ORIGINAL PAPER
The Itajaı´ foreland basin: a tectono-sedimentary record
of the Ediacaran period, Southern Brazil
M. A. S. Basei • C. O. Drukas • A. P. Nutman • K. Wemmer • L. Dunyi •
P. R. Santos • C. R. Passarelli • M. C. Campos Neto • O. Siga Jr •
L. Osako
Received: 8 April 2010 / Accepted: 5 September 2010 / Published online: 21 October 2010
 Springer-Verlag 2010
Abstract The Itajaı´ Basin located in the southern border
of the Luı´s Alves Microplate is considered as a peripheral
foreland basin related to the Dom Feliciano Belt. It pre-
sents an excellent record of the Ediacaran period, and its
upper parts display the best Brazilian example of Pre-
cambrian turbiditic deposits. The basal succession of Itajaı´
Group is represented by sandstones and conglomerates
(Bau´ Formation) deposited in alluvial and deltaic-fan
systems. The marine upper sequences correspond to the
Ribeira˜o Carvalho (channelized and non-channelized
proximal silty-argillaceous rhythmic turbidites), Ribeira˜o
Neisse (arkosic sandstones and siltites), and Ribeira˜o do
Bode (distal silty turbidites) formations. The Apiu´na
Formation felsic volcanic rocks crosscut the sedimentary
succession. The Cambrian Subida leucosyenogranite rep-
resents the last felsic magmatic activity to affect the Itajaı´
Basin. The Brusque Group and the Floriano´polis Batholith
are proposed as source areas for the sediments of the upper
sequence. For the lower continental units the source areas
are the Santa Catarina, Sa˜o Miguel and Camboriu´ com-
plexes. The lack of any oceanic crust in the Itajaı´ Basin
suggests that the marine units were deposited in a restricted,
internal sea. The sedimentation started around 600 Ma and
ended before 560 Ma as indicated by the emplacement of
rhyolitic domes. The Itajaı´ Basin is temporally and tecton-
ically correlated with the Camaqua˜ Basin in Rio Grande
do Sul and the Arroyo del Soldado/Piria´polis Basin in
Uruguay. It also has several tectono-sedimentary character-
istics in common with the African-equivalent Nama Basin.
Keywords Dom Feliciano Belt  Ediacaran  Foreland
basin  U–Pb SHRIMP ages  Provenance
M. A. S. Basei (&)  C. O. Drukas  P. R. Santos 
C. R. Passarelli  M. C. Campos Neto  O. Siga Jr
Geosciences Institute, USP, Sa˜o Paulo, Brazil
e-mail: baseimas@usp.br
C. O. Drukas
e-mail: cesarosorio_8@hotmail.com
P. R. Santos
e-mail: dosantos@usp.br
C. R. Passarelli
e-mail: crpass@usp.br
M. C. Campos Neto
e-mail: camposnt@usp.br
O. Siga Jr
e-mail: osigajr@usp.br
A. P. Nutman
School of Earth and Environmental Sciences,
University of Wollongong, Wollongong, NSW, Australia
e-mail: allen.nutman@gmail.com
K. Wemmer
Gottingen University, Go¨ttingen, Germany
e-mail: kwemmer@gwdg.de
L. Dunyi
Beijing SHRIMP Center, Chinese Academy of Sciences,
Beijing, China
e-mail: liudunyi@bjshrimp.cn
L. Osako
Geosciences Institute, UFC, Ceara´, Brazil
e-mail: lilianaso@hotmail.com
123
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
DOI 10.1007/s00531-010-0604-4
Introduction
The best record of the transition between the collisional
events that culminated with the constitution of the western
Gondwana (end of the Ediacaran) and the stable conditions
that enabled the installation of the Parana´ Basin (Lower
Paleozoic) is found in the northern portion of southern
Brazil, in a series of sedimentary and volcano-sedimentary
basins that do not show the deformation and metamor-
phism that characterize the units in the adjacent fold belts.
Among the existing Neoproterozoic basins (the Itajaı´,
Camarinha, Corupa´, Campo Alegre, Guaratubinha, and
Castro basins) can be divided into two major groups:
foreland and extensional basins (continental rifts): The
Camarinha and Itajaı´ basins, which are predominantly
sedimentary and situated at the borders of the Ribeira
and Dom Feliciano belts respectively, are interpreted
as peripheral foreland basins. The Castro, Guaratubinha,
Campo Alegre, and Corupa´ basins are extensional and were
installed on an old gneissic substrate. They are predomi-
nantly filled with bimodal volcanic material, and are here
classified as continental rifts.
Except for the Castro Basin, which is the youngest of all
(ca. 550 Ma), the available radiometric information indi-
cates that the main magmatic phase that affected the
extensional basins (ca. 600 Ma) preceded up to 40 Ma that
of the Itajaı´ foreland basin (ca. 560 Ma), with both mag-
matic events taking place between the two main com-
pressional periods of 610 and 535 Ma that can be observed
in southern Brazil. Despite older, but due to their intraplate
setting, the extensional basins are undeformed, whereas the
Itajaı´ and Camarinha foreland basins clearly record defor-
mation associated with the proximity of the adjacent belts.
Geologic Context of Itajaı´ Basin
The northeastern portion of southeastern Brazil encom-
passes five tectonic domains, juxtaposed around
600 ± 10 Ma as part of the western Gondwana assembly
processes (Fig. 1). Two of the four major domains are
constituted by the Paleoproterozoic gneissic-migmatitic
rocks of the Curitiba and Luı´s Alves Microplates, which
separate the Neoproterozoic Ribeira (N) and Dom Felici-
ano (S) belts from one another. The fifth segment occurs in
the coastal region, being represented by the Neoproterozoic
Costeiro Granitic Belt, constituted by a variety of grani-
toids and supracrustal remnants (Basei et al. 1998b).
The Ribeira Belt is predominantly composed of Meso-
proterozoic metasedimentary successions deposited in a
passive margin setting on the eastern edge of the Paran-
apanema Craton. In the Neoproterozoic, this belt behaved
as an active margin, and was intensely affected by calc-
alkaline magmatism represented by large granitic batho-
liths that constitute the roots of the Neoproterozoic Treˆs
Co´rregos, Cunhaporanga, and Agudos Grandes magmatic
arcs. The main metamorphism and deformation overprints
also occurred at this time (Basei et al. 1992, Siga et al.
2009).
The granulite-migmatitic terrains that constitute the
basement of the Curitiba Microplate were grouped into the
Atuba Complex (Siga et al. 1995). These are constituted
by banded biotite-amphibole gneisses, amphibolites, and a
variety of granitoids, which underwent medium- to high-
grade metamorphism. The history of these gneisses starts
with magmatism in the Mesoarchean, around 3.0 Ga (Sato
et al. 2003), with a first migmatization phase in the Oros-
irian (*2,100 Ma) and a second migmatization phase by
the end of the Ediacaran (*600 Ma). The Atuba Complex
has a metasedimentary cover (Capiru and Setuva Forma-
tions) probably of Neoproterozoic age and is crosscut by
several Ediacaran anorogenic granitoids.
The Santa Catarina Granulitic Complex (Hartmann et al.
1979; Kaul 1980; Basei et al. 2009) is a crustal segment
consisting of high-grade metamorphic rocks, predomi-
nantly charno-enderbites and migmatitic gneisses with
occasional mafic–ultramafic bodies and paragneiss rem-
nants. The Campo Alegre Basin (*600 Ma) represents
the main cover recognized in the Luis Alves Microplate
central region. The north–northeast limit with the Curitiba
Microplate is defined by the Pieˆn Suture Zone (Basei et al.
1992; Machiavelli et al. 1993; Harara 2001, Harara et al.
2002).
The evolution of the Santa Catarina Granulitic Complex
started with the emplacement of a 2,600 Ma TTG suite,
which was later affected by regional, Siderian (2,350 Ma)
granulite-facies metamorphism and by an Orosirian (2,000 Ma)
granulite/amphibolite-facies metamorphic event (Basei
et al. 2009). After *1,900 Ma, the region became tec-
tonically stable and was the only block in the southeastern
Brazil that remained cold (\300C) since the end of the
Paleoproterozoic, showing no evidence of the Neoprote-
rozoic tectono-thermal overprint that is characteristic of the
other terranes in the region. Its southern border is covered
with the Itajaı´ Basin sediments, which are in tectonic
contact with the Dom Feliciano Belt supracrustal rocks,
with inverse faulting responsible for tectonic imbrications
related to low-angle thrusts. The domain situated farther
south is represented by the Dom Feliciano Belt northern
termination. As the other segments of this Belt, it is inter-
nally organized into three major compartments (Fig. 2):
the Granitoid Belt (Floriano´polis Batholith arc-related
granitoids), the Schist Belt (Brusque Group sedimentary
covers metamorphosed to the greenschist- to amphibolite-
facies), and the Foreland Belt (Itajaı´ Basin supracrustal
rocks).
544 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
The Floriano´polis Batholith is predominantly composed
of calc-alkaline to alkaline granitoid rocks and late iso-
tropic alkaline granitoids. It represents the roots of an
Ediacaran magmatic arc formed between 620 and 590 Ma
as a result of the eastward subduction of an oceanic crust
(Adamastor Ocean). The supracrustal rocks related to
the Kaoko/Damara/Gariep belts represent the back–arc
deposits (Basei 2000; Basei et al. 2005; 2008b). The
Brusque Group stretches out in a NE–SW belt of ca. 40 km
in width. It is composed of two metavolcano-sedimentary
units separated by the Valsungana Batholith. Metavolcano-
sedimentary successions predominate and represent the
Brusque paleo-basin rift phase. They are characterized by
tourmalinites associated with metabasalts, banded iron
formations, quartzites and calc-silicate rocks, tectonically
overlain by a thick metasedimentary sequence composed
of micaceous quartzites, quartz-sericite schists, sericite
schists, and local acid metavolcanic rocks. The granitic
magmatism is characterized by three isotropic to slightly
deformed granitoid suites of metaluminous to peralumi-
nous composition marked by crustal contribution.
The Itajaı´ Basin
The Itajaı´ Basin represents a foreland-type basin of the
Dom Feliciano Belt deposited by the end of the Neopro-
terozoic, between 600 and 560 Ma. It comprises a thick
pile of sedimentary rocks with a marked turbiditic contri-
bution and was affected by important felsic volcanic
activity (Basei et al. 1998a). It is an asymmetric basin,
elongated approximately in the N60E direction and having
the shape of a sigmoidal prism, with thickening of sedi-
ments from north to south (Rostirolla 1991, Rostirolla et al.
1992). It occupies an area of ca. 700 km2 and extends for
more than 80 km from the coast of Santa Catarina to its
Fig. 1 Tectonic domains
resulting from the
amalgamation of Western
Gondwana. 1 Tertiary and
quaternary covers; 2 Parana´
Basin; 3 Serra do Mar Suite
Granites; 4 Campo Alegre
Basin, 5 Ribeira Belt Southern
Portion; 6 Capiru and Setuba
Metasedimentary sequences; 7
Atuba Complex; 8 Rio Pieˆn
Batholith; 9 Costeiro Granitic
Belt (Paranagua´ and Mongagua´
Batholiths); 10 Santa Catarina
Granulitic Complex; 11 Itajaı´
Foreland Basin; 12 Brusque
Group; 13 Camboriu Complex;
14 Granitoid Belt (Floriano´polis
Batholith); 15 thrusting; 16
inferred contact; 17 tectonic
transport (Simplified after Basei
et al. 2009)
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 545
123
southeastern extremity, covered by the Parana´ Basin sedi-
ments. The northern and southern limits of the Itajaı´ Basin
are well defined in the field and distinct from one to
another. The sediments of the northern border rest on Santa
Catarina Granulitic Complex, the Paleoproterozoic base-
ment of Luis Alves Microplate. In contrast, the southern
border contact is predominantly tectonic, with the basal
units being overthrusted by banded tonalitic-granodioritic
gneisses of the Sa˜o Miguel Complex and by the metavol-
cano-sedimentary rocks of the Brusque Group.
Studies involving the Itajaı´ Basin started at the begining
of the 20th century with countless works focusing on
stratigraphy, such as Carvalho and Pinto (1938), Freitas
(1945), Maack (1947) and Salamuni et al. (1961). In this
phase, the Itajaı´ Basin sediments were grouped into two
formations and the importance of the conglomerates was
recognized. In later studies (Schulz Jr et al. 1970; Kaul
1976; Silva and Dias 1981), the two formations were
described in detail and correlated with basins situated to the
north, the Campo Alegre Formation being defined in this
period. Basei (1985) reiterated the stratigraphic division of
the Itajaı´ Basin into two units. The lower sandy unit,
equivalent to the Gaspar Formation, is composed of mas-
sive arkosic sandstones, volcanic tuffs, and thick poly-
mictic conglomerates lenses representing proximal fluvial
deposits. These are overlain by a rhythmic sandy-silty
package formed by alternating silty and sandy layers and
conglomeratic sandstone levels, related to proximal turbi-
dites with channelized portions. The upper unit starts with
silty-sandy deposits, interpreted as intermediate to distal
turbidites. The top sediments are homogeneous, bluish,
laminated argillites and siltites, related to distal, diluted
turbidity currents associated with the vertical deposition.
