the Central African Fold Belt Proterozoic links between the

Transcription

Geological Society, London, Special Publications
Proterozoic links between the Borborema Province, NE Brazil, and
the Central African Fold Belt
W. R. van Schmus, E. P. Oliveira, A. F. da Silva Filho, S. F. Toteu, J. Penaye and I. P.
Guimarães
Geological Society, London, Special Publications 2008; v. 294; p. 69-99
doi:10.1144/SP294.5
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Proterozoic links between the Borborema Province, NE Brazil,
and the Central African Fold Belt
W. R. VAN SCHMUS1, E. P. OLIVEIRA2, A. F. DA SILVA FILHO3, S. F. TOTEU4,
J. PENAYE4 & I. P. GUIMARÃES3
1
Department of Geology, University of Kansas, Lawrence, Kansas, 66045 USA
(e-mail: [email protected])
2
Instituto Geociências, UNICAMP, Campinas, 13083-970 Brazil
3
Departamento de Geologia, Universidade Federal de Pernambuco, 50739 Recife, Brazil
4
Centre de Recherches Géologiques et Minières, BP 333, Garoua, Cameroon
Abstract: The Congo (CC) and the São Francisco (SFC) cratons were joined at about 2.05 Ga;
northern parts of Palaeoproterozoic basement subsequently underwent extension at about 1 Ga,
forming intracratonic basins. Neoproterozoic metasedimentary rocks in these basins yield detrital
zircons as young as 630 Ma. The Brasiliano and Pan-African (c. 620– 580 Ma) assembly of West
Gondwana extensively altered this system. The Sergipano domain occurs north of the SFC, and the
comparable Yaoundé domain occurs north of the CC. Crust north of the Sergipano domain comprises the Pernambuco– Alagoas (PEAL) domain. The NE– SW-striking Tcholliré –Banyo fault in
Cameroon may extend southwestwards between the PEAL and Sergipano domains, defining
northern limits of abundant SFC/CC basement. The Adamawa –Yadé domain in Africa does
not appear to extend into Brazil. The Transverse domain of Brazil is a collage of Palaeoproterozoic
crustal blocks, the 1.0 Ga Cariris Velhos orogen (CVO), late Neoproterozoic basins, and Brasiliano granites. The CVO extends ENE for more than 700 km in Brazil, but eastern continuation
into Africa has not been identified. North of the Transverse domain contiguous c. 2.15 Ga gneisses
comprise basement of Rio Grande do Norte and Ceará domains, which continue eastwards into
western Nigeria and western Sahara.
This report presents a summary of continuing
studies in Brasiliano and Pan-African domains of
the Borborema Province in NE Brazil and of the
Central African Fold Belt in west-central Africa
(Fig. 1). It has long been recognized that there is
strong geological correlation between NE Brazil
and west-central Africa (e.g., Caby 1989; Castaing
et al. 1994; Trompette 1997; Neves 2003), but
detailed understanding of the Proterozoic history
of the association is far from complete (see Brito
Neves et al. 2002). We believe that the overall
relationships are consistent with a model in which
late Mesoproterozoic to early Neoproterozoic
break-up of a Palaeoproterozoic supercontinent
(e.g., Atlantica, Rogers 1996) created a large
region between the Congo–São Francisco and
West African –Amazonian cratons, consisting of
extensional basins floored by Palaeoproterozoic
crust, local basins approaching small oceans, and
a larger ocean between the northern edge of extensional crust and the West African –Amazonian
craton. At present, there is no clear link between
this tectonism and formation or break-up of
Rodinia (see Kröner & Cordani 2003). During the
middle to late Neoproterozoic the major cratons
converged, forming juvenile oceanic terranes and
major collisional belts. The convergent phase culminated with final assembly of West Gondwana,
followed by post-collisional tectonic adjustments,
mainly post-tectonic magmatism, and transcurrent
faulting. Note: In this paper we will use ‘craton’
to refer to relatively rigid, large continental
masses against which major Pan-African and
Brasiliano orogenic domains formed about
600 Ma and which were not significantly affected
internally by that tectonism and metamorphism (in
this case, since 2.0 Ga).
Several types of data are crucial for developing a
stratigraphic and tectonic history for the regions
concerned. Traditional K –Ar and Rb–Sr results
have been available for four decades, and these
quickly established the major craton–orogenic
belt architecture of Africa and South America.
Over the past 15 years U –Pb geochronology of
zircon and other minerals, Sm –Nd model crustformation ages (TDM), and Ar/Ar thermochronology have provided major refinements and, in some
cases, significant reinterpretations. Most of the
recent and current U –Pb data for primary ages or
major secondary crystallization events are based
From: PANKHURST , R. J., TROUW , R. A. J., BRITO NEVES , B. B. & DE WIT , M. J. (eds) West Gondwana:
Pre-Cenozoic Correlations Across the South Atlantic Region. Geological Society, London, Special Publications,
294, 69– 99. DOI: 10.1144/SP294.5 0305-8719/08/$15.00 # The Geological Society of London 2008.
70
W. R. VAN SCHMUS ET AL.
Fig. 1. A portion of West Gondwana about 500 Ma showing inferred geological provinces and potential correlations
from Brazil to west-central Africa. Legend: Br/PA, Brasiliano/Pan-African orogenic domains; PalaeoPr,
Palaeoproterozoic crust. Major domains and regions used in this paper: AYD, Adamawa–Yadé domain; MK, Mayo
Kebi terrane; NWCD, NW Cameroon domain; OU, Oubanguide fold belt; PEAL, Pernambuco–Alagoas domain;
RGND, Rio Grande do Norte domain; SD, Sergipano domain; Transv. Dom., transverse domain; YD, Yaoundé domain.
Faults and shear zones: AF, Adamawa fault; Pa, Patos fault zone; Pe, Pernambuco fault zone; SF. Sanaga fault; TBF,
Tcholliré– Banyo fault; TBL, Transbrasiliano Lineament. Cities: D. Douala; G, Garoua; K, Kaduna area of Nigeria;
R, Recife; N, Natal; S, Salvador; Y, Yaoundé.
BORBOREMA–CENTRAL AFRICA CONNECTIONS
on work from several laboratories using standard
thermal ionization mass spectrometry (TIMS)
methods (single and multi-grain approaches) and
Pb-evaporation 207Pb/206Pb ages. Determination
of ages for individual grains in large suites of detrital zircon from metasedimentary rocks to examine
provenance and to set limits on depositional ages
is an important and growing avenue of research in
Precambrian terranes and is based largely on
secondary-ion mass spectrometry (SIMS, e.g.,
SHRIMP) methods and laser-ablation ICP
(LA-ICP) methods. Sm –Nd whole-rock analyses
yield depleted-mantle crustal formation ages (e.g.,
TDM, DePaolo 1981), which provide very important
constraints for crustal provenance, not only for
igneous and orthogneiss suites, but also for metasedimentary and paragneiss sequences. Although such
data are not precise, they still allow determination
of maximum ages of crystallization or deposition
that can be crucial to defining crustal provinces.
Detrital zircon ages are able to set maximum
(but not actual or minimum) ages of sedimentation,
although maximum ages can often bracket depositional ages narrowly in the context of other
information. Detrital zircons can also give an
indication of major provenance, which in some
cases can be important for interpretation of assembly histories of crustal collages. TDM ages are, similarly, maximum ages for mantle extraction and can
often be used to determine whether a crustal terrane
is Archaean (or Palaeoproterozoic) crust, derived
from such crust, or must be younger. For example,
although an orthogneiss having a TDM age of
1.50 Ga must be Mesoproterozoic or younger; the
exact age cannot be determined from this data; the
TDM age could be a mixture of older crustal material
(up to and including Archaean) with juvenile
material of an unknown younger age. Regional geological relationships in conjunction with other
dating methods (e.g., U –Pb ages of zircons) must
be used to constrain the age of a crustal block or
terrane further. Nonetheless, Sm– Nd model ages
are essential for working in large, often poorly
defined, regions such as NE Brazil and west-central
Africa and are used extensively in this report.
Northern São Francisco Craton, Brazil
The São Francisco Craton underlies the southern
boundary of the Borborema Province of NE Brazil
(Fig. 2), and it is also the structural buttress
against which terranes to the north were accreted.
Its main geological features are outlined by Teixeira
& Figueiredo (1991), Teixeira et al. (2000), and
Bizzi et al. (2001). In general, the São Francisco
Craton consists of Archaean to Palaeoproterozoic
high-grade (migmatite, granulite) gneisses and
71
granite –greenstone supracrustal terranes overlain
by middle to late Proterozoic platform-type cover.
In the northern part of the craton there are several
greenstone belts ranging in age from c. 3.3 Ga to
c. 2.1 Ga.
The high-grade metamorphic terranes in the
northern part of the craton are traditionally separated
into an Archaean block (the Jequié migmatite–
granulite complex) and a Palaeoproterozoic mobile
belt known as the Itabuna –Salvador–Curaçá
orogen (Barbosa & Sabaté 2002; Oliveira et al.
2004). Geochronological data of Marinho et al.
(1994), Ledru et al. (1994), and Barbosa & Sabaté
(2004) on the southern segment of this orogen
suggest that plate collision occurred after 2.4 Ga
and that metamorphism reached its peak at about
2.05 Ga.
The northern segment of the Itabuna–Salvador–
Curaçá orogen originated by collision between two
Archaean blocks (Barbosa & Sabaté 2002, 2004),
namely the Gavião block to the west, and the Serrinha block to the east. The Serrinha block, of
major interest as potential sediment sources for
the Sergipano domain, contains an Archaean basement with U– Pb ages between 3120 Ma and 2980
Ma covered by volcanic rocks of the Rio Itapicuru
greenstone belt (2200–2100 Ma, Silva 1992),
both of which were intruded by granites with U –
Pb ages in the range 2160–2080 Ma (Rios 2002;
Oliveira et al. 2004). This basement crops out
along the southern edge of the Sergipano domain
(Fig. 2), where it forms basement to platform deposits. The northern edge of contiguous São Francisco
Craton basement is marked by the São Miguel do
Aleixo shear zone, which also delineates southernmost occurrences of Brasiliano granites and first
appearance (going northward) of Mesoproterozoic
TDM ages (Van Schmus et al. 1995). Palaeoproterozoic to Archaean rocks that are probably correlative
with São Francisco Craton basement also occur as
smaller uplifted, possibly isolated, blocks to
the north.
Borborema Province, NE Brazil
The Borborema Province of NE Brazil (e.g., Brito
Neves et al. 2000) can be divided into several geotectonic fold belts, domains, massifs, or terranes. In
this paper we will group them into six major regions
(Fig. 2) under the terminology of domains. Northward from the São Francisco Craton they are: (1)
the Sergipano domain; (2) the Pernambuco –
Alagoas (PEAL) domain; (3) the Riacho do Pontal
domain, to the west of the PEAL domain; (4) the
Transverse domain (Ebert 1970; Jardim de Sa
1994); (5) the Rio Grande do Norte and Ceará
domains in Rio Grande do Norte state and central
72
Fig. 2. Borborema Province. Major domains and terranes: CE, Ceará domain (Or, 1.8 Ga Orós fold belt); MCD,
Médio Coreaú domain; PEAL, Pernambuco Alagoas domain; RGN, Rio Grande do Norte domain (SJC, São José
do Campestre Archaean nucleus); RP, Riacho do Pontal domain; SD, Sergipano domain; SFC, São Francisco Craton;
SLC, São Luı́s Craton; TD, Transverse domain (AP, Alto Pajeú terrane; AM, Alto Moxoto terrane; CB, Cachoerinha
belt; CV, Cariris Velhos orogenic belt; RC, Rio Capibaribe terrane). Faults and shear zones: AIF, Afagados do
Ingrazeira fault; BCsz, Boqueirão dos Conchos shear zone; PAsz, Patos shear zone; PEsz, Pernambuco shear zone;
SCF, Serra do Caboclo fault; SMAsz, São Miguel do Aleixo shear zone; TBL, Transbrasiliano Lineament. Cities and
towns: Fo, Fortaleza; Na, Natal; Re, Recife; Sa, Salvador. Neoproterozoic plutons or supracrustal units in Ceará domain
are not shown. Inset: general distribution of Brasiliano granites.
73
Fig. 2. (Continued. )
to eastern Ceará state; (6) the Médio Coreaú
domain, west of the Sobral fault in NW Ceará
state. The PEAL domain is not a distinct lithostratigraphic terrane, but a region of higher grade derivatives of rocks similar to those in the Transverse and
Sergipano domains; therefore it will be discussed
after these two regions. The Riacho do Pontal, Rio
Grande do Norte –Ceará and Médio Coreú
domains are important in the overall synthesis, but
will not be covered in as much detail, in part
because others (Santos et al. 2008) will discuss
the latter two areas, and the first is not well
known in detail at present.
Brasiliano plutonism, deformation and
metamorphism
Brasiliano granites comprise a significant portion of
outcrop in the Borborema Province (Fig. 2, inset).
These granites are important because their genesis
can tell us much about composition of deeper
levels of crust in the province (e.g., Sial 1986; Ferreira et al. 1998) and their isotopic characteristics,
especially Sm–Nd TDM model ages, can tell us
much about the age of the rocks from which the
magmas were derived, as discussed below. In
addition, age relationships among various types of
granites, in conjunction with their modes of occurrence, can help substantially to define the tectonic
history of the Brasiliano orogeny in the province.
The duration of deformation is best controlled
by U –Pb ages of pre-, syn- and post-tectonic Brasiliano plutons, and over the past 15 years many new
U –Pb ages on zircon, monazite, and titanite have
been reported for the Borborema Province (e.g.,
Jardim de Sá 1994; Van Schmus et al. 1995;
Fetter 1999; Dantas 1997; Kozuch 2003; Guimarães
et al. 2004; Neves et al. 2006). Several pre-tectonic
plutons, now often gneissic granites, have ages of
640 to 620 Ma, indicating that deformation began
after 620 Ma; plutons in the 620–640 Ma range
are generally found south of the Patos shear zone,
in the central and southern regions. U –Pb crystallization ages of syn-deformational igneous rocks or
U –Pb ages on metamorphic zircon, monazite, or
titanite suggest that thermal activity peaked at
about 600 Ma. Post-tectonic plutons in all regions
commonly have ages of 580 to 570 Ma, indicating
that compressive ductile deformation had essentially ceased by 580 Ma.
The Borborema Province also contains many
Brasiliano shear zones (Brito Neves et al. 1982;
Jardim de Sá 1994; Vauchez et al. 1995). Some,
such as the Patos and Pernambuco shear zones
(Fig. 2), can be traced into comparable shear
zones in Africa (e.g., Toteu et al. 2004, and as
discussed below). In many cases the shear zones
represent major faults within former continental
blocks; others, however, may represent major
terrane boundaries (Brito Neves et al. 2000). For
example, the eastern part of the Patos shear zone
probably represents a major terrane boundary,
formed by convergence between the Rio Grande
do Norte domain and the Alto Pajeú terrane of the
Transverse domain prior to the Brasiliano orogeny
(Van Schmus et al. 2003; Brito Neves et al.
2001a). On the other hand, the Pernambuco shear
zone is mainly intracontinental (e.g., Neves &
Mariano 1999). A major shear couple formed
between the Patos and Pernambuco shear zones
during later stages of Brasiliano deformation,
resulting in the creation of many transverse
faults with block rotation and internal
deformation within the Transverse domain (Jardim
de Sá 1994), which complicate internal tectonic
reconstructions.
Sergipano domain
The Sergipano domain (formerly ‘belt’ or ‘fold
belt’) is one of the most important Precambrian
74
orogenic regions of NE Brazil, not only because it
was early considered as evidence for continental
drift (Allard & Hurst 1969), but also because it contains several structural and lithological subdomains
that allow it to be compared with Phanerozoic
orogens. This domain has been interpreted previously as a typical geosyncline (Humphrey &
Allard 1968; Silva Filho & Brito Neves 1979), as
a collage of lithostratigraphic domains (Davison
& Santos 1989; Silva Filho 1998), or as a Neoproterozoic fold-and-thrust belt produced by inversion
of a passive margin basin located at the northeastern
edge of the ancient São Francisco plate (D’el-Rey
Silva 1999). Much of the Sergipano domain was
formed by compression between the São Francisco
Craton and the Borborema Province during the Brasiliano orogeny (Brito Neves et al. 1977); during
this convergence the PEAL domain acted as a
major crustal block, or ‘massif’, compressing units
of the Sergipano domain against the São Francisco
Craton and thrusting many units southward over it.
