Carboniferous siliciclastic and silicic magmatic rocks from the
Santa Susana–São Cristovão and Cabrela regions contain valuable
information regarding the timing of synorogenic processes in SW Iberia. In
this region of the Ossa-Morena Zone (OMZ), late Carboniferous terrigenous
strata (i.e., the Santa Susana Formation) unconformably overlie early
Carboniferous marine siliciclastic deposits alternating with volcanic rocks
(i.e., the Toca da Moura volcano-sedimentary complex). Lying below this
intra-Carboniferous unconformity, the Toca da Moura volcano-sedimentary
complex is intruded and overlain by the Baleizão porphyry. Original
sensitive high-resolution ion microprobe (SHRIMP) and laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) U–Pb zircon are presented in this paper, providing
chronostratigraphic and provenance constraints since available
geochronological information is scarce and only biostratigraphic ages are
currently available for the Santa Susana–São Cristovão region. Our
findings and the currently available detrital zircon ages from Paleozoic
terranes of SW Iberia (Pulo do Lobo Zone – PLZ – South Portuguese Zone – SPZ – and OMZ) were jointly analyzed using the K–S test and multidimensional scaling (MDS) diagrams to
investigate provenance. The marine deposition is constrained to the age
range of ca. 335–331 Ma (Visean) by new U–Pb data for silicic tuffs from the Toca da Moura and Cabrela volcano-sedimentary complexes. The
Baleizão porphyry, intrusive in the Toca da Moura volcano-sedimentary
complex, yielded a crystallization age of ca. 318 Ma (Bashkirian), providing
the minimum age for the overlying intra-Carboniferous unconformity. A
comparison of detrital zircon populations from siliciclastic rocks of the
Cabrela and Toca de Moura volcano-sedimentary complexes of the OMZ suggests
that they are derived from distinct sources more closely associated with the SPZ
and PLZ than the OMZ. Above the intra-Carboniferous unconformity, the Santa
Susana Formation is the result of the recycling of distinct sources
located either on the Laurussian side (SPZ and PLZ) or Gondwanan side (OMZ) of the
Rheic suture zone. The best estimate of the crystallization age of a granite
cobble which was found in a conglomerate from the Santa Susana Formation yielded ca. 303 Ma (Kasimovian–Gzhelian), representing the maximum depositional age for
the terrestrial strata. The intra-Carboniferous unconformity seems to
represent a stratigraphic gap of approximately 12–14 Myr, providing evidence
of the rapid post-accretion and collision uplift of the Variscan orogenic belt
in SW Iberia (i.e., the OMZ, PLZ, and SPZ).
Introduction
The Variscan orogen that extends from central Europe to Iberia was reworked
through discrete Carboniferous sedimentary cycles during the
Laurussia–Gondwana convergence, giving rise to the formation of marine and
terrestrial basins. In SW Iberia, stratigraphic correlation has been
proposed for the Carboniferous synorogenic strata found in the three main
tectonostratigraphic divisions of the Variscan orogen: the Ossa-Morena
(OMZ), Pulo do Lobo (PLZ), and South Portuguese (SPZ) zones (Quesada and
Oliveira, 2019, and references therein).
The Carboniferous siliciclastic strata in the Santa Susana–São
Cristovão and Cabrela regions (OMZ) include fossils indicating
Carboniferous to Kasimovian biostratigraphic ages (Teixeira, 1938–1940, 1941;
Lemos de Sousa and Wagner, 1983; Wagner and Lemos de Sousa, 1983; Pereira et
al., 2006; Machado et al., 2012; Lopes et al., 2014). In the Santa
Susana–São Cristovão region, late Carboniferous siliciclastic strata
of the Santa Susana Formation unconformably overlie (i) the Baleizão
volcanic–subvolcanic suite that was previously dated with whole-rock Rb–Sr
isochrones (Priem et al., 1986) and (ii) the early Carboniferous Toca da
Moura volcano-sedimentary complex, which includes volcanic rocks that have
never been dated. This intra-Carboniferous unconformity was generated as a
consequence of regional uplift and falling sea level, leading to a change in the
depositional environment from early Carboniferous marine to late
Carboniferous terrestrial (Gonçalves and Carvalhosa, 1984; Oliveira et
al., 1991; Machado et al., 2012). The provenance of the abovementioned
Carboniferous strata has been discussed based on petrographic,
paleontological, and detrital zircon geochronology evidence (Pereira et al., 2006; Machado et al., 2012; Lopes et al., 2014; Dinis et al., 2018).
In this paper, sensitive high-resolution ion microprobe (SHRIMP) and laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) U–Pb analyses were performed on zircon
grains from silicic volcanic, subvolcanic, and siliciclastic rocks sampled
in the Santa Susana–São Cristovão and Cabrela regions (OMZ; SW
Iberia). The aim of this geochronological study is to establish the
chronostratigraphic framework of these Carboniferous strata and to discuss
their provenance using a statistical approach (Kolmogorov–Smirnov test and
multiscaling diagrams). Thus we pay tribute to José Ramón Martínez-Catalán, who devoted part of his career to investigating the Carboniferous synorogenic basins of NW Iberia.
Geological setting
In SW Iberia, the tectonic limit between the OMZ (Gondwanan side) and the
PLZ and SPZ (Laurussian side) has been regarded as constituting the
tectonically reworked suture zone of the Rheic Ocean (Andrade, 1983; Quesada
et al., 1994; Simancas et al., 2005; Díaz-Apiroz et al., 2006; Ribeiro
et al., 2007; Pereira et al., 2017a) (Fig. 1). This Paleozoic suture zone
has been defined along the Beja–Acebuches Ophiolitic Complex (Fonseca et
al., 1999, and references therein). The Beja–Acebuches Ophiolitic Complex is
separated from the Beja Igneous Complex (Jesus et al., 2007, 2016) by a
strike-slip fault. Metabasalts and metagabbros (i.e., the Mombeja unit of
Andrade, 1983) from the Beja–Acebuches Ophiolitic Complex have been dated at
ca. 340–332 Ma (U–Pb zircon; Azor et al., 2008), while in the Beja Igneous
Complex gabbro and granitic rocks are relatively older, yielding
crystallization ages of ca. 353–342 Ma (U–Pb zircon; Jesus et al., 2007; Pin
et al., 2008). Trace element and isotopic signatures of Beja Igneous Complex
plutonic rocks indicate crustal contamination of parental magmas deriving
from a depleted asthenospheric mantle reservoir (Santos et al., 1990; Pin et
al., 2008; Jesus et al., 2016). The plutonic rocks of the Beja Igneous
Complex show well-defined intrusive contacts with previously deformed and
metamorphosed sedimentary and igneous rocks of the OMZ basement (Rosas et
al., 2008; Pin et al., 2008). The Beja Igneous Complex also includes the
São Cristovão–Alcáçovas subvolcanic complex (Gonçalves
and Carvalhosa, 1984), composed of silicic subvolcanic and volcanic rocks
(i.e., the Baleizão unit of Andrade, 1983), granophyres, and porphyries
dated at ca. 319 Ma (whole-rock Rb–Sr isochrones; Priem et al., 1986),
associated with diabases. Porphyry dikes are found cutting across the OMZ
basement that is here formed by Cambrian igneous rocks from ca. 527 Ma
(Alcáçovas gneiss; Chichorro et al., 2008) deformed and
metamorphosed in the early Carboniferous at 340±6 Ma (Pereira et
al., 2009). The major and trace element geochemistry of the Baleizão
porphyries indicates a calc-alkaline rhyolitic, rhyodacite, and andesitic
composition typical of magmas produced at convergent plate boundaries
(Santos et al., 1987; Caldeira et al., 2007; Ferreira et al., 2014). The
Baleizão porphyries occur as dikes and sills (Andrade, 1927) (Fig. 3a, b), overlying (Gonçalves and Carvalhosa, 1984) the early Carboniferous
siliciclastic and volcanic rocks of the Toca da Moura volcano-sedimentary
complex (Santos et al., 1987, and references therein) (Fig. 2).