Applying sequence stratigraphy, Krebs et al. (1988; 1990);
Appi (1991); Appi and Cruz (1990); Rostirolla et al. (1992,
1999) and Fonseca (2004) described the sedimentary
environments in detail and proposed a series of major
sequences divided into several sedimentary facies. Differ-
ing from the previous proposal, the last three works pro-
pose a third unit, which marks the return of progressively
Fig. 2 Tectonic
compartmentation of the Dom
Feliciano Belt (modified after
Basei 2000 and Basei et al.
2008a, b, c)
546 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
more continental depositional systems. Citroni (1993),
from the recognition of depositional paleo-environments
and their succession, presents a stratigraphic column rep-
resented in terms of facies associations, from base to top:
Continental Associations, subdivided into interlacing flu-
vial sandy paleo-environments, followed by rudaceous
alluvial fans; Transitional Associations, with shallow-water
sandstones, deltaic sandstones, and coastal-plain sand-
stones; Basinal Associations, with subaqueous sliding
deposits followed by hemipelagic deposits; Turbiditic
Associations, with diluted turbidites; classic, medium-
density turbidites; graded, dense turbidites; and sandy to
conglomeratic, dense turbidites.
In the tectonic context, by means of structural frame-
work, sedimentation pattern, regional tectonic scenario,
and geochronology, several classification proposals were
presented for the Itajaı´ Basin, which can be gathered in
two main groups, one of which being the Rift-type Basin
(Citroni 1993) or, in a broader sense, Molassic Foredeep,
Foreland, Peripheral Foreland (Basei 2000; Basei et al.
2008b; Rostirolla 1991, Rostirolla et al. 1992, 1999;
Guadagnin 2007). In the second group, the mechanism
in question is flexural subsidence, related to overload
of allochthonous terrains of the Dom Feliciano Belt,
tectonically transported NW. Alternatively, Gresse et al.
(1996), considering subduction to SW, classifies the
Itajaı´ Basin as a foreland back-arc basin. It is here sug-
gested, in accordance with Dickinson (1974), that the best
classification for the Itajaı´ Basin be ‘‘peripheral foreland
basin’’.
The Itajaı´ Basin lithostratigraphic units
The geologic map of Fig. 3 is a synthesis of the informa-
tion collected in the Itajaı´ Basin over the past 20 years. The
layout of the five lithostratigraphic units that constitute the
Itajaı´ Group results from the deformation (folding and
faulting) that affected the Basin. This deformation has
always been neglected and consequently its great impor-
tance in the present configuration of the basin has not been
appreciated. Detailed NW–SE-trending geologic-structural
Fig. 3 Geologic map of the Itajaı´ Basin: 1 Quaternary; 2 Basic sill; 3
Parana´ Basin; 4 Cambrian Subida granite; 5 Apiu´na volcanics; 6
Ribeira˜o do Bode Fm; 7 Ribeira˜o Neisse Fm; 8 Ribeira˜o Carvalho
Fm; 9 Bau´ Fm; 10 Brusque Group; 11 Sa˜o Miguel Complex; 12 Santa
Catarina Granulite Complex. The foliation attitudes were excluded for
clarity
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 547
123
sections (Fig. 4) largely contributed to the definition of the
units, of the stratigraphy and to calculate the apparent
thickness of each unit. To reach these aims, the surface
bedding (S0) and sedimentary features indicative of top and
base were used. One of the main contributions from the
geologic map was finding out that the units in the southern
border represent the tectonic repetition of the basal units
that are better represented in the northern border of the
Basin. The proposed stratigraphic sequence must be
understood as valid for the Itajaı´ Basin as a whole. Locally,
some of the units described in the complete sequence may
be lacking.
The proposed stratigraphic column (Fig. 5) was estab-
lished from field relationships and the analysis of the
spatial behavior of the lithostratigraphic units. From base to
top, the complete sequence comprises the Bau´ Formation,
the Ribeira˜o Carvalho Formation, the Ribeira˜o Neisse
Formation, the Ribeira˜o do Bode Formation, and the Api-
u´na Formation.
The continental Bau´ Formation represents the basal unit
and occurs in both borders. It is composed of clast-sup-
ported, polymictic conglomerate lenses that extend for
hundreds of meters, having a sandy-arkosic matrix. The
clasts vary from granules to boulders. They are composed
predominantly of gneisses, granites, vein quartz, quartzites,
and mylonites (Fig. 6a). Mica-schist clasts and fragments
of rock types of the Itajaı´ Basin itself are volumetrically
less important. Toward the top, dark red, micaceous arkosic
sandstones tend to predominate (Fig. 6b). They contain
sub-angular to sub-rounded grains of moderate sphericity.
These rocks are poorly sorted, medium- to coarse-grained
or even conglomeratic and can grade to a granule-rich
conglomerate. Volcanic tuffs occur intercalated with sandy
levels. The primary sedimentary structures are clast
imbrication and sigmoidal cross-stratification. Neverthe-
less, the conglomerates are frequently chaotically orga-
nized. The sandy levels form lenticular layers with
thickness varying from 0.2 to 1.2 m and show an internal
massive structure or normal graded bedding, plane-parallel
stratification, tabular cross-stratification, tangential cross-
stratification at the base, and low-angle, small, channelized
cross-stratification. The estimated thickness of this unit is
1,350 m. The deposition of this pile can be attributed to
deltaic fan systems, representing immature, coarse-grained
alluvial sediments that entered the basin transversally, the
basal conglomeratic level representing the gravelly deltaic
plain facies and the upper sandy level representing the
proximal deltaic front facies (Fonseca 2004).
Overlying the Bau´ Formation there occur the rhythmic
sediments of the Ribeira˜o Carvalho Formation. This 650-
m-thick unit is composed of rhythmites resulting from
proximal turbiditic contribution and can be divided into
two main rock types: (1) Rhythmites represented by tabular
bodies with rippled top and rare erosion features, composed
of medium- to fine-grained sandstones intercalated with
centimeter- to decimeter-sized layers of shale (Fig. 6c),
Fig. 4 Geologic-structural
sections that show the spatial
relationships between the
mapped units. Same colors as
presented in Fig. 3
548 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
siltites, and thicker, medium-grained sandstones. They
present as sedimentary structures the TA, TB, TC, and TD
Bouma facies, turboglyphs, and overload structures. The
best examples occur close to Apiu´na, along the BR-470
highway, and are interpreted as turbiditic lobes and lobe
fringes formed under a non-confined regime (Santos et al.
2008); (2) Rhythmites represented by apparently massive,
slightly channelized bodies, composed predominantly of
medium-sand- to coarse-sand-graded sandstones and thin
sandstones intercalated with shale. These rhythmites are
interpreted as channelized and lobe-channel transition
turbidites (Santos et al. 2008), and are intercalated with
polymictic conglomerate levels of massive structure.
Locally they exhibit upward-fining and are formed by
centimeter- to decimeter-sized angular to sub-angular
clasts composed of quartz, milky quartz, fragments of
varied Itajaı´ Basin rock types, and abundant acid volcanic
rock clasts.
The rhythmites are overlain and in gradational contact
with the 1,000 m-thick Ribeira˜o Neisse Formation. This
formation is composed of immature, poorly sorted, fine- to
medium-grained, gray arkosic sandstones, showing plane-
parallel stratification, climbing-ripple cross-stratification
(Fig. 6d), small- and medium-scale channelized cross-
stratification, and slumps.
The upper Ribeira˜o do Bode Formation represents the
youngest sedimentary unit of the Itajaı´ Group with esti-
mated thickness of 1,500 m. It is composed of finely
laminated siltites alternating with silty-argillaceous layers
containing silty-sandy levels (Fig. 6e). Massive siltite
levels occur subordinately. The greenish-gray laminated
siltites constitute meter-sized layers with plane-parallel
lamination, wavy, linsen, slump structures, and graded
bedding. Intercalations of polymictic conglomerates with
acid volcanics clasts occur associated with this unit.
Completing the lithostratigraphic column, rhyolitic
rocks of the Apiu´na Formation occur. The Subida leu-
cosyenogranite represents the last magmatic activity to
affect the Itajaı´ Group sediments, the emplacement taking
place after the units that constitute the Basin had been
deformed (Basei et al. 2008b).
Structural geology
The deformation pattern observed in the Itajaı´ Basin is
characterized by two main folding phases with distinct
axial orientations. The surface bedding S0 is the main
surface in the whole Basin. Several primary structures can
be recognized, which have not been transposed by any
foliation generated by the tectonic events that followed
sedimentation. On the map of Fig. 7, the stereograms
constructed with the attitudes of the bedding poles mea-
sured throughout the Itajaı´ Basin are represented. The
dispersion of the foliation S0 poles indicate that the basin
was affected by two phases of cylindrical folding: the first
Fig. 5 Itajaı´ Group
lithostratigraphic column, Santa
Catarina
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 549
123
and more intense presents preferential axial orientation
between E–W and NE–SW, parallel to the length of the
basin; the second strikes approximately N–S.
The first phase (D1) is the main deformation phase
affecting the Itajaı´ Group as a whole. It is genetically
associated with the thrusting that deformed the southern
portion of the Basin. It is characterized by cylindrical folds,
with axes parallel to the Basin elongation and to the
thrusting front, which resulted from the Brusque Group
overthrusting the Basin sediments, causing the repetition of
the Itajaı´ Basin basal units in its southern flank.
Figure 8a represents phase D1 folds affecting the bed-
ding (S0) of the Ribeira˜o Neisse Formation sandstones,
localized in the vicinity of Faxinal da A´gua Fria.
Cylindrical folds (Fig. 9a) with axial orientation N70E/6
and N64E/16 are represented in this figure, the oblique
cleavage poles S1 dipping much more strongly to SE,
indicating tectonic vergence to NW. Figure 8b shows
cylindrical folds of the same phase, which were charac-
terized in rhythmites localized close to the Basin southern
border. By using the maximum concentration of oblique
cleavage S1 (Fig. 9b) data in the same section (Fig. 8c), the
preferential vergence of the structures generated by D1 is
confirmed to be toward NW. Phase D1 axial orientation can
be clearly seen in the NW–SE sections, which are trans-
versal to the Basin long axis. In several places, pencil
structures formed by the intersection between the S1 foli-
ation and the S0 bedding can be found (Fig. 9c).
Fig. 6 a Clast-supported
conglomerate of the Bau´
Formation, north of Gaspar.
Imbricated clasts of gneisses,
granites, vein quartz, quartzites
and mylonites; b arkosic
sandstone level in the Bau´
Formation; c proximal turbiditic
rhythmites of the Ribeira˜o
Carvalho Formation alternating
medium- to fine-grained
sandstones and shale and siltite
layers. Ribeira˜o Carvalho
Formation, outcrop along the
BR-470 highway, between
Ibirama and Apiu´na; d poorly
sorted, medium-grained,
immature arkosic sandstones
with medium-scale cross-
stratification, Ribeira˜o Neisse
Formation, south of Apiu´na;
e laminated silty-argillaceous
sediments intercalated with
decimeter- to meter-sized silty-
sandy levels, Ribeira˜o do Bode
Formation, south of Apiu´na
550 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
In the section of Fig. 10, phase D1 deformations are
characterized by ample and open folds, represented by
synforms and antiforms with vertical axial planes in the
northern portion, which grade to inverse faults and thrust-
ing close to the southern border of the Itajaı´ Basin, where
the units of the Sa˜o Miguel Complex and Brusque Group
overthrust the Basin younger units. Section CD, located in
the proximity of the Ilhota municipality, and EF, close to
the Gaspar municipality (Fig. 4), shows that the changes
from one sedimentary unit to another are frequently tran-
sitional. For bedding, strikes of ENE–WSW and dips of
15 to 40 SE predominate. In the northern border, the
contact between the basal unit sediments and the gneisses
of the Luı´s Alves Microplate basement (Santa Catarina
Fig. 7 Stereograms (Schmidt diagrams, lower hemisphere) with attitudes of the poles of the main surface S0. Continuous girdles represent phase
D1 folds; dashed girdles represent phase D2. The stereograms are drawn close to the areas where the data were collected
Fig. 8 D1 cylindrical folds in a Ribeira˜o Neisse Formation sand-
stones, and b Ribeira˜o Carvalho Formation rhythmites, representing
the Itajaı´ Group first deformation phase—southern border, close to
Faxinal da A´gua Fria; c oblique cleavage S1 along the Apiu´na-
Faxinal da A´gua Fria section (concentrations represented in descend-
ing order, from darker to lighter gray; total of 74 data; attitude of the
maximum: N50E/42NW)
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 551
123
Granulitic Complex) is normal, whereas in the southern
portion, the contact with the Brusque Group and the Sa˜o
Miguel Complex is tectonic by inverse faulting (Fig. 9d).
