Cap XII INTERMEDIATE TO ACIDIC MAGMATISM AND … filemarcam o final do ciclo Brasiliano ... e...
Transcript of Cap XII INTERMEDIATE TO ACIDIC MAGMATISM AND … filemarcam o final do ciclo Brasiliano ... e...
Cap XII
Resumo:
O magmatismo granítico no domínio da Zona
Transversal da Província Borborema, NE do Brasil,ocorreu em três intervalos de tempo principais: 650-
620 Ma, 590-570 Ma e 545-520 Ma. O intervalo mais
antigo é caracterizado por intrusões de granitóides sin-cinemáticos cálcio-alcalinos de alto K com epidoto
magmático, cálcio-alcalinos e shoshoníticos. O segun -
do intervalo de tempo é marcado por intrusões abun -dantes de magmas cálcio-alcalinos de alto K sem epi -
doto magmático, além de magmas sieníticos peral -
calinos, metaluminosos de alto K, ultrapotássicos eraros shoshoníticos. Magmas peralcalinos e do tipo A
marcam o final do ciclo Brasiliano na região. Os gra -
nitóides mais antigos apresentam valores de TDM maisjovens (< 2.0 Ga) e valores menos negativos de εNd(cerca de -2 a -14) comparados com aqueles para os
granitóides de 590-570 Ma, para os quais os valores deTDM variam de cerca de ca 1,5 a 2,5 Ga, e os de εNdde cerca de -8 a -20. Os valores mais altos e variáveis
das razões iniciais 87Sr/86Sr são observados nos grani -tóides de 650-620 Ma. Esses dados indicam uma
mudança importante da fonte do magma com o tempo
geológico. Os granitóides mais antigos parecem repre -sentar uma mistura de magma derivado do manto juve-
nil, neoproterozóico, com magma derivado de fusão de
crosta continental paleoproterozóica, o que produziriaidades modelo Nd intermediárias, de cerca de 1,2 a 1,4
Ga. Isto é compatível com a mistura de magmas deriva -
dos do manto e crosta, como indicado por relações decampo que indicam um forte relacionamento entre mag -
mas granitíticos e dioríticos. Os plútons de 590-570 Ma
apresentam valores isotópicos de Sr e Nd compatíveiscom magmas formados por refusão de crosta continen -
tal inferior paleoproterozóica, o único reservatório
geoquímico com aquelas características. A únicaexceção entre as rochas dessa idade são os sienitos
peralcalinos ultrapotássicos, que apresentam razões
iniciais de Sr alta e valores muito negativos de εNd“values”, interpretados como derivados de uma fonte
no manto enriquecida em elementos incompatíveis. O
grupo mais antigo de rochas apresenta assinaturas geo -químicas típicas de granitos sin-tectônicos, enquanto
que o grupo de 590-570 Ma mostra assinaturas típicas
de magmas tardi-a pós-tectônicos.
Palavras-chave: Granitos, Granitos Cálcio-Alcalinos,
Sienitos Peralcalinos, Granitos Shoshoníticos, Epidoto
INTERMEDIATE TO ACIDIC MAGMATISM AND CRUSTAL EVOLUTION IN THE TRANSVERSAL
ZONE, NORTHEASTERN BRAZIL
Valderez P. FerreiraNEG-LABISE, Departamento de Geologia, UFPE, Recife, PE
Alcides N. SialNEG-LABISE, Departamento de Geologia, UFPE, Recife, PE
Márcio M. Pimentel
Instituto de Geociências, UnB, Brasília, DF
Cândido A.V. MouraCentro de Geociênciss, UFPA, Campus do Guamá, Belém, PA
Magmático, Evolução Crustal, Zona Transversal,
Província Borborema.
Abstract:
Granitic magmatism in the Transversal Zone domain of
the Borborema province, NE Brazil, occurred in three maintime intervals: 650-620 Ma, 590-570 Ma and 545-520 Ma.
The oldest is characterized by intrusions of syn-kinematic
magmatic-epidote bearing high-K calc-alkalic, calc-alkalicand shoshonitic granitoids. The second time interval is
marked by abundant intrusions of magmatic epidote-free
high-K calc-alkalic magmas, as well as peralkalic, metalumi-nous high-K syenitic, unique ultrapotassic, and rare
shoshonitic magmas. Peralkalic and rare A-type magmas
mark the end of the Brasiliano cycle in the region. The oldestgranitoids present younger TDM (< 2.0 Ga) and less negative
εNd (ca. -2 to -14) compared with the 590-570 Ma granitoids,
for which TDM varies from ca 1.5 to 2.5 Ga, and εNd fromca. -8 to -20. The highest and more variable initial 87Sr/86Sr
values are observed in the 650-620 Ma granitoids. These data
indicate an important change in the magma source with time.The oldest granitoids seem to represent a mixture of
Neoproterozoic, juvenile, mantle-derived material with
magma derived from the melting of Paleoproterozoic conti-nental crust, which yielded intermediate Nd model ages, of
ca. 1.2-1.4 Ga. This is compatible with the mixture of mantle-
derived and crustal magmas, as indicated by field relation-ships that show close relationships between host granitoid
and K-dioritic magmas. The 590-570 Ma plutons have Sr and
Nd isotopic values compatible with magmas formed byremelting of Paleoproterozoic lower continental crust, the
only geochemical reservoir with these characteristics. The
only exception among these rocks are the ultrapotassic peral-kalic syenitoids, which present high initial Sr ratios and very
negative εNd values, interpreted as derived from an incom-
patible element enriched mantle source. The oldest group ofrocks has signatures typical of syn-tectonic granites, while
the 590-570 Ma group has signatures typical of late- to post-
tectonic magmas.
Keywords: Granites, Calc-Alkalic Granites, Peralkalic
Syenites, Shoshonitic Granites, Transversal Zone, MagmaticEpidote, Crustal Evolution, Borborema Province.
Resumen:Magmatismo granítico en la Zona Transversa de la
Província estructural de Borborema, en el nordeste de Brasil,
se produjo en tres intervalos de tiempo: 650-620 Ma, 590-570Ma y 545-520 Ma. El grupo más viejo está caracterizado por
intrusiones de rocas graníticas calco-alcalinas con alto pota-
sio, calco-alcalinas y shoshoníticas, sin a tardi-cinemáticas,con epidota magmática. El segundo intervalo de tiempo de
intrusiones está marcado por abundantes magmas calco-
alcalinos de alto potasio sin epidota magmática, sienitas per-alcalinas o metaluminosas de alto potasio, magmas ultra-
potásicos y, raramente, shoshoníticos. Magmas peralcalinos
y escasos magmas del tipo-A marcan el final del cicloBrasiliano en esta región. Los granitos más viejos presentan
TDM más joven (< 2.0 Ga) y valores menos negativo εNd(desde -2 hasta -14) comparados con los granitos con 590-570 Ma para los cuales TDM varía desde 1.5 hasta 2.5 Ga, y
εNd desde ca. -8 hasta -20. Valores más altos y más variables
de razones iniciales 87Sr/86Sr son observados en el grupo degranitoides con 650-620 Ma. Estos datos indican un impor-
tante cambio de fuente de magma con el tiempo. Los grani-
toides más viejos parecen representar una mezcla de materialjoven derivado del manto, en el Neoproterozoico, con magma
derivado de la fusión de la corteza continental Paleoproterozoica
que ha generado edades modelos intermediarias desde 1.2
hasta 1.4 Ga. Esto es compatible con un proceso de mezcla de
magmas derivados de la corteza, como lo indican las rela-ciones de campo que muestran íntima relación entre magmas
graníticos y magmas dioríticos potásicos. Los plutones con
590-570 Ma tienen valores isotópicos de Sr y Nd compatiblescon magmas formados por refusión de la corteza continental
Paleoproterozoica inferior, el único reservatorio con estas
características. La excepción entre estas rocas correspondena las sienitas peralcalinas ultrapotásicas que presentan alta
razón isotópica inicial de Sr y valores de εNd muy negativos,
interpretados como derivados de una fuente en el manto muyrica en elementos incompatibles. El grupo de rocas graníti-
cas más viejas posee signaturas geoquímicas típicas de gra-
nitos sintectónicos, mientras los granitos más jóvenes pre-sentan signaturas típicas de magmas tardías pos-tectónicos.
