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Rem: Rev. Esc. Minas vol.61 no.3 Ouro Preto July/Sept. 2008
Sedimentological characterization of the quaternary deposits in the region between Marília and Presidente Prudente, São Paulo State, Brazil
Caracterização sedimentológica dos depósitos quaternários da região entre Marília e Presidente Prudente, Estado de São Paulo, Brasil
Alethéa Ernandes Martins SallunI; Kenitiro SuguioII
IDoutora, Pesquisadora Científica do Instituto Geológico (IG/SMA-SP). E-mail: firstname.lastname@example.org
IIProf. Emérito, Instituto de Geociências (IGc-USP), Prof. Titular, Universidade Guarulhos (UnG-CEPPE). E-mail: email@example.com
Sedimentologic characterization and provenance studies of quaternary colluvial deposits (9±1 to 980±100 ky B.P. - dated by luminescence) were based on textural and mineralogical analyses. These deposits occur extensively between Marília and Presidente Prudente (São Paulo State, Brazil), superimposed on the Bauru Group sedimentary rocks or the Serra Geral Formation basaltic rocks, both of Cretaceous age. They are distributed irregularly throughout the study area and are studied by sedimentologic and morphologic methods. These deposits are composed of very fine to coarse-grained unconsolidated sands, mostly constituted by quartzose monocrystalline grains reddened by iron oxide and hydroxide impregnation. Analyses of grain sizes indicated that total granulometric distributions are richer in the clay fraction than in the sedimentary rocks located. Non-micaceous transparent heavy minerals studied microscopically in fine-grained as well as in very fine-grained sands showed that zircon, tourmaline, staurolite and rutile are present in all the samples. Differences in grain sizes among the colluvial deposits and the Bauru Group sedimentary rocks are attributable to pedogenetic processes.
Keywords: Quaternary, colluvio-eluvial, sedimentological characterization, heavy minerals, São Paulo.
Para caracterização sedimentológica e estudos de proveniência de depósitos coluviais de idade quaternária (9±1 a 980±100 ka A.P. - datados por luminescência), foram realizadas análises textural e mineralógica. Tais depósitos ocorrem extensivamente entre Marília e Presidente Prudente (SP), superpostos às rochas sedimentares do Grupo Bauru ou rochas basálticas do Grupo Serra Geral (Formação Serra Geral), ambas de idade cretácica. São distribuídos irregularmente na região e foram estudados por métodos sedimentológicos e morfológicos. Os depósitos coluviais são compostos de areias muito finas a grossas e inconsolidadas, em sua maioria formada por grãos monocristalinos de quartzo, de coloração avermelhada por impregnação de óxidos e hidróxidos de ferro. As análises granulométricas mostraram que os depósitos coluviais apresentam contribuição maior de areia argilosa do que as rochas sedimentares sotopostas. O estudo microscópico de minerais pesados transparentes não-micáceos mostrou que, tanto nas areias finas, quanto nas muito finas, zircão, turmalina, estaurolita e rutilo estão presentes em todas as amostras analisadas. As diferenças granulométricas constatadas entre os depósitos coluviais e as rochas sedimentares do Grupo Bauru são perfeitamente explicáveis por processos pedogenéticos.
Palavras-chave: Quaternário, colúvio, caracterização sedimentológica, minerais pesados, São Paulo.
Quaternary deposits related to distinct geologic contexts can be found at several locations in the State of São Paulo, Brazil. Due to their lack of structure and similarity with material resulting from the weathering of regional rock, colluvial deposits are sometimes confused with eluvial deposits. In the studied area between Marília and Presidente Prudente (western portion of the State of São Paulo) there are Quaternary deposits superimposed on Cretaceous sandstones of the Marília and Adamantina formations (Bauru Group) and on Cretaceous basalts of the Serra Geral Formation (São Bento Group), both belonging to the Paraná Sedimentary Basin (Dias Brito et alli, 2001, Renne et alli, 1992, Figure 1).
The Quaternary deposits were subdivided into colluvial and alluvial deposits, according to compositional similarities and provenance interpretations compared to present morphologic features of the study area. Luminescence dating proved the deposits to be from the Pleistocene ages for the colluvial (9±1 to 980±100 ka B.P.) and the alluvial (14±2 to 240±30 ka B.P.) deposits (Tatumi et alli, 2006).