Here, the basement overthrusts the Basin sedimentary
units and stratigraphic inversion also occurs, as seen
between Apiu´na and Faxinal da A´gua Fria (sections a, b
and c, d in Fig. 4). The amount and importance of the
displacements related to the thrusts are hidden, in many
cases, by shear planes parallel to the bedding surfaces
(Fig. 9e).
Fig. 9 Structural features—
a Crest of phase D1, meter-sized
fold, with NE-SW axial
orientation. Siltites, south of
Blumenau; b traces of S1
cleavage surface obliquous to
S0 bedding in laminated
siltstone; c pencil structures
developed by S1/S0 interaction
in siltstones, BR470, near
Gaspar; d inverse faults in the
contact between Itajaı´
conglomerates and Brusque
metasediments, southern Itajaı´
border; e Sc/Ss relationship
associated with fault movement
parallelal to bedding plane with
top displacement to NNW
(right-hand side of the photo).
Laminated siltites, Ribeira˜o do
Bode Formation, South of
Apiu´na
Fig. 10 Geologic section
between Apiu´na (NW) and
Faxinal da A´gua Fria (SE).
Stereographic projections
(Schmidt-Lambert diagrams,
lower hemisphere) of surface S0
for each unit. The colors for
each unit correspond to those of
the geologic map
552 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
The second deformation phase D2 is represented by
ample and discontinuous folds of large wavelength and
approximately N–S axial orientation, in general plunging
slightly southward. The stereogram of Fig. 11a, con-
structed with structural data for the Ribeira˜o Neisse For-
mation south of Apiu´na, shows the interference of phase
D2 (dashed girdle) on phase D1. This second folding of
axial orientation S5 W/25 causes a dispersion both of
bedding poles, represented by approximately N–S-trending
layers, and the attitudes of the oblique cleavage S1 poles.
The same interference pattern is seen in Fig. 11b, con-
structed with data from the Ribeira˜o do Bode Formation
siltites, from near Faxinal da A´gua Fria. Phase D2 axis
strikes S5E/50, causing strong dispersion of bedding poles
and of cleavage S1.
The comparison between the deformations recognized in
the Itajaı´ Basin sediments and in the Brusque Group leads
to the correlation of the two deformation phases in the
Itajaı´ Basin, respectively, with the Brusque Group defor-
mational phases D4 and D5, which affected it after the
metamorphic peak (Basei 1985).
Lithogeochemistry
The geochemical study of the sedimentary rocks was car-
ried out using 23 samples (Table 1) collected along three
sections traversing the Itajaı´ Group units. This study aimed
at understanding the variabilities between different Itajaı´
Basin lithostratigraphic units. The chemical composition of
the terranes that acted as source areas of the Itajaı´ Basin
sediments is probably the major controller of the geo-
chemical signature of the Basin rocks (Rollinson 1993).
The diagram in Fig. 12a was used to classify the sam-
ples into major sandstone classes, the SiO2/Al2O3 ratio
serving to distinguish quartz-rich sandstones from Al-rich
sandstones, and the Na2O/K2O ratio to distinguish wackes
from arkoses (Pettijohn et al. 1972). In this diagram, the
sandstones from the Bau´ Formation and the Ribeira˜o do
Bode Formation are classified as arkoses, lithic sandstones
and wackes, whereas the sandstones from the Ribeira˜o
Carvalho and Ribeira˜o Neisse Formations are characterized
as lithic sandstones. This classification is maintained in the
diagram involving Fe2O3 ? MgO, Na2O and K2O contents
(Fig. 12b), except for the sandstones of the Sa˜o Pedro and
Ribeira˜o Neisse Formations, which plot in the arkose field.
According to Fig. 12c, practically all samples plot on or
above the Na2O/K2O = 1 line, indicating that they are
quartz-rich. In Fig. 12d the SiO2/Al2O3 ratio is used not
only to distinguish quartz-rich sediments, wackes, and ar-
gillites but also to evaluate mineralogical maturity (Petti-
john et al. 1972). In turn, the Fe2O3/K2O ratio is very
useful to distinguish lithic feldspathic fragments present in
sandstones. It is possible then to classify with this diagram
the sediments of the Bau´ Formation as predominantly
wackes; the sediments of the Ribeira˜o Carvalho and Ri-
beira˜o Neisse formations as arkoses and shale, and the
sediments of the Ribeira˜o do Bode Formation as predom-
inantly shale with subordinate arkoses and wackes. It was
also possible to characterize all the Itajaı´ Basin sediments
as mineralogically immature.
The ‘‘spidergrams’’ constructed using chondrite-nor-
malized REE contents (McLennan and Taylor 1985) reveal
a gradual increase in negative Eu anomaly and decrease in
HREE fractionation from base to top. As can be seen in
Fig. 13, the spidergram corresponding to the basal Bau´
Formation differs from those corresponding to the upper
units. It shows a slight negative Eu anomaly, when com-
pared to the intermediate values for the Ribeira˜o Carvalho
and Ribeira˜o Neisse Formations and to the high values for
the Ribeira˜o do Bode Formation. The Bau´ Formation
shows the strongest HREE fractionation, which gradually
decreases in the Ribeira˜o Carvalhos and Ribeira˜o Neisse
Formations and is the weakest in the Ribeira˜o do Bode
Fig. 11 Schmidt stereonet,
lower hemisphere,
demonstrating D2 folding and
its overprint on D1. a Ribeira˜o
Neisse Formation, south of
Apiu´na, and b Ribeira˜o do Bode
Formation siltites, close to
Faxinal da A´gua Fria
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 553
123
Table 1 WR geochemical data (major, trace and rare-earth elements)
IA-01 IA-02 IA-03 IA-08 IA-09A IA-09C IG-01 IG-02 IG-04a IG-05B IG-06B
SiO2 76.2300 78.1200 72.8600 62.5100 64.1000 63.5200 69.3200 61.5600 60.9800 62.8400 63.4600
Al2O3 12.3200 10.7400 12.8600 17.8600 16.2600 17.2500 13.9000 17.9000 17.7900 17.7000 16.9500
MnO 0.0590 0.0830 0.0420 0.0630 0.0730 0.0630 0.0400 0.0950 0.1680 0.0900 0.1050
MgO 0.2300 0.4400 0.5200 1.5900 2.3000 2.2800 1.1600 1.8800 2.0200 1.9600 2.0400
CaO 0.0800 0.4100 0.8000 0.8900 0.3600 0.2900 1.6500 0.1100 0.0900 1.3000 0.6900
Na2O 3.6900 2.2900 2.0500 1.4000 2.4000 2.2400 3.0900 0.9900 0.8900 2.3700 1.8500
K2O 3.0500 3.4700 4.3700 4.8700 3.5700 4.1100 2.9800 5.0600 4.9900 4.3000 4.3000
TiO2 0.3050 0.3240 0.5240 0.8640 0.8020 0.8180 0.4880 0.9980 0.9210 0.8420 0.7210
P2O5 0.0240 0.0710 0.1070 0.1570 0.1720 0.1450 0.1140 0.0360 0.0260 0.1680 0.1550
Fe2O3 2.4400 2.1400 2.6600 5.6700 6.5000 5.9000 3.7200 7.4200 7.7700 5.9100 6.3300
Loi 1.1800 1.4200 2.4800 3.7900 3.0300 3.1000 3.0600 3.3600 3.8400 1.9400 3.0600
Total 99.6080 99.5080 99.2730 99.6640 99.5670 99.7160 99.5220 99.4090 99.4850 99.4200 99.6610
Ba 514.4000 575.3000 586.5000 470.8000 625.7000 618.5000 993.0000 1266.4000 884.5000 800.1000 576.5000
Ce 65.0000 56.4000 89.3000 106.6000 90.5000 88.5000 81.1000 76.2000 89.8000 91.7000 92.6000
Cl \50 \50 \50 \50 \50 \50 \50 \50 \50 \50 \50
Co 52.3000 63.0000 37.7000 25.1000 22.8000 18.8000 33.9000 25.5000 25.6000 22.0000 23.9000
Cr 26.3000 24.0000 29.3000 64.5000 76.7000 80.5000 98.6000 75.5000 95.5000 84.7000 75.3000
Cu 18.2000 8.9000 \5 30.1000 23.2000 5.4000 10.4000 \5 18.6000 23.7000 31.3000
F \550 \550 844.8000 1362.4000 1537.7000 1459.6000 \550 967.3000 929.8000 1091.0000 1210.9000
Ga 16.2000 13.8000 17.8000 27.1000 21.7000 24.3000 17.2000 25.0000 27.9000 25.5000 24.8000
La 29.3000 35.5000 50.7000 55.8000 39.1000 37.5000 46.1000 56.1000 40.6000 54.1000 41.4000
Nb 26.3000 23.1000 25.4000 26.4000 16.8000 16.6000 17.9000 21.5000 18.6000 23.5000 21.2000
Nd 39.9000 26.7000 41.7000 56.7000 49.6000 56.8000 36.6000 58.8000 61.1000 57.8000 48.6000
Ni 9.7000 10.9000 11.4000 28.5000 36.2000 35.3000 31.6000 37.0000 40.0000 35.4000 42.4000
Pb 25.7000 29.5000 32.6000 22.6000 12.4000 4.6000 16.5000 12.1000 32.7000 18.0000 18.5000
Rb 160.9000 155.5000 204.3000 251.3000 179.4000 198.8000 70.7000 234.9000 246.7000 210.5000 215.5000
S \300 \300 \300 \300 \300 \300 \300 \300 \300 \300 \300
Sc \14 \14 \14 17.8000 16.3000 15.7000 \14 17.7000 17.7000 16.8000 14.4000
Sr 85.1000 142.4000 149.1000 65.8000 75.7000 63.1000 368.1000 89.2000 50.1000 180.0000 124.8000
Th 20.8000 16.2000 25.4000 27.6000 12.7000 16.3000 15.8000 19.1000 16.4000 18.1000 12.7000
U 13.5000 12.4000 12.4000 13.7000 13.7000 15.8000 6.8000 16.1000 17.3000 11.6000 13.0000
V 25.8000 31.8000 41.0000 90.0000 103.1000 123.5000 63.1000 93.2000 83.2000 101.8000 84.6000
Y 45.6000 26.6000 38.6000 48.4000 38.0000 36.1000 17.7000 44.1000 38.2000 48.2000 37.9000
Zn 62.1000 37.7000 48.5000 99.1000 113.1000 100.0000 37.8000 86.2000 101.2000 99.4000 121.1000
Zr 184.6000 172.6000 358.9000 280.3000 214.3000 178.8000 179.0000 271.1000 221.5000 247.1000 213.4000
Sm 7.1946 5.8621 10.0652 10.1051 7.3379 6.3941 5.7650 7.0130 7.7255 8.7093 6.7026
Hf 6.7319 4.6484 10.7984 9.0700 6.5983 5.6438 5.3940 8.4414 6.9247 7.2027 6.3209
IG-07 CTI-01 CTI-03 CTI-06 CTI-08 CTI-12A CTI-18A CTI-22 CTI-28 CTI-29A CTI-37
SiO2 71.1300 62.9800 63.7100 61.8600 72.2300 63.6200 67.3200 72.4400 62.8200 70.7300 64.9400
Al2O3 14.8300 17.6000 16.7600 17.3000 12.7200 17.3600 16.1600 14.1300 17.4700 13.8200 15.6500
MnO 0.0540 0.0070 0.0400 0.0600 0.0500 0.0400 0.0400 0.0400 0.0900 0.0700 0.1100
MgO 1.1800 1.6400 1.9900 1.8000 1.0700 1.6100 0.6800 0.3500 2.1600 1.3600 2.0000
CaO 0.4400 0.2100 0.3700 1.0000 1.0800 0.3400 0.1700 0.3800 0.4400 0.3300 0.8900
Na2O 1.9000 1.6400 1.9100 1.4200 2.6200 1.9300 1.5100 3.4500 1.8600 2.7500 2.4500
K2O 5.1700 4.6300 3.9600 4.8900 3.8000 4.6200 5.6700 3.5400 4.3500 4.2300 3.3000
TiO2 0.2860 0.6900 0.7100 0.8400 0.5600 0.7800 0.5000 0.3300 0.8000 0.4400 0.7800
P2O5 0.0370 0.1100 0.1300 0.1800 0.1400 0.1500 0.0800 0.0700 0.1500 0.0900 0.1600
554 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
Formation. The lithogeochemical pattern yielded by the
Bau´ Formation is similar to that obtained by Basei et al.