Palabras llave: Granitos, Granitos Calco-Alcalinos,Sienitas Peralcalinas, Granitos Shoshoníticos, Epidota
Magmática, Magmas Ultrapotásicos, Zona Transversa,
Evolución Cortical, Província Borborema.
Introduction
The Borborema structural province, northeastern
Brazil, is a mosaic of metasedimentary fold belts and massifs
separated by a complex system of continental-scale strike-slipshear zones (Almeida et al., 1981), which together with the
voluminous granitic magmatism, are the most outstanding
features of this province (Caby et al., 1991). The tectonic evolution of the province has been
explained by models involving the accretion of tectonostrati-
graphic terranes as the major mechanism of crustal growth(eg. Brito Neves et al., 1995; Santos, 1996; Santos et al.,
1997, Santos & Medeiros, 1999; Brito Neves et al., 2000).
Mafic to ultramafic complexes, some of them interpreted asoceanic crust remnants (Beurlen et al., 1992), occur nearby
suspect terrane boundaries, and were used by Santos et al.
(1997) as argument to reinforce the hypothesis of collision ofcontinental blocks. Juxtaposition of blocks during the
Brasiliano cycle has been invoked by many authors, on the
basis of structural geology (eg. Bittar & Campos Neto, 2000),U-Pb zircon ages and Sm-Nd isotopic data from orthogneisses
(e.g. Fetter et al., 2000), as well as from undeformed granitic
rocks (eg. Sampaio et al., 2000; Silva Filho et al., 2000).This process of terrane collage took place during
assembly of the western Gondwana (Santos & Brito Neves,
1993; Brito Neves et al., 2000). Some authors, however, pres-ent alternative hypothesis to the generally accepted model of
terrane accretion, based on geochemical signatures of high-K
calc-alkalic and associated dioritic rocks (e.g. Mariano et al.,2000; Neves et al., 2000), as well as on the lack of some
parameters indicative of continental margin, such as ophio-
lites (Neves, et al., 2000; who proposed an intracontinentalorogen for the whole province).
In the present study, the geochemical and isotopic char-
acteristics of the intermediate to acidic magmatism intrusiveduring the Brasiliano orogeny in the Transversal zone domain
of the Borborema Province, will be reviewed and discussed,
aiming to understand their meaning in the scenario of crustalevolution of the region.
Geological setting
The Borborema province is characterized by a gently-
dipping regional foliation observed in both supracrustal andbasement rocks (Caby et al., 1995), and by a network of con-
tinental scale transcurrent ductile shear zones (Vauchez et al.,
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alkalic, and shoshonitic granitoids at 650-620 Ma. (2) a late to post-collisional period (590-570 Ma),
marked by relative movements of terranes partially amalga-
mated, and migration of terranes along E-W Pernambuco andPatos mega shear zones, as well as along the narrower NE-
trending shear zones connecting these major shear zones, as
indicated by the synkinematic crystallization of several plu-tons emplaced along these shear zones. This period is charac-
terized by intrusions of voluminous magmatic epidote-free
high-K calc-alkalic magmas, peralkalic, metaluminous high-K syenitic, and rare shoshonitic magmas, as well as unique
ultrapotassic magmas, until most movements along shear
zones stopped. Peralkalic and rare A-type magmas mark the end of the
Brasiliano cycle in the region.
The Transversal Zone domain
The Transversal Zone domain of the Borboremaprovince has been interpreted as a superterrane (Santos, 1996;
Santos et al., 1997) assembled after a collage of several ter-
ranes and belts, which are from east to west: Granjeiro,Cachoeirinha (Brasiliano age), and the pre-Brasiliano ter-
ranes Riacho Gravatá, Alto Pajeú, Alto Moxotó and Rio
Capibaribe (Fig. 1). The consolidation of the pre-Brasilianoterranes is related to the Transamazonian and Cariris Velhos
cycles, but they have been reworked during the Brasiliano
cycle (Santos et al., 2003). A complete picture of the tectonic setting and crustal
evolution of the Transversal Zone is still far from being solved
and consensual, but geochronological data, including Rb-Sr,zircon TIMS and SHRIMP U-Pb on a significantly large num-
ber of granitic plutons, led Brito Neves et al. (2003) to propose
three main stages of granitic magmatism in the province: 650-625 Ma, 580-570 Ma e 545-520 Ma.
Almeida et al. (1967) were pioneers in the study of gran-
ite types in this part of the Borborema province. They describedin the Granjeiro and Cachoeirinha terranes, on the basis of pet-
rography, the granitoids of the so-called Itaporanga and
Conceição types, terminology that is still used in the region.Eight petrogenetic suites were described in the
Transversal Zone by Sial (1987) and Ferreira et al. (1998),
including the two types recognized by Almeida et al (op cit.),on the basis of petrography and mineralogy, chemistry, and
1995). These Neoproterozoic shear zones are believed to havedeveloped within a continental plate to accommodate the
deformation imposed by oblique collision active at the mar-
gin (Vauchez et al., op cit.). The structural characteristics and rock types of the
Borborema province were developed mainly during the late
Mesoproterozoic to early Neoproterozoic (Cariris Velhosevent) and late Neoproterozoic-Cambrian (Brasiliano/Pan
African orogeny) (Brito Neves et al., 2000; 2003). The
Brasiliano cycle (670-570 Ma) promoted reworking of thecrust formed during the earlier Cariris Velhos event and was
the major tectonothermal event in the Borborema province.
This is attested by the structures and by a large volume ofgranitic magmatism (~30% of the exposed rocks) that was
added to the crust during this event. The Cariris Velhos-age
rocks have been observed only in the Transversal Zonedomain of the Borborema province (Brito Neves et al., 2000).
Two of the shear zones in the province, the E-W-trend-
ing dextral Pernambuco and Patos shear zones, stand out fortheir large dimensions, which reach over 500 km and 2 km in
width, linked with narrower (typically 1 km) N- NE-trending
shear zones (Neves, 1996). They subdivide the province intothree major domains (Fig. 1): (a) setentrional domain, north
of the Patos shear zone, (b) Transversal zone domain,
between the two shear zones and (c) the meridional domain,south of the Pernambuco shear zone. These domains are inter-
preted as representing a collage of smaller lithotectonic
domains (Brito Neves et al., 2000). Spatial association ofgranitic plutons and shear zones, as well as peralkalic syenitic
dike sets parallel to or slightly oblique to the shear zone, has
led many authors to believe that shear zones have controlledthe magma ascent and emplacement (eg. Ferreira & Sial,
1986; Neves, 1991; Jardim de Sá, 1993; Archanjo et al., 1994;
Neves & Vauchez, 1995; Araújo et al., 1995; Hollanda et al.,1998). However, regional deformation, magma emplacement
and shear zone development are interpreted as successive
events in the Transversal Zone (Neves & Vauchez, 1995).