According to Santos & Souza (1988), Davison &
Santos (1989), and Silva Filho (1998) the Sergipano
domain consists of six lithostratigraphic subdomains which are, from south to north: Estância,
Vaza Barris, Macururé, Marancó, Poço Redondo
and Canindé, each separated from the other by
major shear zones (Fig. 3). The first three are
mostly composed of metasedimentary rocks, with
metamorphic grade increasing from weakly or nonmetamorphic in the Estância subdomain through
greenschist grade in the Vaza Barris subdomain to
amphibolite facies in the Macururé subdomain.
Higher-grade equivalents of the Macururé subdomain (granulite retrograded to amphibolite) occur
within the PEAL domain (Silva Filho & Torres
2002; Silva Filho et al. 2003). Brasiliano granitoid
plutons occur in all regions north of the São
Miguel do Aleixo fault, but they are absent in the
southernmost Vaza Barris and Estância subdomains. These last two areas are underlain by Palaeoproterozoic to Archaean basement contiguous with
the Sao Francisco Craton and are relatively undeformed; geotectonically they could be regarded as
part of that craton.
The Estância subdomain comprises, from base
to top, sandstones and argillites of the Jueté
Formation, dolomites and limestones of the Acauã
Formation, sandstones and argillites of the
Lagarto Formation, and sandstone and minor conglomerate lenses of the Palmares Formation (Silva
Filho & Brito Neves 1979); primary sedimentary
structures are ubiquitous. The Vaza Barris subdomain mostly consists of greenschist facies clastic
and chemical sedimentary rocks. D’el-Rey Silva
& McClay (1995) subdivided rocks of this area
into the Miaba Group (quartzite –conglomerate,
at the base, followed upwards by phyllites,
Fig. 3. Sergipano domain (modified from Oliveira et al. 2006). BMJsz, Belo Monte– Jeremoabo shear zone; Isz,
Itaporanga shear zone; Msz, Macururé shear zone; SMAsz, São Miguel do Aleixo shear zone.
6
(a)
5
Macururé
Vaza Barris
4
Estância
3
2
Number of analyses
meta-greywackes, chlorite-schist, and metalimestone), Simão Dias Group (sandstones, mudstones, meta-siltites, meta-greywackes, phyllites,
and meta-rhythmites), and the Vaza –Barris Group
(meta-diamictites, phyllites, and meta-limestone).
D’el-Rey Silva (1999) interpreted sediment
deposition in the Estância and Vaza Barris subdomains as recording two cycles of sedimentation
onto a passive continental margin of the ancient
São Francisco plate. In this model, the São Francisco Craton should be the source of detritus.
However, on the basis of detrital zircon populations
with ages between 570 Ma and 657 Ma (Fig. 4b, c),
Oliveira et al. (2005a, b) proposed that the uppermost clastic sedimentary rocks of the Vaza Barris
and Estância subdomains were deposited in
foreland basins, with detritus sources from the
Sergipano fold belt and other sources farther north
in the Borborema Province. Depleted-mantle Sm–
Nd TDM model ages of 1.8 to 1.2 Ga for fine-grained
clastic metasedimentary rocks from the Macururé
and Estância subdomains (Fig. 5a) are also
75
1
0
0.8
1.2
1.6
2.0
2.4
2.8
3.2
3.6
4.0
2.4
2.8
3.2
3.6
4.0
20
(b)
16
CSF
PEAL
12
D. Itabaiana
P. Redondo
8
4
0
0.8
1.2
1.6
2.0
TDM (Ga)
32
Fig. 5. Sm–Nd TDM model ages from Sergipano
domain (modified from Oliveira et al. 2006). CSF, São
Francisco Craton; D. Itabaiana, Itabaiana Dome;
P. Redondo, Poço Redondo subdomain; PEAL,
Pernambuco– Alagoas domain.
977
28
Macururé
quartzite
FS-89
24
20
16
12
8
1990
4
(a)
0
1039
Number of analyses
12
10
Frei Paulo
metagreywacke
FS-118
657
1934
8
6
4
2715
2
(b)
0
20
16
570
Estância
sandstone
FS-F
634
12
958
8
4
(c)
0
0.4 0.7 1.0 1.3 1.6 1.9 2.2 2.5 2.8 3.1 3.4 3.7 4.0
206
Pb/238U (Ga)
Fig. 4. Detrital zircon populations from Sergipano
domain (modified from Oliveira et al. 2006).
consistent with provenance from sources other
than the São Francisco Craton, although a minor
contribution from the craton cannot be firmly
ruled out. U –Pb SHRIMP ages on detrital zircon
grains from the Frei Paulo meta-greywacke in the
Simão Dias Group cluster about 657 Ma, 1039
Ma, 1934 Ma and less often about 2715 Ma
(Fig. 4b); the youngest zircon grain is 615 Ma,
thus constraining deposition of the original sediment to less than this age.
The Macururé subdomain lies to the north of the
Vaza Barris subdomain and extends the width of
the belt. The São Miguel do Aleixo shear zone separates these two domains and is a major crustal
boundary. Brasiliano plutons do not occur south
of the shear zone, and all Brasiliano plutons north
of it have Mesoproterozoic Sm –Nd TDM ages
suggesting that São Francisco Craton crust, if
present, must lie below the depth of magma
genesis (Van Schmus et al. 1995; Oliveira et al.
2006). The Macururé subdomain mostly consists
of garnet–mica schists and phyllites with minor
quartzite and marble, all intruded by granitic
plutons (628 –625 Ma: Bueno et al. 2005; Long
et al. 2003) and a few mafic to ultramafic
sheets. Detrital zircon grains cluster mostly in the
intervals 980–1100 Ma and 1800–2100 Ma
(Fig. 4a); there are no zircons younger than
76
900 Ma (Oliveira et al. 2006), resulting in a relatively unconstrained depositional age between 900
Ma and 625 Ma.
The Marancó subdomain contains a
metavolcanic– metasedimentary sequence (quartzite, conglomerate, micaschists, phyllites, and
lenses of andesite, dacite and quartz-porphyry)
with peridotite and amphibolite lenses. Andesite
and dacite lenses occur conformably interleaved
with phyllites and yield U –Pb SHRIMP ages
between 602 and 603 Ma (Carvalho et al. 2005).
Detrital zircon grains from four samples of clastic
metasedimentary rocks have U –Pb SHRIMP ages
clustering mostly between 950 and 1100 Ma, with
the youngest zircon at 914 Ma, indicating deposition after this age and with detritus provenance
dominantly from late Mesoproterozoic and early
Neoproterozoic sources similar in age to the Poço
Redondo gneisses (Carvalho et al. 2005). Intercalated lenses of 603 –602 Ma andesites and dacites
and stocks of granodiorite dated at 595 + 11 Ma
(Rb– Sr isochron, Silva Filho et al. 1997a) that
cross-cut the sedimentary sequence indicate that
deposition probably occurred in the late
Neoproterozoic.
The Poço Redondo subdomain is composed of
migmatites, biotite gneisses and several granitic
intrusions, such as the Serra Negra augen gneiss
(952 + 2 Ma; U –Pb SHRIMP, Carvalho et al.
2005), and leucogranite sheets similar to ones in
the Canindé subdomain (below). Grey gneisses
from the palaeosome of migmatites yield U –Pb
SHRIMP ages from 960 to 980 Ma (Carvalho
et al. 2005), equivalent to orthogneisses and metavolcanic rocks of the Cariris Velhos orogen in the
Transverse domain (discussed below). Sm–Nd
TDM model ages are typically between 1.7 and
1.3 Ga (Fig. 5b) showing that provenance includes
sources that are Mesoproterozoic or younger. This
subdomain is particularly important since it is the
primary evidence for c. 1.0 Ga igneous rocks
south of the PEAL domain.
The Canindé subdomain is composed of (i) an
elongated pink granite sheet (Garrote unit) dated
at about 715 Ma by Van Schmus (unpublished
data in Santos et al. 1998); (ii) a metavolcanic –
sedimentary sequence (Novo Gosto unit) represented by fine-grained amphibolite, marble,
graphite schist, mica-schist, and meta-greywacke
containing younger detrital zircon grains dated
between 625 and 629 Ma (U– Pb SHRIMP; Nascimento et al. 2005); (iii) a sub-volcanic microgabbro
– quartz-monzodiorite complex (Gentileza unit)
with microgabbro, porphyritic quartz-monzodiorite
(688 + 15 Ma, U –Pb SHRIMP, Nascimento et al.
2005), Rapakivi granite (684 + 7 Ma U – Pb
TIMS, Nascimento et al. 2005) and quartzporphyry; (iv) the Canindé gabbro–leucogabbro
complex with gabbro, gabbro-norite, leucogabbro,
peridotite, and pegmatitic gabbro (690 + 16 Ma,
U –Pb SHRIMP, Nascimento et al. 2005); (v)
several granitoid bodies such as tonalite
(634 + 10 Ma, U –Pb SHRIMP, Nascimento
et al. 2005), granodiorite, quartz-syenite
(617 + 7 Ma, Rb–Sr isochron, Silva Filho et al.
1997a) and leucogranite sheets (609 + 11 Ma,
Rb –Sr isochron, Silva Filho et al. 1997a). On the
basis of major and trace elements, and Nd-isotope
geochemistry, Nascimento et al. (2005) suggested
that the Canindé domain is the root of an inverted
continental rift sequence.
Structural evolution of Sergipano domain. The
Sergipano domain underwent three main deformation episodes related to the Brasiliano collisional
event (D1 –D3, Jardim de Sá et al. 1986; Campos
Neto & Brito Neves 1987; D’el-Rey Silva 1995;
Araújo et al. 2003). These deformations are best
recognized in supracrustal sequences of the Vaza
Barris and Macururé subdomains, as well as in the
basement rocks exposed in domal uplifts. The collisional event reworked older gneiss– migmatitic
fabrics (Dn) that can be either remnants of a preBrasiliano deformation event or an early structure
related to the very beginning of the collision. D1
is characterized by south-verging nappes and
thrust zones that transported the metasedimentary
rocks of the Macururé, Vaza Barris, and Estância
subdomains large distances southwards over the
São Francisco Craton. D2 deformation is marked
by extensive reactivation of the D1 episode and
is associated with a transpressive regime that
affected the entire belt. Some 625 Ma granites in
the Macurure subdomain were intruded between
D1 and D2, since they are affected by the D2
phase of deformation. D3 probably took place
after 600 Ma when the domain experienced a
large amount of uplift during which the rock units
had a brittle to ductile–brittle behaviour.
Transverse domain
The Transverse domain is a complex, heterogeneous collage of several crustal units, ranging
from Palaeoproterozoic (Transamazonian, c.
2.15 Ga) terranes and isolated basement blocks to
late-Brasiliano, post-collisional (c. 540–580 Ma)
granite plutons, all cut by late transcurrent faults
within the shear couple formed by the Patos and
Pernambuco shear zones (Fig. 6; Jardim de Sá
1994). In spite of this complexity, several specific
geotectonic units have been recognized on the
basis of geochronology, isotopic studies, and field
studies over the past 30 years (e.g., Brito Neves
1978; Brito Neves et al. 2000; Santos & Brito
Neves 1984; Santos et al. 1997). Terminology has
77
Fig. 6. General geology in the Transverse domain. TTNH, Teixeira– Terra Nova structural high, which coincides
with trend Brasiliano syenitic plutons (Syenitoid Line). Major fault zones in the DZT that are pertinent to this
discussion include AIsz (Afogados da Ingazeira shear zone), BCsz (Boqueirão dos Conchos shear zone), CGsz
(Campina Grande shear zone), SCF (Serra do Caboclo fault). Boundaries of Alto Pajeú terrane (APT), Alto Moxotó
terrane (AMT), and Rio Capibaribe terranes (RCT) are from Santos et al. (1997). CFB, Cachoerinha fold belt; CV,
Cariris Velhos orogen; PEAL, Pernambuco– Alagoas domain; RGND, Rio Grande do Norte domain. Map modified
from Kozuch (2003), Bittar (1998) and Brito Neves et al. (2005).
also changed significantly, and current conventions
will be followed, with annotations to former terminology as needed.
The eastern part of the area, the former ‘Pajeú –
Paraı́ba fold belt’ of Brito Neves (1978) was
divided into several fault-bounded tectonic ‘terranes’ by Santos et al. (1997): from ESE to NNW
they are the Rio Capibaribe, Alto Moxotó, and
Alto Pajeú terranes (Figs 2 & 6). The Rio Capibaribe terrane in the ESE part of the Transverse
domain is underlain mainly by Palaeoproterozoic
basement, but it includes areas of undated metasedimentary rocks which, at least in some cases, represent
sequences
correlative
with
late
Neoproterozoic units found to the west and north
(Neves et al. 2005, 2006). The Alto Moxotó
terrane (Brito Neves et al. 2001b) lies north of
the Rio Capibaribe terrane and is dominated by
large areas of Palaeoproterozoic basement with
relatively few Brasiliano granites. Several metasedimentary sequences are known to be Palaeoproterozoic, but some areas mapped as Palaeoproterozoic
may include late Mesoproterozoic to late
Neoproterozoic sequences.
Recent and current studies (Van Schmus et al.
1995; Brito Neves et al. 1995, 2000, 2001a;
Kozuch 2003; Guimarães et al. 2004) show that
the Alto Pajeú terrane is dominated by the 990–
940 Ma Cariris Velhos orogen (CV in Fig. 6; see
following section) and intrusive Brasiliano plutonic
rocks, with some remnants of Palaeoproterozoic
gneiss. An important aspect of this terrane is that
Brasiliano plutons along its western part are
mainly high-K syenitic rocks that yield Palaeoproterozoic Sm –Nd TDM ages and form the core of a
major topographic ridge called the ‘Teixeira –
Terra Nova High’, or ‘Syenitoid Line’ (Sial 1986;
Brito Neves et al. 2005; TTNH in Fig. 6). These
rocks have been difficult to date precisely because
of lack of zircon and/or complication by inherited
Palaeoproterozoic zircons. The western part of the
Alto Pajeú terrane consists of metasedimentary
and metavolcanic rocks of the early Neoproterozoic
Riacho Gravatá sequence (Bittar 1998), which
occurs on the west side of the TTNH and is
bounded to the west by the Serra do Caboclo fault.
Guimarães et al. (2004) reported U– Pb zircon
ages for several plutons in the eastern part of the
78
Transverse domain, with samples coming from all
three terranes mentioned above. The ages ranged
from 512 to 640 Ma and were divided into four
main groups: 640 –610 Ma, 590 –580 Ma, c. 570
Ma, and 545 –512 Ma. The oldest group is syntectonic, whereas the other three post-date the
peak of compressive, ductile deformation.
Cariris Velhos orogen. Bimodal (but mostly
felsic) volcanism and granitic plutonism 1.0 to
0.9 Ga is widespread in the Alto Pajeú terrane.
Such ages had been postulated on the basis of
Rb–Sr data a decade prior to the first zircon work
(Brito Neves et al. 1984, 1995), but many workers
attributed ages in the range of 1 Ga to partial degradation of Transamazonian (c. 2.1 Ga) systems
during the Brasiliano orogeny. More recent U– Pb
zircon ages confirm that ages of 1.0 to 0.9 Ga
reflect a distinct event and lithostratigraphic assemblage (Van Schmus et al. 1995; Kozuch 2003).
Campos Neto et al. (1994) proposed the term
Cariris Velhos orogeny for 1 Ga events in the
central part of the Transverse domain (Figs 2 &
3). Based on data currently available, the Cariris
Velhos orogen is a 50–100 km wide belt
that extends for more than 700 km, from the
northeastern part of the Transverse domain
west-southwestwards to the Riacho Pontal fold
belt (Fig. 6).
The core of the orogen is comprised of augen
gneisses representing granitic plutons that were
intruded into bimodal (but mostly felsic) volcanic
successions, which crop out on both sides of the
gneissic core. The age of the orogen is currently
constrained between 990 and 940 Ma based on detrital zircons in metasedimentary rocks (Van
Schmus et al. 1999) and U –Pb ages of Cariris
Velhos plutons and volcanic rocks (Kozuch 2003).