(1998b) for Luı´s Alves Microplate basement rocks.
Provenance of the sediments inferred
from the lithogeochemical data
First and foremost, the available geochemical data were
treated in order to identify the possible sources of sedi-
ments for the Itajaı´ Basin. Even considering the limitations
inherent to this approach, e.g. materials coming from tec-
tonically distinct settings yielding geochemically similar
products (McLennan et al. 1990), our study allowed the
definition of several parameters to characterize source
areas for the Itajaı´ Group sediments.
Taking into account that Th has affinity with differen-
tiated continental crustal rocks (Faure 2005) and Sc is
abundant in the mantle, Th/Sc ratios higher than 1 reveal
a contribution of upper crustal rocks as source areas
(Fig. 14a), favoring tectonic settings associated with con-
tinental collision, passive margins, and magmatic arcs. In
Fig. 14b (SiO2/Al2O3 vs. K2O/Na2O diagram), the prefer-
ential involvement of passive margin, continental collision,
and subordinately magmatic arc settings is also indicated.
In this diagram, the field related to continental collision is
the one that best matches with the data corresponding to the
upper sequences of the Itajaı´ Basin, whereas the data cor-
responding to the basal units are closest to the field related
to the passive margin setting.
The relationship between La/Th ratios and Hf contents
(Fig. 14c) indicates for all the basin units an origin related to a
magmatic arc setting with important contribution of sediments
associated with a passive margin setting. This suggestion is
possible because, due to the low La/Th ratios yielded by the
Basin sediments, which indicate Th enrichment in relation to
La, a provenance from the erosion of upper crustal rocks can
be suggested (Floyd and Leveridge 1987).
The comparison between present eNd values and Th/Sc
ratios (Fig. 14d) indicates that the source area for the Bau´
Table 1 continued
IG-07 CTI-01 CTI-03 CTI-06 CTI-08 CTI-12A CTI-18A CTI-22 CTI-28 CTI-29A CTI-37
Fe2O3 2.2800 5.3800 5.7900 6.0900 3.4100 5.4000 3.9400 2.7300 6.2800 3.5300 6.0200
Loi 2.1800 4.7000 4.4000 4.3000 2.0000 3.9000 3.7000 2.3000 3.3000 2.4000 3.4000
Total 99.4870 99.5870 99.7700 99.7400 99.6800 99.7500 99.7700 99.7600 99.7200 99.7500 99.7000
Ba 446.7000 1045.0000 558.0000 593.0000 656.0000 606.0000 741.0000 650.0000 620.0000 866.0000 610.0000
Ce 46.2000 90.2000 79.4000 92.1000 84.9000 128.5000 92.8000 84.8000 100.5000 71.6000 92.1000
Cl \50
Co 17.2000 49.8000 29.8000 24.3000 98.4000 27.2000 23.5000 38.4000 22.8000 59.3000 23.2000
Cr 16.5000
Cu 8.9000 24.4000 18.0000 30.2000 119.8000 22.8000 11.0000 5.0000 22.7000 4.1000 28.1000
F 1526.5000
Ga 23.6000 25.4000 22.1000 23.2000 17.0000 25.6000 22.9000 19.4000 23.7000 16.9000 20.4000
La 27.8000 38.6000 36.7000 40.6000 38.1000 58.3000 55.7000 36.6000 46.6000 34.0000 42.5000
Nb 29.2000 19.7000 19.4000 23.8000 25.5000 23.8000 27.0000 24.9000 20.1000 16.1000 20.2000
Nd 30.3000 38.1000 35.8000 44.8000 36.7000 55.5000 61.3000 41.9000 45.5000 26.5000 39.4000
Ni 7.2000 67.4000 33.0000 34.1000 20.1000 25.6000 12.5000 23.2000 42.8000 32.2000 35.5000
Pb 9.0000 11.4000 10.2000 17.8000 13.4000 8.5000 9.2000 13.9000 5.0000 8.6000 25.5000
Rb 299.7000 246.1000 205.9000 267.1000 176.3000 256.1000 327.3000 192.8000 206.5000 175.4000 174.3000
S \300
Sc \14 16.0000 15.0000 16.0000 10.0000 15.0000 12.0000 7.0000 17.0000 8.0000 14.0000
Sr 57.4000 76.2000 73.4000 83.1000 157.2000 84.4000 87.5000 89.4000 84.1000 187.1000 164.7000
Th 33.5000 15.1000 15.8000 25.9000 18.4000 19.2000 22.9000 23.0000 19.0000 10.5000 18.6000
U 17.6000 3.5000 3.4000 5.9000 3.9000 5.1000 6.8000 5.1000 4.7000 1.5000 3.7000
V 19.4000 104.0000 96.0000 102.0000 66.0000 102.0000 58.0000 35.0000 112.0000 55.0000 91.0000
Y 52.5000 43.6000 29.3000 46.1000 24.7000 41.9000 70.9000 52.6000 36.0000 15.4000 33.8000
Zn 83.1000 130.0000 86.0000 83.0000 42.0000 86.0000 100.0000 40.0000 86.0000 45.0000 90.0000
Zr 190.4000 155.1000 164.6000 248.4000 264.3000 221.9000 195.8000 194.9000 192.2000 143.2000 245.9000
Sm 8.4271 7.1200 6.4700 9.0300 6.5600 9.7900 13.3300 9.5700 8.2700 4.0500 7.2900
Hf 7.6535 4.7000 5.0000 7.6000 7.5000 6.5000 6.3000 7.5000 6.0000 4.3000 7.1000
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 555
123
Formation sediments (lower sequence) were rocks associ-
ated with an old crust, whereas the source area for the
Ribeira˜o Carvalhos, Ribeira˜o Neisse, and Ribeira˜o do Bode
Formations (upper sequence) were rocks associated with
more juvenile, upper crustal rocks.
The geochemical studies of the Itajaı´ Basin sedimentary
rocks helped characterize the rock types analyzed as min-
eralogically immature, represented by wackes, arkoses, and
shale. The interpretation of REE data shows that different
samples coming from the same units yielded very homo-
geneous results, whereas significant differences occur
between samples from the continental unit and from the
marine units, which attests for the reliability of the pro-
posed lithostratigraphic column.
As indicated by the present study, the continental col-
lision, passive margin, and magmatic arc settings can be
suggested as probable settings related to the source areas
for the Itajaı´ Basin sediments. It was equally possible to
characterize the predominance of sediments coming from
an old crust to the basal unit (Bau´ Formation) and from a
younger upper crust to the upper units.
Isotopic Geochemistry
The Nd, Sr, and Pb isotopic study was carried out using the
same 23 Itajaı´ Basin stratigraphic sequence samples as for
the lithogeochemical studies. For the 143Nd/144Nd and
207Pb/204Pb data (Fig. 15), more radiogenic values corre-
spond to the Carvalho, Ribeira˜o Neisse, and Ribeira˜o do
Bode Formations, whereas less radiogenic values corre-
spond at least to the basal portions of the Bau´ Formation.
This fact strengthens the lithostratigraphic organization
proposed and supports the suggestion that the sandstone
and conglomerate units of the Itajaı´ Basin southern border
constitute, as indicated in the geologic map, the same Bau´
Formation described in the northern border, therefore rul-
ing out a third unit as suggested by Appi (1990), Appi and
Cruz (1991), Rostirolla et al. (1992, 1999); Fonseca (2004)
and Guadagnin (2007).
Still aiming at identifying the possible source areas for
the Itajaı´ Basin sediments, eNd values for samples of the
Itajaı´ Basin and the adjacent terranes were calculated for
580 Ma, which is the mean age estimated for the Itajaı´
Fig. 12 Classification of sedimentary rocks according to major
element contents. a Geochemical classification of terrigenous sand-
stones (Pettijohn et al. 1972); b Chemical classification of sandstones
(Floyd and Leveridge 1987); c Classification according to quartz
content in the sediment (Floyd and Leveridge 1987); d Geochemical
classification of terrigenous sandstones and shale (Herron 1988)
556 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
sedimentation (Basei et al. 2008b). As seen in Fig. 16a, the
calculated eNd values for the distinct crustal segments that
host the Itajaı´ Basin are organized according their geo-
graphic distribution along a NW–SE section. This figure
shows the predominance of more negative eNd values in the
Bau´ Formation. These values are similar to those obtained
for the Santa Catarina Granulitic Complex gneisses and
indicate that the source area for the Itajaı´ Basin basal unit
are old rocks with long crustal residence, which is in
agreement with the other geochemical-isotopic information
that points to these gneisses as source for these sediments.
On the other hand, the values obtained for the Itajaı´ Basin
upper units are similar to those for the Brusque Group
metasediments and granites, and even to those for the
Floriano´polis Batholith. Comparing the eNd (580) and eSr
(580) calculated for the Itajaı´ Basin sediments values, two
distinct evolution trends are depicted (dashed arrows in
Fig. 16b). The upper units yield approximately constant
and slightly negative eNd values and eSr values falling in a
large interval. These data plot close to the points corre-
sponding to the Brusque Group and Floriano´polis Batho-
lith. On the other hand, it is possible to suggest a second
trend defined by the Bau´ Formation points that indicates
more negative values, closer to the points corresponding to
the Luı´s Alves Microplate basement gneisses. Thus, it is
again suggested that the possible source areas for the Bau´
Formation are the Santa Catarina Granulitic Complex, the
Camboriu´ Complex, and the Brusque Group granites.
The same provenance relationships can be inferred from
Fig. 16c, where the fields of Nd evolution through time
(DePaolo 1988) are presented. The field defined by the
Itajaı´ Basin completely overlaps the field defined by the
Brusque Group metasediments and partially overlaps
with the fields that represent the Santa Catarina Granulitic
Complex, the Floriano´polis Batholith, and the Brusque
Group granites. The field corresponding to the Camboriu´
Complex model ages is very ample and almost totally
overlaps the other fields.
Fig. 13 Chondrite-normalized REE distribution (McLennan et al. 1995). a Bau´, b Ribeira˜o Carvalho, c Ribeira˜o Neisse and d Ribeira˜o do Bode
Formations, evidencing similar characteristics of samples from the same unit and differences between the Bau´ Formation and the upper units
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 557
123
In conclusion, the isotopic study indicates that the
rhythmites and siltites of the Itajaı´ basin upper sequence
(Ribeira˜o Carvalho, Ribeira˜o Neisse and Bode Formations)
are isotopically homogeneous and but significantly differ-
ent from the lower sequence (Bau´ Formation) constituted
by the continental sandstones and conglomerates. For the
Fig. 14 Geochemical characterization of the provenance areas for the
Itajaı´ Group sediments. a Th/Sc diagram (McLennan et al. 1990);
b SiO2 ? Al2O3 vs. K2O ? Na2O diagram (McLennan et al. 1990);
c La/Th vs. Hf diagram (Floyd and Leveridge 1987); d eNd vs. Th/Sc
diagram (McLennan et al. 1990)
Fig. 15 207Pb/204Pb and
143Nd/144Nd ratios versus
stratigraphic column,
characterizing similar isotopic
behavior between the upper
marine units and differences
between these units and the
lower continental unit (Bau´
Formation)
558 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
upper sequence, the 143Nd/144Nd and 207Pb/204Pb ratios are
always more radiogenic and the eNd values less negative
than those yielded by the lower sequence. Model ages (Nd
TDM) indicate for all the Basin units a long crustal resi-
dence, with values similar to those observed in the Brusque
Group, the Floriano´polis Batholith and the Camboriu´
Complex, and subordinately similar to those of the Santa
Catarina Granulitic Complex.
The isotopic data suggest the continental sandstones and
conglomerates of the Bau´ Formation originated by the
erosion of the basement, notably the Santa Catarina
Granulitic Complex, and for the source area for the
rhythmites, sandstones, and siltites of the upper marine pile
it was the Brusque Group metavolcano-sedimentary
sequence, with contributions from the Floriano´polis Bath-
olith. This provenance is confirmed by field data. In the
Bau´ Formation, centimeter- to meter-sized gneiss, granite,
vein quartz, quartzite, and mylonite clasts, related to the
Santa Catarina Granulitic Complex, and rare mica-schist
fragments related to the Brusque Group are observed. In
the upper units, the provenance associated with the Brus-
que Group is observed in thin sections, where the pre-
dominance of mica schists fragments is observed.