Integration of geochronological, geochemical and field
data, on both granitic and regional metamorphic rocks, sug-gest two major episodes in the Brasiliano cycle:
(1) collisional period (670-620 Ma), characterized by
low-angle foliation, and by intrusion of abundant syn-kine-matic magmatic-epidote bearing high-K calc-alkalic, calc-
191Cap XII
Fig. 1. Transversal Zone of the Borborema structural province, northeastern Brazil, emphasizing Neoproterozoic granitic andsyenitic plutons. Terranes are named after Santos et al.(1997)
- Zona Transversal da província estrutural da Borborema, Nordeste do Brasil, enfatizando os plútons neoproterozóicos graníticose sieníticos. Os terrenos são nomeados de acordo com Santos et al.(1997)
isotopic characteristics, four of which are magmatic epidote-
bearing (mEp). These are: mEp metaluminous high-K calc
alkalic, metaluminous high-K calc alkalic epidote-free, mEptrondhjemitic, mEp metaluminous calc-alkalic, mEp
shoshonitic, peralkalic, peralkalic ultrapotassic, and metalu-
minous high-K syenitoids. Further work focussing the AltoPajeú terrane, confirmed this grouping (eg. Guimarães et al.,
1998). One A-type calc-alkalic anorogenic complex is
described in the Alto Moxotó terrane (Melo et al., 1996).Large areas of the Granjeiro terrane are covered by
Mesozoic sediments of the Araripe Basin and are not well
known. Only a few plutons are described in this terrane.Among them are the 580 Ma magmatic epidote-free high-K
calc-alkalic granitoids (Itaporanga, Bodocó and Serra da
Lagoinha granitoids) and peralkalic syenitic, foliated plutons,emplaced next to the boundary with the Cachoeirinha terrane.
The Cachoeirinha terrane corresponds to a late
Neoproterozoic foldbelt that contains low-grade psammitic andpelitic rhythmite beds with a few intercalations of mafic to fel-
sic volcanic rocks (Brito Neves et al., 2000). This terrane used
to be described together with the Riacho Gravatá terrane as asingle belt, and known as the Piancó-Alto Brígida (Brito
Neves, 1983) or as the Cachoeirinha-Salgueiro foldbelt (Sial,
1984). The Brasiliano magmatism during the 650-620 Mainterval, in this terrane, is mainly calc-alkalic (e.g. the plutons
regionally known as Conceição-type granitoids), with subordi-
nate throndhjemite (e.g. Serrita pluton), whereas during the590-570 Ma interval rocks are more K-enriched, shoshonitic to
peralkalic in composition (e.g. Serrote dos Cavalos stock).
The Riacho Gravatá belt comprises volcanic rocks(mainly felsic, with subordinate mafic and intermediate) with
minor sedimentary rocks, metamorphosed in greenschist
facies. Brasiliano granitoids are rare in this domain.
The Alto Pajeú terrane is a metavolcano-sedimentary
domain with peak metamorphic age around 960 Ma, during
the contractional Cariris Velhos event (Santos et al., 2003).This terrane was deformed once more during the Brasiliano
cycle, which in this domain is characterized by voluminous
magmatism in three time intervals, beginning with high-Kcalc-alkalic and shoshonitic magmas, intruded during the
650-620 Ma interval (e.g. Tavares batholith, Pessôa, 2001;
Conceição das Creoulas batholith, Brasilino et al., 1998).Magmatism in the 590-570 Ma interval began with high-K
calc-alkalic series followed by unique ultrapotassic magmas
(eg. Triunfo syenite, Ferreira et al., 1994) so far not found inany other domain of the Borborema province. Peralkalic
dikes cutting across the boundary between this and the
Cachoeirinha and Rio Capibaribe terranes (Silva Filho et al.,1993; Ferreira & Sial, 1997; 2002) register the end of the
Brasiliano cycle (520 Ma) in the Borborema province.
The Rio Capibaribe terrane consists of Transamazonian(2.2-1.8 Ga) basement covered by two major complexes. The
oldest is the Vertentes complex that encompasses a migma-
tized volcano-sedimentary sequence probably related to theCariris Velhos event (Brito Neves et al., 2000). The younger
sequence (Surubim complex) is mainly composed of
metapelites and metacarbonates of probable Neoproterozoicage. Mesoproterozoic anorogenic magmatism (gabbro,
anorthosite, mafic dikes and A-type granites) is a characteris-
tic of this terrane (Brito Neves et al., op cit.). Neoproterozoicgranitic magmatism in this terrane started with high-K calc-
alkalic magmas at ca. 690 Ma (Bezerros pluton; Silva et al.,
1996). The peak of magmatism at 580 Ma was mostly of met-aluminous high-K (eg. Bom Jardim syenite; Guimarães and
Silva Filho, 1997) to high-K calc-alkalic rocks (e.g. Fazenda
Nova and Serra da Japecanga complexes, Neves & Vauchez,1995). Post-kinematic magmatism is characterized by silica-
oversaturated peralkalic intrusions (e.g. Moderna pluton,
Ferreira & Sial, 2002).The Alto Moxotó terrane consists of large areas of
Paleoproterozoic basement, including some Archean rem-
nants, and some early Neoproterozoic supracrustal sequences(Lagoa das Contendas, Sertânia, Caroalina complexes; Brito
Neves et al, 2000). Brasiliano granitic magmatism is rare in
this terrane compared to other terranes, but it contains one ofthe two A-type granitic complexes described in the
Transversal Zone (Prata complex, Melo et al., 1996).
192
Fig. 2. QAP diagram for neoproterozoic granitic and syenitic plutons ofthe Transversal Zone. The magma series trends are from Lameyre andBowden (1982). TH = trondhjemite, LKCA = low-K calc-alkalic,MKCA = medium-K calc-alkalic. Shaded areas represent modal com-positions for the studied granitoids and syenitoids, classified accordingto one of these series
- Diagrama QAP para plutons Neoproterozócios graníticos e sieníticosda Zona Transversal. As séries de magmas são de Lameyre e Bowden(1982). TH = trondhjemito, LKCA = cálcio-alcalino de baixo K, MKCA= cálcio-alcalino de médio K. As áreas sombreadas representam ascomposições modais dos granitóides e sienitóides estudados, classifica-dos de acordo com uma dessas séries
Fig. 3. Amphibole-rich clots hosted by diorite enclave, which isin turn hosted by 650-620 Ma magmatic epidote-bearing gran-
odiorites, in the Cachoeirinha-Salgueiro terrane, TransversalZone
- Agregados ricos em anfibólios inclusos em enclave diorítico,que por sua vez está incluso em granodioritos com epidoto
magmático de 650-620 Ma, no terreno Cachoeirinha-Salgueiro,Zona Transversal
bole, biotite, microcline, epidote, and sphene, a mineral com-position typical of I-type granitoids, as defined by Chappell &
White (2001). Unlike the high-K calc-alkalic (HKCA) grani-
toids in the Transversal Zone, megacrysts in these CA plutonsare plagioclase. Two plutons, Santo Antonio and Angico
Torto, exhibit kyanite-bearing black-spotted aureoles a few
meters from the contact with these plutons, characterized byfine-grained mica foliation, and the assemblage garnet, kyan-
ite, staurolite, muscovite with Si < 3.1, biotite, plagioclase
and quartz. Quartz and rutile inclusions in garnet suggestpeak P9 kbar during garnet growth (Caby & Sial, 1996)
Amphibole-rich clots are common and widespread in
all plutons of this kind in the Cachoeirinha terrane (Fig. 3).They consist of deep green calcic amphibole aggregates frac-
tionated from host magma, or as fine-grained, angular amphi-
bolite containing calcic plagioclase that is regarded as frag-ments from the source rock for the tonalite-granodiorite mag-
Fig. 4. Photomicrographs ofmagmatic epidote in 650-620 Ma
granitoid from the TransversalZone: (a) euhedral, 1 mm long,
partially enclosed by biotite(nicols crossed). (b) subhedral
(ca. 1.2 mm long) with allanitecore, partially enclosed bybiotite (nicols not crossed)
- Fotomicrografias de epidotomagmático em granitóides de
650-620 Ma da ZonaTransversal: (a) euédrico, 1 mm
de comprimento, parcialmenteenglobado por biotita (nicóis
cruzados); (b) subédrico (ca de1.2 mm de comprimento) com
núcleo de allanita, parcialmenteenglobado por biotita (nicóis
paralelos)
193Cap XII
a
b
Field relationships and petrography
650-620 Ma-old, syn-kinematic magmatism:Magmatic epidote-bearing granitoids
Magmatic epidote (mEp)-bearing calc-alkalic (CA)granitoids in the Cachoeirinha terrane are metaluminous to
slightly peraluminous tonalites to granodiorites, forming
batholiths and stocks that constitute the so-called Conceição-type granitoids, as described by Almeida et al. (1967). They
intruded low-grade metaturbidites and metapelites (Sial,
1993; Sial et al., 1999). All intrusions have crystallizationages around 630 Ma. They form a compositional trend in the
QAP diagram following the low-K calc-alkalic trend of
Lameyre & Bowden (1982) (Fig. 2). They usually formequigranular, medium- to coarse-grained, round to elongate
plutons composed of zoned plagioclase, quartz, calcic amphi-
194
ning and inclusions of zircon that display inherited cores.