The colluvial deposits occur in patches on the Western Plateau of the State. They consist of structureless sands and rudites less than 10 m thick (Figure 2). When the contact with the underlying sandstones or basalts is exposed, it is unconformable. The presence of ferricretes and/or stonelines at the base of the colluvial deposits suggests the existence of a depositional hiatus. The basal ferricretes constitute locally interrupted, wavy beds, 2 to 40cm thick, that contain fragmented ferricretes, rounded centimetric quartz or quartzite pebbles. These horizons always occur at the contacts between colluvial deposits and the Adamantina Formation, or as reworked and scattered fragments within colluvial deposits superimposed on the Serra Geral, Adamantina or Marília formations (Figure 3). The undulating beds or pseudofolding could represent a simple adaptation to a paleotopographic surface, but it is possible that the ferricrete bed faulting could be atectonic or even related to eventual neotectonic activities (Sallun, 2006).
The outcrop units are studied in detail from a sedimentologic viewpoint to determine their characteristics and provenance. The data obtained contributed to a better understanding of the region, the Quaternary geologic evolution of which remains largely unknown (Sallun, 2006).
2. Materials and methods
The field work consisted of sampling and visual description of geologic outcrops, distributed all over the studied area for sedimentologic analysis (Figure 1).
To determine the textural and mineralogical characteristics, 112 samples of colluvial deposits and 31 samples of sandstones of the Adamantina and Marília formations were collected. Where the colluvial deposits occurred above these sandstones, they were sampled for comparative textural and mineralogical studies. To characterize the textures, conventional grain-size analysis was performed. The fine (0.250 - 0.125 mm) and very fine (0.125 - 0.062 mm) sand fractions from 22 samples were separated into light and heavy minerals (Rittenhouse, 1943) according to differences in their density (Parfenoff, et alli 1970; Carver, 1971) using bromoform (CHBr3). After separation, the light minerals were treated with 5% oxalic acid on hot aluminium plate for the lixiviation of ferruginous films found on the sand grains.
The light minerals were mounted on thin glass board. One hundred quartz grains were counted for morphologic and typological purposes. To determine quartz/feldspar ratios semiquantitatively, X-ray diffraction analysis was performed after the rest of grains had been powdered in an agate mortar.
The heavy minerals were weighed to obtain the amount within the total sample. The heavy opaque minerals were separated using a hand magnet, according to Friedman (1958), 100 non-micaceous transparent heavy minerals were identified and counted on the thin glass board. Remnant opaque minerals and clay-limonite nodules were excluded from counting on the thin glass boards.
To better interpret the meanings of non-micaceous transparent heavy minerals, the found frequencies of the assemblages were classified according to Coutinho and Coimbra's (1974) method, and ZTR index values were determined. These reflected the mineralogical maturity and corresponded to the content summation of the occurrences of zircon, tourmaline and rutile among these minerals.
In this study, similarities between the Quaternary and Cretaceous units were studied by comparing the grain-size data. Established statistical treatments for determinate types of environments were used, without any intention of defining or considering depositional environments for units, because the sediments can preserve the inherent characteristics of other depositional cycles.
For grain-size distribution data, the Folk and Ward (1957) graphic method was used to characterize the colluvial deposits and to enable comparison with the underlying Cretaceous sandstones of the Marilia and Adamantina formations that constitute the substrate. The statistical parameters were calculated for total and sandy distributions, because pelitic fractions can be subjected to illuviation during pedogenesis, which changes the original grain-size frequency.
After obtaining the Folk and Ward (1957) parameters, calculated for the sandy fractions of the samples, statistical analysis was used, as proposed by Friedman (1961, 1967) and Friedman and Johnson (1982).
For a more complete characterization of the ferruginous concretions, the following steps have been performed: chemical analysis (McFarlane, 1983) by X-ray fluorescence; petrographic study on a thin section; and surface textural analysis by scanning electron microscope (SEM). Chemical analyses of major, minor and trace elements have been performed on powdered representative samples.
In order to compare the differences and similarities of the colluvial deposits and their underlying substrate, petrological and petrographic data were obtained from both colluvial cover and the Adamantina and Marília formations. Only a few outcrops of colluvial deposits superimposed on the Serra Geral Formation were studied so there is no statistical data; however, these deposits were subjected to mineralogical analysis and provenance studies.