Geochronology
The first Itajaı´ Group geochronological results were pre-
sented by Macedo et al. (1984) who, on the basis of Rb–Sr
isochrons of whole rock fine fractions, placed the sedi-
mentation and diagenesis around 560 Ma. Based on Rb–Sr
ages and U–Pb (TIMS) zircon analysis, Basei 1985 and
Basei et al. (1999) also confined the depositional history of
the Itajaı´ Basin to the Neoproterozoic. In disagreement
Fig. 16 Isotopic diagrams
comparing eNd values for the
Itajaı´ Basin and the main
regional geologic units (Santa
Catarina Granulitic Complex,
Camboriu´ Complex,
Floriano´polis Batholith,
Brusque Group metasediments
and intrusive granites), a values
of eNd(580) for all regional units
organized geographically
according to a NW–SE section;
b eNd (580) vs. eSr(580) indicating
distinct evolutionary trends for
upper and lower Itajaı´ Group
units
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 559
123
with what was mentioned above, the identification of fossil
traces and evidence of Chancelloria led Pain et al. (1997) to
place the Itajaı´ sedimentation in the Cambrian, with the
oldest possible age at 540 Ma. The deformation that
affected the Itajaı´ Basin transformed to quartz-sericite
schists by shearing the tuffaceous sediments intercalated
with the basal arkosic sandstones yielded a 535 ± 11 Ma
(Basei 1985). K–Ar fine fractions analysis (\2 lm) of two
siltstone quarries located near Blumenau and Apiu´na show
517 ± 5.0 Ma and 535 ± 11 Ma, respectively Macedo
et al. (1984). These two different groups of ages suggest
diachronism among the low-temperature events that char-
acterize the thermal evolution of the Itajaı´ Basin.
A large detrital muscovite crystal of the Bau´ Formation
conglomerates (BR 470 highway, in the proximity of Pedra
de Amolar) were dated at Georg-August University, Got-
tingen, Germany, yielding ages of 1,754 ± 37 Ma and
1,711 ± 39 Ma (Table 2). These ages reinforce the sug-
gestion given by the isotopic geochemistry, which points to
the Paleoproterozoic Luı´s Alves Microplate gneissic
basement as source for the basal continental successions.
Similar conclusion was obtained by Guadagnin et al.
(2010) who, on the basis of Nd and Pb isotopes, also
indicated the importance of the Brusque Group as the main
supplier of material for the Itajaı´ Basin (Guadanin et al.
2010). It is interesting to stress that this author showed
(main) concentrations of ages around 600 Ma and a second
group of ca. 800 Ma for the detrital zircons from the sandy
sediments. The first group can be easily attributed to the
Brusque Group granitoids, whereas the provenance for the
second is still uncertain, once rocks of such age are rare,
restricted to the Parapente Suite A-type magmatism (Basei
et al. 2008c) of very local expression in the region.
For the zircon, SHRIMP ages presented in this paper,
mineral separation was by standard gravimetric and iso-
dynamic techniques, and the mounting of selected zircons
into epoxy resin discs were carried out at the Instituto de
Geocieˆncias, Universidade de Sa˜o Paulo. Prior to analysis,
cathodo-luminescence (CL) images were obtained to pick
sites for analysis. Age determinations were performed at
the Beijing Shrimp Center, China and Research School of
Earth Sciences, Australia, according to standard procedures
(Compston et al. 1984; Williams 1998; Stern 1998; Sir-
combe 2000). Data are portrayed in Tera Wasserburg
diagrams generated by the program Isoplot/Ex (Ludwig
2001; Table 3). The SHRIMP method was applied to
zircons from sample MBAN 1 of the same tuffaceous
levels investigated by the Rb–Sr method (Fig. 18a). A
weighted mean 206Pb/238U age of 596 ± 10 Ma (Fig. 17a)
was obtained for the volcanogenic components and is the
best estimate for the beginning of the deposition of the
Itajaı´ Group basal portion. In two distinct localities, con-
glomerate levels rich in felsic volcanic clasts (Fig. 18b, c)
caused much controversy regarding the stratigraphic posi-
tion of this felsic magmatism. Geochronologic studies
using zircons extracted from centimeter-sized fragments of
felsic rock clasts (from both outcrops resulted in 206Pb/238U
ages around 609 Ma (Fig. 17b, c). Considering the age
errors, these results are coeval with the MBAN 1 tuffa-
ceous sample of Bau Formation and with those observed in
the Campo Alegre Basin. It represents a volcanic event,
whose products were already recycled by erosion, which
occurred prior to the felsic magmatism that can be recog-
nized in the Itajaı´ Basin and represented by lava domes. No
relationship exists between the felsic rich clast conglom-
erates and the late, felsic volcanism.
The best age for the Itajaı´ Basin felsic volcanism
(Apiu´na Formation) was obtained for the dome that occurs
south of Apiu´na (Morro do Gravata´), composed of felsic
rocks (Fig. 18d) that crosscut the basin units. The
206Pb/238U age of 558 ± 6.6 Ma (Fig. 17d) represents the
youngest age possible for the Itajaı´ Group sedimentation.
The Subida syenogranite (Fig. 18e), intrusive in the It-
ajaı´ Basin sediments, represents the youngest anorogenic
granitoid recognized in the region. Its 206Pb/238U age of
520 ± 5.5 Ma (Fig. 17e) is circa 80–60 Ma younger than
the A-type granitoids of the Serra do Mar Suite (Kaul 1984,
Vlach and Gualda 2007), with which it has always been
correlated.
Comparative analysis
Considering the importance of the recently published paper
by Guadagnin et al. (2010) to our manuscript, a brief
comparison of both works is carried out here. In a general
way, both works make use of stratigraphic, isotopic, and
geochronologic information on the Itajaı´ Basin units and
present a proposal for the Itajaı´ Basin tectonic evolution,
on the basis of their own data. Despite the tools used (LA
ICPMS and SHRIMP) led to comparable results, they were
applied to distinct materials: detrital zircons (Guadagnin
Table 2 K-Ar data of muscovite crystal
Field number Geological unit Rock type Mineral K2O (wt%) 40 Ar* [nl/g] STP 40 Ar* (%) Age (Ma) 2 s Error (Ma)
BR 24 Bau Fm. Conglomerate Muscovite 10.62 1015.53 99.47 1754.40 37.40
BR 25 Bau Fm. Conglomerate Muscovite 10.69 983.10 99.57 1711.00 39.00
560 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
Table 3 U-Pb SHRIMP analytical data
Labels Site U (ppm) Th (ppm) Th/U ± Th/U Pb* (ppm) 204 (ppb) 238U/206Pb ± 38/6
MBAN-1—Siltstone with tuffaceous contribution—Bau´ Formation (corrected using measured 204Pb)
1.1 e,osc,p 285.51 263.56 0.92314 0.02286 34 2 9.83396 0.45643
2.1 e,osc,p 427.97 168.33 0.39332 0.00587 41 4 10.67875 0.52071
3.1 e,osc/hd,p 1203.27 596.74 0.49593 0.01932 113 36 11.03623 0.8314
4.1 e,osc,p 647.1 779.85 1.20515 0.01952 79 4 10.15616 0.43155
6.1 m,osc,p 304 288.41 0.94873 0.03036 33 3 10.64369 0.69462
5.1 e,osc,p 335.43 188.88 0.56309 0.01309 37 0 9.64532 0.59014
9.1 e,h,p 417.45 245.59 0.58831 0.01795 41 9 10.66171 0.70708
7.1 m,hd,p 1453.97 805.87 0.55426 0.07225 142 318 10.99862 1.87312
8.1 m,dd,p 2404.28 1700.25 0.70718 0.03159 115 945 23.08662 2.33238
10.1 e,osc,p 452.49 350.83 0.77534 0.01601 161 5 3.23886 0.17454
CT31 and CT 32—clasts of felsic volcanic—Itajaı´ conglomerates (corrected using measured 204Pb)
31-1.1 m,osc,p 124.58 40.74 0.32702 0.00351 16 6 7.4654 0.18198
31-2.1 m,osc,p,fr 61.81 40.19 0.65021 0.0095 6 0 10.62627 0.36401
31-3.1 e,osc,p,fr 46.95 37.11 0.79047 0.01219 5 2 10.1916 0.31442
31-4.1 m,osc,fr 127.87 97.83 0.76507 0.00808 14 0 10.12963 0.30119
31-5.1 e,osc,p,fr 200.21 146.29 0.73068 0.00689 23 6 9.48737 0.23723
31-6.1 e,osc/h,p 158.01 203.54 1.28816 0.02637 19 5 10.38479 0.4046
31-7.1 e,osc,p 139.27 192.63 1.38316 0.01961 17 5 10.30378 0.26595
31-8.1 m,osc,p,fr 181.77 54.4 0.29927 0.00537 18 2 9.72529 0.34106
31-9.1 e,osc,p,fr 116.64 135.94 1.16549 0.01266 14 2 10.13557 0.26576
31-10.1 e,osc,p 652.68 118.86 0.18211 0.0051 66 17 9.55815 0.75126
32-1.1 m,osc,p 90.66 158.56 1.74904 0.02591 12 1 10.40936 0.3242
32-2.1 e,osc,p,fr 154.2 238.14 1.54432 0.01988 22 1 9.49905 0.32357
32-3.1 e,osc,p 525.74 380.38 0.72351 0.01496 55 2 10.60783 0.414
32-4.1 e,osc,p 34.71 95.64 2.75507 0.06982 6 1 10.25406 0.39509
32-5.1 e,osc,p 321.15 211.03 0.65711 0.00774 37 3 9.44281 0.25074
32-6.1 e,osc,p 328.45 774.78 2.3589 0.03898 51 1 9.91756 0.18395
32-7.1 e,osc,p 184.03 263.48 1.43169 0.05636 23 4 10.11287 0.47959
32-8.1 m,osc/h,p 122.32 128.01 1.04657 0.01497 13 6 10.60417 0.32207
32-9.1 e,osc,p,fr 83.21 82.44 0.99071 0.00934 9 0 10.51133 0.2621
32-10.1 e,osc,p,fr 119.99 62.26 0.51888 0.00564 13 2 10.0703 0.18618
32-12.1 e,osc,p,fr 140.63 141.95 1.00942 0.02793 16 4 10.57562 0.60027
32-15.1 m,osc,p 426.95 187.19 0.43844 0.00398 44 13 9.87361 0.24513
32-17.1 e,osc,p,fr 52.75 78.5 1.48807 0.05665 7 2 10.30806 0.53613
32-18.1 m,osc,p 196.43 139.34 0.70933 0.00856 21 1 10.18354 0.29523
32-13.1 e,osc,p 159.89 178.36 1.11549 0.01255 82 6 2.43406 0.06579
32-14.1 e,osc,p 146.21 41.77 0.2857 0.00524 30 5 4.94949 0.23435
32-11.1 m,osc,p 194.58 64.51 0.33156 0.00359 25 2 7.79364 0.21668
32-16.1 e,osc,p 316.45 160.23 0.50634 0.00341 45 1 7.42249 0.1326
Felsic volcanic—Apiu´na Formation (corrected using measured 204Pb)
API-1.1 e,h,p 40.83 29.13 0.71356 0.00871 4 0 11.03503 0.34407
API-2.1 e,h,p 47.7 49.1 1.02937 0.01716 5 0 10.90571 0.34625
API-4.1 e,h,p 83.14 92.11 1.10787 0.0134 9 0 11.00483 0.25872
API-5.1 e,h,p 54.64 34.69 0.63482 0.00933 5 0 11.03706 0.28964
API-6.1 e,h,p 59.91 63.18 1.05445 0.01317 6 1 11.33351 0.32143
API-3.1 e,h,p 34.65 34.36 0.9918 0.01666 4 2 11.2193 0.37863
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 561
123
Table 3 continued
Labels Site U (ppm) Th (ppm) Th/U ± Th/U Pb* (ppm) 204 (ppb) 238U/206Pb ± 38/6