Some primary epidote grains have allanite core. The HKCA plutons in this terrane are porphyritic monzodi-
orites to granodiorites characterized by K-feldspar
megacrysts, up to 15 cm long. Magmatic epidote in these plu-tons occupies up to 5% per volume and is included in plagio-
clase or rimmed by biotite, sometimes with allanite core.
They present magmatic structures indicative of highfluid dynamics and minor mingling with K-dioritic magmas.
These structures are observed in all plutons of this type in this
terrane, but the Tavares and Brejinho plutons, in particular,are the ones where magmatic structures are very well devel-
oped and preserved. Among the structures (Fig. 5) are
(Pessôa, 2001): (a) elliptical and circular structures character-ized by rythmic, concentric banding, in which mafic and fel-
sic bands alternate, in a pattern observed in vertical and hori-
zontal expositions, indicating a tridimensional nature; (b)Ladder dikes, and up a 1 m long snail structures, in which
magma flow is at a high angle to the magmatic foliation. They
are characterized by concave mafic-rich bands that alternatewith felsic-rich bands, and mineral composition similar to the
host granite, and in many of them K-feldspar cumulates occur
in the nucleus; (c) “channel” composed of pillow-like K dior-ites sitting in a felsic matrix. These structures are indicative of
convection during the formation of the magma chamber due
to intermittent heat input from external source. These fea-tures are interpreted to be due to convective currents origi-
nated by underplating of mafic magma (Weinberg et al.,
2001), implying in contrast of temperatures within the
mas (Sial, 1993; Sial et al., 1999). High δ18O (zircon) values
(11.1‰-11.8‰) are found in the Emas granitoid, one pluton
of this type in this terrane (Ferreira et al., 2003). These highmagmatic values are compatible with altered seafloor basalt,
which has suffered oxygen exchange with low-temperature
oceanic water, as protolith. Amphibole-rich clots showinghigh δ18O (whole-rock) values (9.9‰-11.5‰), usually 1.5‰
lower than in corresponding host granitic rocks (Sial et al.,
1998) support this hypothesis. Several plutons in the Alto Pajeú terrane contain mag-
matic epidote (Sial et al., 1999) (Fig. 4): Teixeira granitoid
(shoshonitic), Brejinho, Tavares, Conceição das Creoulas,Murici, and Riacho do Icó plutons (metaluminous high-K
calc alkalic).
The E-W-trending Teixeira composite batholith isformed by three intrusions: (a) shoshonitic monzonite (cen-
tral-eastern part), (b) throndhjemitic tonalite (western por-
tion), and (c) peralkalic syenite (a small eastern intrusion).The shoshonitic granitoids predominate over the other types.
They are mostly equigranular, fine- to medium-grained pera-
luminous quartz monzonites to monzogranites, forming atrend between that of the high-K and medium-K calc alkalic
series in the QAP diagram (Fig. 2). In these rocks, perthitic
microcline (flake and veined perthite) predominates over pla-gioclase and quartz. Plagioclase in contact with microcline
usually exhibits drop-like quartz inclusions, and myrmekite,
and is often deformed with bent twinning plane and wavyextinction. Among the mafic phases, ferro edenite is the most
common, sometimes forming agglomerates, showing twin-
Fig. 5. Magmatic structures in high-K calc-alkalic granitoids of the Transversal Zone: (a) snail structure; (b) ladder dike; (c) channel ofpillow-like K-diorite in a more felsic matrix; (d) snapshot of a structure in a vertical section across a thermal plume head
- Estruturas magmáticas em granitóides cálcio-alcalinos de alto K da Zona Transversal: (a) estrutura em caracol; (b) diques em escada;(c) canal de K-dioritos com estrutura em almofada em matriz mais félsica; (d) estrutura de uma seção vertical do topo de uma pluma tér-mica
a
b
c
d
that is 580-570 Ma old and another one that is 520 Ma old,
and will be discussed in the next section.
The older group consists of ultrapotassic syenitoidsthat occur within the southwestern region of the terrane (Serra
do Man batholith, Ferreira et al., 2002), or are part of the
syenitoid line recognized by Ferreira & Sial (1986), whichoccur along the boundary between the Alto Pajeú and
Cachoeirinha terrane (Triunfo, Serra do Casé, Serra do
Livramento, Serrote das Duas Irmãs, Serrote do Paulo, andBom Nome plutons). The ultrapotassic alkali feldspar syeni-
toids are mineralogically very simple, consisting of perthitic
microcline and aegirine-augite as main phases, and sphene,apatite, quartz, and rare magnetite and richterite after pyrox-
ene, as accessory phases. Alkalic pyroxenites are found as co-
magmatic inclusions, syn-plutonic, and late-stage dikes in theplutons along the syenitoid line, and have the same mineral
phases as the host syenite, although in different proportions
(Fig. 6). Host syenite and alkalic pyroxenite inclusions areinterpreted as formed after liquid immiscibility process from
a single mafic syenite magma (Ferreira et al., 1994).
Mica-pyroxenite xenoliths found in the Triunfo syeniteare interpreted as derived from the lithospheric mantle source
of the syenite (Ferreira et al., 1995). They are composed of
diopside-salite (80% of the bulk rock), with subordinate (andin variable amounts) F-rich phlogopite, which shows chem-
istry comparable with that observed in kimberlites and high
195Cap XII
magma chamber at short distances. The concentric struc-
tures represent magma flow in conduits and a frozen snap-
shot of thermal plume. Mafic-intermediate syn-plutonicdikes, indicative of mingling of magmas, are also present.
Ages of plutons of this type range from 651 ± 15 Ma
(TIMS zircon U-Pb, Tavares pluton, Brito Neves et al.,2003) to 638 ± 5 Ma (TIMS zircon U-Pb, Brejinho pluton;
Guimarães & Silva Filho, 2000). A Rb-Sr isochron yields an
age of 638 ± 29 Ma for the Conceição das Creoulas pluton(Brasilino et al., 1998). Pb-Pb zircon evaporation method
indicates an age of 643 ± 2 Ma for the Remédios pluton.
The plutons in the Alto Pajeú terranes are interpreted,on the basis of geochemistry, as emplaced in an early- to
syn-orogenic event in a collisional setting (e.g.Guimarães et
al., 1998; Brasilino et al., 1998; Brito Neves et al., 2003).The plutons in the Cachoeirinha terrane are interpreted as
emplaced syn-tectonically in a contractional event (Sial,
1993).