(a) Inset with location of SW Iberia in the Iberian Variscan belt with regional distribution of the main Paleozoic terranes: CIZ – Central Iberian Zone; CZ – Cantabrian Zone; GTMZ – Galicia-Trás-os-Montes Zone; OMZ – Ossa-Morena Zone; PLZ – Pulo do Lobo Zone; SPZ – South Portuguese Zone; and WALZ – West Asturian-Leonese Zone. (b) Simplified geological map of SW Iberia showing the South Portuguese, Pulo do Lobo, and Ossa-Morena zones (modified from Pereira et al., 2017a, 2019, and references therein; Quesada
and Oliveira, 2019).
Simplified geological map and schematic stratigraphy of the Santa
Susana–São Cristovão region (Ossa-Morena Zone; modified from
Gonçalves and Carvalhosa, 1984; Machado et al., 2012). Sampling
locations of the Carboniferous sedimentary and igneous rocks used for
geochronology are indicated with yellow stars.
The Toca da Moura volcano-sedimentary complex is mainly composed of pelites
(i.e., Xistinhos; Teixeira, 1944; Fig. 3a) and greywackes associated
with andesite to rhyolite volcanic rocks (lava flow and tuffs; Fig. 3c–e), andesitic basalt, chert layers (Gonçalves and Carvalhosa, 1984), and
a few olistoliths of basalt and limestone. Siliciclastic rocks contain
well-preserved in situ palynomorph assemblages of Tournaisian to Visean age
and reworked palynomorphs ranging in age from the middle Cambrian to the
early Tournaisian (Pereira et al., 2006; Lopes et al., 2014). Based on
geochemical information, this volcanism was interpreted by Santos et al. (1987) as deriving from calc-alkaline magma produced in a continental
magmatic arc. A stratigraphic correlation was established between the Toca
da Moura volcano-sedimentary complex and the Cabrela volcano-sedimentary
complex (Pereira et al., 2006), which is located 15 km to the NW in the
Évora Massif (Pereira et al., 2007, 2012a) (Fig. 1b). The presence of
variable-scale soft-sediment structures (i.e., slumps, intraclast
conglomerates, and olistoliths) in both complexes indicates gravity-induced
instability during marine sedimentation. Detrital zircon ages of a
siliciclastic rock from the Cabrela volcano-sedimentary complex interbedded
with silicic tuffs (Fig. 3f) are mainly middle to late Devonian (82 %) and
early Carboniferous (14 %) and also include a few older grains (sample
OM-200 from Pereira et al., 2012a).
Photographs of the Carboniferous igneous rocks of the Santa
Susana–São Cristovão region: (a) Baleizão porphyry intrusive contact (yellow arrow) with siliciclastic rocks of the Toca da Moura volcano-sedimentary complex; (b) Baleizão porphyry; (c, d) rhyolitic tuffs of the Toca da Moura volcano-sedimentary complex; (e) volcanic breccia with fragments of siltstone (black) and rhyolite (yellow) at the base of the silicic tuffs of the Toca da Moura volcano-sedimentary complex; and (f) silicic volcanic rock interbedded with siltstones of the Cabrela volcano-sedimentary complex.
The Santa Susana Formation (i.e., Santa Susana Basin; Domingos et al., 1983;
Quesada et al., 1990; Oliveira et al., 1991) siliciclastic rocks that outcrop
along a narrow, NNW–SSE-trending discontinuous band, which is 0.1–5 km wide
and 12 km long, overlie unconformably the Baleizão porphyry and the Toca
da Moura volcano-sedimentary complexes (Fig. 2), forming the geological
contact between these stratigraphic units often defined by faults
(Gonçalves and Carvalhosa, 1984). The Santa Susana Formation is divided
into two members (Machado et al., 2012, and references therein): (i) the
lower member is mainly composed of coarse-grained sandstone and conglomerate
beds (Fig. 4a–d), and these conglomerates include pebbles and cobbles of
silicic porphyry, rhyolite, andesite, basalt, granite, felsic tuff, pelite,
sandstone, greywacke, quartzite, phyllite, chert, and quartz (Fig. 4e, f);
(ii) the upper member represents a repetitive sequence of alternating beds of
pelite and sandstone interbedded with coal seams and a few beds of
conglomerate (Fig. 2). These terrestrial deposits were most probably
deposited in an alluvial, fluvial-to-fluvial, and/or lacustrine (floodplain lakes
and/or abandoned channels with abundant vegetation) system (Machado et al., 2012, and references therein). The plant fossils identified in the
siliciclastic rocks of the Santa Susana Formation indicate a
Moscovian–Kasimovian biostratigraphic age (Wagner and Lemos de Sousa, 1983).
Pelitic beds from the upper member include palynomorph assemblages assigned
a Kasimovian age (Machado et al., 2012). Palynomorphs ranging in age from
the middle Cambrian to the early Moscovian were also found in siliciclastic
rocks of the Santa Susana Formation sampled from a borehole at a depth of
around 400 m (Lopes et al., 2014). Detrital zircon ages from upper member
sandstones (Dinis et al., 2018) are mainly distributed over the
Devonian–Carboniferous (41 %–51 %), Paleoproterozoic (23 %–30 %), and Ediacaran–Cryogenian (16 %–23 %) groups, as well as a few Stenian–Tonian and Archean grains.
Photographs of the Carboniferous sedimentary rocks of the Santa
Susana Formation lower member: (a) view of dipping meter-thick beds of medium–coarse grained sandstone intercalated with conglomerate; (b) planar-bedded coarse-grained sandstone; (c) plant imprints in sandstone; (d) conglomerate with cobbles and pebbles of granite (G), quartzite (Q), silicic porphyry (SP), and mafic volcanic rock (M); (e, f) conglomerate with pebbles of rhyolite (R), phyllite (P), felsic tuff (T), and quartzite (Q).
