The Evolution of Neoproterozoic Magmatism in Southernmost Brazil: Shoshonitic, High-k Tholeiitic and Silica-saturated, Sodic Alkaline Volcanism in Post-collisional Basins

The Neoproterozoic shoshonitic and mildly alkaline bimodal volcanism of Southernmost Brazil is represented by rock assemblages associated to sedimentary successions, deposited in strike-slip basins formed at the post-collisional stages of the Brasilian/Pan-African orogenic cycle. The best-preserved volcano-sedimentary associations occur in the Camaquã and Campo Alegre Basins, respectively in the Sul-rio-grandense and Catarinense Shields and are outside the main shear belts or overlying the unaffected basement areas. These basins are characterized by alternation of volcanic cycles and siliciclastic sedimentation developed dominantly on a continental setting under subaerial conditions. This volcanism and the coeval plu-tonism evolved from high-K tholeiitic and calc-alkaline to shoshonitic and ended with a silica-saturated sodic alkaline magmatism, and its evolution were developed during at least 60 Ma. The compositional variation and evolution of post-collisional magmatism in southern Brazil are interpreted as the result mainly of melting of a heterogeneous mantle source, which includes garnet-phlogopite-bearing peridotites, veined-peridotites with abundant hydrated phases, such as amphibole, apatite and phlogopite, and eventually with the addition of an asthenospheric component. The subduction-related metasomatic character of post-collisional magmatism mantle sources in southern Brazil is put in evidence by Nb-negative anomalies and isotope features typical of EM1 sources.


INTRODUCTION
The Neoproterozoic in southernmost Brazil is characterized mainly by plutonism along large trans-Paleoproterozoic granulitic rocks of the Luiz Alves Craton (Campo Alegre Basin) and diverse older igneous and metamorphic terrains (Camaquã Basin) (Fig. 1).These basins are related to the post-collisional stages of the Brasiliano-Pan-African cycle and are considered as strike-slip basins, although there are controversies on their classifications and mechanisms of generation (Almeida et al. 1981, Brito Neves and Cordani 1991, Chemale Jr. 2000, Gresse et al. 1996, Paim et al. 2000).The concept of post-collisional setting assumed in this paper is taken from Liégeois (1998) and Bonin (2004), as the complex period which postdates the main collision and can include large movements along transcurrent shear belts, oblique collision, lithosphere delamination, rifting, subduction of small tectonic oceanic plates, and strike-slip basin volcanism and sedimentation.
Important volcanic cycles have been identified mainly in the Camaquã and Campo Alegre Basins.In the former three distinct cycles have been identified (Wildner et al. 2002): (i) the older volcanic rocks show shoshonitic affinity (Bom Jardim Group, Hilario Formation), are dominantly of intermediate composition, with some basic and acidic occurrences; (ii) shoshonitic rocks are succeeded by a bimodal sodic mildly alkaline volcanism (Cerro do Bugio Group, Acampamento Velho Formation), represented mainly by acidic effusive/ explosive episodes and a minor basic pole; (iii) the youngest volcanic rocks (Guaritas Group, Rodeio Velho Member) are characterized by basic to intermediate lava-flow deposits of sodic mildly alkaline to high-K tholeiitic (Fig. 1a).In the Campo Alegre Basin the volcanic sequence is bimodal, sodic, alkaline and silica saturated, similar to that observed in the Camaquã Basin (Fig. 1b).
Petrographic, geochemical and geochronological data of Neoproterozoic volcanism in some of the post-collisional basins of southernmost Brazil are reviewed and discussed in this paper, in order to re-evaluate the evolution of post-collisional magmatism and its probable sources.

THE CAMAQUÃ AND CAMPO ALEGRE BASINS
The Camaquã Basin shows an evolution characterized by the alternation of depositional intervals, with accumulation of thick sedimentary and volcano sedimentary sequences and dominantly erosive intervals.During the filling phase volcanic deposits were formed, alternated with siliciclastic sedimentation.The sedimentary sequence of the Camaquã Basin represents an evolution from shallow marine to lacustrine-alluvial and desertic settings in a typical continental environment (Paim et al. 2000).Important volcanic cycles were developed in this basin (Fig. 1a).Intermediate effusive deposits, associated to volcaniclastic sequences and hypabissal bodies, constitute the Hilario Formation, which presents shoshonitic affinity, and most of it is included in the Lavras do Sul Shoshonitic Association (Lima and Nardi 1998).It is succeeded by a bimodal volcanism -Acampamento Velho Formation -of silica-saturated-sodic-alkaline affinity, dominated by an expressive acidic magmatism and represented mainly by effusive and pyroclastic flow deposits (Sommer et al. 2005, Wildner et al. 2002, Almeida et al. 2002).The youngest unit -Rodeio Velho Member -is constituted mainly by intermediate to basic lava flows, with transitional or tholeiitic affinity (Almeida et al. 1997).