590-570 Ma-old, late-kinematic magmatism
The magmatic epidote-free high-K calc alkalic granitoids
Plutons of this type are intruded in the Granjeiro ter-
rane (Bodocó, Itaporanga and Serra da Lagoinha plutonsthat constitute the so-called Itaporanga-type granitoids as
described by Almeida et al., 1967), and in the Alto Pajeú ter-
rane (e.g. Fazenda Nova, Serra da Japecanga, Brejo daMadre de Deus, Campina Grande, Esperança batholiths).
They have been emplaced near terrane boundaries, and have
peak emplacement age around 580 Ma, except for theBezerros batholith, which is the oldest (687 Ma), and the
only one that presents solid-state foliation (Silva et al.,
1996).Similarly to the mEp-bearing calc-alkalic granitoids,
these plutons are characterized by porphyritic textures, with
up to 8 cm long K-feldspar megacrysts. They range in com-position from quartz monzonite, quartz syenite to monzo-
granite, forming a trend in the QAP diagram in the field of
high-K calc alkalic granitoids (Fig. 2). As in the case of thethe mEp-bearing HKCA granitoids, these plutons feature
magma mingling with dioritic magma, and among these, a
mixing of magmas of contrasting compositions, which wasan important petrogenetic process (e.g. Mariano, 1989,
McMurry, 2001, Neves and Vauchez, 1995, Sial et al.,
1989). Evidence of successive mafic magma supplies,which continued at a declining rate, can be observed in the
Fazenda Nova/Serra da Japecanga complex. This led to the
production of stromatic-like structures, followed by theintrusion of contorted syn-plutonic dikes, and of late-stage
dikes, some of which have chilled finer-grained margins
(Neves and Vauchez, 1995).Mixing of granitic and dioritic magma was more
intense in some plutons (e.g. Itaporanga and Bodocó) and
favoured the expressive development of hybrid granodior-ites showing field and petrographic evidence of mingling,
such as pillow-like and net-veined structures, and mantled
feldspar megacrysts captured from the host quartz mon-zonite. Large mixed zones can be mapped in these plutons at
small scales (e.g. Mariano, 1989; McMurry, 2001).
The Itaporanga pluton in the Granjeiro terrane had itsemplacement in a transpressive shear zone system, with the
ascent of magma facilitated by pre-existing steep fault zone
that bounds crustal discontinuities (Archanjo et al., 1999).
The peralkalic potassic to ultrapotassic syenitoids
The Transversal Zone is the domain in the Borboremaprovince that presents the largest and more widespread peral-
kalic syenitoid and granitoid plutons. Syenitoids form a group
Fig. 6. Field relationships between the 570 Ma Triunfo ultrapotassicsyenites and coexisting alkalic pyroxenite, formed by a liquid immisci-bility process (a) co-magmatic alkalic pyroxenite enclaves; (b) syn-plu-
tonic dike of alkalic pyroxenite
- Relações de campo entre os sienitos ultrapotássicos de Triunfo de 570Ma e piroxenitos alcalinos coexistentes, relacionados por um processode imiscibilidade de líquidos: (a) enclaves co-magmáticos de piroxeni-
to alcalino; (b) dique sin-plutônico de piroxenito alcalino
a
b
pressure xenoliths in kimberlites, calcite, hyalophane, sphene,
apatite, and traces of barite.
A gravimetric study performed on the Triunfo batholith(Motta, 2000), the largest known peralkalic ultrapotassic
body in the Borborema province, confirms the existence of a
denser layer, below the syenite, with a density compatiblewith that of alkalic pyroxenite. The gravimetric modeling
suggests a proportion of 97.5/2.5 (syenite/pyroxenite), a lat-
eral extension of 20 km and maximum thickness of 8.5 km,the pyroxenite being only 200 m thick, and a structure inter-
mediate between a lacolith and a lapolith (Motta op cit.).
Magnetic fabrics and microstructures in the Triunfobatholith suggest that it has a tabular shape, and that magma
emplacement occurred by lateral migration along a flat-lying
crustal structure after fracture propagation and ascension ofmagma, during a crustal extension event with a minimum
compressive stress (Archanjo & Bouchez, 1997).
Peralkalic potassic granitoids are quartz alkali syen-ites to alkali feldspar granites that occur as ring dikes around
mEp-bearing trondhjemites in ring structures (Serrita and SW
Serrita stocks; Neves; 1987; Ferreira & Sial, 1987); as a dikeset near Catingueira town, and as small stocks (Guandu,
Cavalos, Bernardo Vieira, and Cana Brava) (Ferreira & Sial,
op cit). Only one pluton of this type has been dated (U-Pb zir-con age of 573 ± 45 Ma for the Catingueira pluton; Brito
Neves et al., 2003). These rocks contain aegirine-augite and
alkalic amphibole as major mafic phases, with magnetite andapatite as main accessory phases. Fluorite and cassiterite are
locally present at amounts < 0.5%, and albitization is locally
an important phenomenon (e.g. ring dikes at Serrita stocks;Ferreira & Sial, op cit.).
The metaluminous high-K syenitic plutonsPlutons with these characteristics are found in the
Cachoeirinha (Terra Nova pluton), Alto Pajeú (Pajeú) and Rio
Capibaribe (Toritama and Bom Jardim plutons) terranes. The 150 km2 Terra Nova pluton is mainly composed
of porphyritic syenite and quartz syenite in which hornblende
and feldspars are up to 2 cm long phenocrysts in a matrixcomposed of hornblende, plagioclase, quartz, sphene, biotite,
epidote, and ferro-augite (Silva Filho et al., 1987). The
emplacement of this pluton, at 556 ± 79 Ma (Rb-Sr; Silva
196
Fig. 7. Photomicrographs of 545-520 Ma peralkalic dikes of theTransversal Zone: (a) richterite-bearing syenite (largest crystal is c. 0.5mm long) (nicols not crossed); (b) aegirine-augite syenite (pyroxenecrystal is ca. 0.4 mm across) (nicols crossed)
- Fotomicrografia de diques peralcalinos de 545-520 Ma da ZonaTransversal: (a) sienito com richterita (cristal maior tem cerca de 0,5mm de comprimento) (nicóis paralelos); (b) aegirina-augita sienito(cristal de piroxênio tem cerca de 0,4 mm de comprimento (nicóiscruzados)
Fig. 8. SiO2 vs. K2O diagramfor Transversal Zone grani-toids and syenitoids. Fieldsare from Peccerillo andTaylor (1976). SH= shoshon-ite, HK = high-K calc-alkalic,MK = medium-K calc-alka-lic, Low-K = low-K calc alka-lic fields.Epi = epidote;HKCA = high-K calc-alkalic;SH = shoshonitic; MHK =metaluminous high-K;Trondh = trndhjemite; CA =calc-alkalic
Fig. 8. Diagrama SiO2 vs.K2O para granitóides e sieni-tóides da Zona Transversal.Os campos são de Peccerilloand Taylor (1976). SH=shoshonito, HK = cálcio-alcalino de alto K, MK = cál-cio-alcalino de médio K,Low-K = cálcio-alcalino debaixo K. Epi = epidoto;HKCA = cálcio alcalino dealto K; SH = shoshonito;MHK = metaluminoso dealto K; Trondh = trond-hjemito; CA = cálcio alcalino
b
a
migmatites of the Alto Pajeú terrane. They comprise mafic
syenite-monzonites, mesocratic syenites and leucosyenites in
which mafic syenites occur as enclaves and synplutonic dikes(Guimarães & Silva Filho, op cit.). These authors interpreted
the complex as intrusive into the later stage of the Brasiliano
cycle and magmas generated in a metasomatized lithosphericmantle.