Rational and analytical methods
U–Pb geochronology of detrital zircon from siliciclastic rocks has been
extensively used in stratigraphic correlation studies for estimating the
maximum depositional age and investigating the provenance of sedimentary
sequences (Fedo et al., 2003; Dickinson and Gehrels, 2009). The youngest
detrital zircon grains found in siliciclastic rock commonly provide useful
information about depositional age, especially in areas that experienced
active volcanism during sediment accumulation (Gehrels, 2014). The maximum
depositional age obtained for siliciclastic rock is often not necessarily
coincident with the biostratigraphic age as defined by key fossil
assemblages (Pereira et al., 2019). Therefore, in order to overcome any
doubt about the true age of deposition, it is desirable that volcanic rocks
interstratified with fossiliferous siliciclastic rocks should be dated (Fedo
et al., 2003; Bowring et al., 2006). Furthermore, the application of zircon
U–Pb geochronology to volcano-sedimentary and sedimentary sequences, which are
separated by unconformities by means of the comparative analysis of their
age populations, may be useful for estimating time intervals and revealing
changes in provenance. Volcanic rocks that lie beneath or overlie
sedimentary sequences and unconformities can provide maximum and minimum
ages, respectively. When detrital zircon geochronology is linked to the
geochronology of crosscutting younger igneous rocks, then both a maximum and
minimum age bracket for deposition can be determined (Fedo et al., 2003).
In this study, SHRIMP U–Pb analyses were performed for the first time on
magmatic zircon from two tuffs from the Toca da Moura volcano-sedimentary
complex (TM-1 and SCV-2; Fig. 3c, d), one tuff from the Cabrela
volcano-sedimentary complex (CBR-12), one from the Baleizão silicic
porphyry (SCV-30; Fig. 3b), and a cobble of granite (SCV-7; Fig. 4e) found
in a conglomerate from the lower member of the Santa Susana Formation.
Estimations of the crystallization age of samples SCV-2, TM-1, and CBR-12
(syndepositional volcanism) and sample SCV-30 (post-depositional) were used
to validate the Tournaisian–Visean biostratigraphic age previously
attributed to the Toca da Moura and Cabrela volcano-sedimentary complexes
based on palynological assemblages (Pereira et al., 2006; Lopes et al., 2014). The presence of granite cobbles and pebbles in conglomerate layers
from the lower Santa Susana Formation indicates denudation and recycling of
a crystalline basement involving granite whose age is unknown. The dating of
the granite cobble (sample SCV-7) is useful for discussing provenance and
estimating the maximum depositional age of the Santa Susana conglomerate. In
addition, LA-ICP-MS U–Pb analyses were performed on detrital zircon grains
from two samples of sandstone from the upper and lower members of the Santa
Susana Formation (samples SS-1 and SS-2, respectively; Fig. 5g, h) and a
sample of pelite from the Toca da Moura volcano-sedimentary complex (sample
TM-3; Fig. 5e). These new U–Pb data are useful for discussing provenance and
determining the maximum depositional ages of the two sedimentary sequences
separated by an intra-Carboniferous unconformity. Sample locations in the
Santa Susana–São Cristovão region are indicated in Fig. 2. Finally, detrital zircon grains of siliciclastic rock from the Cabrela
volcano-sedimentary complex (sample CBR-11; Fig. 5f; equivalent to sample
OM-200 of Pereira et al., 2012a) were analyzed to test for the existence of
pre-Devonian ages. The new U–Pb results obtained in the present study are
compared with previously reported age spectra for pre-Kasimovian
siliciclastic rocks from the OMZ, PLZ, and SPZ siliciclastic sequences of SW
Iberia using statistical tools.
Petrographic images of the Carboniferous sedimentary and igneous
rocks of the Santa Susana–São Cristovão region: (a) rhyolitic–rhyodacite tuff of the Toca da Moura volcano-sedimentary complex showing quartz and feldspar phenocrysts enclosed in an ash matrix; (b) rhyolitic tuff showing flattened dark-brown millimeter-sized pumice and lithoclasts enclosed in an ash matrix; (c) porphyritic texture of the Baleizão rhyodacite–rhyolite characterized by quartz, plagioclase, K-feldspar, biotite, and amphibole phenocryst embedded in a fine-grained silicic matrix; (d) cobble of fine-grained granite showing graphic intergrowths of quartz and alkali feldspar, found in conglomerate from the Santa Susana Formation; (e) siltstone of the Toca da Moura volcano-sedimentary complex mostly composed of quartz grains and a few grains of plagioclase (P), tourmaline (T), and rock fragments (L); (f) siltstone of the Cabrela volcano-sedimentary complex showing fining upward grading and a slump fold; and (g, h) sandstones from the Santa Susana Formation with a high percentage of lithoclasts (L) and feldspar (F).
Zircon grains for U–Pb geochronology were selected using traditional
techniques: density separation with a Wilfley table (Universidad
Complutense de Madrid, Spain) and also a granulometric separation using
sieves with a mesh size of less than 500 µm, density (panning) separation procedures, and mineral identification using a binocular lens and
preparation of epoxy resin mounts with zircon grains (Universidade de
Évora, Portugal). U–Pb measurements were obtained at IBERSIMS
(Universidad de Granada, Spain) using SHRIMP and also at the Senckenberg
Naturhistorische Sammlungen Dresden (Museum für Mineralogie und
Geologie, Germany) using LA-ICP-MS. U–Pb measurements using SHRIMP and
LA-ICP-MS followed the procedures previously described by Dias da Silva et
al. (2018) and Pereira et al. (2012a), respectively. U–Pb results are listed
in Tables S1 and S2 in the Supplement. Concordia curves and
weighted average means were obtained using Isoplot 4 (Ludwig, 2003) (Figs. 6
and 7). Kernel density estimation (KDE) diagrams were produced with 90 %–110 % concordant 206Pb/238U ages for grains younger than 1.0 Ga and 207Pb/206Pb ages for older grains (for further details, see Frei and Gerdes, 2009) using IsoplotR (Vermeesch, 2018) (Fig. 8a, b). Cathodoluminescence imaging was performed at TU Bergakademie Freiberg (Germany) and at IBERSIMS.
Concordia diagrams and weighted mean of 206Pb/238U ages of analyzed zircon grains extracted from silicic volcanic rocks of the Toca da Moura and Cabrela volcano-sedimentary complexes.
Concordia diagrams and weighted mean of 206Pb/238U ages of
analyzed zircon grains of (a) the Baleizão porphyry and (b) the cobble of granite found in conglomerate from the Santa Susana Formation.
Pie diagrams and kernel density estimation (KDE) with U–Pb
detrital zircon ages of siliciclastic rocks from (a) the Toca da Moura (TM-3; this study) and Cabrela (CB; CBR-11; this study; OM-200; Pereira et al., 2012a) volcano-sedimentary complexes and (b) the Santa Susana Formation (SS-1 and SS-2; this study; SS upper member, StSz2, and StSz4; Dinis et al., 2018). (c) U–Pb age cumulative frequency plots applied to the U–Pb ages (90 %–110 % concordance) of detrital zircon grains from the Toca da Moura and Cabrela volcano-sedimentary complexes and the Santa Susana Formation.