Sm– Nd model ages of 1.2 to 1.9 Ga for igneous
rocks yielding c. 0.94 to 0.99 Ga crystallization
ages (Fig. 7) indicate that some older, probably
Palaeoproterozoic, crust was involved in magma
genesis, yielding hybrid Sm –Nd TDM ages. Detrital
zircons from metasedimentary units are dominated
by c. 1 Ga grains (Fig. 8) indicating that their
Sm– Nd model ages are inherited primarily from
igneous rocks of the orogen that provided most of
the detritus. The Sm –Nd TDM ages of the igneous
rocks are, in turn, presumably hybrids of c. 1 Ga
juvenile magma contaminated by Palaeoproterozoic
crust.
The northern boundary of the Cariris Velhos
orogen (and, hence, the Alto Pajeú terrane),
occurs along the eastern part of the Patos shear
zone, and then it swings southwest along the Serra
Fig. 7. Sm–Nd TDM model ages within the Transverse domain (mostly from the Alto Pajeú terrane and Cachoerinha
fold belt).
79
40
Cariris Velhos & Cachoerinha metasedimentary rocks
West of Serra do Caboclo Fault
(94-98, 95-239)
East of Serra do Caboclo Fault
(94-103, 95-231, 97-16 &17)
20
0
0.6
1.0
1.4
1.8
2.2
2.6
3.0
3.4
3.8
TDM (Ga)
Fig. 8. Detrital zircons from Transverse domain (mostly from the Alto Pajeú terrane and Cachoerinha fold belt, Van
Schmus et al. 1999 unpublished).
do Caboclo fault. There is a major contrast in Sm –
Nd TDM ages on either side of the eastern part of the
shear zone (Archaean model ages to the north and
Mesoproterozoic model ages to the south),
suggesting that it represents a major terrane boundary. It is presently unclear, however, whether the
Serra do Caboclo fault, on the west side of the
Riacho Gravatá sequence, is also a major terrane
boundary; it may include significant vertical offset
(east side up) between the Cariris Velhos orogen
and the Cachoerinha Belt to the west.
Two distinctly different models have been proposed for the Cariris Velhos orogen: (a) that it represents a continental margin magmatic arc
(overlying Palaeoproterozoic crust: Van Schmus
et al. 1995; Brito Neves et al. 1995; Kozuch et al.
2003) or (b) that it represents a major extensional
belt that formed about 1 Ga (Guimarães & Brito
Neves 2005). Up to now geochemical data on the
orthogneisses are equivocal, but overall consideration of the geochemistry, petrology, isotopic data
and regional geology tends to favour an extensional
environment for the Cariris Velhos orogen
(Guimarães & Brito Neves 2005).
Cachoerinha Belt. The former ‘Piancó–Alta
Brı́gida fold belt’ of Brito Neves, (1978; Brito
Neves et al. 1984) or Salgueiro –Cachoerinha fold
belt of Sial (1986) included both higher-grade metasedimentary rocks in the east and lower-grade metasedimentary rocks in the west. The eastern units
(Riacho Gravatá sequence, Bittar 1998) are now
known to be early Neoproterozoic and related to
the Cariris Velhos orogen, so that they are now
included within the Alto Pajeú terrane. They are
separated from lower grade rocks to the west by a
major fault system (Serra do Caboclo fault). The
lower grade rocks to the west yield detrital zircon
populations 625 Ma (Van Schmus et al. 1999),
similar to those from the Seridó Group to the
north (cf. Van Schmus et al. 2003). The metasedimentary sequences also include intercalated c.
625 Ma metavolcanic rocks (Kozuch 2003),
showing that they were deposited just prior to the
peak of the Brasiliano orogeny. These units comprised the ‘Cachoerinha’ part of the Salgueiro –
Cachoerinha fold belt of Sial (1986), and that
terminology will be retained here. Metasedimentary
rocks of the Cachoerinha Belt are intruded by
a variety of Brasiliano granites (Sial 1986,
Ferreira et al. 1998) ranging in age from 640 to
580 Ma (Brito Neves et al. 2003; Kozuch 2003).
In its northern part the Cachoerinha Belt is
bordered on the west by the Boqueirão dos
80
Conchos shear zone; the western boundary in the
south is not well defined at present. To the west of
the belt the geology is relatively poorly known,
although it is clear that much of it includes
Palaeoproterozoic basement.
A major characteristic of this belt is the
presence of numerous Brasiliano granites having
Mesoproterozoic Sm –Nd TDM ages that are
similar to or slightly older than those from the metasedimentary rocks themselves (Fig. 7). Thus, it is
possible to conclude that Palaeoproterozoic basement played a limited role in magma genesis. The
age and nature of basement to the Cachoerinha
Belt is unknown, although Sm –Nd results for the
granites suggest that Palaeoproterozoic crust, if
present, must be very deep. Since the western side
of this belt appears to be faulted against blocks of
Palaeoproterozoic basement, the Cachoerinha Belt
could be a deep intracratonic basin.
Riacho do Pontal domain
The Riacho do Pontal domain occurs west of the
Sergipano and PEAL domains, along the northwestern part of the São Francisco Craton (Fig. 2). This
region is not known in as much detail as domains to
the east, but the data that are available (e.g., Van
Schmus et al. 1995; Brito Neves et al. 2000) show
that it contains units potentially correlative with
Palaeoproterozoic basement, with the Cariris
Velhos orogen of the Transverse domain, with
younger (late Neoproterozoic) metasedimentary
sequences similar to those in the Cachoerinha Belt
and the Sergipano domain, and with various Brasiliano granite suites. In any case, this domain is peripheral to our discussions about Brazil –Africa
correlations and will not be discussed further.
Pernambuco – Alagoas domain
The Pernambuco– Alagoas (PEAL) domain is bordered on the north and south by inward dipping
thrust faults and is a large region of high-grade
gneisses, migmatites and Brasiliano granites that
acted as a large structural massif during late Brasiliano deformation. This domain was originally
identified in the Borborema Province (Brito Neves
et al. 1982) as the ‘Pernambuco –Alagoas Massif’.
At that time it was thought to consist primarily of
Archaean to Palaeoproterozoic (Trans-Amazonian)
basement gneisses with intrusive Brasiliano granites. It was also interpreted as a crystalline core
(‘massif’) within the Borborema Province. Subsequent work (Van Schmus et al. 1995; Silva
Filho et al. 2002; Oliveira et al. 2006), now
shows that the PEAL complex is a collage of
many units of diverse ages (Fig. 9a), and Sm–Nd
model ages of 1.0 to 1.5 Ga require that large
parts of the protolith (including sources for many
Brasiliano plutons) must be Mesoproterozoic or
younger (Silva Filho et al. 2002, 2005a, b),
although many gneisses also show Archaean to
late Palaeoproterozoic origin (Figs 9b & 10).
Thus, the PEAL domain is not a distinct lithostratigraphic terrane, but instead, it is comprised of
higher-grade derivatives of rocks similar to those
in the Transverse domain. In order to reflect this
reality, we will not use ‘massif’, but will refer to
the region as a domain.
Brasiliano plutonic rocks in the PEAL domain. Brasiliano plutonic rocks are abundant in the PEAL
domain and can range from highly deformed, preto syn-tectonic units to late- to post-tectonic
plutons that are largely undeformed except for late
transcurrent faulting. The pre-to syn-tectonic Brasiliano plutons are commonly deformed or migmatized and thus often very difficult to distinguish in
the field from older (Mesoproterozoic to Palaeoproterozoic) crustal rock, and it is necessary to rely on
isotopic results for identification. Silva Filho et al.
(1996, 1997b, 2002) identified various late-tectonic
granitic intrusions and suites in the eastern part of
the PEAL domain, with compositions ranging
from high-K, calcalkaline, shoshonitic, mildly alkaline, rocks to various peraluminous (+ garnet
bearing) granites. Based on locations, petrography,
and geochemistry, these intrusions may be grouped
into four major suites. The Buique–Paulo Afonso
suite (PAB, Fig. 9a) is comprised of several granitic
plutons of wide compositional range, which were
intruded into tonalitic orthogneisses to the northnortheast of Paulo Afonso. The Águas Belas –
Canindé suite (ABC, Fig. 9a) is bordered on the
south by the Sergipano domain and lies between
the towns of Paulo Afonso and Palmeira dos
Indios. This suite contains small plutons of biotite
monzogranite, amphibole granodiorite, amphibole
tonalite to diorite, and shoshonitic composition
intruded into metatexites and diatexites of tonalitic
bulk composition. The granitic intrusions are both
metaluminous and peraluminous, syn- to latetectonic, with compositions ranging from medium
to high-K calc-alkaline. The Ipojuca– Atalaia
suite (IA, Fig. 9a) runs parallel to the present
coast southwest of Recife and is bordered on the
west by migmatites and orthogneisses. It consists
of leucocratic peraluminous granitic plutons
intruded into diatexites. The Marimbondo–
Correntes suite (MC, Fig. 9a) is a cluster of
plutons northeast of Palmeira dos Indios; it contains
calc-alkaline peraluminous and metaluminous
plutons which intrude older gneisses and migmatites. A fifth group of plutons called the Garanhuns
batholith by Silva Filho et al. (2002) is not utilized
here. There are relatively few published U –Pb
81
Fig. 9. (a) Eastern part of Pernambuco –Alagoas domain showing geological units being defined through on-going
field, petrological, and isotopic studies (modified from Silva Filho et al. 2002). ABC, Aguas Belas–Canindé magmatic
suite; BPA, Buique– Paulo Afonso magmatic suite; IA, Ipojuca– Atalaia magmatic suite; MC, Marimbondo–Correntes
magmatic suite; I, Inhapi metamorphic suite; P, Palmares metamorphic suite; V, Venturosa metamorphic suite.
(b) Distribution of Sm–Nd TDM ages in the Pernambuco –Alagoas domain.
crystallization ages for plutons of these suites, but
results that are available (Silva Filho & Guimarães
2000) show that they typically range from 625 Ma
to 590 Ma, with some post-tectonic plutons as
young as 520 Ma.
Gneiss and migmatite complexes. Santos (1995) and
Medeiros & Santos (1998) recognized two major
subdivisions of metamorphic rocks in the PEAL
domain. Rocks assigned to the Cabrobó Complex
are dominantly derived from metasedimentary to
metavolcanic protoliths and include biotite–garnet
gneiss, orthogneiss, and migmatitic orthogneisses,
plus other migmatitic varieties with intercalation
of quartzite, quartz-schist, calc-silicate rocks and
amphibolite. Rocks assigned to the Belém do São
82
Pernambuco-Alagoas Domain (undifferentiated)
12
8
4
0
0.6
1.0
1.4
1.8
2.2
2.6
3.0
3.4
3.8
TDM (Ga)
Fig. 10. Sm–Nd model ages for a comprehensive suite of rocks from the PEAL domain. The bimodal distribution
shows distinctly different amounts of older lithosphere in various samples. Compare with Figures 5 and 7. From Silva
Filho et al. (2002) and unpublished new data.
Francisco Complex mainly represent deeper crustal
(mainly igneous) rocks and include migmatite,
biotite gneiss, tonalitic orthogneiss, amphibolitic
gneiss and leuco-granodiorite to leuco-monzogranite, with some included remnants of the Cabrobótype supracrustal rocks.
The Cabrobó Complex was further divided by
Medeiros & Santos (1998) into three different
suites based on their lithotypes: Venturosa, Inhapi
and Palmares successions. The Venturosa succession occurs south of the Pernambuco shear zone,
southeast of the town of Arcoverde. Osako (2005)
showed that this succession is composed of quartzites and a series of meta-igneous and metasedimentary migmatites overlying Palaeoproterozoic
basement. This region also includes amphibolebearing migmatites which are considered to be
part of the Belém do São Francisco Complex
(Medeiros & Santos 1998) and which show sharp
contact with the metasedimentary rocks. The
Inhapi succession crops out in a wedge-shaped
area about c. 100 km long and c. 30 km wide
between the Águas Belas–Canindé suite to the
south and the Buique–Paulo Afonso suite to the
north. This succession shows pre- to syn-tectonic,
syn-tectonic and late- to post-tectonic garnetbearing S-type syenogranites intruded into
flat-lying, foliated metasedimentary units. The
metasedimentary rocks are represented mainly
by two associations: (a) locally migmatized
sillimanite –garnet –muscovite–biotite
gneisses,
with small carbonate lenses and common amphibolite lenses and (b) biotite –muscovite–garnet
gneisses, sometimes migmatized, with amphibolite
lenses and calc-silicate lenses. The Palmares succession is about 30 km wide and extends about
200 km NE from Palmeira dos Índios. It is
comprised of garnet gneisses, greywackes, and
amphibolites intruded by syn-tectonic tonalitic to
amphibole– granodioritic gneisses and gabbros.
This complex shows vergence to the NW (Medeiros
& Santos 1998).
The ages of these units are still poorly known,
and it is probable that grouping based primarily
on rock-type has lumped together units having
primary depositional or plutonic ages ranging
from Palaeoproterozoic (or older) to Brasiliano.
Brito Neves et al. (1995) presented Rb– Sr geochronological ages ranging between 1.13 Ga (diatexites)
and 0.96 Ga for rocks assigned to the Cabrobó and
Belém do São Francisco complexes in western
PEAL domain. Pessoa et al. (1978) reported a
Rb –Sr isochron of 1.53 + 73 Ma for tonalitic
orthogneisses from the Ibirajuba area. Very few
U –Pb ages have been reported for the PEAL
domain. Van Schmus et al. (1995) reported a
zircon
upper-intercept
apparent
age
of
1.58 + 73 Ma for garnet-bearing migmatite west
of Palmeira dos Indios. A single U –Pb zircon age
of 2.0 Ga was obtained by LA-ICPMS for migmatized tonalitic orthogneisses in the Jupi area, NE
of Garanhuns (Neves et al. 2005). Thus, in spite
of early interpretations of a Palaeoproterozoic to
Archaean age for most of the PEAL domain, few
direct ages confirm this. Lithostratigraphic terminology and correlations will have to be revised
extensively in the future as primary crystallization
or depositional ages are defined for individual
local units.
Santos (1995) and Van Schmus et al. (1995)
reported Sm–Nd TDM model ages for rocks of the
PEAL domain that range between 1.2 and 1.6 Ga;
a larger data set reported by Silva Filho et al.
(2002, 2005b) expanded this range to 0.9 –2.8 Ga
(Fig. 10). These data have a bimodal distribution,
indicating that most of the primary ages are either
Brasiliano or Trans-Amazonian. The low frequency
of samples with TDM from 1.5 to 1.8 Ga may indicate that Cariris Velhos igneous rocks, which commonly have TDM ages in this range (see Fig. 7), are
scarce or not found in the PEAL domain.
Isotopic subdomains. Silva Filho et al. (2002) evaluated PEAL crustal evolution based on Sm–Nd isotopic data from the Neoproterozoic granitoids, and
they defined two smaller crustal subdomains. New
Sm–Nd isotopic data from the metamorphic complexes, added to the original data, still show a
major two-fold grouping of model ages (Fig. 10).
However, when these data are coupled with geological mapping, the results indicate that the
two-fold subdivision of Silva Filho et al. (2002) is
an oversimplification. Five distinct model age subdivisions can be recognized (Fig. 9b). They are (a)
TDM older than 2.40 Ga, represented by several
local occurrences of gneiss and migmatite, (b)
TDM between 2.00 and 2.20 Ga, represented by
large areas in the northeastern half of the PEAL
domain, (c) TDM between 1.70 and 2.00 Ga, represented by several Brasiliano plutons in the NE
corner of the domain, (d) TDM between 1.20 and
1.50 Ga, represented by large parts of the southwestern half of the PEAL domain and (e) TDM between
0.90 and 1.20 Ga, represented mainly by the
Buique–Paulo Afonso batholith in the west and
the Palmares succession and adjacent orthogneisses
in the east. Of these, (a) corresponds to a small
cluster in Figure 10, (b) and (c) represent the
83
older large cluster in Figure 10, and (d) and (e) represent the younger large cluster in Figure 10. None
of the areas defined here are ‘pure’; that is, each
contains occurrences of younger or older TDM
depending on geological complexities within each
region. As more data become available, both from
the field and the laboratory, we expect that this
general picture will change in detail, in part
because of complexities due to tectonic imbrication.
Rio Grande do Norte and Ceará domains
The basement complex in the Rio Grande do Norte
domain is composed mostly of the 2.15 Ga Rio Piranhas massif, with a 2.6 –3.6 Ga Archaean remnant,
the São José do Campestre massif, in the east (Brito
Neves et al. 2000; Dantas et al. 1998, 2004) and
smaller remnants of Archaean crust dispersed irregularly elsewhere. Rocks with Transamazonian
crystallization or metamorphic ages (c. 2.15 Ga)
typically have Sm –Nd crustal residence ages
(TDM) of 2.4 to 3.0 Ga (Van Schmus et al. 1995;
Dantas 1997), indicating that these units were not
wholly juvenile when they formed (Fig. 11).