The Campo Alegre Basin situated in the northeast portion of the Santa Catarina State (Fig. 1b), presents a non-deformed and non-metamorphosed volcano-sedimentary sequence and a large amount of granitic intrusions.It lies on Archean granulite terrains and its formation is probably related to crustal relaxation due to lithospheric thickening that occurred during the Brasiliano cycle (Basei et al. 1992).The basin alternates deposition and erosive episodes in a shallow marine setting, where the sedimentary sequences were deposited and a subaerial continental setting characterized mainly by volcanic deposits.The volcanism in this basin is represented only by one volcanic cycle, the Campo Alegre Formation (Ebert 1971, Daitx andCarvalho 1980) basin, and constituted by a bimodal volcanic sequence (Waichel et al. 2000).

THE SHOSHONITIC VOLCANISM
The shoshonitic rocks represent the oldest magmatic unit in the Camaquã Basin, and includes volcanic and plutonic rocks, which are intercalated with volcanogenic conglomerates and sandy to muddy deposits related to turbidity flows, that are predominant in the top levels of this stratigraphic unit.
The effusive rocks are represented mostly by potassic trachybasalts and trachyandesites (shoshonites) spatially and temporally associated with monzonitic to quartz-monzonitic and lamprophyric hypabissal rocks, epizonal granitoids and cummulatic leucodiorites (Lima and Nardi 1998).Subordinated subarerial pyroclastic fall and flow deposits are characterized as lapilli lithic to crystal tuffs and crystal rich ignimbrites, with pla-gioclase, K-feldspar and quartz, involved by ash matrix.Volcaniclastic breccias are common and occur predominantly intercalated with trachyandesitic flows and fall tuffs.
Subvolcanic rocks are monzonites and quartz monzonites and occur as small intrusions around the Lavras Granite Complex.These rocks occur in two different facies: a porphyritic one with phenocrysts of plagioclase (oligoclase-andesine), Kfeldspar and amphibole (magnesium-hornblende), joined by biotite in more acidic members, and Ti-magnetite involved by a feldspar-rich groundmass, and an equigranular facies represented by medium-grained rocks with a similar mineralogy.These shallow intrusions are related to the latest magmatic stages of the shoshonitic magmatism.Cumulative leucodiorites occur as metric lenticular bodies involving the monzonitic rocks.They show equigranular texture, with strong flow orientation of plagioclase laths, besides clinopyroxene, magnetite and apatite as cumulus crystals, and small amounts of intercumulus material, mostly actinolite and chlorite.
Lamprophyre dikes and a lava-dome of shoshonitic affinity cut the volcanic sequence.Dykes are subvertical and generally 1 to 5 m wide, with typical panidiomorphic and porphyrytic textures characterized by abundant amphibole phenocrysts sometimes associated with clinopyroxene, engulfed by a feldspathic groundmass constituted mainly by plagioclase.Based mainly on mineralogical and textural evidence Lima and Nardi (1991) classified them as spessartitic.Clinopyroxene compositions vary from diopside to augite, and amphibole compositions vary from magnesiohastingsite to magnesiohornblende.Plagioclase composition ranges from andesine to albite, with high Sr contents (2,000-3,000 ppm).

THE NA-ALKALINE BIMODAL VOLCANISM
The bimodal volcanism represents the extrusive portion of the voluminous sodic, silica-saturated, alkaline, granitic magmatism, mostly metaluminous with minor peralkaline components (Nardi and Bonin 1991).The volcanism occurred under subaerial conditions and is exposed mainly in volcanic plateaus and ridges composed mostly of acidic lavas and pyroclastic deposits with minor intermediate and basic components (Sommer et al. 2005, Wildner et al. 2002, Almeida et al. 2002).Eruptive periods were generally initiated with explosive episodes and closed by effusive events, which suggests a decrease in volatile activity through the progress of volcanic eruption, representing a complete volcanic cycle.