3.1 Grain size characteristics
The analysis of the distribution of the grain-size fractions in the colluvial deposits shows: clays and silts are abundant in the NW and SE portions of the studied area, very fine-grained sand in the NW, fine sand in the centre and medium-grained sand in the SE. The thickest colluvial deposits are associated with sediments with abundant fine-grained sand and scarce clays and silts. These differences can be observed also in the distribution of units in the Bauru Group, and might indicate transport of colluvial sediments from E to W.
The studied units constitute 13 grain-size classes and the total cumulative curves for grain-size distribution demonstrate that, in general, these deposits are homogenous (Figure 4), consisting chiefly of sand, clayey sand and silty sand. Grain-size data for the majority of the samples are summarized in Table 1.
Most of the analyzed samples presented a fine grain size, from fine sand to coarse silt, with the finer portion being the worst sorted (Figure 5). The grain-size distributions were, in general, moderately sorted, which represents peculiarities inherited from most of the Bauru Group samples studied in the area.
Comparison of the units shows that the colluvial deposits present grain-size characteristics that are similar to their closely underlying rocks. The obtained values indicate fluvial and beach environments, but the Marília Formation samples and the colluvial deposits superimposed on the Marília Formation always indicate a fluvial environment (Figures 6A, B, E, F, G and J). The larger are the medium diameters, the smaller are the degrees of skewness and the standard deviations (Figures 6A, C, F and H). The Adamantina Formation and the colluvial deposits superimposed on the Adamantina Formation exhibit higher sorting degrees than the Marília Formation and the colluvial deposits superimposed on the Marília Formation (Table 2).
For all units, the kurtosis values (Figures 6D and I) are concentrated around 0.8 to 1 (platikurtic to mesokurtic), while the medium diameters (Figures 6A, C, F and H) plotted between 3 and 2 F (fine sand), and the degree of skewness (Figures 6B, C, D, G, H and I) lay between -0.1 and 0.1 (approximately symmetrical).
The comparison of results obtained for the total distribution showed that clay contents are higher in the colluvial deposits than in the Bauru Group. The sand distributions of the colluvial deposits and of Bauru Group rocks, when originated from the same outcrop, exhibited a generally good correlation between superimposed and underlying deposits.
3.2 Mineralogical characteristics
The heavy mineral contents of the colluvial deposits vary between 0.03% to 0.66% and 0.50% to 4.86% of the total weight in fine-grained and very fine-grained sands, respectively (Table 3). Their frequencies are higher in very fine sands than in fine-grained sands. The magnetically heavy minerals represent 0% to 1% of the total heavy minerals within fine-grained and very fine-grained sands, except in sample 48-2, where magnetically heavy minerals represent 27.27% of the total heavy minerals. The colluvial deposits superimposed on the Serra Geral Formation exhibit a higher heavy mineral content than the other units studied.
3.2.1 Light minerals
In the analysis of light minerals present in the fine-grained sand fraction, only quartz grains are found in the colluvial deposits, while in the underlying Marília and Adamantina formations, feldspars ranging in content between 7% and 24% were found (Table 4).
As a sample, on site, 11 very fine-grained sands of the colluvial deposits, quartz grains (up to 100%), and feldspar (up to 4%) were found, while in the underlying Marília and Adamantina formations quartz (up to100%), feldspars (up to 30%) and calcite and dolomite (up to 4%) were found.
3.2.2 Heavy minerals
During the petrographic study of non-micaceous transparent heavy minerals separated from fine and very fine-grained sands, the presence of zircon, tourmaline, staurolite and rutile was verified in all samples analyzed. Together with kyanite, they may be called superabundant (Tables 5, 6 and 7). The abundant minerals are sillimanita and garnet, and pyroxene is common.
In grain-size distributions of transparent heavy minerals in colluvial sediments, zircon and rutile are present in higher frequencies in very fine-grained sands, while tourmaline and staurolite r are most abundant in fine-grained sands (Tables 5 and 6), due to differences in the specific gravities of these minerals (Tucker, 2001).
The distribution of heavy minerals in the study area show that in fine-grained sand, tourmaline is the scarcest in the NW, while zircon and rutile are scarce in the E and S of the study area. In the very fine-grained sand, the amount of tourmaline is lower than in the fine-grained sand. Zircon is more abundant and is distributed more extensively. Rutile is the scarcest, but it is more abundant in the very fine-grained sand than in the fine-grained sand. Staurolite is the scarcerin the fine-grained sands.