Subida Granite (corrected using measured 204Pb)
A SUB-1.1 e,osc,p 205.44 125.59 0.6113 0.01425 19 5 11.51098 0.6656
A SUB-2.1 e,osc,p,fr 103.58 77.9 0.75212 0.02191 10 1 11.45334 0.67073
A SUB-3.1 e,osc,p 320.97 160.77 0.5009 0.01819 28 2 11.94992 0.96808
A SUB-4.1 e,osc,p 124.39 92.72 0.74543 0.01704 12 2 11.50705 0.64287
A SUB-5.1 e,osc,p 129.49 101.48 0.78368 0.01671 12 3 11.83973 0.78047
A SUB-6.1 e,osc,p 134.03 78 0.58197 0.01012 12 2 11.49571 0.52939
C SUB-7.1 e,osc,p 98.74 60.86 0.61638 0.01003 9 1 11.78418 0.60083
C SUB-8.1 e,osc,p 148.16 79.29 0.53518 0.00857 13 4 12.17256 0.66257
C SUB-9.1 e,h,p 143.7 99.08 0.68949 0.01244 13 2 12.15569 0.68554
C SUB-10.1 e,osc/hd,p 311.73 304.27 0.97607 0.00899 31 4 11.70655 0.50583
C SUB-11.1 e,hd,p 236.96 250.61 1.05758 0.0131 24 1 11.86382 0.6185
C SUB-12.1 e,hd,eq 553.05 1159.97 2.09741 0.02685 70 1 11.57709 0.56569
NC SUB-2.1 e,osc,p 182.44 151.48 0.83027 0.01486 17 18 11.95746 0.40462
NC SUB-3.1 m,osc,p 143.35 137.69 0.96055 0.01252 14 11 11.8394 0.38049
NC SUB-7.1 m,h,osc 146.48 126.41 0.86301 0.01224 14 17 11.99367 0.37179
NC SUB-1.1 e,osc,p 254.19 162.25 0.6383 0.00898 26 12 10.27715 0.28975
NC SUB-4.1 e,p,og 43.55 37.11 0.85209 0.01207 4 21 12.01428 0.54006
NC SUB-5.1 m,p,osc,h,fr 17.38 40.22 2.31356 0.05317 2 10 12.89028 0.69512
NC SUB-6.1 m,osc,p,fr 71.54 103.04 1.44038 0.02302 8 19 11.79446 0.43072
NC SUB-8.1 m,osc,p 111.72 110.32 0.98743 0.01806 10 12 12.9293 0.44761
Labels 207Pb/206Pb ± 7/6 Age 206/238 ± Age Age (207/235) ± age Age (207/206) ± age Conc (%)
MBAN-1—Siltstone with tuffaceous contribution—Bau´ Formation (corrected using measured 204Pb)
1.1 0.05938 0.00185 624.3 27.7 615.0 27.6 580.9 69.3 107.5
2.1 0.0578 0.00123 577.1 27.0 566.1 24.4 522.1 47.3 110.5
3.1 0.05935 0.00144 559.2 40.5 563.3 36.1 580.1 53.7 96.4
4.1 0.06024 0.00127 605.4 24.6 606.8 23.0 612.3 46.2 98.9
6.1 0.05892 0.00188 578.9 36.2 575.9 34.0 564.0 70.9 102.6
5.1 0.06239 0.00118 635.9 37.2 647.4 32.2 687.6 40.8 92.5
9.1 0.05539 0.0019 577.9 36.8 548.5 33.8 428.1 78.5 135.0
7.1 0.06904 0.01105 561.0 92.2 633.1 124.1 899.8 370.8 62.3
8.1 0.05883 0.00685 273.4 27.1 305.8 44.1 561.0 276.3 48.7
10.1 0.10596 0.00089 1734.6 82.5 1733.0 47.3 1731.1 15.5 100.2
CT31 and CT 32—clasts of felsic volcanic—Itajaı´ conglomerates (corrected using measured 204Pb)
31-1.1 0.06128 0.00321 810.4 18.6 768.6 33.2 649.1 116.8 124.8
31-2.1 0.06078 0.00822 579.8 19.0 590.4 66.5 631.6 321.8 91.8
31-3.1 0.05483 0.00591 603.4 17.8 563.5 51.3 405.4 261.2 148.8
31-4.1 0.05884 0.00221 606.9 17.3 597.3 23.2 561.2 84.2 108.1
31-5.1 0.05734 0.00238 646.0 15.4 615.4 23.9 504.5 94.2 128.1
31-6.1 0.0543 0.00236 592.7 22.1 551.2 26.7 383.6 100.6 154.5
31-7.1 0.05331 0.00344 597.1 14.7 546.7 31.1 341.9 153.1 174.7
31-8.1 0.05841 0.0022 630.9 21.1 612.6 25.4 545.3 84.5 115.7
31-9.1 0.05593 0.00235 606.6 15.2 574.5 23.2 449.7 96.0 134.9
31-10.1 0.06426 0.00153 641.4 48.2 666.0 42.4 750.2 51.3 85.5
32-1.1 0.05898 0.00205 591.3 17.6 586.2 22.3 566.2 77.4 104.4
32-2.1 0.06123 0.00158 645.2 21.0 645.7 21.9 647.2 56.5 99.7
562 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
Table 3 continued
Labels 207Pb/206Pb ± 7/6 Age 206/238 ± Age Age (207/235) ± age Age (207/206) ± age Conc (%)
32-3.1 0.06014 0.00101 580.7 21.7 586.5 20.0 608.7 36.8 95.4
32-4.1 0.05515 0.00612 599.9 22.1 563.3 54.1 418.2 269.1 143.5
32-5.1 0.06003 0.00111 648.9 16.4 639.1 16.3 604.5 40.5 107.3
32-6.1 0.06141 0.00135 619.3 11.0 626.7 14.4 653.7 47.9 94.7
32-7.1 0.05821 0.00168 607.9 27.6 593.3 26.7 537.8 64.5 113.0
32-8.1 0.05074 0.00287 580.9 16.9 514.5 27.6 229.1 136.3 253.5
32-9.1 0.06014 0.00351 585.8 14.0 590.5 30.1 608.5 131.5 96.3
32-10.1 0.05949 0.00247 610.3 10.8 605.0 21.9 584.9 92.8 104.3
32-12.1 0.05743 0.00382 582.4 31.7 567.5 41.1 508.0 153.2 114.7
32-15.1 0.05969 0.00132 621.9 14.7 615.6 16.4 592.4 48.6 105.0
32-17.1 0.0557 0.00561 596.9 29.7 565.4 52.9 440.5 241.2 135.5
32-18.1 0.05841 0.0013 603.8 16.7 591.6 17.5 545.1 49.3 110.8
32-13.1 0.13726 0.00102 2218.8 50.9 2205.4 26.4 2193.0 13.0 101.2
32-14.1 0.07592 0.00136 1186.3 51.5 1153.7 37.0 1092.9 36.2 108.5
32-11.1 0.06471 0.00101 778.2 20.4 774.8 18.3 765.0 33.1 101.7
32-16.1 0.06553 0.001 814.8 13.7 808.5 14.0 791.3 32.3 103.0
Felsic volcanic—Apiu´na Formation (corrected using measured 204Pb)
API-1.1 0.05958 0.00494 559.2 16.7 565.0 40.8 588.2 191.0 95.1
API-2.1 0.05804 0.00288 565.6 17.2 558.7 27.1 531.1 112.4 106.5
API-4.1 0.06 0.00189 560.7 12.6 569.2 18.3 603.5 69.7 92.9
API-5.1 0.05946 0.00307 559.1 14.1 564.1 26.6 584.1 116.1 95.7
API-6.1 0.05621 0.00286 545.1 14.8 529.1 25.6 460.6 117.1 118.3
API-3.1 0.04842 0.00743 550.4 17.8 474.1 63.0 119.8 326.5 459.5
Subida Granite (corrected using measured 204Pb)
A SUB-1.1 0.05413 0.00265 537.0 29.9 507.5 32.6 376.5 114.2 142.6
A SUB-2.1 0.05792 0.00302 539.6 30.4 537.2 35.3 526.9 118.4 102.4
A SUB-3.1 0.05594 0.00157 518.1 40.5 505.7 36.1 449.9 63.5 115.2
A SUB-4.1 0.05606 0.00278 537.2 28.9 521.7 32.8 454.6 113.9 118.2
A SUB-5.1 0.05566 0.00382 522.7 33.2 507.4 41.1 439.0 160.5 119.1
A SUB-6.1 0.05566 0.00227 537.7 23.8 519.3 26.9 439.0 93.6 122.5
C SUB-7.1 0.05866 0.00223 525.1 25.8 530.6 28.2 554.4 85.0 94.7
C SUB-8.1 0.05504 0.00205 509.0 26.7 492.0 27.6 413.9 85.7 123.0
C SUB-9.1 0.0556 0.00205 509.6 27.7 496.5 28.3 436.4 84.3 116.8
C SUB-10.1 0.05587 0.00172 528.4 22.0 513.4 22.9 447.2 70.0 118.2
C SUB-11.1 0.05624 0.00102 521.7 26.2 510.7 23.3 461.9 40.5 113.0
C SUB-12.1 0.05807 0.00053 534.1 25.1 533.8 21.3 532.4 20.1 100.3
NC SUB-2.1 0.05635 0.00398 517.8 16.9 508.4 33.4 466.4 164.6 111.0
NC SUB-3.1 0.05608 0.00474 522.7 16.2 510.4 38.5 455.4 199.3 114.8
NC SUB-7.1 0.0528 0.00607 516.3 15.4 481.7 48.2 320.3 284.7 161.2
NC SUB-1.1 0.05521 0.00318 598.6 16.1 562.8 29.5 420.7 133.9 142.3
NC SUB-4.1 0.04581 0.02987 515.4 22.3 429.0 261.7 0.0 0.0 0.0
NC SUB-5.1 0.02593 0.02533 481.7 25.1 248.6 244.4 0.0 0.0 0.0
NC SUB-6.1 0.03829 0.01468 524.6 18.4 375.6 130.4 0.0 0.0 0.0
NC SUB-8.1 0.05128 0.00714 480.3 16.0 442.9 54.4 253.4 292.0 189.5
Laboratory: A = RSES (Australia); C = BSC (China); NC = new data from BSC (China)
Labels: x, y; grain number followed by analysis number
Grain habit: p prism, anh anhedral, fr fragment
Site: e end or edge, m middle, int interior, og overgrowth, c core
CL image microstructure, osc oscillatory finescale zoning, rex recrystallised, h homogeneous (d dark, b bright)
Data corrected with model Pb of Cumming and Richards (1975) for likely age of rock; all errors are 1 s
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 563
123
Fig. 17 a U–Pb diagram for the tuffaceous levels (sample MBAN 1)
intercalated within Bau´ Formation arkosic sandstones (close to the
Ribeira˜o do Russo, south of Blumenau). The age obtained from
volcanogenic zircons constrains the oldest age limit possible for the
sedimentation of the Itajaı´ Group lower unit; b, c U–Pb plots for
zircons extracted from felsic volcanic rocks that occurs as sub-
decimeter-sized (1–3 cm) in the Itajaı´ Group conglometares (b sample
CT31—foot of Morro Grande, left bank of the Itajaı´ Ac¸u river, in the
proximity of Apiu´na; c CT32 -thick conglomerate level in the upper
Neisse river); d U–Pb diagram for the Morro do Gravata´ felsic
volcanic rock. The age obtained constrains the youngest age limit
possible for the Itajaı´ Group sedimentation; e U–Pb diagram for the
Subida leucosyenogranite. The Cambrian age obtained for this
granitoid intrusive in the Itajaı´ Group attests for its anorogenic
character and rules out any relationship with the much older Serra do
Mar Suite
564 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
et al. 2010) and zircons from igneous rocks (this manu-
script), which means that the former results complement
the latter.
The interpretations based on (Sr, Nd, and Pb) isotopes
presented in both papers are very harmonious, indicating that
the Dom Feliciano Belt was the main source of material for
the Itajaı´ Basin intermediate and upper sedimentary units.
The Santa Catarina Granulitic Complex is indicated in both
papers as the main candidate as source for the sandstones and
conglomerates that composes the basal portion of the Itajaı´
Basin. Therefore, both groups of researchers agree with the
classification of the Itajaı´ Basin as a peripheral foreland basin
located between the Dom Feliciano Belt to the south and the
stable and old terranes to the north.
However, some divergences appear regarding the results
achieved, when specific points are compared. The ages
obtained for tuffs and acid volcanic rocks, which define the
limit values for the beginning and the end of the deposition
of the Itajaı´ Group sedimentary units, are not concordant.
The interval between 596 and 560 Ma presented in this
work is older than the 563–549 Ma interval proposed by
Gaudagnin et al. (2010).
A lower limit of 596 Ma is very close to the age of
volcanism observed for the Campo Alegre Basin, which
would place the deposition of both basins closer in time.
This age is also closer to the well-controlled age of the
basal portion of the Camaqua˜ Basin and also is in agree-
ment with the recently determined deposition interval for
the Arroyo del Soldado Formation in Uruguay (Basei, in
preparation). The older age for the beginning of the Itajaı´
Group deposition is compatible with the age of detrital
zircons presented by Guadagnin et al. (2010), the younger
populations from lower units of the Itajaı´ Basin indicating
values around 590 M. Only for the upper unit of the base of
siltites, the younger population of detrital zircons yields
ages around 563 Ma, both within the interval proposed in
this paper.