520 Ma-old, post-orogenic magmatism
The A-type plutons
Two calc-alkalic A-type plutonic complexes have beenrecognized in the Transversal Zone. One of which is the 570
Ma Queimadas foliated pluton (Almeida et al., 1997). The
other one, which is better known, is the 520 Ma-old Pratacomplex that constitutes a 250 km2 composite intrusion in
gneisses and migmatites (Melo et al., 1996), Alto Moxotó ter-
rane, next to the boundary with the Alto Pajeú terrane. It com-prises several granitic intrusions, and dioritic dikes. The main
pluton consists of porphyritic coarse-grained biotite horn-
blende monzonites and medium-grained equigranular biotitesienogranites, in which rapakivi texture occurs locally.
Fluorite is a common accessory phase, a typical mineral of A-
Filho et al., 1993) is interpreted to have occurred during late-
collisional stage of the Brasiliano cycle, controlled by move-
ments of the Pernambuco shear zone, in a compressiveregime (Silva Filho et al., 1993).
The Pajeú syenite is a large (40 km vs. 20 km) elon-
gate pluton intrusive into gneisses and migmatites of thewesten part of the Alto Pajeú terrane, presenting two major
facies: porphyritic syenite, the major facies, characterized by
2-8 cm K-feldspar megacrysts, and fine-grained syenite. Mineralphases are the same in the two facies (microcline, orthoclase,
quartz, minor plagioclase, calcic amphibole, sphene, epidote,
allanite, apatite, zircon, magnetite) (Reyes et al., 1996).Melanocratic syenitic enclaves, which present acicular
apatite, and net-veined structures, and synplutonic dikes, are
indicative of mingling, and locally mixing of magmas.Enclaves are aligned following the magmatic foliation. TIMS
U-Pb zircon age of 586 ± 21 Ma is reported by Guimarães &
Silva Filho (1998). Reyes et al. (op cit.), on the basis of geo-chemical data, interpret that the emplacement of this pluton
took place in a late to post-collisional setting.
The Bom Jardim (Rb-Sr age of 585 ± 38 Ma; Guimarãesand Silva Filho, 1997) and Toritama complexes are elongate
multiple-injected magmas intrusive into gneisses and
197Cap XII
Terrane
Rio Capibaribe
Rio Capibaribe
Alto Pajeú
Alto Pajeú
Alto Pajeú
Alto Pajeú
Alto Pajeú
Alto Pajeú
Cachoeirinha
Cachoeirinha
Granjeiro
Granjeiro
Rio Capibaribe
Rio Capibaribe
Rio Capibaribe
Rio Capibaribe
Alto Pajeú
Alto Pajeú
Alto Pajeú
Alto Pajeú
Alto Pajeú
Alto Pajeú
Alto Pajeú
Alto Pajeú
Cachoeirinha
Cachoeirinha
Cachoeirinha
Cachoeirinha
Alto Pajeú-
Cachoeirinha
Pajeú boundary
Alto Pajeú-
Cachoeirinha
Pajeú boundary
Alto Pajeú-
Cachoeirinha
Pajeú boundary
Alto Pajeú-
Cachoeirinha
Pajeú boundary
Alto Pajeú-
Cachoeirinha
Pajeú boundary
Magma
series
HKCA
HKCA
HKCA
SH
HKCA
HKCA
SH
HKCA
CA
CA
HKCA
HKCA
MHKS
HKCA
PER/SH
PER
HKCA
SH
HKCA
MHKS
UP
UP
A-type
TROND
CA
SH
MHKS
PER
PER
PER
UP
Pluton
Bezerros
Timbaúba
Tavares
Teixeira
Brejinho
Conceição das Creoulas
Serra do Arapuá
Remédios
Conceição
Emas
Itaporanga
Bodocó
Bom Jardim
Fazenda Nova
Pinheiro
Moderna
S-Caldeirão Encantado
Betânia
Campina Grande
Pajeú
Serra do Man
Triunfo
Prata
Palmeira
Angico Torto
Salgueiro
Terra Nova pluton
Catingueira
Terra Nova dikes
Princesa Isabel dikes
Serra do Livramento
Serrote de Duas Irmãs
Bom Nome
Age Ma
687 ± 34
644 ± 5
651 ± 15
645
638 ± 5
638 ± 29
612 ± 24
643 + 2
635 ± 9 / 633 ± 9
627 ± 19
585 ± 2
559 - 593
592 ± 7 / 585 ± 38
588 ± 12
581 ± 1.6
586 ± 21 592 ± 49
581 ± 28
572
512 ±30
505 ± 4
557 ± 71
556 ± 79
573 ± 45
515 ± 20
Method
Pb-Pb
U-Pb
U-Pb
U-Pb
U-Pb
Rb-Sr
Rb-Sr
Pb-Pb
U-Pb / Rb-Sr
U-Pb
U-Pb
Rb-Sr
U-Pb
U-Pb
U-Pb
U-Pb Rb-Sr
Rb-Sr
Rb-Sr
Rb-Sr
U-Pb
Rb-Sr
Rb-Sr
U-Pb
Rb-Sr
(87Sr/86Sr)i
0.70526
0.7115-0.7080
0.7093
0.71054
0.70598
0.70911
0.7058
0.7057- 0.7063
0.70714
0.70839
0.70903
0.71087
0.710
0.7132
0.71062
0.7047
0.0761
0.71071 / 0.70978
0.7098
0.7088
0.7106
εNd(0.60)
-4.2 to -5.4
-3.4
-13.9
-3.6 to -10.1
- 2.8
-16.6
-1.2
-2.0
-9.0
-19
-12.4
-7.1 -7.6
-13.6
-5.0
-11.9
-16.5
-18.6 -16.0
-17.3
-16.1
-14.2
-3.8
-13.5
-15.6
-17.5
-3.6
T DM
1.4
1.4
2.1
1.84 -1.421.31
2.14
1.23
1.30
1.65
1.9
1.92
1.92
2.14
1.5
1.87
2.10
2.07 2.17
2.47
2.4
2.17
1.40
1.86
2.39
2.37
1.38
reference
Silva et al ., 1996
Guimarães et al., 2001
Brito Neves et al ., 2003*, this work#BBBN oral commu.*; Ferreira, 1991#, this work**
Guimarães e Silva Filho, 2000*, Torres, 2000#Brasilino et al .,**, Brasilino 2003#
This work
This work##, Lins, 2000#
Brito Neves et al ., 2003*, Sial, 1993*#
Van Schmus et al., 1995#, This work*/**
Brito Neves et al ., 2003*, Sial 1987**, Van Schmus
et al., 1995#
McMurry, 2001
Guimarães and Silva Filho, 1997
Van Schmus et al., 1995
This work
This work
This work
Lins, 2000
Almeida et al ., 1997*, Guimarães et al ., 1998#
Guimarães and Silva Filho, 1998
Ferreira et al
Ferreira et al, 1995
Melo et al., 1996
Kozuch et al., 1997
This work
Silva Filho, et al., 1990**, Van Schmus et al., 1995#
Silva Filho et al., 1993**, Van Schmus et al ., 1995#
Brito Neves et al ., 2003*, Van Schmus et al ., 1995#
Silva Filho and Guimarães, 1990**; Ferreira and
Sial, 2002
Ferreira and Sial
Ferreira, 1991
Ferreira, 1991
Ferreira, 1991
Table 1. Radiogenic isotope data for granitoids from the Transversal Zone, Borborema Province, NE Brazil. On the references: * U-Pb data, ** Rb-Sr, data # Sm-Nd, Data## Pb-Pb, data. Group of granitoids: HKCA = high-K calc alkalic; MHKS = metaluminous high-K syenitoids,
PER = peralkalic, SH = shoshonitic, UP = ultrapotassic
type granitoids emplaced at high levels into the crust. Field
evidence for mingling with dioritic magmas, such as syn-plu-
tonic dikes, and net-veined and pillow-like structures, areobserved in most part of the pluton. This complex is inter-
preted by Melo et al. (op cit.) as the result of an extension-
related crustal anorogenic magmatism.
