the sub-Andean Zone. These large 
intracratonic basins (‘IS’, Kingston et al., 1983) resulted 
from extension in response to the thermal contraction of 
the continental lithosphere after the Brasiliano-Pan- 
African Cycle, during which the geothermal gradients were 
considerably elevated (Brito Neves et al., 1984). 
Africa contains a number of basins with similar 
Paleozoic covers (Ghana, Taoudeni, Angola-Oyambo- 
Barotse, Kalahari, Zambeze, Luano, Karoo, etc.). These 
syneclises are generally elliptical and have areas between 
500,000 km and 1,200,000 km 2, with thicknesses of 
sediments in the depocenters up to 7000 m. Some basins 
were connected during their evolution. There is a good 
recent syntheses by Milani and Zalan (1999) about these 
syneclises that emphasizes petroleum accumulation. 
Sediments of Stage 10 were deposited after the 
accretion of Gondwana. Deposition in the Chaco-Paran6 
and Solimdes basins began in the Lower and Middle 
Ordovician, but most sequences range from post-Middle 
Ordovician to Eo-Triassic. The basins underwent a 
polyphase evolution with some local deformation from 
the time of Pangea assembly (ca. 230 Ma), at the climax 
of the Hercynian orogeny, and during its break-up 
(especially from 225 to100 Ma). Sediments are locally 
deformed on the edges of the South American Platform 
by Hercynian movements along western (pre-Andean) fold 
belts on the Pacific margin and the southernmost 
(Ventana-Cape belt/ SAMFRAU) margin of the platform 
(Almeida et al., 2000). 
The shape of South American syneclises commonlyshows a heritage of the Brasiliano framework (Brito Neves 
et al., 1984). Deeper troughs contain sequences associated 
with the late Brasiliano transition stage (stage 9; above), 
and along some sections they display a general steerhead 
(koilogen) configuration. 
Soares et al. (1978) and Almeida et al. (2000) proposed 
that the infilling of the syneclises shows many general 
similarities with the successive deposition of three 
widespread cratonic sequences (sensu Sloss). Silurian- 
Gondwana Research, K 5, No. 1,2002 
192 B.B. BRIT0 NEVES 
72' 52" 32' 
u Paleozoic synedises 
Interior Paleo-Mesozoic 
and Tertiaiy nfls 
Other Cenozoic Basins 
1 GANDARELA 
2 FONSECA 
MIDDLE 
JAGUARIBE t 
I 
E 
Q 
U 
A 
COASTAL (I) EOUATORIAL 
(11) CENTRAL (Ill) SOUTHERN ATLANTIC , 
L 
ARCHES 
A - lquitos 
10 S JOSCBELMONTE 
WESTOF 
16 AGUA BONITA 
. . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . 
S 
0 
U 
. . . . . , . . . . . . . . . . . 
; @ 
E 
R 
E - Purus 
C - Monte Alegre 
D - Gurupa 
E - Tocantins 
F - Guam& 
G - Ferrer IUrbano Santos 
H - S o Francisco 
I -AltoXingu 
J -Alto Paranaiba 
K - Assuncibn 
L - Ponta Grossa 
M - Rio Grande 
Fig. 11. Main Phanerozoic sedimentary basins of Brazil. Adapted from Schobbenhaus et al. (1984). 
Devonian sequences (beta) and Eo-Carboniferous 
(gamma) sequences consist of mature marine sediments 
with chrono-parallel beds developed under humid to 
glacial conditions. The late-Carboniferous to Triassic 
sequence (delta) records several glacial episodes, progressive 
aridity with time, marine regression and ultimately deposition 
of continental sediments containing red beds. 
All basins were completely restructured both internally 
and externally (beginning in the Permian in the north of 
the continent) mostly during the Upper Jurassic and Lower 
Cretaceous. New conditions included development of 
linear uplift zones (arcs), intrusion by diabase dikes, sills 
and plugs and by eruption of widespread lavas, 
particularly in the Parani Basin. Sedimentation was 
restricted to fluvial and eolian deposits (sequence epsilon). 
These processes were diachronous from one part to 
another of the continent and are tectonically related both 
to the accretion of Pangaea, which was completed at 
ca. 230+5 Ma (Veevers, 1989), and partly to its 
contemporaneous break-up from 225 Ma onwards. The 
Triassic is marked by a major interruption of sedimentation 
almost everywhere (except southern Brazil), which 
emphasizes the Paleozoic (post-Ordovician/Lower 
Triassic) character of the Gondwanan syneclises. 
Gondwana Research, V. 5, No. 1,2002 
SEDIMENTARY BASINS OF SOUTH AMEFUCA IN RELATION ‘ro SUPERCONTINENTS 193 
The Activation Stage (Stage 11) 
The Atlantic Ocean began to form when new basins 
were created and old ones were restructured along the 
newly forming continental margin and the interior of 
South America (Chang et al., 1991; Cainelli and Mohriak, 
1999; Matos, 2000). Three oceanic segments (Equatorial, 
Central and Southern), separated by structural highs, 
opened in well-defined phases from the Upper Jurassic 
to the Quaternary. 
