Petrology of Gameleira Potassic Lamprophyres , São Francisco Craton

Gameleira lamprophyres are dykes and mafic microgranular enclaves associated with the shoshonitic Gameleira monzonite. This association belongs to the Paleoproterozoic alkaline magmatism from Serrinha nucleus, northeast Brazil. The liquidus paragenesis is diopside, pargasite, apatite and mica. Reverse zoning was identified in the groundmass alkali feldspar and was related to the undercooling of lamprophyric magma during the emplacement, with high growth rate of pargasite/edenite inducing disequilibrium between feldspars and liquid. Chemical data indicate that the lamprophyres are basic rocks (SiO2 < 48 wt%), with alkaline character (Na2O + K2O > 3 wt%) and potassic signature (K2O/Na2O ≈ 2). High contents of MgO and Cr are consistent with a signature of a primary liquid, and such concentrations, as well as Al, K, P, Ba, Niand light rare earth elements, are consistent with an olivine-free metasomatic mantle source enriched in amphibole, clinopyroxene and apatite. By contrast, the ultrapotassic lamprophyres from Morro do Afonso, contemporaneous alkaline ultrapotassic magmatism in Serrinha nucleus, were probably produced by melting of a clinopyroxene-phlogopite-apatite enriched-source. The identification of different mineral paragenesis in the source of potassic and ultrapotassic lamprophyres from Serrinha nucleus can contribute to the understanding of the mantle heterogeneities and tectonic evolution of this region.


INTRODUCTION
Alkaline magmatism is frequent in within-plate settings (Whalen et al. 1987, Bonin 1996), associated to extensional processes, where it exhibits elevated concentrations of High Field Strength Elements (HFSE) in opposition to moderate and low amounts of Large Ion Lithophile Elements (LILE).This sort of alkaline anorogenic magmas support the usual concept of alkaline series and their evolution (Lameyre and Bowden 1982).Examples of withinplate magmatism in Bahia State, northeast Brazil, are the Paleoproterozoic Angico dos Dias carbonatites (Silva et al. 1988) and the alkaline and peralkaline granites from Campo Alegre de Lourdes (Plá Cid et al. 2001).In the Neoproterozoic, the best examples are the southern occurrences of undersaturated and saturated syenitic province (PASEBA;Rosa et al. 2002Rosa et al. , 2005)).During the last twenty years numerous occurrences of alkaline rocks in recent and ancient subduction-related settings have been studied (Thompson and Fowler 1986, Leat et al. 1988, Ringwood 1990, Nardi and Bonin 1991, Corriveau and Gorton 1993, Plá Cid et al. 2002, Sommer et al. 2005, and references therein).Compared to the within-plate, anorogenic and post-orogenic alkaline rocks, subduction-related alkaline magmas are depleted in HFSE and show strong enrichments in LILE and Light Rare Earth Elements (LREE), which has been interpreted by several authors, as related to a mantle source previously modified by dehydration-melting from a subducted-slab.In this sense, arc-related magmas are characteristically potassic, identified as belonging to the shoshonitic and potassic-ultrapotassic series, whereas the anorogenic within-plate magmas are dominantly sodic.This paper deals with potassic primary magmas, with arc-affinity, in the Paleoproterozoic of northeast Brazil and discusses mineralogical data obtained by Electron Microprobe in feldspars, amphibole and clinopyroxene.

REGIONAL FRAMEWORK
The São Francisco Craton (SFC) is a crustal segment of the South American Plataform stabilized in the Paleoproterozoic (1.8 Ga) and limited by Neoproterozoic (0.6 Ga) reworked terrains.Internally, the SFC is segmented in three Archaean nuclei: Guanambi, Remanso and Serrinha from west to east, which are separated by NS-trending Paleoproterozoic fold belts formed by collisional events among these nuclei (Mascarenhas 1979).The studied area is located in the SN (Figure 1).
The alkaline magmatism comprises shoshonitic batholiths (e.g.Itareru Massif; Figure 1) and ultrapotassic syenites and lamprophyres (e.g.Morro do Afonso Massif, Rios 2002).The studied area, called Gameleira, is located a few kilometers to the west of Morro do Afonso Massif (Figure 1).Preliminary data of Gameleira lamprophyres were presented by Plá Cid et al. (2007).The magmatism is represented by mafic dykes intrusive in monzonitic and quartz-monzonitic rocks, and mafic microgranular enclaves comingled with the monzonites.The host rocks are medium-to coarsegrained monzonites and consist of plagioclase and alkali feldspar phenocrysts, as well as amphibole, in a groundmass composed of the same minerals.Rare mica crystals were observed; titanite is the main accessory phase together with apatite.No metamorphic textures are present, and the internal crystal orientation is attributed to magma flow.The genetic correlation between the monzonites and the mafic rocks is possible, but this will not be discussed in this paper.
The main aim of this paper is to present geochemical and mineralogical data of the mafic magmatism associated with the Gameleira monzonite, which represents a primary magma derived from a metasomatic mantle-source.PETROLOGY OF GAMELEIRA LAMPROPHYRES