Pyroclastic flows are the main volcaniclastic deposits and are represented by ignimbrites of comenditic affinity.The proximal and basal facies are characterized by co-ignimbritic breccias, constituted dominantly by juvenile, cognate and accidental blocks and lapilli in a tuffaceous matrix.This facies shows lateral gradational changes to ignimbrites with abundant lithoclasts and pumice lapillis, besides K-feldspar and quartz phenoclasts, separated in two main lithofacies: lenticulites and crystal-rich deposits, both presenting K-feldspar and quartz phenoclasts, pumice fragments and scarce lithoclasts with lapilli-size, in an abundant vitroclastic tuffaceous matrix.The pyroclastic flow deposits show evidences of hot, gas-supported emplacement, such as welding, high-temperature devitrification processes (spherulites, axiolites), lithophysae, perlitic fractures, gas-escape structures and vapor-phase crystals, which suggest the deposition from primary pyroclastic flows, generally restricted to subaerial settings.

Basic-intermediate rocks are represented by
An Acad Bras Cienc ( 2006) 78 (3) Acidic lava flows and syn-volcanic intrusions are represented mainly by comenditic rhyolites and minor trachytes erupted through fracture zones, where they exhibit a sub-vertical flow foliation, gradating laterally to auto-breccias, lavas with sub-horizontal flow foliation and massive bodies.Acidic rocks consist of alkali feldspar, usually microperthite, quartz, zircon, and iron oxides as accessory phases.They generally show porphyritic to glomeroporphyritic textures, with low percentages of phenocrysts set in a matrix constituted of a mosaic of quartz and feldspar microlites and crystallites.Mafic phases are scarce and occur as aciculate crystals of amphibole and as rare pyroxene relicts partially replaced by amphibole and chlorite.Amphibole in the acidic rocks presents the compositions of sodic-calcic phase -ferro-winchite, ferrobarroisite and ferro-richterite, and a calcic oneferro-actinolite, which are frequently found in comenditic rocks (Strong and Taylor 1984).The microperthitic alkalli feldspar has the composition Or 84−98 .However there are scarce homogeneous grains with a composition close to sanidine (Or 41−47 ).Plagioclase has been transformed to albite (An 0,5−3 ).Microphenocrysts of Ti-magnetite and ilmenite have compositions similar to those described on peralkaline rhyolites (Sutherland 1975).Incompatible minor and trace elements show very enriched LILE and LREE ocean island basalts (OIB) normalized patterns (Fig. 3a), which are characteristic of shoshonitic rocks.Nb is depleted relative to LREE, which is considered as typical of magmas produced from sources modified by a previous subduction-related metasomatism (e.g.Kelemen et al. 1993).Their low Nb/La and La/Ba ratios are comparable to those reported for orogenic andesites by Davies and Hawkesworth (1994).HFS element contents are higher than in oceanic shoshonites, and similar to those reported by Pearce (1983) for those from continental margin.Y and Yb show lower contents than OIB (Fig. 3a), which may be ascribed to the presence of garnet in the residuum of this magmatism or to equilibration of ascendingslab melts with garnet peridotites as suggested by Kelemen et al. (1993).Ce/Sm and Sm/Yb ratios, as suggested by Davies and Hawkesworth (1994), also point out to the presence of garnet as a residual phase in the source of this magmatism.Chondrite normalized REE patterns (Fig. 3b) are characterized by Ce N values close to 100, Yb N about 4 and absence of Eu anomalies; such features are also indicative of shoshonitic or high-potassium calc-alkaline magmas (Nardi and Lima 2000).
Intermediate and acidic terms keep the same patterns of incompatible elements relative to OIB (Fig. 3a).The regularity of REE patterns (Fig. 3b) observed for basic, intermediate and acidic rocks suggests their cogeneticity and consequently the origin of acidic rocks through the differentiation of basic and intermediate magmas.
Because several authors ascribe a significant role to lower crust as the source or a significant contaminant to shoshonitic magmas, the LSSA rocks were compared to the lower crust averages calculated by Wedepohl (1995), in order to evaluate its petrogenetic involvement.The basic and intermediate terms show enriched patterns for most elements, particularly for Ba, Sr and LREE, while Y and Yb are depleted relative to lower crustal values.It seems thus, that lower crust is not compositionally suit-able as a source for shoshonitic magmas or even as a contaminant capable of explaining the increase of LILE or HFS element contents.Since plagioclase is usually an abundant residual phase during crustal melting, high Sr magmas are not expected, particularly if low-melt fractions are presumed.Granitic rocks maintain approximately the same geochemical trends, with Sr contents too high to be produced by crustal melting, whereas the enriched patterns for incompatible LILE would be an evidence of small melt fractions.