Younger Sm– Nd model ages in the Ceará domain
indicate greater amounts of juvenile Transamazonian contribution in the west (Fetter 1999).
Several metasedimentary and metavolcanic –
metasedimentary basins are present in the RGN/
CE domain. The oldest ones are the 1.8–1.7 Ga
intracratonic Orós and Jaguaribeano fold belts in
the eastern part of Ceará state (e.g., Sá et al.
1995), but few other sequences of similar age
20
Rio Grande do Norte Domain
Brasiliano plutons
Rio Piranhas basement (2.15Ga)
São José do Campestre nucleus
10
0
0.6
1.0
1.4
1.8
2.2
2.6
3.0
3.4
3.8
TDM (Ga)
Fig. 11. Sm– Nd TDM model ages from the Rio Grande do Norte domain. Mostly from Van Schmus et al. (1995) and
Dantas (1997).
84
have been documented in NE Brazil. The Seridó
fold belt is the largest Neoproterozoic fold belt in
the Rio Grande do Norte domain (Fig. 2).
SHRIMP U –Pb dating of detrital zircons in metagreywackes of the Seridó fold belt (Van Schmus
et al. 2003) shows the presence of a large, lateNeoproterozoic (c. 640 –650 Ma) population, indicating that the basin developed just prior to or
during the early phases of the Brasiliano orogeny
which caused its deformation and metamorphism
at c. 620 –580 Ma. C- and Sr-chemostratigraphic
data for marbles from the Jucurutu Formation in
the lower Seridó Group (Nascimento et al. 2004)
also support late Neoproterozoic (640–570 Ma)
deposition. Sm–Nd TDM ages of 1.1 to 1.5 Ga for
metasedimentary rocks of the Seridó fold belt
show that most of it was probably derived from
distal, younger sources rather than proximal, underlying Palaeoproterozoic basement (Van Schmus
et al. 2003). On the other hand, Palaeoproterozoic
Sm–Nd TDM ages for Brasiliano plutons which
intrude the Seridó Group (Dantas 1997; Hollanda
et al. 2003) show that it must overlie continuous
basement of the Rio Grande do Norte domain.
Médio Coreaú domain
The Médio Coreaú domain in the northwest corner
of the Borborema Province consists of Palaeoproterozoic basement with Neoproterozoic supracrustal rocks and Brasiliano plutons. This domain
separated from the Ceará domain by a major fault,
the Sobral fault, which is part of the Transbrasiliano
Lineament. Santos et al. (2008) discuss this domain
in detail and its correlation with the SE part of the
West African Craton and SW part of the
Pan-African fold belt. This domain is not central
to our discussion and will not be presented in
further detail.
Northern Congo Craton
The northern part of the Congo Craton is composed
of an Archaean core, the Ntem Complex, and peripheral Palaeoproterozoic rocks of the Nyong
Complex along the northwest margin of the Ntem
Complex. U –Pb zircon geochronology allows definition of three main stages of crustal evolution in
the Ntem Complex: (a) formation of greenstone
belt (ortho-amphibolites and metasedimentary
rocks) formed about 3.1 Ga, (b) a major phase of
crustal formation with emplacement of charnockite
and tonalite (TTG) about 2.9 Ga and (c) a final stage
corresponding to melting of greenstone belts and
TTG at deeper levels to form K-rich granitoids
between 2.7 and 2.5 Ga (Nédélec et al. 1990;
Toteu et al. 1994; Tchameni et al. 2000; Shang
et al. 2004). Most Sm–Nd TDM ages are similar
to U– Pb zircon ages indicating that this Archaean
core is essentially juvenile.
The Nyong Complex is dominated by metasedimentary rocks, including quartzite, paragneiss,
schist and migmatite. This complex is largely at
granulite grade as a result of the c. 2050 Ma
(Eburnian–Transamazonian) fusion of the Congo
and São Francisco cratons (Ledru et al. 1994;
Penaye et al. 2004; Lerouge et al. 2006) during
assembly of a middle to late Palaeoproterozoic continent (e.g., ‘Atlantica’ of Rogers 1996). Lerouge
et al. (2006) summarized detrital zircon ages from
Nyong Complex metasedimentary rocks and
found a range of 2400 to 3100 Ma, similar to that
for the core of the Congo Craton. These ages and
compositions should be reflected in any material
in the Central African Fold Belt that was derived
from the Congo Craton.
Central African Fold Belt
The late Neoproterozoic (Pan-African) Central
African Fold Belt north of the Congo Craton was
recognized in the early 1960s by the widespread
occurrence of c. 500– 600 Ma Rb–Sr whole rock
and mineral ages (Lasserre 1967). This fold belt
underlies Cameroon, Chad, and the Central
African Republic, between the Congo Craton to
the south and the Western Nigerian Shield to the
north (Figs 1 & 12) and corresponds to the southern
part of the Saharan metacraton (Abdelsalam et al.
2002; Toteu et al. 2004). Interactions between this
mobile domain and the major cratons are only partially understood. Along the eastern border of the
West African Craton evolution seems to be well
constrained between 630 and 580 Ma, with eastward subduction followed by the collision
between the craton and the Tuareg –Nigerian
shield (Caby 1989; Santos et al. 2008). On the
northern edge of the Congo Craton, the tectonic
evolution is still enigmatic since no clear evidence
of oceanic rocks has yet been found, despite many
features that characterize a collisional belt: longlived (800– 600 Ma) arc-type magmatism, external
nappes of regional extent, granulitic metamorphism, intensive plutonism associated with crustal
melting, regional strike-slip faults (some of which
extend to NE Brazil), and the possible presence of
molasse basins. Proposed tectonic models broadly
correspond to collision between the Congo Craton
and the mobile belt (Abdelsalam et al. 2002) or collision among different blocks within the mobile belt
(Toteu et al. 2004).
The following domains can be distinguished in
the Central African Fold Belt north of the Congo
Craton (Toteu et al. 2004). The Yaoundé domain
extends east– west north of the Congo Craton and
85
Fig. 12. Geological map of Cameroon showing major lithotectonic suites and domains. Modified from Toteu et al.
(2001). AF, Adamawa fault; KCF, Kribi– Campo fault; SF, Sanaga fault; TBF, Tcholliré–Banyo fault.
in large part consists of units thrust southwards over
the craton; it continues eastwards as the Oubanguide
Belt in the Central African Republic. The
Adamawa–Yadé domain extends eastwards from
central Cameroon and is bordered on the north by
the Tcholliré–Banyo fault and on the south by the
Yaoundé domain; it is a complex and heterogeneous
domain of Palaeo- to Neoproterozoic high-grade
86
20
All Central Africa
Fold Belt Samples
NW Cameroon Domain
Adamawa-Yade Domain
Yaoundé Domain
Congo Craton
10
0
0.6
1.0
1.4
1.8
2.2
TDM (Ga)
2.6
3.0
3.4
3.8
Fig. 13. Sm–Nd TDM model ages from the Central African Fold Belt.
rocks extensively intruded by Pan-African granitoids and cut by late transcurrent faults. The NW
Cameroon domain occurs NW of the Tcholliré –
Banyo fault and is characterized by lesser contributions of Palaeoproterozoic crust in the
Pan-African plutonic rocks, suggesting that Palaeoproterozoic basement is discontinuous to absent. Its
westward continuation is ambiguous since isotopic
data indicate that Palaeoproterozoic inheritance is
more important in the Eastern Nigeria terrane. Geophysical information across the Benue Trough will
be necessary in the future to determine whether or
not the Eastern Nigeria terrane belongs to a different
block and is separated from the NW Cameroon
domain by a major crustal boundary.
Yaoundé domain of Cameroon and Central
African Republic
The Yaoundé domain (Fig. 12) contains three major
units: (a) low to medium-grade schists of the
Mbalmayo group, passing in continuity northwards
to (b) a unit of garnetiferous micaschists and
gneisses, granulites and migmatitic gneisses of the
Yaoundé Group (Nédélec et al. 1986; Nzenti et al.
1988); (c) a Bafia Group of assumed Palaeoproterozoic age that consists of high-grade gneisses and
orthogneisses (Noizet 1982; Tchakounté 1999).
The Mbamayo and Yaoundé groups are
dominated by metasedimentary rocks (pelites,
meta-greywackes, quartzites, amphibolites, talcschists) and meta-plutonic rocks (meta-diorites,
meta-gabbros, meta-syenites, meta-granites and
meta-peridotites), all of which were involved in
Pan-African nappe formation (Toteu et al. 2006b).
Figure 13 illustrates Sm–Nd TDM ages for rocks
of the Yaoundé domain and their potential
sources. The bulk of the detritus in Yaoundé
domain metasedimentary rocks may have come
from sources to the north, rather than from the
Congo Craton (Penaye et al. 1993; Toteu et al.
1994, 2001), which is comparable to the case for
the Sergipano domain in Brazil (Oliveira et al.
2006). The presence of c. 626 Ma detrital zircon
in a Yaoundé mica-schist suggests it was deposited
after this age (Toteu et al. 2006a), making sedimentary units of the Yaoundé domain essentially coeval
with units from the Sergipano domain. The
Yaoundé domain metasedimentary rocks are interpreted as the products of reworking of Neoproterozoic Pan-African arc rocks developed in the
southern part of the Adamawa–Yadé domain
(Toteu et al. 2006a).
The Bafia Group is poorly known. From the tectonic point of view it is part of the Yaoundé domain
as it is involved in the nappe tectonics. However,
available Sm–Nd TDM ages (all Palaeoproterozoic)
suggest that this group may be part of the
Adamawa– Yadé domain. It may comprise a tectonic intercalation of Neoproterozoic, Mesoproterozoic (?) and Palaeoproterozoic units (Toteu et al.
2001, 2006a). The main difference relative to the
Yaoundé Group is the scarcity of metapelitic
rocks and abundance of meta-greywackes (biotite
and amphibole gneisses) and amphibolites. Both
groups were intruded by Pan-African granitoids
prior to nappe formation.
Deformation history in the Yaoundé domain
involved two successive episodes, D1 and D2,
87
with peak conditions of the Pan-African granulite
facies metamorphism occurring between D1 and
D2. D2 regional flat-laying foliation is the result of
southward-directed thrusting (Toteu et al. 2004,
2006b) or extension (Mvondo et al. 2003). The lowgrade rocks of the Mbalmayo Group are interpreted
as the sole of the nappes (Nédélec et al. 1986). The
high-grade metamorphism in the Yaoundé region is
constrained between 620 and 610 Ma (Penaye et al.
1993; Toteu et al. 1994, 2006b; Stendal et al. 2006).
The Yaoundé Group underwent a rapid evolution
(deposition, burial and metamorphism to granulite
facies, followed by exhumation and thrusting onto
the Congo Craton) in a time span of about 20 Ma
(Toteu et al. 2006b).
underlain by Palaeoproterozoic crust, but the
younger Sm –Nd model ages indicate that significant amounts of detritus must have come by
lateral transport from presently unknown, but
younger and probably Neoproterozoic, sources.
The Yadé massif in the Central African Republic
is a poorly surveyed complex of granitic gneiss that
has been assumed to be Archaean (Poidevin 1991).
However, its proximity with the Adamawa domain
in Cameroon and the continuity of structures
suggest that the Yadé massif is probably an
eastern continuation of that domain, consistent
with current field work and Sm –Nd isotopic
studies indicating that the Yadé massif is underlain
by Palaeoproterozoic crust.
Adamawa – Yadé domain
NW Cameroon domain
The Adamawa –Yadé domain (Toteu et al. 2004) is
characterized by Palaeoproterozoic upper intercept
ages for zircons and by Palaeoproterozoic to
Archaean Sm–Nd TDM ages recorded in both metasedimentary rocks and orthogneisses. This indicates
that the domain is underlain by Archaean –
Palaeoproterozoic basement. However, although
2.1 Ga granulitic metamorphism has been proposed
(Toteu et al. 2001), no clear Palaeoproterozoic
relict metamorphic age (garnet or titanite) has so
far been recorded. The domain includes: (a) remnants of metasedimentary rocks and orthogneisses
showing retrogressed granulitic metamorphism;
(b) the Lom schist belt, which is composed of
low- to medium-grade metasedimentary rocks and
felsic volcaniclastic rocks with Pan-African amphibolite facies metamorphism; (c) the poorly known
‘Yadé Massif’ in the Central African Republic;
(d) widespread syn- to late-tectonic granitoids of
transitional composition and crustal-derived origin.
Although Palaeoproterozoic juvenile material
exists in some areas of this domain, Sm –Nd TDM
ages (Fig. 13) and inherited zircons show that
most basement rocks were derived from recycling
(melting or erosion and sedimentation) of Archaean
crust similar in age to the Congo Craton. This is also
the case for the Nyong Series in SW Cameroon,
which is regarded as southern extension of
basement rocks of the Adamawa region (Toteu
et al. 2001) but which has remained linked
with the Congo Craton during Neoproterozoic
fragmentation.
Toteu et al. (2006a) reported U –Pb ion microprobe ages for zircons from metasedimentary and
metavolcanic rocks of the Lom Basin of the
Adamawa –Yadé domain in eastern Cameroon.
These data show that depositional ages for the
supracrustal rocks are late Neoproterozoic, with
detrital zircons up to 2800 Ma and Sm –Nd TDM
ages of 1.4 to 2.2 Ga. This basin is probably
The NW Cameroon domain lies west of the
Tcholliré –Banyo shear zone and continues into
eastern Nigeria and southwestern Chad (Figs 12 &
14). It consists of (a) Neoproterozoic medium- to
high-grade schists and gneisses of volcanic and
volcano-sedimentary origin (Poli Group) that were
formed c. 700 Ma on, or in the vicinity of, young
magmatic arcs (Toteu et al. 2006a), (b) Pan-African
pre-, syn-, to late-tectonic calk-alkaline granitoids
emplaced between 660 and 580 Ma (Toteu et al.
1987, 2001; Penaye et al. 2006), (c) post-tectonic
alkaline granitoids which comprise mafic and
felsic dykes cross-cut by sub-circular granites and
syenites and (d) numerous basins with low-grade
metasedimentary and metavolcanic rocks that may
correspond to molasse deposits of the Pan-African
orogeny (Montes-Lauar et al. 1997). Rocks of the
NW Cameroon domain commonly yield Mesoproterozoic to Neoproterozoic Sm– Nd model ages,
without the abundant Palaeoproterozoic ages
found in the Adamawa –Yadé domain (Fig. 13).
This, along with Rb–Sr and U – Pb data, indicate
that most of the gneissic and granitic rocks of this
domain are Neoproterozoic with relatively low contribution from 2.1 Ga crust. No Archaean inheritance has yet been recognized (Toteu et al. 2001),
but sampling is still relatively sparse.
Toteu et al. (2006a) reported new U –Pb ages
and Sm–Nd TDM ages for various units in the Poli
region in NW Cameroon. They documented
c. 920–730 Ma metavolcanic rocks and detrital
magmatic zircons in the supracrustal suite. Sm–
Nd TDM ages of 0.8 to 1.1 Ga for these rocks indicate a substantial juvenile component. To the NE
of Poli, in the Mayo Kebi region of SW Chad,
Penaye et al. (2006) reported U –Pb zircon ages of
c. 740 Ma with Sm–Nd TDM ages of 0.6 to 0.8 Ga
for gabbroic to dioritic rocks that have been interpreted as part of a juvenile arc that lies parallel to
and on the NW side of the Tcholliré– Banyo shear
88
Fig. 14. Geological map of northern Cameroon, adjacent parts of Nigeria, Chad, and the Central African Republic, and
areas in the Saharan region to the north. Modified from Figure 7 of Penaye et al. (2006). ‘1 Ga’ denotes region from
which de Wit et al. (2005) reported c. 1000 Ma gneisses. TBF, Tcholliré–Banyo fault.
zone. Other plutonic units in the Mayo Kebi area
yield U –Pb ages of 640 to 665 Ma, with one late
pluton at c. 567 Ma. This region is particularly
notable because it clearly documents the existence
of Pan-African juvenile rocks in the Central
African Fold Belt (Penaye et al. 2006; Pouclet
et al. 2006). It also suggests that the Tcholliré–
Banyo shear zone is a major terrane boundary in
Cameroon, with dominantly juvenile Neoproterozoic upper crust on the NW side and Palaeoproterozoic crust on the SE side.