Peralkalic syenitic dikes
The second group of peralkalic rocks as referred to insection “The peralkalic potassic to ultrapotassic syenitoids”
consists of potassic, silica-saturated syenitoids intrusive into
low-metamorphic grade metapelites of the Cachoeirinha ter-rane (Riacho de Santo Antônio dikes, Ferreira & Sial, 2002),
at the Rio Capibaribe terrane (Moderna and associated dike,
Ferreira & Sial, op cit) or forms two dike sets, intrusive at the
southernmost Cachoeirinha terrane, next to the boundary with
the Alto Pajeú terrane (Terra Nova dikes) or across the bound-ary of the two terranes (Princesa Izabel dikes) (Silva Filho et
al., 1993, Ferreira & Sial, 1997). Each dike set is composed
of about 50 dikes each, and are texturally and mineralogical-ly similar.
They are silica saturated to slightly oversaturated
alkali feldspar trachyte/syenite, presenting large textural vari-ation, including aphanitic, fine- to medium-grained types,
which have equigranular, inequigranular or microporphyritic
textures. Main phases in both dike sets are zoned orthoclase,aegirine-augite to aegirine and amphibole (early crystallized
pargasite to Fe-pargasite or late-crystallized ferro-richerite)
198
Fig. 9. Shand index diagram for Transversal Zone granitoids and syenitoids. Symbols are the same as for Fig. 8
- Diagrama de índice de Shand para granitóides e sienitóides da Zona Transversal. Os símbolos são os mesmos da Fig. 8
Fig. 10. R1 vs. R2 diagram (Batchelor and Bowden, 1985) for Transversal Zone granitoids and syenitoids. Symbols are the same as forFig. 8
- Diagrama R1 vs. R2 (Batchelor & Bowden, 1985) para granitóides e sienitóides da Zona Transversal. Os símbolos são os mesmos daFig. 8
tallization as major petrogenetic process, in spite of the field
evidence for an important mixing and assimilation process ofmore mafic magma in the high-K calc alkalic plutons. The
metaluminous character of these two suites is compatible
with generation from anatexis of a hornblende-rich source(eg. Whitney, 1988), probably in the lower crust. Higher Rb
and Sr contents, and higher Rb/Sr ratios for the HKCA gran-
itoids than for other suites are compatible with the presenceof coexisting, although volumetrically small, mafic magmas.
The mEp-bearing shoshonitic rocks (SH) are metalu-
minous in composition (Fig. 9), exhibit a relatively wide rangeof SiO2 (from ca. 60 up to 75% SiO2), and are characterized
by lower MgO, TiO2, Fe2O3T, and P2O5 contents, higher
Al2O3 and Na2O, and higher Ba/Rb and Sr/Rb ratios than theother groups. They present decreasing Na2O and Al2O3 with
increasing silica contents, in contrast with the other series in
which these oxides have positive correlation (Na2O) orremain constant (Al2O3) with increasing silica.
The potassic and ultrapotassic (UP) plutons are peralka-
lic (Fig. 9), characterized by enrichment in incompatible ele-ments (K, Sr, Ba, P, REE), have low Zr and Nb concentrations,
and present Nb and Ti negative anomalies in MORB-normal-
ized diagrams (Ferreira, 1991). Enrichment in these elementsin the ultrapotassic syenites, as well as in their alkalic pyroxen-
ite co-magmatic inclusions are interpreted as inherited from a
metasomatized-mantle source. This hypothesis is reinforced bythe chemistry of the mica-pyroxenite xenoliths that show also
high K and Ba contents (K2O = 1-5wt%; Ba = 1400-1500ppm),
variable Cr (21-3000 ppm) and Ni (20-280ppm), very low Nb(6 ppm), and high F (0.4-1.8 wt%) contents, being LREE-
enriched (Ferreira et al., 1995).
The trondhjemitic granitoids are all peraluminous, havea major chemistry similar to that of continental trondhjemites,
with high Al2O3 contents (usually > 16%), low MgO (0.10 to
0.53%) and CaO (0.33 to 1.7%), and predominance of Na2Oover K2O (Na2O/K2O varies from 1.19 to 2.6) (Neves, 1986).
Alumina contents decrease with increasing silica contents,
and together with very high Sr (1800-3700 ppm) and Ba(1800 to 7400 ppm) contents, indicate early crystallization of
(Fig. 7). Amphibole in the Terra Nova dikes has more variable
compositions, and has crystallized straight from the magma,while in the Princesa Isabel dikes, amphibole was largely pro-
duced after pyroxene, with few exceptions. Larger textural
variation is observed in the Terra Nova dikes, which cut,among other rocks, the peralkalic ultrapotassic Serra do Casé
and Serra do Livramento plutons (570 Ma), attesting their
younger ages (Rb-Sr age of 515 ± 20 Ma; Silva Filho et al.,1993).
On the basis of marked differences in magnetic suscep-
tibility, O and Nd isotopic data for the two dike sets, Ferreira& Sial (1997) concluded that they are derived from different
mantle sources. The Princesa Izabel dike set is interpreted as
emplaced in a post-orogenic, extensional setting, and marksthe amalgamation after collision between the Cachoeirinha
and Alto Pajeú terranes. The emplacement of the Terra Nova
dike set is interpreted as controlled by the strike-slip regimeof the Pernambuco shear zone in the Early Cambrian (Silva
Filho et al., 1993).
Geochemistry and tectonic setting
Magmatic epidote-bearing granitoids from all seriesgroup close to each other in a SiO2 vs. K2O diagram, in the
HKCA field of Peccerilo & Taylor (1976), with a few samples
lying in the calc-alkalic and shoshonitic fields (Fig. 8).Samples from the other series plot in the shoshonitic field in
this diagram. Trondhjemitic plutons are medium- to high-K
calc-alkalic, peraluminous in composition.The high-K calc alkalic (HKCA), both magmatic epi-
dote bearing and free, and calc alkalic (CA) granitoids are
metaluminous to peraluminous (Fig. 9), being undistinguish-able from each other on the basis of major and minor ele-
ments, as they form overlapping trends in most variation dia-
grams. They show negative correlations between SiO2 andTiO2, CaO, MgO, MnO, and Fe2O3, the opposite behavior
being observed with Na2O and K2O, while Al2O3 remains
constant with increasing silica. Positive correlations betweenBa/Rb vs. Zr/Rb, and Zr/Rb vs. Sr/Rb attest to fractional crys-
199Cap XII
Fig. 11. log Rb vs. Log (Y + Nb) diagram of Pearce et al. (1984) for Transversal Zone granitoids and syenitoids. Syn-colg = syn-collisionalgranites; WPG = within-plate granites; VAG = volcanic-arc granitoids. Symbols are the same as for Fig. 8
Diagrama log Rb vs. Log (Y + Nb) de Pearce et al . (1984) para granitóides e sienitóides da Zona Transversal. Syn-colg = granites sin-col-isionais, WPG = granites intra-placas, VAG = granites de arco vulcânico. Os símbolos são os mesmos da Fig. 8
plagioclase, which is reflected in the peraluminous nature of
the granitoids. Low Rb/Sr precludes the use of the Rb-Sr sys-
tematics for dating (Neves, op cit.). This author proposed thatthe Serrita stock was generated through partial melting of
altered basaltic rocks, where amphibole and garnet remain in
the residue, and subsequent crystallization at pressures above6 kbar.
The high-K syenitoids are metaluminous to slightly
peraluminous (Fig. 9), have SiO2 contents varying from ca.55 to 65wt%, plotting in the field of ultrapotassic rocks in the
SiO2 vs. K2O% diagram (Fig. 8). Likewise the peralkalic plu-
tons, these syenitoids do not show Eu anomaly in REE chon-drite-normalized diagrams. Guimarães & Silva Filho (1990)
found high Ba (2000-4500 ppm) and very high Sr (1000-2200
ppm) contents, as well as high Cr (up to 470 ppm) and Ni (30-250 ppm) in the Bom Jardim complex, compatible with man-
tle-derived magmas, with minor crustal contamination.