Granitic and rhyolitic rocks are metaluminous, with typically high Ba and Sr contents and mod-  The bimodal volcanism is characterized by a basicacidic rock association related to mildly alkaline series, as displayed on TAS (Le Bas et al. 1986) diagram, where the compositional trends are situated close to the limit between subalkaline and silica saturated alkaline fields (Fig. 2a; Table I).Rhyolites of comenditic affinity are predominant in the volcanic sequence.Basic rocks are mostly hawaiites and basalts, whilst mugearitic terms are scarce.The sodic character is indicated by (Na 2 O -2) > K 2 O values, in spite of their high loss on ignition (LOI) values.Two evolutionary trends with contrasting Ti-P contents were identified and referred to as high-and low-Ti-P basalt-rhyolites (Sommer et al. 2005) (Figs. 2c, 2d).A third compositional group probably represents the last magmatism in the Camaquã Basin, still related to the Brasiliano-Pan-African post-collisional stage, which is referred to as high-Nb rhyolites (Figs. 2c,2d,4b).
The alkaline affinity of this bimodal association is observed in the sliding normalization scheme of Liégeois et al. 1998, where most rocks plot in the field characterized by high SNX-SNY values (Fig. 2b).
The less differentiated rocks present relatively high FeOt/MgO ratios usually observed in tholeiitic series, which is corroborated by the behavior of some incompatible elements as Nb, Zr and Y, as displayed in Meschede's (1986) diagram (Fig. 4a), and by the Al 2 O 3 contents, which are similar to those of continental flood basalts of Paraná Basin (Piccirillo et al. 1988).
Trace elements of basic rocks are similar to those of ocean island basalt (OIB), except for the lower Nb, Ta and P contents and higher Ba values (Fig. 3c).
A roughly flat normalized REE pattern is characteristic of the low-Ti-P basic rocks, with a slight LREE enrichment relative to HREE, with La N /Yb N ratios around 3, and absence of Eu anomaly (Fig. 3d).High-Ti-P types are REE enriched when compared to low-Ti-P basalts, have higher LREE/HREE ratios (La N /Yb N close to 10-11) and negative-Eu anomalies.
The basic magmatism lies predominantly in the within plate field in diagrams using incompatible elements as observed in figure 4a.They show a transitional pattern when compared to OIB-normalized patterns of within-plate tholeiitic and high-K basaltic magmas (Pearce 1982, Ewart 1982).This behavior is characteristics for basalts of transitional or moderately alkaline affinity, usually related to continental rifts or post-collisional settings, as pointed out by Leat et al. (1986).
The acidic rocks generally have SiO 2 values higher than 70 wt%, and are probably crystallized from peralkaline liquids; however, due to loss of alkaline elements during crystallization (Leat et al. 1986) show agpaitic index values close to 1 or even lower.The originally peralkaline affinity of this association is corroborated by Zr contents generally over 300 ppm (Table I).Volcanic rocks with lower Zr contents -about 150 ppm -and low agpaitic index are less abundant and show characteristics similar to those of subalkaline metaluminous associations.
Assuming the primary peralkaline character of rhyolitic magmas, their comenditic affinity is confirmed on the FeO t × Al 2 O 3 diagram (MacDon-   4c).The high-Nb comendites show more peralkaline compositions than high and low-Ti acidic rocks, with higher Ta contents, which are commonly referred to in pantelleritic associations (Hildreth 1981).The acidic rocks have FeOt/(FeOt+MgO) ratios dominantly higher than 0.9, which are typical of rhyolites associated to alkaline series (Ewart 1979(Ewart , 1982)).
Trace element patterns of rhyolites normalized against the ORG values (Pearce et al. 1984.) are displayed in the figure 3e, where rhyolites show patterns similar to those found in within plate granitic rocks, particularly of attenuated continental lithosphere.Their high Ce/Nb ratios are like those found in post-orogenic magmatic associations, such as Snowdon Rhyolites (Leat et al. 1986).The lower Ce and Sm and, higher Rb and Ta contents, together with the lower Ce/Nb ratios of high-Nb rhyolites suggest that this magmatism is related to sources with less influence of subduction-related metasomatism, like the Naivasha Rhyolites, Kenya (Mac-Donald et al. 1987).