On the other hand, the upper limit for the deposition of
the sediments is given by the age of the felsic rocks that
affect the Basin sediments. The values for this magmatism
were obtained in both papers by dating the Gravata´ dome
felsic rocks (south of Apiu´na). The results were 558 and
549 Ma, the older presented in this paper. One of the
possible causes for such difference can be attributed to the
methods used—LA ICPMS by Guadagnin et al. (2010) and
SHRIMP (our work).
Other divergent points reside in the implications that
result from the different stratigraphic columns presented in
Fig. 18 Dated Rocks
a Volcanic tuffs associated with
sandy levels intercalated with
Bau´ Formation conglomerates,
south of Blumenau, close to
Ribeira˜o do Russo; b Polymictic
conglomerate with abundant
felsic volcanic rock clasts;
c Acid volcanic rock of Apiu´na
Formation, Morro do Gravata,
south of Apiu´na; d Pink facies
of the Subida syenogranite
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 565
123
both works. In our paper, sandstones, conglomerates, and
acid tuffs that occur on the southern border of the Itajaı´
Basin are interpreted as a tectonic recurrence of the Bau
Formation (lower unit), whereas in Guadagnin et al. (2010)
these rocks integrate the upper unit, which would indicate
the return of continental conditions that predominated in
the beginning of the Itajaı´ Basin evolution. Our stratigra-
phy reflects the reading of the geological map presented in
this paper, where the modifications introduced by the epi-
dermal tectonics, which deforms the basin, characterizes it
as a typical example of a thrust and fold belt, and explains
the occurrence of the same rocks on both borders. The
major deformation of the southern border units, the simi-
larities observed in the sedimentary associations of both
borders, a compatible isotopic signature (Nd and Pb) and
comparable provenance ages, led us to consider that a more
correct interpretation is that the rocks from both borders
compose a single lithostratigraphic unit.
Another point in favor of a proposal that involves the
repetition of the lower unit in the southern border is the
pattern yielded by detrital zircons presented by Guadagnin
et al. (2010), which shows that the provenance of the zir-
cons from sandstones and conglomerates attributed by
these authors to the upper units is similar to the pattern
presented by the lower units that occur on the northern
border (Bau Formation) and quite different from the ages
observed at the base of the siltite unit, which for us rep-
resents the true top of the Itajaı´ Basin, that yields detrital
zircon ages restricted to Neoproterozoic values.
Conclusions
The integrated approach, involving information coming
from cartography, lithostratigraphy, structural geology,
lithogeochemistry, isotopic geochemistry, and geochro-
nology, helped reinforce a new and more detailed inter-
pretation for the Itajaı´ Basin tectonic evolution.
The proposed lithostratigraphic column assigns the Itajaı´
Group rocks into two major sequences: a basal continental
and an upper marine sequence. The lower sequence (the
Bau´ Formation) is represented by sandstones and con-
glomerates deposited in alluvial and retrograding deltaic
fan systems, with facies varying from gravelly and sandy
deltaic plain, grading to proximal and distal deltaic front, to
prodelta. This sequence grades laterally and toward the top to
the upper sequence, constituted by the Ribeira˜o Carvalho
Formation rhythmites, which represent the proximal chan-
nelized and non-channelized turbiditic facies, the Ribeira˜o
Neisse Formation arkosic sandstones, and laminated siltites of
the Ribeira˜o do Bode Formation distal turbiditic facies.
Based on the similarities between the sandstones and
conglomerates that occur in both borders of the Itajaı´
Basin, it is emphasized that these rock types belong to the
Bau´ Formation. Besides the similar geochemical-isotopic
characteristics, the continuity of these rocks can be
checked in the geologic map, which shows the Pedra de
Amolar region as the junction between the units of both
borders. The proposal that the sandstones with continental
characteristics that occur in the southern border represent a
third unit is thus ruled out. They in fact represent tectonic
repetitions of the basal unit by inverse faulting.
The structural studies indicate that the intensity of phase
D1 was highest in the SE portion of the Itajaı´ Basin, close
to the orogenic belt, with NE–SW axial orientation char-
acterized by folds with vertical axial planes close to the
northern border, grading to megafolds of inverse flanks,
inverse faults and thrusting in the southern portion, with
clear tectonic vergence to NW, toward the foreland.
Thrusting with a NW direction of transport and preferen-
tially affecting the southern border of the Basin is associ-
ated with this phase. Phase D2 is restricted to discontinuous
folds of large wavelength and approximately N–S axial
orientation and slight southwards plunge. The interference
of phase D2 on phase D1 is observed at various scales, in
the outcrops and in the regional map. These phases are
directly related to the deformational phases that followed
the metamorphic climax in the Brusque Group.
The study of the susceptibility anisotropy and remanent
magnetization in two sites of the Gravata rhyolitic dome
has shown that these igneous rocks were affected only by
the Itajaı´ Basin second deformational phase, which places
the first phase between 600 and 560 Ma and the second
phase syn- to post-560 Ma. Additionally, this chronology
of events indicates, in agreement with the information
obtained by magnetostratigraphy, a short period between
deposition and deformation phase D1, implying possible
syn-tectonic sedimentation (Drukas 2009).
The lithogeochemical (major, trace and rare earth
elements) and isotopic (Sr, Nd and Pb) analyses of the
sedimentary rocks gives support to the proposed lithostrati-
graphic column. A very homogeneous behavior is observed
in the units that compose the upper sequence, which is at
the same time significantly different from that of the lower
sequence. Among the various tectonic settings possible, it
is proposed that the precursors of the Itajaı´ Group sedi-
ments were generated in settings geochemically associated
with continental collision, passive margins and magmatic
arcs. The probable candidates to source areas of the upper
sequence sediments, with marked contribution from the
upper crust, are the Brusque Group and the Floriano´polis
Batholith. The proposed candidates for the continental and
lower units, whose geochemical signature shows consid-
erable contribution from reworked old crust, are the terr-
anes of the Luis Alves, Sa˜o Miguel, and Camboriu´
Complexes.
566 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
The Itajaı´ Basin is thus interpreted as a peripheral
foreland basin directly related to the evolution of the Dom
Feliciano Belt. The late-collisional shortening of the fold
belt, represented by the Brusque Group, led to the forma-
tion of the Itajaı´ Basin by flexural subsidence. The depo-
sition of the basal continental sequence started with the
erosion of its basement, notably the Santa Catarina Gran-
ulitic Complex, with some contribution from the Dom
Feliciano Belt. With the increasing proximity of the adja-
cent Brusque Group orogenic belt and the Floriano´polis
Batholith (magmatic arc), these became the main sources
for the sediments of the upper, turbiditic marine sequences.
The Itajaı´ Basin and the Brusque Group would then be
situated in the lower plate of this passive margin context
(Luı´s Alves Microplate southern border), whereas the
Floriano´polis Batholith, representing the roots of a Neo-
proterozoic magmatic arc, south of the Major Gercino
Suture Zone, would be situated in the upper plate in the
active margin setting. The generation of the Itajaı´ Basin
occurred in a late-collisional setting that followed the ter-
mination of the subduction of oceanic crust southeast-
wards, around 600 Ma.
The lack of records indicating a rift-type opening lead-
ing to the development of an oceanic crust implies that the
Itajaı´ Basin upper marine units were deposited in an
environment similar to a restricted and internal sea. The
geologic history of the Itajaı´ Basin must have started
around 600 Ma, with the deposition of the lower units on
the gneisses of the Luı´s Alves Microplate southern border.
Around 560 Ma, the sedimentation ceased, as attested by
the Apiu´na Formation felsic magmatism, expressed as
dikes and domes crosscutting the whole sedimentary suc-
cession. The emplacement of the felsic volcanism after the
first deformation phase (Drukas 2009) implies a maximum
time interval of 40 Ma for the deposition and the first
deformation phase. In the Cambrian, close to 520 Ma, after
the stabilization of the Itajaı´ Basin, the intrusion of the
anorogenic Subida leucosyenogranite took place.
Based on the available radiometric data, it is demonstrated
that the deposition of the Itajaı´ Basin was exclusively
restricted to the Neoproterozoic. Respecting the differences
inherent to the details acquired during their evolutions, the
Itajaı´ Basin can be temporally and tectonically correlated with
the Camaqua˜ Basin in Rio Grande do Sul (Pain et al. 1990,
Fragoso Cesar 1991) and the Arroyo del Soldado/Piria´polis
Basin in Uruguay (Gaucher and Sprechmann 1998, Gaucher
et al. 1996, 2009). It also presents several tectonic-sedimen-
tary characteristics in common with the Nama Basin, its
equivalent in Africa (Gresse et al. 1996, Frimmel and Miller
2009, Germs et al. 2009; Guadanin et al. 2010).
Acknowledgments The authors are grateful to many colleagues of
the Institute of Geosciences—USP for the fruitful discussions. Most
of field and laboratory work were supported by grants from the Sa˜o
Paulo State Foundation of Research Support (FAPESP—2005/58688-1).
References
Appi CJ (1991) Ana´lise estratigra´fica da sec¸a˜o metassedimentar do
Grupo Itajaı´ no estadode Santa Catarina. Dissertation, Federal
University of Rio de Janeiro
Appi CJ, Cruz CES (1990) Estratigrafia de sequ¨eˆncias na Bacia do
Itajaı´. In: Cong. Bras. Geol., 36, Natal, Anais, vol 1. Natal, SBG.
pp 93–106
Basei MAS (1985) O Cintura˜o Dom Feliciano em Santa Catarina.
Unpublished Ph.D thesis, University of Sa˜o Paulo.191 pp
Basei MAS (2000) Geologia e modelagem geotectoˆnica dos terrenos
Pre´-Cambrianos das regio˜es Sul- Oriental brasileira e uruguai-
ana: possı´veis correlac¸o˜es com provı´ncias similares do sudoeste
africano. Livre Doceˆncia Thesis, University of Sa˜o Paulo. p 18
Basei MAS, Siga O Jr, Machiavelli A, Mancini F (1992) Evoluc¸a˜o
tectoˆnica dos terrenos entre os Cinturo˜es Ribeira e Dom
Feliciano (PR - SC). Rev Bras Geoc 22(2):216–221
Basei MAS, Citroni SB, Siga O Jr (1998a) Stratigraphy and age of
fini-Proterozoic basins of Parana´ and Santa Catarina States,
Southern Brazil. Bol IG-USP, Se´r Cient 29:195-216
Basei MAS, McReath I, Siga O Jr (1998b) The Santa Catarina
granulite complex of Southern Brazil, a review. Gond Res
1:383–391
Basei MAS, Siga O Jr, Cordani UG, Sato K, Lima PS (1999) The
magmatism of the Itajaı´ Basin, SC, Southern Brazil, and its
importance to define the Proterozoic-Phanerozoic limit. II South
American symposium on isotope Geology, Cordoba, Argentina,
Actas, pp 287–290
Basei MAS, Frimmel HE, Nutman AP, Preciozzi F, Jacob J (2005)
The connection between the Neoproterozoic Dom Feliciano
(Brazil/Uruguay) and Gariep (Namibia/South Africa) orogenic
belts. Prec Res 139:139–221
Basei MAS, Frimmel HE, Nutman AP, Preciozzi F (2008a) West
Gondwana amalgamation based on detrital zircon ages from
Neoproterozoic Ribeira and Dom Feliciano belts of South
America and comparison with coeval sequences from SW
Africa. Geol Soc Spec Public 294:239–256
Basei MAS, Drukas CO, Santos PR, Osako L, Arcaro NP (2008b)
Estratigrafia, idade e provenieˆncia dos sedimentos da Bacia do
Itajaı´, SC, Brasil. In: 44CBG, Anais, SBG,Curitiba
Basei MAS, Grasso C, Vlach SRF, Nutman AP, Siga O Jr, Osako LS
(2008c) A-type rift related granite and the Lower Cryogenian
age for the beginning of the Brusque Belt basin. In: South
American Symposium on Isotope Geology, 6, San Carlos de
Bariloche, Argentina. Proceedings, CD-ROM
Basei MAS, Nutman A, Siga O Jr, Passarelli CR, Drukas CO (2009)
The evolution and tectonic setting of the Luis Alves Microplate
of Southeastern Brazil: an exotic terrane during the assembly of
Western Gondwana. In: Gaucher C, Sial AN, HalversonGP,
Frimmel HE (eds) Neoproterozoic-Cambrian tectonics, global
change and evolution: a focus on southwestern Gondwana, vol
16. Develop Prec Geol, pp 273–291
Carvalho PF,Pinto EA (1938) Reconhecimento Geolo´gico no Estado
de Santa Catarina. DGM/DNPM, Rio de Janeiro. Boletim
(92):30
Citroni SB (1993) Ambientes deposicionais e significado geotectoˆ-
nico da sedimentac¸a˜o do Grupo Itajaı´-SC. Master Thesis,
University of Sa˜o Paulo
Compston W, Williams IS, Meyer C (1984) U–Pb geochronology of
zircons from lunar breccia 73217 using a sensitive high mass-
resolution ion microprobe. J Geophys Res Supp 89:525–534
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 567
123
Cumming GL, Richards JR (1975) Ore lead isotope ratios in a
continuously changing Earth. Earth Plan Sci Lett 28:155–171
DePaolo DJ (1988) Neodymium isotope geochemistry. Springer,
Berlin, 187 p
Dickinson WR (1974) Plate tectonics and sedimentation. In: Dickinson
WR (ed) Tectonic and sedimentation, special publication society of
economic paleontologists and mineralogists, 22. Tulsa, Oklahoma,
pp 1–272
Drukas CO (2009) Estratigrafia, estudos magne´ticos e provenieˆncia
dos sedimentos da Bacia do Itajaı´, SC. TF-2009/05, Geosciences
Institute, USP, Sa˜o Paulo, 68p
Faure EG (2005) Principles of isotope geology. Willey. New York,
589 pp
Floyd PA, Leveridge BE (1987) Tectonic environment of the
Devonian Gramscatho basin, south Cornwall: frame work mode
and geochemical evidence from turbiditic sandstones. J Geol Soc
144:531–542
Fonseca MM (2004) Sistemas Deposicionais e Estratigrafica de
Sequ¨eˆncias da Bacia do Itajaı´ (SC) e Detalhamento do Complexo
Turbidı´tico Apiu´na. PhD thesis, UNISINOS
Fragoso Cesar ARS (1991) Tectonica de Placas no Ciclo Brasiliano:
As orogenias dos cinturo˜es Dom Feliciano e Ribeira no Rio
Grande do Sul. PhD thesis, University of Sa˜o Paulo
Freitas RO (1945) O Conglomerado do Bau´ (Serie Itajaı´ - SC). Bol
Inst Geo Fac Filos Letras USP 2:37–115
Frimmel HE, Miller RM (2009) Continental rifting. Neoproterozoic to
early palaeozoic evolution of Southwestern Africa In: Gaucher
C, Sial AN, Halverson GP, Frimmel HE (eds) Neoproterozoic-
Cambrian tectonics, global change and evolution: a focus on
Southwestern Gondwana. Elsevier, Amsterdam, pp 153–159
Gaucher C, Sprechmann P (1998) Grupo Arroyo del Soldado:
Paleontologia, Edad y Correlaciones (Vendiano-Cambrico Infe-
rior, Uruguay). Actas del II Gongreso Uruguayo de Geologia,
Punta del Este, Uruguay, pp 183–187
Gaucher C, Sprechmann P, Schipilov A (1996) Upper and middle
proterozoic fossiliferous sedimentary sequences of the Nico
Perez Terrane of Uruguay: lithostratigraphic units, paleontology,
depositional environments and correlations. N Jb Geol Pala¨nont
Abh 199(3):339–367
Gaucher C, Frimmel HE, Germs GJB (2009) Tectonic events and
palaeogeographic evolution of southwestern Gondwana in the
Neoproterozoic and Cambrian In: Gaucher C, Sial AN, Halver-
son GP, Frimmel HE (eds) Neoproterozoic tectonics, global
change and evolution: a focus on Southwestern Gondwana.