Figures 10 and 11 show tectonic discrimination dia-grams for the studied suites of rocks. The oldest (650-620
Ma) plutons display signatures typical of syn-tectonic mag-
matism (destructive plate margins and volcanic-arc granites).On the other hand, the 590-570 and 545-520 Ma plutons are
similar to late to post-tectonic granites (late orogenic and vol-
canic arc granites transitional to within plate granites).
Sr and Nd isotopes
Sr and Nd isotopic data for plutons of the Transversal
Zone compiled from literature and from this work are listed
in Table 1.The initial (87Sr/86Sr) ratios of the shoshonitic grani-
toids are the lowest among the studied granitoids, varying
from 0.7047 (Salgueiro pluton) to 0.70526 (Teixeira grani-toid), compatible with limited crustal contribution. Initial Sr
ratios for the mEp-bearing CA granitoids are variable, rang-
ing from 0.70598 to 0.710621. These values are lower,
although partially overlapping, than the values for the mEp-
bearing HKCA group (0.70839-0.71002). Low initial Sr
ratios are observed for the epidote-free HKCA granitoids,around 0.706, in spite of field evidence for local mixing
between crustal and mantle-derived magmas. The A-type
granitoid presents high initial 87Sr/86Sr (0.71320; Melo et al.,1996), which suggests an important crustal component
involved in their source.
The peralkalic potassic and ultrapotassic syenitoidshave high initial Sr ratios, 0.710, which together with strong-
ly negative εNd values (ca. -19) are interpreted as inherited
from a contaminated upper mantle source (Ferreira et al.,1997).
The values of εNd (0.6 Ga) for all groups are negative,
and there is a tendency for younger suites to have more neg-ative values, compatible with interaction with a thicker crust.
Magmatic epidote-bearing CA granitoids from the
Cachoeirinha terrane display εNd (0.6Ga) in the -1 to -2range, and TDM model ages between 1.2 and 1.4 Ga (Sial
et al., 1999). These data, together with the low initial Sr ratios
and widespread presence of amphibole-rich clots, are com-patible with the hypothesis of generation of these tonalites
and granodiorites by partial melting of a metabasalt.
Values of εNd for these mEp-bearing CA granitoids arelower and with a restricted range compared to the values for
the mEp-bearing HKCA granitoids that occur in the Alto
Pajeú terrane (-2.8 to - 10.1). The values of εNd are morevariable also in a single pluton (e.g. from -3.6 to -10 in the
Brejinho granitoid) and are compatible with variable degrees
of interaction of mantle-derived magma with crustal material. The peralkalic syenite dikes present two distinct εNd
and TDM values: less negative εNd (-3.6) and younger TDM(1.38 Ga) for the Princesa Izabel dikes, that occur across andin both sides of the Cachoeirinha and Alto Pajeú terrane
boundary, at the northernmost part of the syenitoid line, and
more negative εNd (-17) and older TDM (2.37 Ga) for the
200
Fig. 12. Nd vs. Nd model age plot for Transversal Zone granitoids and syenitoids. Symbols are the same as for Fig. 8
- Diagrama Nd vs. idade modelo Nd para granitóides e sienitóides da Zona Transversal. Os símbolos são os mesmos da Fig. 8
ships that show close relationships between the host granitoid
with K-dioritic magmas. An alternative hypothesis is that the
oldest granitoids are the product of remelting ofMesoproterozoic continental crust.
Most works on the Borborema province have conclud-
ed studies that during the Brasiliano cycle no juvenile materi-al was added to the crust, although mantle material is very
common and presence of two magmas is observed in most
suites of the region (Sial et al, 1992). A tectono-thermal evo-lution with intralithospheric differentiation is interpreted for
the Brasiliano cycle at this part of the Borborema province
(Neves et al., 2000). Positive εNd isotopic data determinedon calc-alkalic granodiorites emplaced at the easternmost
extension of the Patos shear zone (B.B. de Brito Neves, writ-
ten communication, 2003), however, suggest presence ofjuvenile material. This evidence, although observed so far in
only one Neoproterozoic pluton, coupled with the possibility
that juvenile Neoproterozoic mantle-derived magma wasinvolved in the production of the 650-620 Ma granitoids,
must be taken into account in the models for the tectonic
model for the evolution of the province.The 590-570 Ma plutons have Sr and Nd isotopic
values of magmas formed by remelting of Paleoproterozoic
lower continental crust, the only geochemical reservoir withthese characteristics. The only exception among these
younger rocks are the ultrapotassic peralkalic syenitoids,
which present high initial Sr ratios and very negative εNdvalues, interpreted as derived from an incompatible element
enriched-mantle source.
The 545-520 Ma peralkalic dikes present PaleoproterozoicNd model ages, but the less negative εNd values for the
Manaíra-Princesa Izabel dikes suggest smaller degree of con-
tamination, probably during ascent and emplacement at lowpressure, as also suggested by oxygen isotope values ( δ18O
from +8 to +9‰ SMOW; Ferreira & Sial, 1997) for these
rocks. Strongly negative εNd value for the Terra Nova dikessuggest an incompatible element enriched mantle source,
similar to that for the syenites along the syenitoid line.
Acknowledgments
Part of the field and laboratory work was made pos-sible by means of a grant from CNPq to VPF process n.
463029/00-3.
Terra Nova dikes, that occur in the Cachoeirinha terrane, next
to the boundary with Alto Pajeú terrane, at the southernmost
syenitoid line.Depleted mantle Nd model ages tend to be older in
the younger suites. The mEp-bearing CA and HKCA grani-
toids from the Cachoeirinha and Alto Pajeú terranes havesource of Mesoproterozoic age, while the other suites, includ-
ing the mEp shoshonitic granitoids have Paleoproterozoic
model ages (Fig. 12).
Discussion and conclusion
Predominance of magmatic epidote-bearing granitoids
(solidification pressures around 6 kbar) in the 650-620 Ma
interval in contrast with the presence of magmatic epidote-free (solidification pressure around 3-4 kbar) in the 590-570
Ma time interval for magmas of similar composition is prob-
ably due to contrasting oxidation state of the magma, andmode of emplacement to different stages of tectonic evolu-
tion. Late collision is characterized by a gradual change of
motion from perpendicular to the collision zone to transcur-rent motion, which is initially achieved by ductile deforma-
tion, while the collision is still hot, and is superseded by brit-
tle fracturing (Shackleton, 1986). Hot crust and ductile defor-mation would allow magma to have a rather fast emplace-
ment and solidification rate, which prevented epidote dissolu-
tion (e.g. Sial et al., 1999), as compared with epidote-freesimilar suites emplaced later in the Brasiliano cycle (ca. 580
Ma), in a post-collisional, extensional setting, in brittle con-
ditions, and in which thicker crust was formed.The 650-620 Ma old granitoids present younger εNd
model ages (< 2.0 Ga) and less negative Nd (ca. -2 to -14)
than the 590-570 Ma granitoids, for which TDM varies fromca 1.5 to 2.5 Ga, and εNd from ca. -8 to -20. The highest and
more variable initial 87Sr/86Sr values, on the other hand, are
observed in the oldest granitoids, while lower initial Sr ratiosare found in the 590-570 Ma magmas. These data indicate an
important change of type of magma source with time. The
oldest granitoids could represent a mixture ofNeoproterozoic, juvenile, mantle-derived material with
magma derived from melting of Paleoproterozoic continental
crust, which would yield intermediate Nd model age, of ca.1.2-1.4 Ga. This is compatible with mixture of mantle-
derived and crustal magmas, as indicated by field relation-
201Cap XII