Chondrite-normalized REE patterns (Fig. 3f) show a slight enrichment of REE in the high-Ti rhyolites, particularly for LREE, with a La N /Yb N ratio about 10-12.The high-Nb acidic rocks present La N /Yb N ratio close to 1 or 2, larger negative Eu anomalies and a strong LREE depletion in the most differentiated liquids, which probably reflect the presence of LREE-rich minerals, like allanite, among the fractionated phases or a different source.
In the Y × Nb diagram (Fig. 4d), the sodic alkaline rocks plot mainly in the field of postcollisional magmatism, whilst high-Nb rocks occupy the field closer to that of within-plate associations.A similar behavior is observed in the Zr × Nb diagram (Fig. 4e) where the rhyolitic rocks in general present Zr/Nb ratios > 10, which indicate that this magmatism is related to sources modified by subduction, such as those of post-collisional settings.This kind of magmatic association has been described in provinces such as Snowdonia, Avoca and Parys Mountain, within the Southern British Caledonides (Leat et al. 1986).The high-Nb rocks show Zr/Nb ratios < 10, which is usually related to anorogenic settings as that of Naivasha volcanic association, Kenya (MacDonald and Bailey 1973).
Isotopic data obtained from bimodal volcanism supplied ages varying from 549 to 602 Ma.U-Pb ages within this range were obtained in zircons from different volcanic types (Siga Jr et al. 1995, Cordani et al. 1999, Chemale Jr 2000, Sommer et al. 2005).

FINAL CONSIDERATIONS
The Neoproterozoic shoshonitic and mildly alkaline bimodal volcanism of Southernmost Brazil is represented by rock assemblages associated to volcanosedimentary successions, deposited in strike-slip basins formed at the post-collisional stages of the Brasilian/Pan-African orogenic cycle.The geotectonic setting during this period in southern Brazil can be envisaged as resultant from the collisional system associated with the amalgamation of Rio de La Plata, São Francisco, Congo, Kalahari and Paraná cratons, as suggested by Brito Neves and Cordani (1991), leading to the formation of Gondwana supercontinent.The influence of collisions related to the Pampean Orogeny (Rapela et al. 1998) in the development of Cambrian shear belts in southern Brazil can not be discarded, particularly for late-transcurrent events such as that related to the Caçapava Granite Complex intrusion with age of 550 Ma (Nardi and Bitencourt 1989).This long period of transcurrent tectonics with associated strike-slip basin formation and associated magmatism, related to the consolidation of Gondwana supercontinent, explains the wide time interval of Brasiliano post-collisional magmatism in southern Brazil (650-540 Ma).
The best-preserved volcano-sedimentary associations occur in the Camaquã and Campo Alegre Basins, respectively in the Sul-rio-grandense and Catarinense Shields and are outside the main shear belts or overlying the unaffected basement areas.These basins are characterized by alternation of volcanic cycles and siliciclastic sedimentation developed dominantly on a continental setting under sub-  An Acad Bras Cienc ( 2006) 78 (3) aerial conditions (Paim et al. 2000, Wildner et al. 2002), associated to coeval plutonism that evolved from high-K tholeiitic and calc-alkaline to shoshonitic and ended with a silica-saturated sodic alkaline magmatism.Ultrapotassic lamprophyres and silicasaturated syenitic rocks coeval with the shoshonitic magmatism were described by Stabel et al. (2001) andPlá Cid et al. (2003).
The shoshonitic component is represented by Hilário Volcanism in the Camaquã Basin, while the alkaline signature is typical of the younger Acampamento Velho and Campo Alegre volcanisms, respectively in the Camaquã and Campo Alegre basins.
The available isotopic data indicate that shoshonitic Hilário volcanism occurred between 608 Ma and 592 ± 5 Ma and the bimodal mildly alkaline magmatism of the Acampamento Velho and Campo Alegre volcanism between 602 Ma and 549 Ma.These ages are coherent with those found in the coeval extensional granitic plutonism, indicating that evolution of shoshonitic and mildly alkaline bimodal magmatism was developed during at least 60 Ma.