The westward extent of this juvenile belt is not
well constrained. Geological control in the region
(Penaye et al. 2006) and Sm –Nd TDM ages (Toteu
et al. 2001) suggest that it is a narrow juvenile
belt with rocks to the west, especially in eastern
Nigeria, containing a greater Palaeoproterozoic
component (see following).
Nigeria and Sahara
The eastern part of the Nigerian shield appears to be
westward continuation of the Central African Fold
Belt. U –Pb results and Sm– Nd TDM ages reported
by reported by Dada (1998), Ekwueme & Kröner
(2006) and Ferré et al. (1996, 1998, 2002) show
that, while Pan-African metamorphism and
magmatism dominate the tectonic history of the
region from 660 to 580 Ma, Palaeoproterozoic
basement, presumably c. 2.2–2.0 Ga (Birimian/
Eburnian-age) crust, is ubiquitous and dominates
the Sm –Nd model ages. This is also true for
Pan-African granites, which have TDM ages of
c. 2.0 Ga; Mesoproterozoic or younger TDM ages
seem to be lacking in eastern Nigeria. This is consistent with the suggestion above that the Poli–
Mayo Kebi terrane is a narrow juvenile belt, with
western parts of the NW Cameroon domain more
similar to eastern Nigeria or to the Adamawa –
Yadé domain.
Ferré et al. (1996, 2002) argued that there is a
major north–south boundary in Nigeria which separates the Eastern Nigeria terrane from a dominantly
Palaeoproterozoic –Archaean
Western
Nigeria terrane. Ekwueme & Kröner (1993) and
Bruguier et al. (1994) reported Archaean U –Pb
ages of c. 3.5 Ga in the Kaduna region in the northern part of the Western Nigeria terrane, enhancing
the contrast with the Eastern Nigeria terrane.
Liégeois et al. (1994) presented a tectonic history
for the Aı̈r Massif in the southeastern Tuareg
Shield, to the north of the Nigerian terranes. They
argued for a major terrane boundary between the
eastern and western part of the massif, and this
boundary can be continued southwards to match
up with the terrane boundary between the Western
Nigeria and Eastern Nigeria terranes (Fig. 14).
Gneissic basement in eastern Chad (western
89
Darfur region) yields U –Pb zircon ages of c.
1.0 Ga with Sm –Nd TDM ages of 1.70 to 3.0 Ga
(de Wit et al. 2005). This suggests that the Darfur
region may be northeastward continuation of the
Adamawa –Yadé domain.
Geological links between the
Borborema Province and the Central
African Fold Belt
Sm –Nd model ages, in conjunction with U –Pb
zircon ages and other geological data, show that
Palaeoproterozoic (and locally Archaean) basement
gneisses occur discontinuously throughout most of
the Borborema Province and the Central African
Fold Belt, either as discrete basement blocks and
terranes, lower crust inferred from isotopic studies
of younger plutons, or as protoliths to Brasiliano
and Pan-African metamorphic complexes. These
same data show that Neoproterozoic supracrustal
sequences also occur throughout the region, as
thin units on Palaeoproterozoic basement, as thick
sequences in deep basins with no known basement,
or as clearly juvenile terranes between major structural boundaries. The presence or absence of
Palaeoproterozoic basement, either at the surface
or at depth, and the distribution of Neoproterozoic
supracrustal sequences are an important aspect of
correlation between Brazil and Africa. In this
section we will examine these correlations, beginning in the south with the stable cratons.
Correlation between Congo Craton and São
Francisco Craton
It is widely accepted that before the Mesozoic
break-up of Gondwana the São Francisco and the
Congo cratons were part of a larger continent, and
these cratons are deformed on their margins by
Pan-African/Brasiliano orogens (e.g., Alkmim
et al. 2001). Both cratonic areas contain Archaean
nuclei such as the Jequié, Gavião, and Serrinha
blocks in Brazil and the Ntem, Equatorial Guinea,
Gabon, and Congo blocks in western Central
Africa. These nuclei have ages ranging from 3.4
to 2.6 Ga (Toteu et al. 1994; Barbosa & Sabaté
2004; Caen-Vachette et al. 1988; Campos et al.
2003; Kosin et al. 2003; Oliveira et al. 2004;
Shang et al. 2004; Milesi et al. 2006 and were
amalgamated during 2.2–2.0 Ga orogenesis. This
amalgamation is represented in Brazil by the
Itabuna –Salvador–Curaçá orogen (e.g., Teixeira
& Figueiredo 1991; Barbosa & Sabaté 2004;
Oliveira et al. 2004) and in Africa by the West
Central African Belt, which is a Palaeoproterozoic
structure that extends south from Cameroon, along
the western side of the Congo Craton (Feybesse
90
et al. 1998, Penaye et al. 2004). These two Palaeoproterozoic collisional belts match each other very
well on a pre-drift reconstruction of South
America–Africa and are mainly composed of highgrade gneisses, syn- to late tectonic granitoids and
terrigenous molasse (Jacobina Basin and upper
units of Francevillian Basin).
The Palaeoproterozoic collisional belt between
the northeastern part of the São Francisco Craton
and the northwestern part of the Congo Craton is
continuous on pre-drift reconstructions, without evidence of any Brasiliano/Pan-African suture. To the
south, however, there is evidence of opening of a rift
in the southern part of the Palaeoproterozoic craton,
forming a south-facing oceanic basin that was closed
at the north end (Pedrosa-Soares et al. 1992). Correlative late Mesoproterozoic to early Neoproterozoic
(1100–910 Ma) magmatic and sedimentary
sequences on the eastern edge of the São Francisco
Craton and western edge of the Congo Craton
include the Ilhéus–Salvador mafic dyke swarms
(Correa-Gomes & Oliveira 2000) and the West
Congo Supergroup (Tack et al. 2001). Closure of
this basin during assembly of West Gondwana
produced the Araçuaı́–West Congo orogen.
Alkmim et al. (2006) have presented a ‘nutcracker’
model in which they argue that the northern end
remained closed because of rotation between the
São Francisco and Congo cratons, with an early
Neoproterozoic opening phase followed by a late
Neoproterozoic (Brasiliano/Pan-African) closing
phase and a pivot point at the north end of
the orogen.
Correlation between the Sergipano and
Yaoundé domains
The major feature of the Sergipano and Yaoundé
domains is their formation as a result of the continental collision between the Pernambuco –Alagoas
(PEAL) and Adamawa –Yadé massifs to the north
and the São Francisco and Congo cratons to the
south. The resulting structure in both regions is
the nappe stacking of tectono-stratigraphic units
with different characteristics.
Dating of detrital zircons in the Sergipano
domain shows that lithostratigraphic domains are
broadly young (,650 Ma) and probably formed
between 630 and 600 Ma apart from the Estância
subdomain foreland basin (Fig. 3). The Macururé
subdomain, which does not yield detrital zircons
younger than 850 Ma, could be older; the
628–625 Ma intrusive granitoids indicate that they
may have been deposited at any time between 850
and 625 Ma. Except for the Estância subdomain,
for which an equivalent has not yet been found in
Cameroon, ages obtained for the other domains of
the Sergipano domain can be found in Cameroon.
For example, the Yaoundé mica-schists yield a
detrital zircon age of 626 Ma comparable to that of
Vaza Barris and Canindé subdomains. On the other
hand, detrital zircon from the Mahan amphibolite
in Cameroon yielded ages of 1072 and 820 Ma
(Toteu et al. 2006a), comparable to the ages recorded
in the Macururé and Marancó subdomains in Brazil.
New SHRIMP geochronology, Sm–Nd model
ages, and major and trace element data for units of
the Sergipano domain indicate that the Canindé
subdomain is the root of a 715–680 Ma rift-related
volcano-plutonic-sedimentary sequence (Nascimento et al. 2005). The Poço Redondo gneiss
migmatite subdomain is possibly the root of a
980–960 Ma Andean-type batholith intruded by a
post-collision A-type batholith (c. 950 Ma) and
intensively reworked during the Late Neoproterozoic (Carvalho et al. 2005). Sedimentary provenance studies on the Marancó and Macururé
metasedimentary subdomains indicate detritus provenance mostly from 980–1020 Ma old terranes,
possibly the Poço Redondo subdomain or Cariris
Velhos-age terranes farther north (Oliveira et al.
2006); no detrital zircons younger than 900 Ma
were found in these metasedimentary rocks. On
the other hand, the southernmost Vaza Barris and
Estância
subdomains
contain
Brasiliano/
Pan-African age detrital zircons (680–570 Ma)
probably derived from Brasiliano/Pan-African
granitoids, in addition to older Meso- to Neoproterozoic (920– 1110 Ma) and Archaean zircon grains.
The uppermost sedimentary units of these two subdomains are interpreted as having been deposited
on peripheral foreland basins, with detritus coming
mostly from terranes to the north (Oliveira et al.
2006). Zircon provenance studies in Cameroon are
scarce: Toteu et al. (2006a) and Toteu et al. (2001)
suggested that metasedimentary rocks in the
Yaoundé domain are mainly the product of detritus
from Neoproterozoic magmatic arcs and Palaeoproterozoic igneous basement of the Adamawa–Yadé
domain, although a few Archaean xenocrysts are
also present. Sm–Nd model ages (Toteu et al.
2001) are compatible with sediment transport from
the north with insignificant or no contribution from
the Congo Craton. Geological units in the age
range 980–950 Ma, comparable to rocks from the
Cariris Velhos orogen (Brito Neves et al. 1995),
have not yet been found in Cameroon, but there is
a strong possibility that they might be found in the
future as zircons of this age are already reported
elsewhere in Central Africa (de Wit et al. 2005;
Toteu et al. 2006a).
Both domains are dominated by south-verging
Brasiliano/Pan-African thrusting that lead to nappe
stacking upon the Congo–São Francisco cratons.
Boundaries between tectono-stratigraphic units are
well defined in the Sergipano domain. In the
Yaoundé domain they are assumed, since detailed
geological mapping is lacking in much of the
region. All plutonic rocks of both belts are involved
in this thrusting and nappe formation. To the north of
both belts, e.g., in the PEAL domain of the Borborema Province and Adamawa–Yadé domain of the
Central African Fold Belt, there is extensive development of late- to post-tectonic granitoids and strikeslip shear zones. This suggests that plutonism in both
regions continued after nappe emplacement.
Both regions are characterized by a decrease in
metamorphic grade towards the cratons. In the Sergipano domain there is no direct estimate of the age
of the metamorphism. However, the minimum age
of Pan-African/Brasiliano collision is constrained
by a pre-D2 tonalite intrusion in the Sergipano
domain dated at 628 + 12 Ma (Bueno et al.
2005). Consistent Sm– Nd whole rock–garnet pair
and Pb –Pb step-leaching ages on garnet constrain
metamorphism in the Yaoundé domain between
616 and 611 Ma, which broadly corresponds to
the onset of nappe formation that continued until
about 600 Ma (Toteu et al. 2006b; Stendal et al.
2006). The presence of 620 + 10 Ma, pré-D2 granulite facies meta-diorite in the Yaoundé series
(Toteu et al. 1994) suggests that the collisional
event is broadly coeval in both belts.
Correlation of PEAL and Transverse
domains of NE Brazil with the Central
African Fold Belt
A common feature within the central domains of
both the Borborema Province (Pernambuco–
Alagoas and Transverse domains) and the Central
African Fold Belt (Adamawa –Yadé and NW
Cameroon domains, Eastern Nigeria terrane) is the
prevalence of metasedimentary, metavolcanic, and
meta-plutonic rock units with Sm–Nd model ages
(TDM) between 1.0 and 1.6 Ga, substantially
younger than in domains to the south (São
Francisco and Congo cratons) and north (Rio
Grande do Norte domain, Western Nigeria
terrane). U –Pb ages of detrital zircons in metasedimentary rocks or of igneous zircons in plutons show
that most of the rock units with Mesoproterozoic
TDM ages probably formed between 1.0 and
0.6 Ga, with the apparent Mesoproterozoic model
ages being due to mixing of variable amounts of
Palaeoproterozoic to Archaean crustal material
with 1.0 to 0.6 Ga juvenile material. Brasiliano
and Pan-African plutons emplaced into Palaeoproterozoic crust normally show Palaeoproterozoic
Sm–Nd model ages, reflecting the sources of the
magmas. Young plutons emplaced into Neoproterozoic metasedimentary rocks overlying older basement may also show Palaeoproterozoic Sm–Nd
model ages, but in this case they reflect magma
91
generation from older crust underlying the
younger supracrustal rocks.
In many Neoproterozoic metasedimentary
sequences in NE Brazil (e.g., Cariris Velhos,
Cachoerinha, Sergipano, parts of the PEAL
domain) the Sm –Nd model ages in Brasiliano
plutons are Mesoproterozoic (1.0–1.6 Ga), often
virtually the same as the TDM ages of the host metasedimentary rocks. In these cases it is difficult to
argue for significant contribution of underlying
Palaeoproterozoic crust to generation of the
magma. Although Sm –Nd model ages alone can
usually delineate regions of thick post-Palaeoproterozoic (probable Neoproterozoic) crust,
zircon ages are required to determine accurate and
precise crystallization or maximum depositional
ages within the Neoproterozoic. For these supracrustal sequences we must conclude that either the
basins were very deep (.20 km, with or without
Palaeoproterozoic basal crust) so that they could
be melted to form the granite magmas, or that
juvenile, late Neoproterozoic mantle-derived
magma fortuitously mixed with Palaeoproterozoic
crust to yield Mesoproterozoic TDM ages.
Neoproterozoic rocks with Mesoproterozoic
model ages also occur in the Central African Fold
Belt, notably in the Yaoundé Group (presented
above), the Lom basins in the Adamawa domain,
and the Poli Basin in the NW Cameroon domain.
Pan-African granites in the region also commonly
show Mesoproterozoic TDM ages, although they
are more dominant in the NW Cameroon domain
than in the Adamawa–Yadé domain (Fig. 13). In
general, however, the abundance and distribution
of such plutons are not as well known in the
Central African Fold Belt, making precise
correlations with the Borborema Province of
Brazil difficult.
There are two major structures in Cameroon that
project westwards toward Brazil: the Tcholliré –
Banyo fault and the cross-cutting Adamawa fault.
As argued above, the Tcholliré –Banyo fault
appears to be a significant terrane boundary, with
lesser contributions from Palaeoproterozoic crust
in the NW Cameroon domain than in the
Adamawa –Yadé domain. A potential counterpart
in Brazil, based on geology (Fig. 9) and spatial
relationships (Fig. 1) could be the northern margin
of the Sergipano domain, which continues westwards as the Macururé shear zone (Fig. 3), separating the Sergipano domain from the central part
of the PEAL domain. A consequence of this correlation is that the c. 750–640 Ma Poli–Mayo Kebi
terrane in Cameroon– Chad (Figs 12 & 14) and
the c. 720–630 Ma Canindé subdomain in Brazil
(Fig. 3) would both lie on the north side of the
boundary, perhaps being remnants of juvenile complexes along a major rift and/or suture.
92
The Adamawa fault is a younger transcurrent
feature within the Adamawa domain and has commonly been extrapolated to join with the Pernambuco shear zone, which is similarly a late-tectonic
transcurrent feature (Neves & Mariano 1999).
Neither appears to represent a significant terrane
boundary, so that although the correlation is permissible, it is not well constrained by geological
relationships. The extrapolation of these two structures towards each other is not well aligned in the de
Wit et al. (1988) reconstruction used (Fig. 1),
suggesting either that they are not correlated or
that the fit between Cameroon and NE Brazil
needs to be modified.
There are also some major structures in the
Transverse domain of Brazil which project eastwards toward Africa. One is the boundary
between the Alto Moxotó terrane and the Rio Capibaribe terrane (Fig. 6). The Rio Capibaribe terrane
consists of Palaeoproterozoic basement, late Neoproterozoic supracrustal rocks (e.g., Suburim
schists, Neves et al. 2005, 2006), and Brasiliano
granites. This terrane bears superficial resemblance
to western parts of the NW Cameroon domain, NW
of the Poli–Mayo Kebi terrane, although an exact
comparison is not possible with the limited data
currently available.
The Alto Moxotó terrane is somewhat different
from the two terranes which flank it in the Transverse domain. Unlike the Rio Capibaribe terrane,
the Alto Moxotó terrane contains relatively few Brasiliano plutons or supracrustal rocks and is dominated by c. 2.1 Ga Palaeoproterozoic crust (Brito
Neves et al. 2001b). In this respect it is more like
the Eastern Nigeria terrane, which is dominated by
Palaeoproterozoic crustal parentage (TDM c.