Only six minerals appear in more than 25% of the studied samples of colluvial deposits: zircon, rutile and staurolite are more frequent in very fine-grained sands, and tourmaline, kyanite and sillimanite are more frequent in fine-grained sands. Seven minerals appear in more than 25% of the studied samples of Bauru Group sedimentary rocks: rutile, kyanite, sillimanite, zircon (more frequent in very fine-grained sands), and tourmaline, staurolite and pyroxene (more frequent in fine-grained sands).
The most peculiar characteristics of these heavy minerals are as follows (Figure 7):
a) Tourmaline: the shapes are spherical and well-rounded (Figures 7A and B), followed by rounded-edge prismatic forms (Figures 7C, D and F), while little-rounded prismatic forms with euhedral extremities are rarely found (Figures 7J, I and G). Some grains exhibit inclusions (Figures 7C, E and J), and brownish (ferromagnesian) and greenish (Figure 7G) colored grains are frequent but yellowish (magnesian - Figures 7C, E, B, F and I), bluish (indicolite - Figures 7A and H) and pinkish (Figures 7D and J) colored grains are less common.
b) Zircon: the grains are colorless (Figure 7K) to slightly pinkish. Equidimensional and well-rounded shapes (Figure 7M) are most frequent, followed by rounded-edge prismatic (Figures 7L and N), and bipyramidal prismatic forms. Zoning and inclusions are observed (Figures 7K and L).
c) Rutile: the grains are reddish (Figure 7O), yellowish, yellowish red and almost opaque. They exhibit spherical and subrounded (Figure 7O) forms, as well as prismatic forms suggestive of pyramidal terminations (Figure 7P). There are knees, heart or elbow-like twinnings with longitudinal and oblique striations (Figure 7O).
d) Garnet: the most common grains are colorless; few pinkish grains occur as well. Spherical and well-rounded shapes are dominant, but in Bauru Group sedimentary rocks there are elongated forms (Figure 7Q). Rectangular or losangular surface alteration (perforation) patterns are common.
e) Kyanite and sillimanite: the colorless grains (Figure 7R) exhibit elongated to spherical subrounded and euhedral shapes and display inclusions. Optical characteristics were used to distinguish between these polymorphs.
f) Staurolite: there are irregular (Figures 7T and U) and rounded-edge prismatic (Figure 7S) grains with yellowish and yellow-reddish colors. They often exhibit zigzag saw-like edges (Figures 7T, U and V), providing the surface with a scale-like pattern (evidence of dissolution). They can present inclusions (Figure 7S).
g) Pyroxene: the grains exhibit elongated and rounded shapes with weathering features caused by indentations. Greenish (probably augite) or emerald-greenish (probably aegirine) colors are very common.
h) Epidote: the grains exhibit greenish color and are spherical.
i) Anatase: these grains occur only in the Bauru Group sedimentary rocks, displaying yellowish, light-bluish tones. They have a square and euhedral shape, which suggests that they are of authigenic origin.
The ferricretes appear as aggregated blocks of concretions and nodules, concentric or nonconcentric, millimetric to centimetric, with irregular or spherical shapes and reddish colors (Figure 8). The aggregates contain fine- to coarse-grained sands, essentially quartzose, with ferruginous (goethite) cementation. According to Bourman (1993), in similar deposits in Australia, this material could be interpreted as clastic deposits transformed into pisolitic and nodular ferricretes. They are found only overlying the colluvial deposits superimposed on the Adamantina Formation in 14 localities (Points 19, 21, 28, 43, 45, 48, 64, 71, 102, 108, 134, 156, 157 and 158) and as stoneline fragments at the base of colluvial deposits.
The ferricretes appear as aggregated blocks of concretions and nodules, concentric or nonconcentric, millimetric to centimetric, with irregular or spherical shapes and reddish colors (Figure 8). In thin sections, the aggregates contain fine- to coarse-grained sands, essentially quartzose, with ferruginous (goethite) cementation. According to Bourman (1993), in similar deposits in Australia, this material could be interpreted as clastic deposits transformed into pisolitic and nodular ferricretes. They are only found overlying the colluvial deposits superimposed on the Adamantina Formation in 14 localities (Points 19, 21, 28, 43, 45, 48, 64, 71, 102, 108, 134, 156, 157 and 158) and as stoneline fragments at the base of colluvial deposits.