Bimodal volcanism was carried out over Paleoproterozoic granulitic complexes or over metamorphic terrains with juvenile protoliths and in spite of these basement differences, volcanic episodes and facies architecture in the studied basins are similar, with a predominance of acidic over basic magmatism and an less expressive occurrence of intermediate rocks, mainly trachytic lavas and small syenitic plutons (Wildner et al. 2002, Waichel et al. 2000).The bimodal magmatism according to mineralogical, trace and major element data belongs to the silica-saturated sodic alkaline series and shows high FeO T /MgO ratios comparable to those of continental flood basalts.Two magmatic sequences were identified and referred to as high-Ti-P basalts-rhyolites and low-Ti-P basalts-rhyolites.
The compositional differences observed in the high-and low-Ti-P groups are attributed to different melt fractions from a dominantly lithospheric mantle, previously affected by subduction (Wildner et al. 2002, Sommer et al. 2005).
The volcanic cycles investigated in Neoproterozoic basins of southernmost Brazil represent part of evolutionary sequences that are typical of postcollisional magmatism.This magmatism marks the final stages of the post-collisional period and the exhausting of mantle reservoirs hydrated and metasomatized by processes related to a previous subduction.The latest volcanism, characterized by the high-Nb rhyolites, probably represents an asthenospheric contribution and can be interpreted as result of slab break-off and asthenospheric upwelling as proposed by Atherton and Ghani (2002).
The post-collisional magmatism evolution from high-K subalkaline to shoshonitic and eventually to sodic mildly alkaline observed in southernmost Brazil (Nardi and Bonin 1991, Bitencourt and Nardi 1993, 2000, Gastal and Lafon 1998, 2001, Wildner et al. 2002, Waichel et al. 2000, Sommer et al. 2005, Nardi and Lima 2000) is referred elsewhere as in Snowdonia and Parys Mountain associations in the British Caledonides (Leat et al. 1986), Devine Canyon Tuff -USA (Greene 1973) and Miocene post-collisional volcanism of the Eastern Rif in Morocco (El Bakkali et al. 1998).This evolution is characterized by development of shear belts associated to predominantly granitic magmatism and strike-slip basins where a typical and voluminous volcanism and associated sedimentation was developed and preserved, as envisaged by Bonin (2004) for the evolution of the Alpine Belt since the end of Variscan orogeny in Europe.
The post-collisional magmatism in southern Brazil shows some particular features that should be emphasized: (i) the last post-collisional magmatic events are sodic instead of potassic or ultrapotassic and (ii) the early magmatic stages of mafic magmatism are dominantly high-K tholeiitic instead of calc-alkaline (ii) the ultrapotassic lamprophyresyenitic magmatism (611 Ma;Plá Cid et al. 2003) is approximately coeval with the shoshonitic one.The compositional variation and evolution of postcollisional magmatism in southern Brazil is interpreted as result mainly of melting of a heterogeneous mantle source, which includes garnet-phlogopite-bearing peridotites, veined-peridotites with abundant hydrated phases, such as amphibole, apatite and phlogopite, and eventually with the addition of an asthenospheric component.Crustal melts are significative within the major post-collision shear belts where peraluminous acidic rocks have been described by several authors (e.g.Bitencourt and Nardi 1993).The subduction-related metasomatic character of post-collisional magmatism mantle sources in southern Brazil is put in evidence by Nbnegative anomalies and isotope features typical of EM1 sources.
Fig. 1 -Localization and simplified geological maps of the Camaquã (a) and Campo Alegre (b) basins (modified from Wildner et al. 2002).
Basic-intermediate volcanic rocks plot in the trachybasalt and basaltic trachyandesite fields of the TAS diagram (Fig.2a) and their potassic character is indicated by K 2 O values greater than Na 2 O-2 (Table I), which classify them as potassic trachybasalts and shoshonites (Le Maitre 2002).They are generally silica saturated with normative olivine, hypersthene and diopside.According toLima and Nardi (1998) the Ni, Cr and Co contents in trachybasalts from LSSA are lower than those typical of primary magmas.In the sliding normalization diagram proposed byLiégeois et al. (1998), the rock association plot in the shoshonitic field, characterized by high SNY (=mean [Rb-U-Th-Ta]NYTS) values and low SNX (=mean [Zr-Ce-Sm-Y-Yb]NYTS) values (Fig 2b).
CARLOS A. SOMMER et al.