2.0 Ga). Although the Eastern Nigeria terrane has
abundant Pan-African plutons (see Ferré et al.
2002), this could be a local manifestation in an
otherwise dominantly Palaeoproterozoic terrane. If
this correlation is valid, then the boundary
between the Alto Moxotó and Rio Capibaribe terranes could continue from eastern Brazil (Fig. 6)
into the covered region (Benoue Trough) between
eastern Nigeria and NW Cameroon (Figs 1 & 14).
The Alto Pajeú terrane, with its included Cariris
Velhos orogen, is quite different from all other terranes in both Brazil and Africa. Although it includes
some Palaeoproterozoic remnants, it is dominated
by early Neoproterozoic crustal rocks formed at
990– 940 Ma. There are major contrasts with terranes on either side: the Alto Moxotó terrane on
the south is dominantly Palaeoproterozoic gneiss,
whereas the Palaeoproterozoic basement of the
Rio Grande do Norte domain on the north includes
a significant Archaean component as well as a discrete 3.5 Ga Archaean block (Fig. 2). So far no
counterpart to the Alto Pajeú terrane is known in
Africa, and it is shown in Figure 1 as pinching out
eastward. Thus, its northern and southern boundaries merge to become a major terrane boundary
in Nigeria and to the north (see below).
One consequence of the correlations proposed
above is that, whereas the Pernambuco–Alagoas
and Transverse domains in Brazil correlate with
the NW Cameroon and Eastern Nigeria domains
in Africa (Fig. 1), there is no major counterpart on
the Brazilian side to the Adamawa–Yadé domain
of Africa. Furthermore, because of relatively poor
geological control, there is no clearly defined
boundary in Cameroon between the Yaoundé
domain and the Adamawa domain. These are problems that will have to await future resolution.
Western Nigeria terrane – Tuareg Shield– Rio
Grande do Norte/Ceará domains
The eastern part of the Patos shear zone in Brazil
represents a major terrane boundary between
Archaean and Palaeoproterozoic cratonic rocks of
the Rio Grande do Norte domain and dominantly
early Neoproterozoic (Cariris Velhos) to Brasiliano
rocks of the Alto Pajeú terrane. Recent work (e.g.,
Brito Neves et al. 2001a) shows that this terrane
boundary follows a fault that swings northeast
before it leaves the continent north of João Pessoa
(Fig. 2). In Gondwana reconstructions, this boundary trends into Nigeria and can easily be aligned
with the major terrane boundary (Fig. 14) that separates the Archaean –Palaeoproterozoic Western
Nigeria terrane from the Eastern Nigeria terrane
(Ferré et al. 1996). This boundary can, in turn, be
aligned northward with a major terrane boundary
in the Aı̈r massif and which separates Central
Hoggar from Eastern Hoggar in the Tuareg Shield
(Liégeois et al. 1994; Caby 2003; Fig. 14). This proposed alignment separates older cratonic basement
on the north and west (Rio Grande do Norte
domain, Western Nigeria terrane, Central Hoggar)
from terranes which consist of a collage of isolated
Palaeoproterozoic blocks and Neoproterozoic
basins (Transverse domain in Brazil, NW Cameroon domain, Eastern Nigeria terrane, and western
parts of the Saharan metacraton) (Figs 1, 2 & 14).
Continuation of this boundary west and SW of the
city of Patos in Brazil is not well constrained,
although it probably trends SW along the west
side of the Cachoerinha Belt (Boqueirão dos
Conchos shear zone, Fig. 2).
Médio Coreaú domain and West African
Craton
The northwestern part of the Borborema Province
contains a major fault where the Médio Coreaú
domain is joined to the Ceará domain. This Sobral
fault is part of the Transbrasiliano lineament
(Fig. 2), and it has commonly been correlated with
the Kandi fault east of the West African Craton
(Caby 1989; Castaing et al. 1993, 1994; Brito Neves
et al. 2002; Fetter et al. 2003; Santos et al. 2008).
São Francisco/Congo craton – Boborema
Province/Central African Fold Belt/Sahara –
West Africa/Angola craton history
We believe that the São Francisco and Congo
cratons are relatively undeformed remnants of a
large Palaeoproterozoic continent that extended
northwards throughout the Borborema Province
and central and northern Africa. At some time the
northern part of this continent underwent major
crustal extension, creating a large expanse of
faulted Palaeoproterozoic crust with major depositional basins created over down-dropped blocks or
where extension may have created small oceanic
rifts. Because the oldest metasedimentary and metavolcanic rocks associated with these basins are earliest Neoproterozoic (about 1 Ga; Cariris Velhos in
Brazil), we believe that this is a likely time for onset
of extensional tectonics. Because extension was
also occurring to the south in the subsequent
Araçuaı́ –West Congo orogen, extension in the Borborema Province –West African Fold Belt may
have resulted largely from northward movement
of crustal blocks farther north, perhaps during
separation of the Amazonian–West African
craton from the São Francisco Craton– Congo
Craton –Saharan metacraton to form a major Neoproterozoic ocean (e.g., Alkmim et al. 2001).
Kröner & Cordani (2003) argued that, while the
West African Craton and the Amazon Craton
were part of Rodinia, there was a major
Neoproterozoic ocean between them and the São
Francisco –Borborema–Central
African
Fold
Belt –Sahara –Congo continental complex.
Evidence for c. 700 –800 Ma sequences and
igneous rocks in both Brazil and Africa may
testify to a second pulse of extension in the
middle Neoproterozoic, and some of the oceanic
rifts may have closed about 640 Ma, preserving
remnants of juvenile terranes (e.g., Poli– Mayo
Kebi terrane in the Central African Fold Belt,
Canindé subdomain in Brazil). Subsequent late
Neoproterozoic convergence resulted in assembly
of West Gondwana, with substantial terranes of
juvenile crust accreted between the Amazon
and São Francisco cratons (Pimentel et al. 2000)
and between the West African Craton and the
Saharan metacraton. The assembly of all these
terranes, domains and cratons resulted in
extensive deformation, metamorphism, and
93
granitic magmatism from about 640 to 540 Ma,
with the major peak of activity between 620 and
580 Ma. The proposed ‘nutcracker’ cycle proposed
for the Araçuaı́ –West Congo orogen (Alkmim
et al. 2006) further indicates that motions
between and among cratons during assembly of
this part of West Gondwana must have been
very complex.
Van Schmus acknowledges support from several NSF
grants from 1983 to 2002 in support of his studies in
Brazil and Cameroon, with additional support from the
Department of Geology, University of Kansas. He also
gratefully acknowledges the collaborative research with
many students and colleagues during this time, including
but not limited to Marly Babinski, B. Bley de Brito
Neves, Umberto Cordani, Elton Dantas, Allen Fetter,
Peter C. Hackspacher, Emanuel F. Jardim de Sá, and
Marianne Kozuch.
E. P. Oliveira acknowledges the financial support of
the Brazilian agencies CNPq (301025/2005-3) and
FAPESP (02/03085-2, 02/07536-9). A.F. da Silva Filho
acknowledges the financial support of the Brazilian
agencies CAPES (AEX0753/99-8), CNPq (521.031/
95-8, 520.012/96-8) and FINEP (88.98.0745.00). He
also acknowledges the important contribution of research
students M. F. Lyra de Brito, L. Osako, C. Carmona, E.
B. Luna and D. V. Siqueira, and the colleagues B. Bley
de Brito Neves, E. J. dos Santos and J. M. Rangel da
Silva. The isotopic work was carried out in the Isotope
Geochemistry Laboratory (IGL), University of Kansas.
He is very grateful to M. Kozuch and to Allen Fetter for
their technical support in the IGL. Cameroon portions of
this work were supported in early phases by the Institute
for Geological and Mining Research (IRGM) in Cameroon, which supported field work in northern Cameroon
and isotopic analyses at CRGP, Nancy (France). In
1993, S. F. Toteu benefited from special funding from
Cimentéries du Cameroun (CIMENCAM) to organize a
field trip for sample collection in north-central Cameroon.
He also wishes to pay special tribute to the United States
Information Agency, which awarded him a Fulbright
Grant in 1993 for a six-month visit at the IGL, University
of Kansas.
Much research that forms the basis for this report was
done in conjunction with IGCP-426, Granite Systems and
Proterozoic Lithospheric Processes, and IGCP-470, The
600 Ma Pan-African belt of Central Africa. Support of
UNESCO and IUGS for these projects is gratefully
acknowledged. Thoughtful reviews by Alcides Sial and
Maarten de Wit substantially improved this paper.
References
A BDELSALAM , M. G., L IÉGEOIS , J. P. & S TERN , R. J.
2002. The Saharan metacraton. Journal of African
Earth Sciences, 31, 119 –136.
A LLARD , G. O. & H URST , V. J. 1969. Brazil-Gabon
geologic link supports continental drift. Science, 163,
528– 532.
A LKMIM , F. F., M ARSHAK , S. & F ONSECA , M. A.
2001. Assembling West Gondwana in the
94
Neoproterozoic: Clues from the São Francisco craton
region, Brazil. Geology, 29, 319–322.
A LKMIM , F. F., M ARSHAK , S., P EDROSA -S OARES , A. C.,
P ERES , G. G., C RUZ , S. C. & W HITTINGTON , A.
2006. Kinematic evolution of the Araçuaı́–West
Congo orogen in Brazil and Africa: Nutcracker
tectonics during the Neoproterozoic assembly of
Gondwana. Precambrian Research, 149, 43–64.
A RAÚJO , M. N. C., O LIVEIRA , E. P. & C ARVALHO , M. J.
2003. Tectônica de endentação na Faixa Sergipana,
NE do Brasil: compatibilização entre os elementos
estruturais e cinemáticos. In: IX Simpósio Nacional
de Estudos Tectônicos, Búzios, Boletim de Resumos,
115– 117.
B ARBOSA , J. S. F. & S ABATÉ , P. 2002. Geological features and the Paleoproterozoic collision of four
Archean crustal segments of the São Francisco
Craton, Bahia, Brazil. A synthesis. Anais da Academia
Brasileira de Ciências, 74, 343– 359.
B ARBOSA , J. S. F. & S ABATÉ , P. 2004. Archean and
Paleoproterozoic crust of the São Francisco Craton,
Bahia, Brazil: geodynamic features. Precambrian
Research, 133, 1– 27.
B ITTAR , S. M. B. 1998. Faixa Piancó-Alto Brı́gida:
Terrenos
tectonoestratigráficos
sob
regimes
metamórficos e deformacionais contrastantes. PhD
thesis, Instituto de Geociências, Universidade de
São Paulo.
B IZZI , L. A., S CHOBBENHAUS , C. ET AL . 2001. Geologia,
Tectônica e Recursos Minerais do Brasil:Sistema de
Informações Geográficas-SIG. Companhia de Pesquisa de Recursos Minerais, Brası́lia, 2001.4
CD-ROM, Scale 1:2.500.000 (http://wwwa.geoambiente.com.br/website/cprm1/viewer.htm).
B RITO N EVES , B. B. 1978. A propósito da evolução
litoestratigráfica do Precambriano Superior do Nordeste. Volume Djalma Guimarães, Jornal de Mineralogia, Recife, 7, 19–27.
B RITO N EVES , B. B., S IAL , A. N. & A LBUQUERQUE ,
J. P. T. 1977. Vergência centrı́fuga residual no
Sistema de Dobramentos Sergipano. Revista Brasileira de Geociências, 7, 102–114.
B RITO N EVES , B. B., S IAL , A. N., R AND , H. M. &
M ANSO , V. V. 1982. The Pernambuco– Alagoas
Massif, northeastern Brazil. Revista Brasileira de
Geociências, 12, 240 –250.
B RITO N EVES , B. B., P ESSOA , D. A. R., P ESSOA , R. J. R.
& C ORTÊS , P. L. 1984, Estudo geocronológico das
rochas do embasamento da Folha Salgueiro, Pernambuco. In: Congresso Brasileiro de Geologia 33, Rio
de Janeiro, Anais. Sociedade Brasileira de Geologia,
2473–2491.
B RITO N EVES , B. B., V AN S CHMUS , W. R., S ANTOS ,
E. J., C AMPOS N ETO , M. & K OZUCH , M. 1995.
O evento Cariris Velhos na Provı́ncia Borborema: integração de dados, implicações e perspectivas. Revista
Brasileira de Geociências, 25, 279–296.
B RITO N EVES , B. B., DOS S ANTOS , E. J. & V AN
S CHMUS , W. R. 2000, Tectonic history of the Borborema Province, Northeastern Brazil. In: C ORDANI ,
U. G., M ILANI , E. J., T HOMAZ F ILHO , A. &
C AMPOS , D. A. (eds) Tectonic evolution of South
America, 31st International Geological Congress,
Rio de Janeiro, Brazil, 151–182.
B RITO N EVES , B. B., C AMPOS N ETO , M. C., V AN
S CHMUS , W. R. & S ANTOS , E. J. 2001a.
O “Sistema Pajeú-Paraı́ba” e o “maciço” São José do
Campestre no leste da Borborema. Revista Brasileira
de Geociências, 31, 173–184.
B RITO N EVES , B. B., C AMPOS N ETO , M. C., V AN
S CHMUS , W. R., F ERNANDEZ , T. M. G. & S OUZA ,
S. L. 2001b. O terreno Alto Moxotó no leste da
Paraiba (“Maciço Caldas Brandão”). Revista Brasileira de Geociências, 31, 185–194.
B RITO N EVES , B. B., V AN S CHMUS , W. R. & F ETTER ,
A. H. 2002. North-western Africa– North-eastern
Brazil. Major tectonic links and correlation problems.
Journal of African Earth Sciences, 34, 275–278.
B RITO N EVES , B. B., P ASSARELLI , C. R., B ASEI ,
M. A. S. & S ANTOS , E. J. 2003. Idades U –Pb em
zircão de alguns granitos clássicos da Provı́ncia
Borborema. Geologia USP, Série Cientı́fica, São
Paulo, 3, 25–38.
B RITO N EVES , B. B., V AN S CHMUS , W. R., K OZUCH ,
M., DOS S ANTOS , E. J. & P ETRONILHO , L. 2005. A
zona
tectônica
Teixeira
Terra
NovaZTTTN-fundamentos da geologia regional e isotópica.
Geologia USP, Série Cientı́fica, São Paulo, 5, 57–80.
B RUGUIER , O., D ADA , S. & L ANCELOT , J. R. 1994. Early
Archean component (.3.5 Ga) within a 3.05 Ga
orthogneiss from northern Nigeria: U– Pb zircon
evidence. Earth and Planetary Science Letters, 125,
89–103.
B UENO , J. F., O LIVEIRA , E. P., A RAÚJO , M. N. C.,
C ARVALHO , M. J. & M C N AUGHTON , N. 2005.
Granitos e a deformação na Faixa Sergipana: o inı́cio
da colisão entre o Cráton São Francisco e o Maciço
Pernambuco-Alagoas. In: III Simpósio sobre o
Cráton do São Francisco, Salvador, Bahia, Anais,
192–195.
C ABY , R. 1989. Precambrian terranes of Benin-Nigeria
and northeast Brazil and the Late Proterozoic
south Atlantic fit. In: D ALLMEYER , R. D. (ed.)
Terranes in the circum-Atlantic Paleozoic orogens.
Geological Society of America, Special Papers, 230,
145–158.
C ABY , R. 2003. Terrane assembly and geodynamic evolution of central-western Hoggar: a synthesis. Journal
African Earth Sciences, 37, 133–159.
C AEN -V ACHETTE , M., V IALETTE , Y., B ASSOT , J. P. &
V IDAL , P. 1988. Apport de la géochronologie isotopique à la connaissance de la géologie gabonaise. Chronique de Recherche Minière, 49, 35–54.
C AMPOS , J. C. S., C ARNEIRO , M. A. & B ASEI , M. A. S.
2003. U–Pb evidence for late Neoarchean crustal
reworking in the southern São Francisco craton
(Minas Gerais, Brazil). Annals of the Brazilian
Academy of Sciences, 75, 497–511.
C AMPOS N ETO , M. C. & B RITO N EVES , B. B. 1987. Considerações sobre a organização e geometria do Sistema
de Dobramentos Sergipano. In: I Simposio Nacional
Estudos Tectonicos, Salvador, Bahia, Abstract
volume, 90– 93.