FIELD AND PETROGRAPHIC FEATURES
The alkaline mafic magmatism occurs as dykes and locally as microgranular enclaves, being contemporaneous to the Gameleira shoshonitic monzonite.Enclaves show elliptical or irregular shapes, are up to 10 m wide, show sinuous contacts with the monzonite host and internal flow structures.They are very fine-grained rocks aligned with the magmatic foliation of the monzonite, and frequently hybridized, as attested by feldspar xenocrysts of the host rock.
The better preserved examples of this magmatism are represented by dykes, which intrude   Inclusions of iron oxides are also observed in the late-magmatic-crystallized felsic minerals, some amphibole rims and in the interstitial apatite, suggesting an increase in the fO 2 -conditions.Based on mineral modal proportions, Gameleira lamprophyres can be classified as melanocratic diorites, as discussed previously by Plá Cid et al. (2007).However, the presence of amphibole, forming the near-liquidus phase, and feldspar restricted to the groundmass, are the typical characteristics that lead to classify them as lamprophyres (Rock 1987, Le Maitre et al. 1989).Close to Gameleira rocks (< 5 km), vogesites and minettes associated with the Paleoproterozoic Morro do Afonso syenitic pluton (Rios 2002, Plá Cid et al. 2006).In the western part of the São Francisco Craton, a similar association was described by Paim et al. (2002) in the Paleoproterozoic Cara Suja Syenitic Pluton, associated mainly with ultrapotassic minette lamprophyres.The dominant mafic phase in the Gameleira dykes is amphibole, whereas alkali feldspar and plagioclase are restricted to the groundmass, indicating that the composition of these rocks range between vogesites and spessartites (Le Maitre et al. 1989).
The chemical analyses of the mineral phases from Gameleira lamprophyres were obtained using a JEOL Electron Microprobe, JXA 8600 model, at the Electron Microprobe Laboratory from São Paulo University (USP).Analytical conditions included a beam current of 10 nA, beam energy of 15 keV and acquisition time of 20s on the peak and 10s on the background.Each element was standardized on either synthetic or natural minerals.The backscattered electron images (BSE) were acquired using a Scanning Electronic Microscope (SEM) at Electronic Microscopy Center of the Catholic Pontific University (PUC) from Rio Grande do Sul.

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PETROLOGY OF GAMELEIRA LAMPROPHYRES FELDSPARS BSE images were obtained using a SEM, and are shown in Figure 2.Such images reveal the non-reactive contacts between felsic minerals, a marked zoning in the alkali feldspar grains and incipient in the plagioclase, and the fine-grained texture of these lamprophyres.
Tables I and II display representative compositions of alkali feldspar and plagioclase crystals of Gameleira lamprophyres, respectively.