In general the ferricretes show high SiO2 contents and lower Fe2O3 and Al2O3 contents (Table 8), or lower SiO2 contents and high Fe2O3. This suggests that they originated from sands or sandstones (Figure 9), and the high content of SiO2 is due to the presence of quartz.
The quartz grains of the ferricretes present corrosion features composed of superficial microfissures that suggest dissolution, which probably occurred due to strong weathering (Figure 10). The dissolution is also responsible for the concentration of iron hydroxides (ferralitization). Goethite is currently present in the outer yellow or brown crust or within the nodules. The precipitation of iron hydroxides as concentric pore fillings suggests that there is iron remobilization through alternating dissolution and precipitation (Figure 11).
There are few differences in the grain-sizes between the Quaternary colluvial deposits and the Cretaceous sedimentary rocks of the Marília and Adamantina formations. Excluding the pelitic fraction (clay+silt) of the samples, the variability in grain-size distribution is diminished. The processes active in the formation of the colluvial deposits did not modify the grain-size distribution of the sand fractions; changes occurred only in pelitic contents. The sorting degrees of the sand fractions were improved during pedogenetic processes and subsequent colluviation, which suggests that the pedogenetic processes attenuated the variability.
In general, the colluvial deposits are characterized by high mineralogical maturity expressed by higher values of the ZTR index (76% to 97% and 79% to 96% in fine-grained and very fine-grained sands, respectively). These values change from 53% to 100% and 67% to 98% within the same fractions of the Bauru Group sedimentary rocks. In fine- and very fine-grained sand fractions, the mineralogical contents of colluvial deposits and of the Marília and Adamantina formations, when occurring at the same locality, show good correlation. However, there is a general enrichment of ultra stable minerals (zircon, turmaline and rutile), by elimination of less stable minerals (pyroxene and garnet), probably during eluviation and colluviation processes. There are small variations in the frequencies from the same outcrop, of tourmaline, staurolite, zircon and rutile in the fine-grained sand, and of tourmaline, staurolite, zircon, rutile and additionally kyanite and sillimanite in the very fine-grained sand fractions,
Moreover, when colluvial deposits and the sedimentary rocks of the Marília and Adamantina sandstones' heavy mineral assemblages from the same outcrop were compared, some minerals of metamorphic origin appeared only in colluvial deposits, including those superimposed on the Serra Geral Formation too. This fact could suggest an eventual contribution of eolian transportation processes or by creeping of the Bauru Group and Serra Geral weathered rocks, which contained heavy minerals (such as sillimanita, staurolite and pyroxene).
The ferricretes could have been formed through remobilization processes and the concentration of iron hydroxides by ancient groundwater level fluctuations induced by paleoclimatic changes and/or by relief uplift. The iron could have been leached from upstream and deposited in ancient vadose and phreatic zone interfaces, where wetter and drier conditions due to paleoclimate oscillations existed, which propitiated the precipitation of iron. Originally, these concretions might have exhibited considerable lateral extension. Later, the probable dismantling of the iron crusts promoted the transformation of hematite in goethite, which originated pisolitic horizons. The presence of quartz and the sandy composition of the ferricretes suggest a pedogenetic origin. The crust must have originated on the Bauru Group rock hills, which became resistant to erosion and, eventually, were molded to ancient surfaces probably of atectonic origin. The fragments could have been transported over short distances as the landscape evolved, and nowadays are mixed within the colluvial cover, as observed by Roquim (1990) in Mali.
The obtained data will subsidize future decisions on anthropogenic occupations, because this quaternary deposit exhibits high susceptibility for erosion and anthropogenic contaminations of soil and groundwater.
To FAPESP (Fundação de Amparo à Pesquisa do Estado de São Paulo) for Master and Doctoral scholarships (Processes 00/10672-6 and 03/01737-5) to the first author, and by a research grant to Kenitiro Suguio (Process 01/07469-7). To CNPq (Conselho Nacional de Desenvolvimento Científico e Tecnológico) by research Grant (Process 47404/2001-9 NV) and productivity scholarship to Kenitiro Suguio (Process 304718/2003-3).
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Artigo recebido em 10/10/2007 e aprovado em 26/02/2008.