C AMPOS N ETO , M. C., B ITTAR , S. M. B. & B RITO
N EVES , B. B. 1994. Domı́nio tectônico Rio
Pajeú-Provı́ncia Borborema: orogêneses superpostas no ciclo Brasiliano/Pan-Africano. In:
Congresso Brasileiro de Geologia 38, Balneário
Camboriú, Anais, 1. Sociedade Brasileira de Geologia,
221–222.
C ARVALHO , M. J., O LIVEIRA , E. P., D ANTAS , E. L. &
M C N AUGHTON , N. 2005. Evolução tectônica do
Domı́nio Marancó - Poço Redondo: registro das orogêneses Cariris Velhos e Brasiliana na margem norte
da Faixa Sergipana. In: III Simpósio sobre o Cráton
do São Francisco, Salvador, Bahia, Brazil, Anais,
204–207.
C ASTAING , C., T RIBOULET , C., F EYBESSE , J. L. &
C HEVREMONT , P. 1993. Tectonometamorphic evolution of Ghana, Togo and Benin in the light of the
Pan-African/Brasiliano orogeny. Tectonophysics,
218, 323– 342.
C ASTAING , C., F EYBESSE , J. L., T HIÉBLEMONT ,
T RIBOULET , C. & C HEVREMONT , P. 1994. Paleogeographical reconstructions of the Pan-African/
Brasiliano orogen: closure of an oceanic domain or
intracontinental convergence between major blocks.
Precambrian Research, 69, 327– 344.
C ORRÊA G OMES , L. C. & O LIVEIRA , E. P. 2000. Radiating 1.0 Ga Mafic Dyke Swarms of Eastern Brazil and
Western Africa: Evidence of Post-Assembly Extension in the Rodinia Supercontinent? Gondwana
Research, 3, 325 –332.
D’ EL -R EY S ILVA , L. J. H. 1995. Tectonic evolution of
the Sergipano Belt, NE Brazil. Revista Brasileira de
Geociências, 25, 315–332.
D’ EL -R EY S ILVA , L. J. H. 1999. Basin infilling in the
southern-central part of the Sergipano Belt (NE
Brazil) and implications for the evolution of
Pan-African/Brasiliano cratons and Neoproterozoic
sedimentary cover. Journal South American Earth
Sciences, 12, 453–470.
D’ EL -R EY S ILVA , L. J. H. & M C C LAY , K. R. 1995. Stratigraphy of the southern part of the Sergipano belt, NE
Brazil: tectonic implications. Revista Brasileira de
D ADA , S. S. 1998. Crust-forming ages and Proterozoic
crustal evolution in Nigeria: a reappraisal of current
interpretations. Precambrian Research, 87, 65– 74.
D ANTAS , E. L. 1997. Geocronologia U/Pb e Sm/Nd de
terrenos Arqueanos e Paleoproterozóicos do
Maciço Caldas Brandão, NE Brasil. PhD thesis,
Instituto de Geociências, Universidade Estadual
Paulista, Brazil.
D ANTAS , E. L., H ACKSPACHER , P. C., V AN S CHMUS ,
W. R. & B RITO N EVES , B. B. 1998. Archean accretion in the São José do Campestre massif, Borborema
Province, northeast Brazil. Revista Brasileira de
D ANTAS , E. L., V AN S CHMUS , W. R. ET AL . 2004. The
3.4– 3.5 Ga São José do Campestre massif, NE
Brazil: remnants of the oldest crust in South
America. Precambrian Research, 130, 113– 137.
D AVISON , I. & S ANTOS , R. A. 1989. Tectonic Evolution
of the Sergipano Fold Belt, NE Brazil, during the
Brasiliano Orogeny. Precambrian Research, 45,
319–342.
D E P AOLO , D. J. 1981. A neodymium and strontium isotopic study of the Mesozoic calc-alkaline granitic
batholiths of the Sierra Nevada and Peninsular
Ranges, California: Journal of Geophysical Research,
86, 10 470–10 488.
95
W IT , M., J EFFERY , M., B ERGH , H. & N ICOLAYSEN ,
L. 1988. Geological map of sectors of Gondwana
reconstructed to their disposition c. 150 Ma. American
Association of Petroleum Geologists, Tulsa,
Oklahoma.
DE W IT , M. J., B OWRING , S., D UDAS , F. & T AGNE K AMGA , G. 2005. Saharan Africa and the tectonic
assembly of the northern margin of Gondwana. In:
P ANKHURST , R. J. & V EIGA , G. D. (eds) Gondwana
12: Geological and Biological Heritage of Gondwana,
Abstracts. Academia Nacional de Ciéncias, Cordoba,
Argentina, 133.
E BERT , H. 1970. The Precambrian geology of the Borborema Belt (states of Paraı́ba and Rio Grande do Norte,
northeastern Brazil), and the origin of its mineral
resources. Geologisches Rundschau, 59, 1299–1326.
E KWUEME , B. N. & K RÖNER , A. 1993. Preliminary
zircon evaporation ages from migmatitic gneisses in
Kaduna, N. Nigeria: evidence for Early Archean (PreLeonian) event in the Nigeria basement complex. In:
NMGS 29th Annual Conference Abstracts. Nigerian
Mining and Geosciences Society, 61.
E KWUEME , B. N. & K RÖNER , A. 2006. Single zircon ages
of migmatitic gneisses and granulites in the Obudu
Plateau: Timing of granulite-facies metamorphism in
southeastern Nigeria. Journal of African Earth
Sciences, 44, 459– 469.
F ERREIRA , V., S IAL , A. N. & J ARDIM DE S Á , E. F. 1998.
Geochemical and isotopic signatures of the Proterozoic granitoids in terranes of the Borborema Province,
northeastern Brazil. Journal of South American Earth
Sciences, 11, 439– 455.
F ERRÉ , E., D ÉLÉRIS , J., B OUCHEZ , J. L., L AR , A. U. &
P EUCAT , J. J. 1996. The Pan-African reactivation of
contrast Eburnéen and Archean provinces in Nigeria:
stuctural and isotopic data. Journal of Geological
Society, London, 153, 719–728.
F ERRÉ , E. C., C ABY , R., P EUCAT , J., C APDEVILA , R. &
M ONIÉ , P. 1998. Pan-African post-collisional,
ferro-potassic granite and quartz-monzonite plutons
of Eastern Nigeria. Lithos, 45, 255–279.
F ERRÉ , E., G LEIZES , G. & C ABY , R. 2002. Obliquely
convergent tectonics and granite emplacement in the
Trans-Saharan belt of Eastern Nigeria: a synthesis.
Precambrian Research, 114, 199–219.
F ETTER , A. H. 1999. U– Pb and Sm– Nd constraints on
the crustal framework and geologic history of Ceará
State, NW Borborema Province, NE Brazil: Implications for the assembly of Gondwana. PhD thesis,
University of Kansas, USA.
F ETTER , A. H., S ARAIVA DOS S ANTOS , T. J. ET AL . 2003.
Evidence for Neoproterozoic Continental Arc Magmatism in the Santa Quitéria batholith of Ceará State, NW
Bornorema Province, NE Brazil: Implications for the
Assembly of West Gondwana. Gondwana Research,
6, 265–273.
F EYBESSE , J. L., J OHAN , V. ET AL . 1998. The West
Central African Belt: a model of 2.5–2.0 Ga accretion
and two-phase orogenic evolution. Precambrian
Research, 87, 161– 216.
G UIMARÃES , I. P. & B RITO N EVES , B. N. 2005. Geoquı́mica e significado tectonico do plutonismo
Eo-Neoproterozóico no limite norte do domı́nio
estructural central da Provı́ncia Borborema. In: XXI
DE
96
Simpósio de Geologia do Nordeste, Recife, Brazil,
Boletim, 19, 68– 70.
G UIMARÃES , I. P., S ILVA F ILHO , A. F. ET AL . 2004.
Brasiliano (Pan-African) granitic magmatism in the
Pajeú-Paraı́ba belt, Northeast Brazil: an isotopic and
geochronological approach. Precambrian Research,
135, 23–53.
H OLLANDA , M. H. B. M., P IMENTEL , M. M. & J ARDIM
DE S A , E. F. 2003. Paleoproterozoic subductionrelated metasomatic signatures in the lithospheric
mantle beneath NE Brazil: inferences from trace
element and Sm–Nd –Pb isotopic compositions of
Neoproterozoic high-K igneous rocks. Journal of
South American Earth Sciences, 15, 885– 900.
H UMPHREY , F. L. & A LLARD , G. O. 1968. The Propriá
Geosyncline, a newly recognized Precambrian
tectonic province in the Brazilian shield. In: 23rd
International Geological Congress, 4, 123– 139.
J ARDIM DE S Á , E. F. 1994. A Faixa Seridó (Provı́ncia
Borborema, NE do Brasil) e o seu significado geodynâmico na cadeia Brasiliana/Pan-Africana. PhD
thesis, Instituto de Geociências, Universidade de
Brasilia, Brazil.
J ARDIM DE S Á , E. F., M ORAES , J. A. C. & D’ EL -R EY
S ILVA , L. J. H. 1986. Tectônica tangencial na Faixa
Sergipana. In: Congresso Brasileiro de Geologia 34,
Goiania, Anais, 3. Sociedade Brasileira de Geologia,
1246–1259.
K OSIN , M., DE M ELLO , R. C., DE Z OUZA , J. D., DE
O LIVEIRA , A. P., C ARVALHO , M. J. & L EITE ,
C. M. 2003. Geology of the northern segment of the
Itabuna-Salvador-Curaçá orogen and field trip guide.
Revista Brasileira de Geociências, 33, 15– 26.
K OZUCH , M. 2003. Isotopic and trace element geochemistry of early Neoproterozoic gneissic and metavolcanic rocks in the Cariris Velhos orogen of the
Borborema Province, Brazil, and their bearing on
tectonic setting. PhD thesis, University of Kansas,
USA.
K RÖNER , A. & C ORDANI , U. 2003. African, southern
Indian and South American cratons were not part of
the Rodinia supercontinent: evidence from field
relationships and geochronology. Tectonophysics,
375, 325–352.
L ASSERRE , M. 1967. Données géochronologiques nouvelles acquises au 1er Janvier 1967 par la méthode
au strontium appliquées aux roches cristallophylliennes du Cameroun. Annales de la Faculté des
Sciences, Université Clermont Ferrand, 36, 109–144.
L EDRU , P., C OCHERIE , A., B ARBOSA , J., J OHAN , V. &
O NSTOTT , T. 1994. Ages du métamorphisme granulitique dans le craton du São Francisco (Brésil). Implications sur la nature de l’orogène transamazonien.
Comptes Rendus de l’Academie des Sciences, Paris,
Série II, 318, 251 –257.
L EROUGE , C., C OCHERIE , A. ET AL . 2006. Shrimp U–Pb
zircon age evidence for Paleoproterozoic sedimentation and 2.05 Ga syntectonic plutonism in the
Nyong Group, South-Western Cameroon: consequences for the Eburnean–Transamazonian belt of
NE Brazil and Central Africa. Journal of African
Earth Sciences, 44, 413–427.
L IÉGEOIS , J. P., B LACK , R. & N AVEZ , J. 1994. Early and
late Pan-African orogenies in the Air assembly of
terranes (Tuareg shield, Niger). Precambrian
Research, 67, 59–88.
L ONG , L. E., C ASTELLANA , C. H. & S IAL , A. N. 2003.
Cooling history of the Coronel João Sá Pluton, Bahia.
Brazil. In: IV South American Symposium on Isotope
Geology, Salvador, Brazil, Short Papers, 1, 92–94.
M ARINHO , M. M., V IDAL , P., A LIBERT , C., B ARBOSA ,
J. S. F. & S ABATÉ , P. 1994. Geochronology of the
Jequié-Itabuna granulitic belt and of the ContendasMirante volcano-sedimentary belt. Boletim IG-USP,
Publicação Especial, 17, 73– 96.
M EDEIROS , V. C. & S ANTOS , E. J. 1998. Folha Garanhuns (SC.24-X-B, escala 1:250.000). Integração Geológica (Relatório Interno), CPRM. Recife-PE, Brazil.
M ILESI , J. P., T OTEU , S. F. ET AL . 2006. An overview of
the geology and major ore deposits of Central Africa:
Explanatory note for the 1:4,000,000 map “Geology
and major ore deposits of Central Africa”. Journal of
African Earth Sciences, 44, 571–595.
M ONTES -L AUAR , C. R., T ROMPETTE , R. ET AL . 1997.
Pan-African Rb-Sr isochron of magmatic rocks from
northern Cameroon. Preliminary results. In: 1st South
American Symposium on Isotope Geology, Brazil,
204–205.
M VONDO , H., DEN B ROK , S. W. J. & O NDOA , J. M. 2003.
Evidence for symmetric extension and exhumation of
the Yaoundé nappe (Pan-African fold belt, Cameroon).
Journal of African Earth Sciences, 36, 215–231.
N ASCIMENTO , R. S., O LIVEIRA , E. P., C ARVALHO , M. J.
& M C N AUGHTON , N. 2005. Evolução Tectônica do
Domı́nio Canindé, Faixa Sergipana, NE do Brasil.
In: III Simpósio sobre o Cráton do São Francisco,
Salvador, Bahia, Anais, 239–242.
N ASCIMENTO , R. S. C., S IAL , A. N. & P IMENTEL ., M. M.
2004. Chemostratigraphy of medium-grade marbles of
the Late Neoproterozoic Seridó Group, Seridó Fold
Belt, Northeastern Brazil. Gondwana Research, 7,
731–744.
N ÉDÉLEC , A., M ACAUDIÈRE , J., N ZENTI , J. P. &
B ARBEY , P. 1986. Evolution métamorphique et structurale des schistes de Mbalmayo (Cameroun). Implications pour la structure de la zone mobile
panafricaine d’Afrique centrale, au contact du craton
du Congo. Comptes Rendus de l’Académie des
Sciences, Paris, 303, 75– 80.
N ÉDÉLEC , A., N SIFA , E. N. & M ARTIN , H. 1990.
Major and trace element geochemistry of the Archaean
Ntem plutonic complex (South Cameroon): petrogenesis and crustal evolution. Precambrian Research,
47, 35–50.
N EVES , S. P. 2003. Proterozoic history of the Borborema
province (NE Brazil): Correlations with neighboring
cratons and Pan-African belts and implications for
the evolution of western Gondwana. Tectonics, 22,
1031– 1044.
N EVES , S. P. & M ARIANO , G. 1999. Assessing the
tectonic significance of a large-scale transcurrent
shear zone system: the Pernambuco lineament, northeastern Brazil. Journal of Structural Geology, 21,
1369– 1383.
N EVES , S. P., B RUGUEIR , O., S ILVA , J. M. R. &
M ARIANO , G. 2005. Age, provenance, and metamorphism of the Suburim Complex (eastern
Borborema Province, NE Brazil): A LA-ICP-MS
study. In: X Congresso Brasileiro de Geoquı́mica e II
Simpósio de Geoquı́mica dos Paı́ses do Mercosul,
Porto de Galinhas, Pernambuco, Brazil, Abstract
CD, 13-512.
N EVES , S. P., B RUGUEIR , O., V AUCHEZ , A., B OSCH , D.,
S ILVA , J. M. R. & M ARIANO , G. 2006. Timing of
crust formation, deposition of supracrustal sequences,
and Transamazonian and Brasiliano metamorphism in
the East Pernambuco belt (Borborema Province, NE
Brazil): Implications for western Gondwana assembly.
N OIZET , G. 1982. Disposition géologique des régions de
Yaoundé et Bafia. Annales de la Faculté des Sciences,
Université de Yaoundé, Cameroun, 1, 95– 103.
N ZENTI , J. P., B ARBEY , P., M ACAUDIÉRE , J. & S OBA , D.
1988. Origin and evolution of the late Precambrian
high-grade Yaoundé gneisses (Cameroon). Precambrian Research, 38, 91–103.
O LIVEIRA , E. P., W INDLEY , B. F., M C N AUGHTON , N.,
P IMENTEL , M. & F LETCHER , I. R. 2004. Contrasting
copper and chromium metallogenic evolution of terranes in the Palaeoproterozoic Itabuna– Salvador–
Curaçá Orogen, São Francisco Craton, Brazil: new
zircon (SHRIMP) and Sm-Nd (model) ages and their
significance for orogen-parallel escape tectonics.