Three distinct rift phases from the Volgian to the 
Barremian developed grabens, semigrabens and rifts that 
were filled by fluvio-deltaic sediments of the ‘continental 
megasequence’. Brasiliano trends greatly influenced the 
outlines of these grabens on the central and southern 
continental margin and in the continental interior (Brito 
Neves et al., 1984). Thermal relaxation that followed 
rifting initiated deposition of a ‘transitional megasequence’ 
(Aptian) that includes black shale and evaporite deposits 
southward from the state of Alagoas. This assemblage 
provides important sources and structures for 
accumulation of oil. The subsequent stage of drift 
produced a ‘marine megasequence’ subdivided into a 
lower (Albian to Turonian) carbonate shelf and an upper 
siliciclastic suite deposited under open marine conditions 
from the uppermost Cretaceous to the Quaternary. 
In the continental interior, besides the complete 
restructuring of the syneclises, siliciclastic sedimentation 
occurred because of the formation of new rift systems, 
deepening of older depocenters and intensification of 
some linear zones of uplift (arcs). This led to the 
fragmentation of a large part of the original Paleozoic 
cover, which was eroded and in part preserved in interior 
and coastal rifts. Some of these interior rifts (Tucano, 
Jatoba, Araripe; Fig. 11) contain sections that include 
sediments of the transition stage (stage 9), Gondwanan 
syneclises stage (stage 10) and the rift and transitional 
suites (stage 11) formed during the opening of the Atlantic 
Ocean. 
Basaltic magmatism was an important part of stage 
11. The Serra Geral flood basalt of the Parana Basin covers 
more than 1,000,000 km and was extruded mostly in 
the Lower Cretaceous, with a climax between the 
Valanginian and Hauterivian. Basaltic magmatism also 
occurred in all syneclises, in some coastal basins and also 
as far as the central-western region of Brazil about 2500 
km from the coastal basins (in Anari and Tapirapuh, 
RondBnia and Mato Grosso). However, basalt flows are 
rare in many rifts in the interior of the continent. 
Soares et al. (1978) designated the entire stratigraphic 
pile of stage 11 as a cratonic sequence (epsilon). This 
grouping is not advisable because of the diversity of rocks 
(sedimentary and igneous) and tectonic environments 
during this stage 11 
Post-Pangea Restabilization (Stage 12) 
A new tectono-sedimentary phase for all parts of South 
America began in the Upper Cretaceous. Continental 
separation and thermal contraction associated with 
basaltic magmatism caused a new phase of syneclise 
formation that created basins filled with fluvial and fluvio- 
lacustrine sediments and local eolian deposits. The 
siliciclastic deposits overlie all vestiges of previous rifts 
and are deepest in areas that underwent differential 
subsidence (Alter do Chiio Formation in Amazonas; Bauru 
Group in Paranh; Itapecuru Formation in Parnaiba; 
Urucuia Formation in the Siio Francisco Basin; etc.). These 
deposits prograded over an inter-regional discontinuity 
and reflect a new phase of tectonic stabilization (leading 
to orthoplatformal conditions) that succeeded the 
dramatic process of rifting and initial drift of the previous 
stage. The designation of a new cratonic sequence (Zeta 
sequence, Soares et al., 1978) is fairly reasonable. 
In almost all basins on the Atlantic continental margin 
new syneclises (‘MS’, Figueiredo and Raja-Gabaglia, 1986) 
formed over deposits of previous rift and drift phases. In 
continental areas of Brasiliano structural provinces and 
syn-Brasiliano cratonic domains, these new tectonic 
conditions led to a series of small rifts mainly filled with 
fluvial and lacustrine sediments. The number and 
distribution of these Cenozoic rift systems and the isolated 
centers of volcanism associated with some of them is not 
totally known yet. Significant data are only available for 
those rifts of southeastern Brazil (mainly Rio Paraiba do 
Sul, Rio Ribeira, Rio Iguaq6, Fonseca, Gandarela). Other 
rifts are being gradually identified as belonging to this 
phase of readjustment, and all of them show evidence for 
differential uplift in the interior of the plate (some of these 
rifts related to accretion along the Atlantic margin, and 
subduction along the Pacific margin). 
Preliminary data suggest that the South American plate 
had rates of continental uplift and Cenozoic volcanism 
less intense than in the African plate during this stage. 
Cenozoic sediments consist of fluvial and lacustrine 
beds (locally eolian) bothin local basins and in widespread 
tablelands east of the Andes. Regions of great stability 
with very low rates of subsidence cover large areas (in 
some places over millions of square kilometers) with 
sediments that prograded disconformably over deposits 
of all previous tectonic stages. They were unaffected by 
structures beneath the discontinuities. One example is 
the Amazonas lowlands, where the axis of the depocenter 
runs diagonally across the Amazonas syneclise in a NNE- 
Gondwana Research, I/: 5, No. 1,2002 
194 B.B. BFUTO NEVES 
SSW direction for about 1500 km from RondGnia to 
Roraima (along the Branco River). Other examples 
include the basins of ‘Alto Xingu’, ‘Alto Araguaia’, the 
Pantanal, the lowlands of the middle course of the S2o 
Francisco River, and others in the far interior of the 
continent. In addition, the Dala Cisandina contains 
tabular marginal sediments of the eastern side of the 
Andes from Venezuela to Patagonia (Llanos, Beni, Chaco/ 
Pantanal, Pampas, see Fig. 1) and is connected to the 
plains of Amazonas, where some components of 
subsidence are derived from the isostatic adjustment of 
the Andean Chain. This entire suite has been included 
in the Zeta stratigraphic sequence, but modifications in 
this scheme are inescapable for the future with further 
investigations. 
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