The K–S test and the multidimensional scaling (MDS) technique were used in conjunction to compare
populations of detrital zircon U–Pb ages obtained from the Carboniferous
siliciclastic rocks of the Santa Susana–São Cristovão region using a
method designed for a recent study of the provenance of Triassic sandstones
(Gama et al., 2020, and references therein). The K–S test is a nonparametric statistical tool that has been successfully used for the
comparison of two populations of detrital zircon U–Pb ages by evaluating
whether they are significantly different, i.e., whether zircon age
populations correlate with a similar source or not, regardless of whether
they are of different sizes, while including at least 20 measurements
(DeGraaff-Surpless et al., 2003). The probability of the observed maximum
vertical difference between the cumulative probability curves (D value)
being unrelated to age differences between the two detrital zircon populations is given by a P value corresponding to a confidence interval of
95 % (Barbeau et al., 2009; Guynn and Gehrels, 2010) (Fig. S1 in the Supplement). High P values and low D values indicate that the
observed difference between the two detrital zircon populations may be
explained by the existence of common sources (Gama et al., 2020, and
references therein). K–S analyses were carried out using an Excel spreadsheet as described in Guynn and Gehrels (2010). The MDS
technique provides a means for the comparison of samples based on quantified
pairwise comparisons of their detrital zircon ages and is extremely useful
for visualizing the degree of similarity between samples in two dimensions;
i.e., greater distances between samples represent a greater degree of
dissimilarity between points on MDS diagrams (Vermeesch, 2013; Spencer et al., 2015; Wissink et al., 2018) (Fig. 9). MDS diagrams were produced
using IsoplotR (Vermeesch, 2018).
U–Pb geochronology: resultsVolcanic silicic rocks of the Toca da Moura and Cabrela
volcano-sedimentary complexes
Sample SCV-2 is a fine-grained banded rhyolitic tuff consisting of quartz and K-feldspar phenocrysts and lithoclasts of varying
size and shape (less than
1 mm in diameter) dispersed in an ash matrix (Fig. 5a). Zircon grains appear as stubby to elongated euhedral prisms (50–150 µm in diameter), mostly showing oscillatory concentric zoning growing on distinct cores or as simple crystals. There are some dark inclusions, unzoned patches, and transgressive variable luminescence and embayments. A total of 44 U–Th–Pb SHRIMP analyses of 44 grains yielded U contents ranging from 262 to 628 ppm. A group of 23 grains with 206Pb/238U ages (discordance ≤5 %) yielded a weighted mean 208Pb/238U age of 331±4 Ma (mean square of weighted
deviates; MSWD=1.2;
Fig. 6a), which probably represents the crystallization age of tuff.
Sample TM-1 is a fine-grained banded rhyolitic tuff consisting of quartz,
K-feldspar, and biotite phenocrysts, flattened dark-brown pumice (i.e.,
fiamme), and lithoclasts (less than 1 mm in diameter) enclosed in an ash matrix (Fig. 5b). The zircon population is characterized by stubby
euhedral- to subeuhedral-sized (30–100 µm in diameter) grains. Magmatic grains are either simple with concentric zoning or composite showing
variable luminescence cores with concentric zoning, no zoning, or banded
zoning. These cores are surrounded by overgrowths with concentric zoning and
are occasionally diffuse or unzoned. A total of 120 U-Th-Pb LA-ICP-MS
analyses yielded U contents ranging from 87 to 4136 ppm. There are 28
206Pb/238U ages (90 %–110 % of concordance) that yielded a weighted mean 208Pb/238U age of 341±10 Ma with a very poor fit (MSWD=6.9; Fig. 6b) as indicated by the scattering of ages along the Concordia curve. A coherent group of 21 grains with 206Pb/238U ages yielded
a weighted mean 208Pb/238U age of 335±6 Ma (MSWD=1.5; Fig. 6b), providing the best age estimate for the volcanic rock (Fig. 6b). The youngest zircon grain (ca. 302 Ma) probably experienced Pb loss. The six oldest zircon grains present Paleoproterozoic (ca. 2 Ga), Neoproterozoic (ca. 715 Ma), and Devonian (ca. 395–378 Ma) ages, suggesting inheritance.
Sample CBR-12 is a fine-grained rhyolitic rock in which feldspar and quartz
phenocrysts and lithic fragments occur embedded in an altered, very fine-grained
matrix of quartz, sericite, and chlorite, including devitrified shards.
Zircon (40–150 µm in diameter) appears as stubby to elongated euhedral
prisms, mostly showing oscillatory concentric zoning and sometimes being disturbed by
inclusions. A few crystals show banded
zoning or are diffuse or unzoned. A total of 32 analyses were performed on this silicic volcanic rock yielding U contents ranging from 288 to 2587 ppm. A total of 22 analyses with discordance ≤5 % yielded a weighted mean 208Pb/238Th age of 335±2 Ma (MSWD=1.2; Fig. 6c). The oldest two grains yielding 206Pb/238U ages of ca. 389 and 371 Ma are interpreted as representing xenocrysts.
Baleizão porphyry
Sample SCV-30 is a porphyritic rhyodacite–rhyolite consisting of quartz,
plagioclase, K-feldspar, biotite, and amphibole phenocryst (less than 3 mm in diameter) embedded in a fine-grained silicic matrix (Fig. 5c). The zircon population contains grains (30–140 µm in diameter) from subrounded
subhedral to prismatic euhedral. Prisms are equant to moderately elongate
showing a simple internal structure characterized by concentric and sector
zoning to unzoned. A concentric zoned or unzoned rim surrounds unzoned cores of a few composite grains. A total of 37 U-Th-Pb SHRIMP analyses for sample SCV-30 yielded U contents ranging from 74 to 4290 ppm. For zircon, 25 analyses were obtained with discordance ≤5 %, distributed along the concordia curve from ca. 355 to 288 Ma, and yielded a weighted mean
208Pb/238Th age of 315±6 Ma (MSWD=12; Fig. 7a). Some of the spread observed could be due to the presence of inheritance. The oldest 10 grains yielding
206Pb/238U ages of ca. 355–337 Ma probably represent xenocrysts derived from the Toca da Moura volcano-sedimentary complex. The 11 grains in the age range ca. 334–311 Ma yielded a weighted mean 208Pb/238U age of 318±2 Ma (MSWD=0.95; Fig. 7a), which is regarded as the best estimate for the crystallization age of subvolcanic silicic rock.
Cobble of granite found in a conglomerate from the Santa Susana
Formation
Sample SCV-7 is a cobble (20 cm in diameter) of pinkish medium-grained
granite consisting of quartz, alkali feldspar, and biotite (Fig. 5d). Most
zircons are stubby and elongated subeuhedral to euhedral prisms (80 to 150 µm in diameter). Morphologically, zircon grains are mostly simple, showing concentric zoning, sector zoning, or no zoning, and a few are composite with irregular and unzoned small cores surrounded by a rim with concentric zoning. In total, 40 U-Th-Pb SHRIMP analyses were performed on sample SCV-7 with U content ranging from 348 to 3177 ppm. Of this total number of analyses, 24 U–Pb ages with discordance ≤5 %, scattered along the concordia curve from ca. 349 to 294 Ma, yielded a weighted mean 206Pb/238U age of 327±7 Ma (MSWD=4; Fig. 7b). A group of six zircon grains in the age range of ca. 309–294 Ma yielded a weighted mean 206Pb/238U age of 303±6 Ma (MSWD=0.98; Fig. 7b), which is taken as the probable crystallization age of the granite. The remaining 19 zircon grains yielded 206Pb/238U ages of ca. 349–326 Ma, suggesting inheritance.