O LIVEIRA , E. P., A RAÚJO , M. N. C. ET AL . 2005a. Timing
and Duration of Collision in the Neoproterozoic Sergipano Belt, NE Brazil: Age Constraints from Major
Shear Zones, Orogenic Granites and Foreland Basin
Filling. In: Atas do XXI Simpósio Geologia do
Nordeste, Brazil, 95– 98.
O LIVEIRA , E. P., C ARVALHO , M. J. ET AL . 2005b. Evidence from detrital zircon geochronology and wholerock Sm-Nd isotopes for off-craton provenance of
clastic metasedimentary units of the Sergipano belt,
NE Brazil. In: X Simpósio Nacional de Estudos Tectônicos, Curitiba, Boletim de Resumos Expandidos,
308–311.
O LIVEIRA , E. P., T OTEU , S. F. ET AL . 2006. Geologic correlation between the Neoproterozoic Sergipano belt
(NE Brazil) and the Yaoundé schist belt (Cameroon,
Africa). Journal of African Earth Sciences, 44,
470–478.
O SAKO , L. 2005. Caracterização geológica da região
entre as localidades de Paranatama e Curral novo,
PE,
porção
centro-norte
do
Complexo
Pernambuco-Alagoas, Provı́ncia Borborema. PhD
thesis, Universidade Federal de Pernambuco, Brazil.
P EDROSA -S OARES , A. C., N OCE , C. M., V IDAL , P.,
M ONTEIRO , R. L. B. P. & L EONARDOS , O. H. 1992.
Toward a new tectonic model for the Late Proterozoic
Aracuai (SE Brazil)-West Congolian (SW Africa)
Belt. Journal of South American Earth Sciences, 6,
33– 47.
P ENAYE , J., T OTEU , S. F., V AN S CHMUS , W. R. &
N ZENTI , J. P. 1993. U –Pb and Sm–Nd preliminary
geochronologic data on the Yaoundé series, Cameroon: re-interpretation of the granulitic rocks as the
suture of a collision in the “Centrafrican belt”.
Comptes Rendus de l’Académie des Sciences, Paris,
317, 789– 794.
P ENAYE , J., T OTEU , S. F. ET AL . 2004. The 2.1 Ga
West Central African Belt in Cameroon: extension
97
and evolution. Journal of African Earth Sciences, 39,
159– 164.
P ENAYE , J., K RÖNER , A., T OTEU , S. F., V AN S CHMUS ,
W. R. & D OUMNANG , J.-C. 2006. Evolution of the
Mayo Kebbi region as revealed by zircon dating: An
early (c. 740 Ma) Pan-African magmatic arc in southwestern Chad. Journal of African Earth Sciences, 44,
530– 542.
P ESSOA , D. R., P ESSOA , R. R., B RITO N EVES , B. B. &
K AWASHITA , K. 1978. Magmatismo tardi-tectônico
brasiliano no Maciço PE-AL: o quartzo-sienito de
Cachoeirinha-PE. In: Congresso Brasileiro de
Geologia 30, Recife, Anais. Sociedade Brasileira de
Geologia, 1279– 1287.
P IMENTEL , M. M., F UCK , F. A., J OST , H., F ERREIRA
F ILHO , C. F. & A RAÚJO , S. M. 2000. The basement
of the Brası́lia fold belt and the Goiás magmatic arc.
In: C ORDANI , U., M ILANI , E. J., T HOMAZ F ILHO ,
A. & C AMPOS , D. A. (eds) Tectonic evolution of
South America. 31st International Geological Congress, Rio de Janeiro, Brazil, 195– 229.
P OIDEVIN , J. L. 1991. Les ceintures de roches vertes de la
République Centrafricaine. Contribution à la connaissance du précambrien du nord du craton du Congo.
Thèse de Doctorat d’Etat, Université Blaise Pascal,
Clermont-Ferrand, France.
P OUCLET , A, V IDAL , M., D OUMNANG , J.-C., V ICAT ,
J.-P. & T CHAMENI , R. 2006. Neoproterozoic crustal
evolution in Southern Chad: Pan-African ocean basin
closing, arc accretion and late- to post-orogenic granitic intrusion. Journal of African Earth Sciences, 44,
543– 560.
R IOS , D. C. 2002. Granitogênese no Núcleo Serrinha,
Bahia, Brasil: Geocronologia e litogeoquı́mica. PhD
thesis, Instituto de Geociências, Universidade
Federal da Bahia, Brazil.
R OGERS , J. J. W. 1996. A history of continents in the past
three billion years. Journal of Geology, 104, 91–107.
S Á , J. M., M C R EATH , I. & L ETERRIER , J. 1995.
Petrology, geochemistry, and geodynamic setting of
Proterozoic igneous suites of the Orós fold belt
(Borborema Province, Northeast Brazil). Journal of
South American Earth Sciences, 8, 299–314.
S ANTOS , E. J. 1995. O Complexo Granı́tico Lagoa das
Pedras:Acresção e colisão na região de Floresta
(Pernambuco), Provı́ncia Borborema. PhD thesis,
Instituto de Geociências, Universidade de São Paulo,
Brazil.
S ANTOS , E. J. & B RITO N EVES , B. B. 1984. Provı́ncia
Borborema. In: A LMEIDA , F. F. M. & Y OCITERU
H ASUI , Y. (eds) O Pré-Cambriano do Brasil. Edgar
Blucher Ltd., São Paulo, 123– 186.
S ANTOS , E. J., V AN S CHMUS , W. R., B RITO N EVES ,
B. B., O LIVEIRA , R. G. & M EDEIROS , V. C. 1997.
Terranes and their boundaries in the Proterozoic Borborema Province, northeast Brazil. In: VII Simpósio
Nacional Estudos Tectônicos, Bahia, Brazil, Extended
Abstracts, 120 –124.
S ANTOS , R. A. & S OUZA , J. D. 1988. Programa Levantamentos Geológicos Básicos do Brasil: Piranhus, Folha
SC.24-X-C-VI, Estados de Sergipe, Alagoas e Bahia.
DNPM/CPRM, Brasilia.
S ANTOS , R. A., M ARTINS , A. A. M., N EVES , J. P. &
L EAL , R. A. 1998. Geologia e Recursos Minerais do
98
Estado de Sergipe. Companhia de Pesquisa de Recursos Minerais/Codise.
S ANTOS , T. J. S., F ETTER , A. H. & N OGUEIRA N ETO ,
J. A. 2008. Comparisons between the northwestern
Borborema Province, NE Brazil, and the southwestern
Pharusian Dahomey Belt, SW Central Africa. In: P ANKHURST , R. J., T ROUW , R. A. J., B RITO N EVES , B. B.
& DE W IT , M. J. (eds) West Gondwana: Pre-Cenozoic
correlations Across the South Atlantic Region. Geo
logical Society, London, Special Publications, 294,
101– 119.
S HANG , C. K., S ATIR , M., S IEBEL , W., N SIFA , N. E.,
T AUBALD , H., L IEGEOIS , J. P. & T CHOUA , F. M.
2004. TTG magmatism in the Congo craton: a view
from major and trace elements geochemistry, Rb-Sr
and Sm-Nd systematics: case of the Sangmelima
region, Ntem Complex, southern Cameroon. Journal
of African Earth Sciences, 40, 61– 70.
S IAL , A. N. 1986. Granite-types in northeast Brazil:
Current knowledge. Revista Brasileira de Geociências, 16, 54–72.
S ILVA , M. G. 1992. Evidências isotópicas e geocronológicas de um fenômeno de acrescimento crustal transamazônico no Cráton do São Francisco, Estado da Bahia.
In: Congresso Brasileiro de Geologia 37, São Paulo,
Anais, 2. Sociedade Brasileira de Geologia, 181–182.
S ILVA F ILHO , A. F. & G UIMARAES , I. P. 2000. Sm/Nd
isotopic data and U/Pb geochronology of collisional
to post-collisional high-K shoshonitic granitoids
from the Pernambuco-Alagoas terrane, Borborema
Province, NE. Brazil. In: 31st International Geological Congress, Rio de Janeiro, Brazil, Abstracts
Volume CD-ROM.
S ILVA F ILHO , A. F., G UIMARÃES , I. P., S AMPAIO , M.A
& L UNA , E. B. A. 1996. A super suite de granitóides
ricos em K Neoproterozóicos tardi a pós - tectônicos
da parte sul do Maciço PE-AL; magmatismo intraplaca? In: Congresso Brasileiro de Geologia 39, Salvador, Resumos Expandidos, 6. Sociedade Brasileira
de Geologia, 318–320.
S ILVA F ILHO , AF., V AN S CHMUS , W. R., G UIMARÃES ,
I. P. & L UNA , E. B. A. 1997a. Nd signature of PE-AL
massif late tectonic granitic rocks, NE Brazil: evidence
of sucessive crustal accretion during the Proterozoic.
In: 1st South American Symposium on Isotope
Geology, 304 –306.
S ILVA F ILHO , A. F., G UIMARÃES , I. P., L YRA DE B RITO ,
M. F. & P IMENTEL , M. M. 1997b. Geochemical signatures of the main Neoproterozoic late tectonic granitoids from the Proterozoic Sergipano fold belt, NE
Brazil and its significance for the Brasiliano orogeny.
International Geology Review, 39, 639 –659.
S ILVA F ILHO , A. F., G UIMARÃES , I. P. & V AN S CHMUS ,
W. R. 2002. Crustal evolution of the
Pernambuco-Alagoas complex, Borborema Province,
NE Brazil: Nd isotopic data from Neoproterozoic
granitoids. Gondwana Research, 5, 409– 422.
S ILVA F ILHO , AF, G UIMARÃES , I. P. ET AL . 2005a.
Caracterização geológica e geoquı́mica dos granitóides e ortognaisses Proterozóicos cálcio-alcalinos
de alto-K do Domı́nio Crustal Garanhuns, Terreno
Pernambuco-Alagoas, e seu significado tectônico. In:
Atas do XXI Simpósio Geologia do Nordeste, Brazil,
119– 123.
S ILVA F ILHO , A. F., V AN S CHMUS , W. R., B RITO
N EVES , B. B., G UIMARÃES , I. P., T OTEU , S. F. &
O SAKO , L. S. 2005b. Geological fit between the
Pernambuco-Alagoas terrane of NE Brazil and
Central African Fold Belt in Cameroon, based on
Proterozoic structures and magmatism. In:
P ANKHURST , R. J. & V EIGA , G. D. (eds) Gondwana
12: Geological and Biological Heritage of Gondwana,
Abstracts. Academia Nacional de Ciéncias, Cordoba,
Argentina, 120.
S ILVA F ILHO , M. A. 1998. Arco vulcânico CanindéMarancó e a Faixa Sul-Alagoana: seqüências orogênicas mesoproterozóicas. In: Congresso Brasileiro de
Geologia 40, Belo Horizonte, Anais. Sociedade Brasileira de Geologia, 16.
S ILVA F ILHO , M. A. & B RITO N EVES , B. B. 1979. O
Sistema de dobramentos Sergipano no Nordeste da
Bahia. Geologia Recursos Minerais do Estado da
Bahia, Textos Básicos, 1, 203–217.
S ILVA F ILHO , M. A. & T ORRES , H. H. F. 2002. A new
interpretation on the Sergipano belt domain. Anais
Academia Brasileira de Ciências, 74, 556– 557.
S ILVA F ILHO , M. A., A CIOLY , A. C. A., T ORRES ,
H. H. F. & A RAÚJO , R. V. 2003. O Complexo Jaramataia no contexto do Sistema Sergipano. Revista de
Geologia, Fortaleza, 16, 99– 110.
S TENDAL , H., T OTEU , S. F. ET AL . 2006. Derivation of
detrital rutile in the Yaoundé region from the Neoproterozoic Pan-African belt in southern Cameroon
(Central Africa). Journal of African Earth Sciences,
44, 443–458.
T ACK , L., W INGATE , M. T. D., L IÉGEOIS , J.-P.,
F ERNADEZ -A LONSO , M. & D EBLOND , A. 2001.
Early Neoproterozoic magmatism (1000-910 Ma) of
the Zadinian and Mayumbian Groups (Bas-Congo):
onset of Rodinia rifting at the western edge of
the Congo Craton. Precambrian Research, 110,
277–306.
T CHAKOUNTÉ , J. 1999. Etude géologique de la région
d’Etoundou-Bayomen dans la série de Bafia (province
du Centre) : tectonique, géochimie-métamorphisme.
Thèse de Doctorat 3è Cycle, Université de Yaoundé
I, Cameroun.
T CHAMENI , R., M EZGER , K., N SIFA , N. E. & P OUCLET ,
A. 2000. Neoarchean crustal evolution in the Congo
craton: evidence from K-rich granitoids of the Ntem
complex, southern Cameroon. Journal of African
Earth Sciences, 30, 133– 147.
T EIXEIRA , W. & F IGUEIREDO , M. C. H. 1991. An outline
of Early Proterozoic crustal evolution in the São Francisco Craton, Brazil: a review. Precambrian Research,
53, 1– 22.
T EIXEIRA , W., S ABATÉ , P., B ARBOSA , J., N OCE , C. M.
& C ARNEIRO , M. A. 2000. Archean and Paleoproterozoic tectonic evolution of the São Francisco Craton.
In: C ORDANI , U. G., M ILANI , E. J., T HOMAZ
F ILHO , A. & C AMPOS , D. A. (eds) Tectonic Evolution
of South America. 31st International Geological
Congress, Rio de Janeiro, 101– 137.
T OTEU , S. F., M ICHARD , A., B ERTRAND , J. M. & R OCCI ,
G. 1987. U– Pb dating of Precambrian rocks from
northern Cameroon, orogenic evolution and chronology of the Pan-African belt of central Africa. Precambrian Research, 37, 71–87.
T OTEU , S. F., V AN S CHMUS , W. R., P ENAYE , J. &
N YOBÉ , J. B. 1994. U– Pb and Sm– Nd evidence for
Eburnian and Pan-African high-grade metamorphism
in cratonic rocks of southern Cameroon. Precambrian
Research, 67, 321–347.
T OTEU , S. F., V AN S CHMUS , W. R., P ENAYE , J. &
M ICHARD , A. 2001. New U– Pb and Sm–Nd data
from north-central Camroon and its bearing on
pre-Pan African history of central Africa. Precambrian Research, 108, 45–73.
T OTEU , S. F., P ENAYE , J. & P OUDJOM D JOMANI , Y.
2004. Geodynamic evolution of the Pan-African
belt of Central Africa with special reference to
Cameroon. Canadian Journal of Earth Sciences, 41,
73– 85.
T OTEU , S. F., P ENAYE , J., D ELOULE , E., V AN S CHMUS ,
W. R. & T CHAMENI , R. 2006a. Diachronous evolution of volcano-sedimentary basins north of the
Congo craton: insights from U– Pb ion microprobe
dating of zircons from the Poli, Lom and Yaounde
Series (Cameroon). Journal of African Earth Sciences,
44, 428–442.
T OTEU , S. F., F OUATEU , R. Y. ET AL . 2006b. U– Pb
dating of plutonic rocks involved in the nappe
tectonic in southern Cameroon: consequence for the
Pan-African orogenic evolution of the central
99
African fold belt. Journal of African Earth Sciences,
44, 479– 493.
T ROMPETTE , R. 1997. Neoproterozic (600 Ma) aggregation of Western Gondwana: a tentative scenario.
Precambrian Research, 82, 101 –112.
V AN S CHMUS , W. R., B RITO N EVES , B. B.,
H ACKSPACHER , P. & B ABINSKI , M. 1995. U/Pb
and Sm/Nd geochronolgic studies of eastern Borborema Province, northeastern Brazil: initial conclusions.
Journal of South American Earth Sciences, 8,
267– 288.
V AN S CHMUS , W. R., F ETTER , A. H., B RITO N EVES ,
B. B. & W ILLIAMS , I. S. 1999. Ages of detrital
zircon populations from Neoproterozoic supracrustal
units in NE Brazil: Implications for assembly of
West Gondwanaland. Geological Society of America
Abstracts with Programs, 31, A-299.
V AN S CHMUS , W. R., B RITO N EVES , B. B. ET AL . 2003.
Seridó Group of NE Brazil, a Late Neoproterozoic pre- to syn-collisional flysch basin in
West Gondwanaland? : insights from SHRIMP U-Pb
detrital zircon ages. Precambrian Research, 127,
287– 327.
V AUCHEZ , A., N EVES , S. ET AL . 1995. The Borborema
shear zone systems, NE Brazil. Journal of South American Earth Sciences, 8, 247–266.

the Central African Fold Belt Proterozoic links between the

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