Elsevier, Amsterdam, pp 295–316
Germs GJB, Miller RM, Frimmel HE, Gaucher C (2009) Syn- to late-
orogenic sedimentary basins of southwestern Africa. Neoprote-
rozoic to Early Palaeozoic evolution of Southwestern Gondwana
In: Gaucher C, Sial AN, Halverson GP, Frimmel HE (eds)
Neoproterozoic tectonics, global change and evolution: a focus
on Southwestern Gondwana. Elsevier, Amsterdam, pp 183–203
Gresse PG, Chemale F, Silva LC, Walraven F, Hartmann LA (1996)
Late to post-orogen basins of Pan-African-Brazilian collision
orogen in southwest Africa and southern Brazil. Basin Res
8:157–171
Guadagnin F (2007) Idade e provenieˆncia das rochas sedimentares da
Bacia do Itajaı´. Porto Alegre, RS, Trabalho de Conclusa˜o de
Curso, IGEO/UFRGS, 119 pp
Guadagnin F, Chemale Jr. F, Dussin IA, Jelinek AR, Santos MN,
Borba ML, Justino D, Bertotti AL, Alessandretti L (2010)
Depositional age and provenance of the Itajaı´ Basin, Santa
Catarina State, Brazil: implications for SW Gondwana correla-
tion. Precambrian Res 180(3-4):156–182
Harara OMM (2001) Mapeamento e investigac¸a˜o petrolo´gica e
geocronolo´gica dos litotipos da regia˜o do Alto Rio Negro
(PR-SC): Um exemplo de sucessivas e distintas atividades
magma´ticas durante o Neoproterozo´ico. PhD Thesis, University
of Sa˜o Paulo
Harara OMM, Basei MAS, Siga O Jr (2002) From subduction to late
and post-collision settings: a record from Neoproterozoic
sucessive magmatic in the upper Rio Negro region. In: XXXXI
Congresso Brasileiro de Geologia, Joa˜o Pessoa, PB, vol 1, p 310
Hartmann LA, Silva LC, Orlandi V (1979) O Complexo Granulı´tico
de Santa Catarina. Acta Geolo´gica Leopoldensia 6:94–112
Herron MM (1988) Geochemical Classification of Terrigenous Sands
and Shales from core or log data. J Sediment Petrol 58(5):
820–829
Kaul PFT (1976) Projeto Brusque Serra do Tabuleiro. Conveˆnio
DNPM/CPRM. Porto Alegre, Brasil. 165 p
Kaul PFT (1980) O Cra´ton Luis Alves. Camboriu´, SC. In: Congresso
Brasileiro de Geologia 31, vol 5, pp 2677–2683
Kaul PFT (1984) Significado dos granitos anorogeˆnicos da Suı´te
Intrusiva Serra do Mar na evoluc¸a˜o da crosta no sul-sudeste do
Brasil no aˆmbito das folhas SG.22-Curitiba e SG.23-Iguape. In:
Congresso Brasileiro de Geologia 33, vol 6, pp 2815–2825
Krebs ASJ, Caldasso ALS, Lopes RC (1988) Interpretac¸a˜o preliminar
da sequ¨eˆncia deposicional da Bacia do Itajaı´ na a´rea da folha
Botuvera´. In: Congresso Brasileiro de Geologia 35, vol 2,
pp 592–605
Krebs ASJ, Silva MA, Dias AA, Camozzato E, Lopes RC (1990) O
Grupo Itajaı´ na folha Botuvera´ (SC). Modelo geome´trico-
cinema´tico e relac¸o˜es com o Cintura˜o granulı´tico e Cintura˜o
Metavulcano-Sedimentar Brusque. In: Congresso Brasileiro de
Geologia 36, vol 6, pp 2966–2975
Ludwig KR (2001) Using Isoplot/Ex. A geochronological toolkit for
Microsoft Excel. Berkeley Geochronology Center, Special
Publications 1. Berkeley, USA
Maack R (1947) Breves notı´cias sobre a geologia dos estados do
Parana´ e Santa Catarina. Arq Biol Tecnol 2:63–154
Macedo MHF, Basei MAS, Bonhomme M, Kawashita K (1984)
Dados geocronolo´gicos referentes a`s rochas metassedimentares
do Grupo Itajaı´, Santa Catarina. Ver Bras Geoc 14(1):30–34
Machiavelli A, Basei MAS, Siga O Jr (1993) Suı´te Granı´tica Rio
Pieˆn: um arco magma´tico do Proterozo´ico superior na Micro-
placa Curitiba. Geochem Brasiliensis 7:113–129
McLennan SM, Taylor SR (1985) The continental crust: its compo-
sition and evolution. Blackwell, Oxford, 311 p
McLennan SM, Taylor SR, McCulloch MT, Maynard JB (1990)
Geochemical and Nd-Sr isotopic composition of deep-sea
turbidites: crustal evolution and plate tectonic associations.
Geochim Cosmochim Acta 54:2015–2050
McLennan SM, Hemming SR, Taylor SR, Erickson K (1995) Early
proterozoic crustal: geochemical and Nd-PB isotopic evidence
from metasedimentary rocks, southwestern North America.
Geochim Cosmochim Acta 59(6):1153–1177
Pain PSG, Faccini UF, Netto RG, Nowatski CH (1990) Estratigrafia
das Bacias do Camaqua˜ e Santa Barbara, Eo-Paleozoico do Rio
Grande do Sul (Brasil). In: IGCP 270 workshop—Eventos do
Paleozoico Inferior da America latina e suas relac¸o˜es com a
geˆnese de Gondwana. Sa˜o Paulo. IG-USP
Pain PSG, Leipnitz II, Rosa ANZ, Rosa AAS (1997) Preliminary
report on the occurrence of Chancelloria sp. In the Itajaı´ Basin,
southern Brazil. Rev Bras Geoc 27(3):303–308
Pettijohn FJ, Potter PE, Siever R (1972) Sand and sandstone.
Springer, Heidelberg 618 p
Rollinson H (1993) Using geochemical data: evaluation, presentation,
interpretation. Longman
Rostirolla SP (1991) Tectoˆnica e Sedimentac¸a˜o da Bacia de Itajaı´—
SC. Umpublished Master Thesis – UFOP, Ouro Preto MG, 132 p
Rostirolla SP, Alkimin FF, Soares PC (1992) O Grupo Itajaı´, Estado
de Santa Catarina, Brasil, exemplo de sedimentac¸a˜o em uma
bacia flexural de antepaı´s. Bol Geoc Petrobra´s 6(3/4):109–122
568 Int J Earth Sci (Geol Rundsch) (2011) 100:543–569
123
Rostirolla SP, Ahrendt A, Soares PC, Carmingnani L (1999) Basin
analysis and mineral endowment of the Proterozoic Itajaı´ Basin,
south-east Brazil. Basin Res 11:127–142
Salamuni R, Bigarella JJ, Takeda FK (1961) Considerac¸o˜es sobre a
estratigrafia e tectoˆnica da Se´rie Itajaı´. Curitiba PR Bol Par
Geogr 415:188–201
Santos JPP, Bettini C, Moraes MAS (2008) Representac¸a˜o espacial de
lobos e canais turbidı´ticos em afloramentos da regia˜o de Apiu´na,
Bacia do Itajaı´, Santa Catarina. Bol Geoc Petrobra´s 16:69–85
Sato K, Siga O Jr, Nutman AP, Basei MAS, McReath I, Kaulfuss G
(2003) The Atuba complex, Southern South American platform:
archean components and paleoproterozoic to neoproterozoic
tectonothermal events. Gond Res 6(2):51–263
Schulz A Jr, Albuquerque LFF, Rodrigues CS (1970) Geologia da
Quadrı´cula de Floriano´polis, SC. DNPM. Porto Alegre, Brasil, 75 p
Siga O Jr, Basei MAS, Reis Neto JM, Machiavelli A, Harara OM
(1995) O Complexo Atuba: um cintura˜o Paleoproterozo´ico
intensamente retrabalhado no Neoproterozo´ico. Boletim IG-USP
Se´rie Cientı´fica 26:69–98
Siga O Jr, Basei MAS, Passarelli CR, Sato K, Cury LF, Mcreath I
(2009) Magmatic records of lower neoproterozoic and upper
neoproterozoic in Itaiacoca Belt (Parana´-Brazil): zircon ages and
lithostratigraphy studies. Gondwana Res 197–208
Silva LC, Dias AA (1981) Projeto Timbo´-Barra Velha, Brasil.
Conveˆnio DNPM/CPRM. Porto Alegre. 282 p
Sircombe KN (2000) Quantitative comparison of large data sets of
geochronological data using multivariate analysis: a provenance
study example from Australia. Geochimica Cosmochimica Acta
64:1593–1616
Stern RA (1998) High resolution SIMS determination of radiogenic
trace-isotope ratios in minerals. In: Cabri LJ, Vaughan DJ (eds)
Modern approches to ore and environmental mineralogy. Short
Course Series, Mineral Assoc, Canada, pp 241–268
Vlach SRF, Gualda GAR (2007) Allanite and chevkinite in A-type
granites and syenites of the Graciosa Province, southern Brazil.
Lithos 97:98–121
Williams IS (1998) U-Th-Pb geochronology by ion microprobe.
In: McKibben MA, Shanks III WC, Ridley WI (eds) Applica-
tions of microanalytical techniques to understanding mineralis-
ing processes. Society of Economic Geologists, Reviews in
Economic Geology 7:1–35
Int J Earth Sci (Geol Rundsch) (2011) 100:543–569 569
123