Siliciclastic rocks from the Toca da Moura and Cabrela
volcano-sedimentary complexes
Sample TM-3 is a laminated, poorly sorted siltstone with quartz-rich silt
layers containing feldspar and tourmaline grains and lithoclasts (Fig. 5e), which are intercalated with darker layers of clay. The zircon
population is mostly characterized by stubby to elongated prismatic small
grains (less than 100 µm in diameter). It includes simple and composite zircons showing concentric, sector, and banded zoning. Of a total of 82 U-Th-Pb LA-ICP-MS analyses with U contents ranging from 19 to 4630 ppm, 36 zircon grains yield 90 %–110 % concordance. The number of grains of sample TM-1 does not conform to the minimum of 60–100 grains often used in provenance studies (Vermeesch, 2004), and therefore percentages based on the proportions of ages need to be interpreted with caution. The Paleozoic population of detrital zircon (36 %) includes early Carboniferous (9 %; ca. 353, 349, and 340 Ma), Ordovician (14 %; ca. 476–456 Ma), Cambrian (7 %; ca. 531–500 Ma), and late Devonian (6 %; ca. 369 and 362 Ma) grains (Fig. 8a). The Precambrian population (64 %) is predominantly Neoproterozoic (36 %; ca. 983–587 Ma) but also includes Paleoproterozoic
(14 %; ca. 2–1.8 Ga), Mesoproterozoic (8 %; ca. 1.3–1 Ga), and Archean (6 %; ca. 2.7–2.5 Ga) grains. The three youngest zircon grains (ca. 353–340 Ma) yielded a maximum depositional age of ca. 348 Ma (Tournaisian), which is in accordance with the sedimentary age inferred from biostratigraphic constraints (late Tournaisian to middle to late Visean; Pereira et al., 2006; Lopes et al., 2014).
Sample CBR-11 is a fine-grained poorly to moderately sorted siltstone
consisting predominantly of quartz and a few feldspar grains and lithoclasts
enclosed in silt–clay-sized particles (Fig. 5g). Most zircon grains are
small (less than 100 µm in diameter) and euhedral to subeuhedral. They are
simple grains (short, stubby to equant prisms) with oscillatory concentric
and banded zoning, and only a few are composite grains with rounded cores. Of
a total of 20 U-Th-Pb LA-ICP-MS analyses with U contents ranging from 54 to
1379 ppm, 10 grains yielded 90 %–110 % of concordance. Five grains are Paleozoic (Carboniferous: ca. 359, 351, and 346 Ma; Cambrian: ca. 514 and 511 Ma) and five are Precambrian (Paleoproterozoic: ca. 2.4, 2.1, and 1.8 Ga;
Mesoproterozoic: 1 Ga; Neoproterozoic: ca. 603 Ma). By combining our new data
with those from sample OM-200 (Pereira et al., 2012a) collected from the
same quarry as sample CBR-11, it was found that the detrital zircon
population (CB, N=54; Fig. 8a) is largely dominated by Paleozoic grains
(90 %): late to middle Devonian (68 %), early Carboniferous (15 %), Cambrian (4 %), and early Devonian (2 %) grains, being distinct from sample TM-3 described above (Fig. 8a). The number of grains of sample CB (N=54), despite being larger than that of sample TM-1, does not conform to the minimum of 60–100 grains, and therefore the proportions of ages obtained also need to be interpreted with caution. The youngest zircon population (N=5), ranging from ca. 353 to 346 Ma, suggests a Tournaisian maximum depositional age which is slightly older than the sedimentary age inferred from biostratigraphic constraints (late Tournaisian to middle to late Visean; Pereira et al., 2006).
Siliciclastic rocks from the Santa Susana Formation
Sample SS-2 represents medium- to coarse-grained, poorly sorted sandstone. It
is mainly composed of lithoclasts (siltstone, mudstone, quartzite, phyllite,
rhyolite, basalt) and quartz grains but also includes muscovite and
feldspar grains (Fig. 5g). The zircon population is mostly characterized by
stubby to prismatic and subrounded to subangular grains (120–300 µm in diameter). Morphologically simple and composite grains were found. Cathodoluminescence imaging shows that most zircon grains have concentric
oscillatory zoning or irregular zoning, or they are banded or unzoned. In total,
153 U-Th-Pb LA-ICP-MS analyses were performed on detrital zircon grains.
They show U contents ranging from 15 to 6158 ppm. A population with 51 grains yielding U–Pb ages with 90 %–110 % concordance (Fig. 8b) is dominated by Precambrian ages (64 %): Neoproterozoic (37 %; ca. 801–551 Ma),
Paleoproterozoic (25 %; ca. 2.4–1.6 Ga), and Neoarchean (2 %; ca. 2.5 Ga). The Paleozoic grains (36 %) are Carboniferous (20 %; ca. 359–303 Ma), late Devonian (14 %; ca. 378–362 Ma), and early Ordovician (2 %; ca. 447 Ma). The youngest two grains (303±4 Ma; Kasimovian–Gzhelian) are
slightly younger than the sedimentary age inferred from biostratigraphic
constraints (middle Moscovian to Kasimovian; Lemos de Sousa and Wagner,
1983; Machado et al., 2012; Lopes et al., 2014).
Sample SS-1 represents a very coarse-grained sandstone consisting of
rounded to subangular mono- and polycrystalline quartz, feldspar, and
muscovite grains and a wide variety of lithoclasts (chert, phyllite,
rhyolite, siltstone, and sandstone; Fig. 5h). Zircon grains are rounded to
subangular, stubby, and elongated prisms (less than 280 µm in diameter).
The zircon population includes simple grains with oscillatory concentric,
banded, and sector zoning and composite grains with cores with distinct
internal morphologies surrounded by variable width rims. A total of 150
U-Th-Pb LA-ICP-MS analyses performed on detrital zircon grains yielded U
contents ranging from 24 to 9819 ppm. A group of 71 grains yielding U–Pb ages
with 90 %–110 % concordance are dominated by Paleozoic ages (82 %), predominantly made up of Carboniferous (49 %; ca. 358–315 Ma) and Devonian (25 %; ca. 389–359 Ma) grains and a few late Ordovician–Silurian (5 %; ca. 434, 429, and 425 Ma) and Cambrian (3 %; ca. 533 and 491 Ma) grains (Fig. 8b). The Precambrian grains (18 %) are Neoproterozoic (10 %; ca. 702–542 Ma), Paleoproterozoic (4 %; ca. 2.1–1.6 Ga), Mesoproterozoic (3 %; ca. 1.4 and
1.6 Ga), and Neoarchean (1 %; ca. 2.8 Ga). The youngest zircon population (N=3; ca. 319–315 Ma) suggests a Bashkirian maximum depositional age, which is slightly older than the sedimentary age inferred from biostratigraphic constraints (middle Moscovian to Kasimovian; Lemos de Sousa and Wagner, 1983; Machado et al., 2012; Lopes et al., 2014).
K–S test and MDS analysis: results
We recognize that the representativeness of the detrital zircon grains of
samples TM-1 and CB is not the most recommended for provenance analyses.
However, we consider it important to present a preliminary comparison of
detrital zircon populations of Visean marine siliciclastic rocks from the
Toca da Moura and Cabrela volcano-sedimentary complexes because it seems to indicate variability in the sources. A table showing the K–S results
(referred to as Fig. S1 throughout the text) can be found in the
Supplement.
The K–S test performed on the Santa Susana sandstones shows that the detrital
zircon populations of sample SS-2 (lower member) and the SS upper member (i.e., it includes samples StSz2 and StSz4 from Dinis et al., 2018) are not
significantly different (all ages: P value =0.169; pre-Carboniferous
ages: P value =0.879) at the 5 % confidence level (Fig. S1). A
comparison of samples SS-1 and SS-2 reveals that they are significantly
different (P value ≤0.01). Unlike sample SS-2, the sample SS-1
detrital zircon population is significantly different (P value <0.01) from the SS upper population (Fig. S1), indicating that they are derived
from distinct sources. Besides this, sample SS-1 is much closer to that of
SS upper (D value =0.323) and more distant from sample SS-2 (D value =0.465) with regards to the distance between cumulative probability curves (Fig. 8c).
In Fig. 9a, the MDS diagram produced with all ages shows sample SS-1 adjacent to Cabrela and Mértola siliciclastic rocks, while sample SS-2 is near the Mira, Santa Iria, and Represa detrital zircon populations. In the MDS diagram for pre-Carboniferous ages, sample SS-2 is juxtaposed with sample TM-3 and closest to the Mira, Phyllite–Quartzite, and Tercenas formations (Fig. 9b), suggesting likely sources. Nevertheless, the probable contribution to SS-2 samples of sediment derived from the oldest siliciclastic rocks from the PLZ, SPZ (i.e., Pulo do Lobo, Gafo, Ribeira de Limas, Atalaia, and Ronquillo formations; P–G–R–A–R), and OMZ sources cannot be excluded. Their detrital zircon populations are not significantly different enough (all ages: P value =0.003) and not significantly different
(pre-Carboniferous ages: P value = 0.113–0.165) at the 5 % confidence level (Fig. S1). This similarity is also illustrated in the approximation between the SS-2, P–G–R–A–R, and OMZ populations in the MDS diagrams (Fig. 9).
Multidimensional scaling diagrams (Vermeesch, 2018) applied to
the U–Pb ages (90 %–110 % concordance) of detrital zircon grains from the Toca da Moura (TM-3) and Cabrela (CB) volcano-sedimentary complexes and the Santa Susana Formation (SS1, SS2, SS upper member) and different potential sources: OMZ (Linnemann et al., 2008; Pereira et al., 2008, 2012c), PLZ (Pereira et al., 2017a; Pérez Cácerez et al., 2017), and SPZ (Braid et al., 2011; Pereira et al., 2012a, 2014a; Rodrigues et al., 2014). Abbreviations: MT – Mértola Formation; MR – Mira Formation; BJ – Brejeira Formation; PQ-TRC – Phyllite–Quartzite and Tercenas formations; SI-REP – Santa Iria and Represa formations; P-G-R-A-R – Pulo do Lobo, Gafo, Ribeira de Lima, Atalaia and Ronquillo formations; HT – Horta da Torre Formation.
K–S test results for the comparison between samples SS-2 and TM-3 indicate
that they present not significantly different detrital zircon populations
(all ages: P value =0.399; pre-Carboniferous ages: P value =0.0.411) at the 5 % confidence level (Fig. S1). Furthermore, their cumulative probability curves are much closer (Fig. 8d): D values are 0.195 (all ages) and 0.203 (pre-Carboniferous ages) (Fig. S1). The close relationship of the two detrital zircon populations suggests that the Toca da Moura volcano-sedimentary complex directly supplied sediment to the Santa Susana Basin. However, the relationship described above does not extend to the entire Santa Susana Basin since sample SS-1 presents a greater degree of
similarity with the Cabrela detrital zircon population as regards the
proximity between cumulative probability curves (Fig. 8d) and MDS diagrams
(Figs. 9a, b).
In addition, Cabrela siliciclastic rocks are significantly different at
the 5 % confidence level from sample TM-3 (P values <0.01) as
regards the significant distance between them on the MDS diagram (Fig. 9a, b) and the significant distance between cumulative curves (Fig. 8d) with a D-value range of 0.712–0.731 (Fig. S1). The difference found in the detrital zircon populations suggests that Cabrela and Toca da Moura siliciclastic rocks probably derived from different sources.
As a result of the K–S test and MDS analyses, the Horta da Torre Formation is
significantly different (Fig. S1) and is clearly separate (Fig. 9a, b)
from all the other detrital zircon populations, ruling out the possibility
of it being a source for the Toca da Moura and Cabrela volcano-sedimentary
complexes or Santa Susana Formation siliciclastic rocks.
DiscussionChronostratigraphic framework
The geochronological data presented in the present study provide the basis
for the first chronostratigraphic record for the Carboniferous basins of the
Santa Susana–São Cristovão region (SW Iberia). Dating of silicic
volcanic rocks interbedded in the Toca da Moura and Cabrela
volcano-sedimentary complexes constrain the interval of felsic magmatism to having
occurred from ca. 335 to 331 Ma (Visean; Fig. 6), complementing
currently available biostratigraphic information for Toca da Moura and
Cabrela siliciclastic rocks (Pereira et al., 2006; Lopes et al., 2014). U–Pb
ages of the youngest detrital zircon grains from the siliciclastic rocks of
the Toca da Moura and Cabrela volcano-sedimentary complexes (TM-3 and CB,
respectively; Fig. 8a) provide maximum age constraints for these marine
deposits. Their maximum depositional ages (ca. 351–348 Ma; Tournaisian) are
slightly older than currently available biostratigraphic ages (Pereira et
al., 2006; Lopes et al., 2014) but provide confirmation that both marine
deposits are broadly contemporaneous.
Furthermore, the best estimate of the crystallization age of the
Baleizão silicic intrusion provides a minimum age of 318±2 Ma
(Bashkirian; Fig. 7a) for the intra-Carboniferous unconformity. Zircon
extracted from a pebble of granite found in a Santa Susana conglomerate
yielded a crystallization age of ca. 303 Ma for plutonic rock (Fig. 7b). This age estimate overlaps with the age range of ca. 305–303 Ma (i.e., the maximum depositional age range) obtained for the youngest population of detrital zircon grains from sandstone of the upper member (Dinis et al., 2018), complementing the currently available biostratigraphic information for the Santa Susana Formation (Machado et al., 2012; Lopes et al., 2014). Given the findings described above, a stratigraphic interval of approximately 13–17 Myr can be established for the intra-Carboniferous unconformity, marking a change in depositional environment from marine to terrestrial in the OMZ. Basin-drainage and infill patterns most probably changed due to the rapid uplift of the Variscan–Appalachian orogenic belt, active during the waning stages of the Laurussia–Gondwana collision (i.e., late Carboniferous).
Provenance and evolutionary model
An initial important finding provides evidence that they are derived from
different sources. The TM-3 population presents 64 % Precambrian detrital
zircon grains, while the CB population contains only 10 % (Fig. 8a). Toca
da Moura siliciclastic rocks have a greater affinity with the
Phyllite–Quartzite, Tercenas, Santa Iria, and Represa formations (Fig. 9),
indicating that detrital zircon populations were reproduced faithfully in
SPZ and PLZ (Laurussian-type) sources. A contribution from the oldest
siliciclastic sequences of PLZ (Pulo do Lobo, Atalaia, Gafo, and Ribeira de
Limas formations) and OMZ (Gondwanan-type) sources cannot be ruled out for
sample TM-3 (Fig. 9). The number of late to middle Devonian zircon grains in
sample TM-3 (6 %) is smaller than that of the CB population (68 %) (Fig. 8a), suggesting that Cabrela siliciclastic rocks were most likely derived largely from a Devonian source consistent with a limited contribution from recycled ancient rocks (Pereira et al., 2012a). This indicates that the
origin of the Visean Toca da Moura and Cabrela basins is most likely more
closely linked to sources located in the SPZ and PLZ (Laurussian type) than
in the OMZ (Gondwanan type). The evidence in the Visean Toca da Moura basin
for the dissection of the inactive Devonian magmatic arc and the erosion of its
plutonic roots, together with the recycling of the PLZ and SPZ
Frasnian–Tournaisian siliciclastic sequences and OMZ basement rocks, differs
from the evidence in the Cabrela basin. The significance of the involvement
of distinct sources is that part of the region located on the boundary
between the OMZ, PLZ, and SPZ (SW Iberia) was subjected to uplift while
the remaining part underwent flexural subsidence. A similar tectonic setting
has been put forward as an explanation for differences in stratigraphy found
in the Pedroches synorogenic basin located along the OMZ–Central Iberian
Zone boundary (Armendáriz et al., 2008, and references therein) (Fig. 1).
Over the past 4 decades, different models have emerged to explain the
geodynamic evolution of SW Iberia with the subduction polarity being widely
discussed (Quesada et al., 1994; Castro et al., 1996; Ribeiro et al., 2007;
Pin et al., 2008; Simancas et al., 2009; Braid et al., 2011;
Pérez-Cáceres et al., 2015; Díez Fernández et al., 2016;
Pereira et al., 2017a). Although in many paleogeographic reconstructions of
the Devonian Iberia is flanked by the Rheic and Paleo-Tethys oceans
(Stampfli et al., 2002, 2013; Cocks and Torsvik, 2006; Stampfli and Kozur,
2006; Torsvik et al., 2012; Arenas et al., 2014; von Raumer et al., 2016),
solely the subduction of the Rheic Ocean is considered in the present geodynamic
models for Iberia. This geodynamic model of a single ocean has been the
trigger of numerous discussions about whether the active magmatic arc was
located in Laurussia or Gondwana margins. Our challenging recent proposal
considers that SW Iberia's geodynamic evolution could have been linked to the
closure of these two oceanic basins (Pereira et al., 2020). The main
assumption is that SPZ and PLZ (Laurussian side) and OMZ
(Gondwana side) have experienced different and independent geodynamic
evolutions before they were juxtaposed with the Variscan sinistral
orogen-parallel motion (Pérez-Cáceres et al., 2016). As illustrated
in Fig. 10a, the subduction of the Rheic Ocean floor beneath the Laurussian margin during the late Devonian (Pérez-Cáceres et al., 2015; Pereira et al., 2017a, and references therein) caused the onset of the Rheic magmatic arc in the Meguma terrane and related synorogenic basins. A slab rollback mechanism similar to the one that caused the opening of the Okinawa Trough behind the Ryukyu-type subduction in the Pacific Ocean (Yamaji, 2003; Boutelier and Cruden, 2013) could explain the lithosphere
extension on the Laurussian side and the late Devonian siliciclastic
sedimentation in SPZ and PLZ (Pereira et al., 2017a). The Laurussian active
margin was progressively accreted to the Gondwana passive margin facing the
Rheic Ocean during the late Devonian (Fig. 10a). A nappe stack was gradually
emplaced in the Gondwana margin as a consequence of ongoing continental
collision (Pérez-Cáceres et al., 2015; Díez Fernández and
Arenas, 2015, and references therein; Díez Fernández et al., 2016)
and orogenic gravitational collapse (Dias da Silva et al., 2020). Following
the closure of the Rheic, Tournaisian magmatic episodes were associated
with lithospheric extension in the Laurussian (Pyrite Belt volcano-sedimentary complex and Gil Márquez pluton) and Gondwanan (Beja
Igneous Complex) margins. A mechanism of steepening and break-off of the
Rheic Ocean slab beneath the Laurussian margin, as in the modern analog of
Eastern Anatolian Alpine–Himalayan collisional mountain belt (Sengör et al., 2003; Keskin, 2007), was possibly the main reason for the early
Carboniferous magma generation in the SPZ (Pin et al., 2008); simultaneously
the Meguma terrane experienced rapid uplift and terrestrial sedimentation
(Fig. 10b1). At the same time, on the Gondwanan side, the upwelling of the asthenosphere could have triggered the partial melting of crustal materials and lithosphere extension (Pereira et al., 2009, 2012b), creating the right conditions for the onset of gneiss domes in the OMZ (Dias da Silva et al., 2018). The emplacement of voluminous subduction-related magmas (Santos et al., 1990; Castro et al., 1996; Jesus et al., 2007; Pin et al., 2008; Lima et al., 2012; Pereira et al., 2007, 2015a; Moita et al., 2009, 2015), including some with boninitic (Castro et al., 1999) and adakitic (Lima et al., 2013) affinities, was coeval with flexural subsidence, marine
sedimentation, and volcanism (Toca da Moura, Cabrela, and Los Pedroches basins)
(Fig. 10b2). The early Carboniferous thermal anomaly recorded in the OMZ has
been interpreted as resulting from the emplacement in the middle crust of a
large volume of mantle plume-related magmas (Simancas et al., 2006). Other
studies have suggested that voluminous early Carboniferous magmatism could
have resulted from the subduction of an oceanic ridge, creating a slab
window beneath the OMZ (Castro et al., 1996, 1999; Díaz-Azpiroz et al., 2006). This model uses the Chile ridge that plunges beneath the South American Plate in Patagonia (Breitsprecher and Thorkelson, 2009) as a modern analog.
Our model assumes the subduction of a ridge of the Paleo-Tethys Ocean's
lithosphere beneath the Gondwana margin (Fig. 10b2) instead of the Rheic
Ocean's lithosphere as a hypothesis to be further explored since the magmatic
activity has extended to the Serpukhovian and Bashkirian in the OMZ (Pavia
pluton, Valencia del Ventoso plutonic complex, and Baleizão porphyry).
Simultaneous with the putative subduction of the Paleo-Tethys Ocean ridge,
other regions of the Variscan–Appalachian orogenic belt, mostly on the
Laurussian side (Fig. 10b1), have experienced an oblique collision, rapid
uplift, and terrestrial sedimentation (Pereira et al., 2020).
Sketches showing inferred tectonic evolution and sedimentation
recorded in SW Iberian Carboniferous stratigraphy during the Laurussian–Gondwana
oblique collision (modified from Pereira et al., 2012b, 2020): (a) late Devonian, (b1, b2) early Carboniferous, and (c1, c2) late Carboniferous.
A second significant finding is that detrital zircon populations from the
Santa Susana Formation (samples SS-1 and SS-2) also show significant
differences (Figs. 8 and 9). Basal conglomerate (sample SS-2) presents a
greater percentage of Precambrian grains (64 %) than uppermost sandstone
(SS-1 sample; 28 %) and presents a great degree of affinity with the
detrital zircon population of sample TM-3. Sample SS-2 presents a great
degree of similarity with the detrital zircon populations of overlying SS
upper-member sandstones (samples StSz-2 and StSz-4; Dinis et al., 2018)
sampled as part of the same stratigraphic profile. SS-2 and SS upper age
populations show a great degree of affinity (Fig. 9), suggesting that
detrital zircon grains were mainly derived from the erosion of the Toca da
Moura volcano-sedimentary complex, the Santa Iria and Represa formations
(PLZ), and the Mira Formation (SPZ). However, regarding the detrital zircon
grains with pre-Carboniferous ages, additional contributions from other PLZ
(Pulo do Lobo, Atalaia, Gafo, and Ribeira de Limas formations), SPZ
(Brejeira, Phyllite–Quartzite, Tercenas, and Ronquillo formations), and OMZ
sources cannot be ruled out (Fig. 9). The zircon age population of sample SS-1, which is distinct from the SS-2 population, presents a great
degree of affinity with the CB population, suggesting lateral changes in
sources during the deposition of Santa Susana's uppermost sandstones. The great
degree of affinity of the SS-1 with both the Cabrela volcano-sedimentary complex and Mértola Formation detrital zircon populations suggests a close
association between the two and a common source. Cabrela and Mértola
siliciclastic rocks may be regarded as the main source for sample SS-1 and
an intermediate sediment repository as they are derived from the erosion of
a Devonian source partially represented by the Cercal porphyries from the
SPZ. As a result of rapid uplift, the progressive erosion of the Devonian
magmatic arc (including its plutonic roots), and of PLZ, SPZ, and OMZ
rocks, is evidenced in the Santa Susana Formation. The volumetrically
significant contribution of Carboniferous sources to the Santa Susana Basin
fill confirms derivation from the erosion of the following: (i) Pyrite Belt volcanic rocks and
Phyllite–Quartzite, Tercenas, Mértola, Mira, and Brejeira
siliciclastic rocks (SPZ); (ii) the Santa Iria and Represas formations (PLZ);
(iii) Gil Marquez granitic rocks and other plutons of the Sierra del Norte
Batholith (SPZ and PLZ); (iv) the Beja Igneous Complex, which includes the
Baleizão porphyries (OMZ) and Évora and Pavia plutonic and
high-grade metamorphic rocks (OMZ); and (v) the Cabrela and Toca da Moura
volcano-sedimentary complexes (OMZ) and Mértola turbidites (SPZ). From the
late Carboniferous to early Permian, large-scale strike-slip motions have
juxtaposed OMZ with PLZ and SPZ (García-Navarro and Fernández, 2004;
Pérez-Cáceres et al., 2016) and simultaneously with the rapid uplift
of the Variscan orogenic belt (Fig. 10c). In Kasimovian–Gzhelian, sedimentation
probably occurred through the opening of the pull-apart terrestrial basin
(Santa Susana Basin) related to the movement of major strike-slip faults
(i.e., Porto–Tomar fault zone; Pereira et al., 2010; Machado et al., 2012;
Gutiérrez-Alonso et al., 2015) during the progressive uplift and
buckling of the linear Variscan–Appalachian orogenic belt (i.e., OMZ, PLZ, and
SPZ; Fig. 10c), related to a change in the regional stress field that
produced the Greater Cantabrian Orocline (Pastor-Galán et al., 2015). U–Pb
dating of magmatic zircon extracted from a pebble of granite (ca. 303 Ma;
Fig. 7b) found in a conglomerate of the Santa Susana Formation lower member
suggests provenance from the direct erosion of Permo-Carboniferous plutons
(i.e., original primary source), such as Santa Eulália-Monforte granitic
and gabbro-dioritic rocks (OMZ). This ca. 303–297 Ma calc-alkaline plutonic
suite is coeval with the Nisa-Albuquerque and Los Pedroches batholiths,
located on the OMZ–Central Iberian Zone boundary (Fig. 1), probably
representing magmatism related to the eastward migration of the Paleo-Tethyan
arc (Permo-Carboniferous Pyrenees plutonic and volcanic rocks; Pereira et
al., 2014, 2015b, 2017b). The Permo-Carboniferous OMZ
plutons were emplaced at shallow crustal levels consistent with the low
assimilation of country rocks and the sharp contacts, and, therefore, they
may have experienced denudation shortly after crystallization without
unrealistic uplift rates being required.
Conclusions
The main conclusions of this study are the following.
Visean marine deposition in the Santa Susana–São Cristovão and Cabrela regions is constrained to the age range of ca. 335–331 Ma by the new U–Pb data for volcanic rocks intercalated within siliciclastic rocks of the Toca da Moura and Cabrela volcano-sedimentary complexes.
U–Pb dating of the Baleizão porphyry provides a minimum age of 318±2 Ma (Bashkirian) for the overlying intra-Carboniferous unconformity.
Visean siliciclastic rocks from the Cabrela and Toca de Moura volcano-sedimentary complexes are derived from distinct sources, which probably include a Devonian continental magmatic arc, and are likely to be more closely associated with the Laurussian-type sources (SPZ and PLZ) than the Gondwanan-type sources (OMZ).
Terrestrial siliciclastic rocks from the Santa Susana Formation are probably the result of the recycling of distinct sources associated with the SPZ, PLZ, and OMZ.
The best estimate of crystallization of a granite pebble found in Santa Susana Formation conglomerate suggests a maximum depositional age of ca. 303 Ma (Kasimovian–Gzhelian); together with the youngest U–Pb ages (< ca. 318 Ma) of detrital zircon grains, these findings provide evidence of the denudation of primary crystalline sources during the rapid post-accretion and collision uplift of the Variscan orogenic belt in SW Iberia (i.e., Gondwanan- and Laurussian-type sources).
The intra-Carboniferous unconformity that separates the Toca da Moura volcano complex and the Baleizão porphyry from the Santa Susana Formation indicates a notable time interval of approximately 13–17 Myr.
Data availability
The only data related to this publication regard the U–Pb results that are listed in Tables S1 and S2 of the Supplement.
The supplement related to this article is available online at: https://doi.org/10.5194/se-11-1291-2020-supplement.
Author contributions
MFP designed the study and, together with CG, ÍDdS, and JBS, performed the geological mapping, sampling, and petrography. The geochronological study was conducted by CG, ÍDdS, MH, and AG and was supervised by MFP and UL. MFP, CG, íDdS, and JBS wrote the paper. Funding acquisition was achieved by MFP, CG, and ÍDdS. All authors have read and agreed to the published version of the paper.
Competing interests
The authors declare that they have no conflict of interest.
Special issue statement
This article is part of the special issue “The Iberian Massif in the frame of the European Variscan Belt”. It is not associated with a conference.
Acknowledgements
This work is a contribution to projects CGL2016-76438-P and PGC2018-096534-B-I00 (Spain). Ícaro Dias da Silva acknowledges the financial support of SYNTHESIS3-ACCESS (DE-TAF-5798), Fundação para a Ciência e a Tecnologia postdoctoral grant SFRH/BPD/99550/2014. This is IBERSIMS publication number 71.
Financial support
This research has been supported by the Fundação para a Ciência e a Tecnologia (grant no. ICT-UID/GEO/04683/2019), the Fundação para a Ciência e a Tecnologia (grant no. UID/GEO/50019/2019-IDL), and the Fundação para a Ciência e a Tecnologia (grant no. SFRH/BPD/99550/2014).
Review statement
This paper was edited by Emilio Clavijo and reviewed by Daniel Pastor-Galán and Antonio Castro.
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