TABLE II
Representative analyses of plagioclase from Gameleira lamprophyres, with structural formulae calculated on the basis of 16 oxygens.Legend: C -core and R -rim analyses.JORGE PLÁ CID, CRISTIANI S. CAMPOS, LAURO V.S. NARDI and LUANA FLORISBAL feldspar, between larger crystals of amphibole, is also observed in the SEM images.Relatively large amounts of Na 2 O were determined (Ab -6.33 wt% to 14.65 wt%), so that the absence of exsolved perthite may be a consequence of the fast crystallization of the lamprophyric magma, above the solvus temperature.High-temperature preserved composition and also points to monoclinic orthoclase instead of triclinic microcline.
Chemically, the alkali feldspar crystals are characterized by high BaO amounts (up to 9.16wt%), with the celsian molecule reaching up to 17.65wt% and belonging to the orthoclasecelsian solid-solution series.Significative anorthite contents are absent, as expected.SrO is between 0.19wt% and 0.59wt%, which suggests a mineral/ melt partition coefficient higher than 1.
is in the range of Ab 6 and Ab 12 , with a higher decreasing observed in grain six (Ab 10.46 to Ab 6.90 ).BSE images of Table II are in agreement with this chemical variation since clearer colors (rims) indicate higher average atomic number (richer in K) and the darker cores a lower average atomic number (richer in Na).Ba and K contents show a clear antipathetic behavior, and mutual substitution is highly probable.The increasing of Al in the borders of most alkali feldspar grains (Table I) associated with decreasing of Si produces charge unbalancing in the tetrahedral sites.The substitution involving larger ions, such as K + , is necessary to charge balancing of the structure.Substitution of K + and Na + by divalent ions of Ba ++ is suggested by the trends in Figure 4, showing the good trending of the coupled substitution including Si and IV Al.As observed in Table I, the albite content is higher in the alkali feldspar cores.Only in two grains, normal zoning was observed: the albite enrichment occurs in the rims.The zoning was detected in the SEM images (Figure 2) as a narrow rim with sinuous contact.In the zoned grains, with analyses in the same crystal, the albite molecule The chemical analyses of plagioclase grains point to a dominant andesine composition (An 30- 35 ) with some grains richer in calcium (An 37-41 ).The orthoclase amounts are very low (Or1.5-4.5 ).Sr contents are low and homogeneous (Table II).Celsian molecule occupies less than 0.3 % of the plagioclase structure.In a general view, the plagioclase compositions are homogeneous, and the slight chemical variations suggest that crystallization of this mineral phase was quite fast.In six grains the albite molecule decreased from core to rims (Table II), although a variation around 2 % that was not detected by SEM (Figure 2).The slight increase of An in some rims is balanced by the increase of Al +3 and the decrease of Si +4 in the tetrahedral site.
Then, some unusual behavior occurred during the crystallization of this magma to induce reverse zoning in the near-solidus felsic mineralogy, which was more evident in the alkali feldspar.Such feature is probably associated with the emplacement of the crystallizing magma in narrow (less than 40cm wide) fractures along the host and cooler granite, inducing a fast temperature decrease.PYROXENE Chemical analyses from core to rim of clinopyroxene grains from Gameleira lamprophyres are given in Table III.Based on the modal classification of Morimoto (1988), these pyroxene grains are classified as diopside (Figure 5) and crystals are composed by high amounts of wollastonite (Wo 48.9-49.9 ) and enstatite (En) up to 39%, and low ferrosilite (Fs) up to 12%.For comparison, compositions of pyroxenes from Morro do Afonso (Plá Cid et al. 2006) andCara Suja (Paim et al. 2002) lamprophyres, which have lower En contents reflecting lower MgO/(MgO+FeO t ) ratio of these magmas, were included in Figure 3. Very low amounts of Al and Na (Table III) in the structure imply in very low contents of acmite and jadeite molecules (lower than 2%).Diopside grains have homogeneous composition, with variations in terms of Wo-En-Fs molecules below 2% (Table III), which suggests a short time of crystallization during the near-liquidus stages.Neumann (1976) and Bonin and Giret (1985) demonstrated the correlation between the composition of magma in terms of some chemical elements and, their distribution in pyroxenes.MgO/ (MgO+FeOt) ratio in the diopside of Gameleira lamprophyres is high and ranges between 0.64 and 0.69, reflecting similar ratios in the magma, between 0.52 and 0.59, considering all iron as ferrous.Similarly, Na 2 O/(CaO+Na 2 O) ratio is very low in diopside, between 0.012 and 0.021, resulting in the very low ratio in the magma (0.072 to 0.089).
The variations of classical fractional crystallization indicators, as Mg, Ca and Na, in the pyroxene grains, show differences between centerborder lower than 0.5 wt% for MgO and CaO, and 0.1 wt% for Na 2 O.This is also a consequence of diopside size, normally less than 100μm and included in larger amphibole crystals.

AMPHIBOLES
Representative analyses of amphiboles in Gameleira lamprophyres are given in Table IV.Based on the amphibole nomenclature of Leake et al. (1997), the amphibole compositions from Gameleira lamprophyres are mainly edenite, and only a few compositions of pargasite occur in crystal's cores (Figure 6a).Three analyses are Mg-hornblende, as indicated by A-site < 0.5 apfu (Figure 6b).Similar compositions of amphiboles from Morro do Afonso and Cara Suja lamprophyres are observed in Figure 6, with lower Mg/(Mg+Fe +2 ) ratio.The amphibole from Gameleira dykes correspond to the lamprophyre magmatic amphibole field (Figure 7) as defined by (Rock 1991)     The trend from pargasite core to edenite rims (Figure 6a) is characterized by progressive decreases in T Al, with the higher contents in pargasite cores (1.96 to 2.1apfu) and the lowest in the Mg-hornblende crystals (1.33 to 1.38apfu).The three Mg-hornblende grains have the lower amounts of Fe +3 (Table IV) and result of the simultaneous crystallization of iron oxides during the later magmatic-stages under higher fO 2conditions.The same feature was reported in the Paleoproterozoic Cara Suja and Morro do Afonso potassic/ultrapotassic lamprophyres (Paim et al. 2002, Plá Cid et al. 2006).Ti contents also decrease with crystallization (Table IV) and reflect the latemagmatic or subsolidus crystallization of titanite.
Alkali (Na + K) elements are relatively enriched in the pargasite, as evidenced by the filling in A-site (55% to 62%), whereas it ranges from 50% to 58% in edenite and from 39% to 42% in Mg-hornblende.The decrease of alkali element contents with amphibole crystallization is illustrated in figure 8.A similar behavior was described in the Cara Suja and Morro do Afonso lamprophyres (Paim et al. 2002, Plá Cid et al. 2006).

WHOLE ROCK GEOCHEMISTRY
The chemical data listed in table V were accomplished in the Acme Analytical Laboratories Ltd. (Canada).Major elements were determined by ICP-ES.Trace and rare-earth elements by ICP-MS.All determinations are above the detection limits and the calculated errors are below 5%.For comparison, in this table are also shown the ultrapotassic lamprophyres from Morro do Afonso Massif (Rios 2002).
Gameleira lamprophyres have low SiO 2 contents (44 -48 wt%), total alkalis close to 3wt% and K 2 O/Na 2 O ratio around 2. In the TAS diagram (Figure 9) these lamprophyres plot in the silica-saturated alkaline field.The relation between K 2 O and Na 2 O, according to the proposition of Le Maitre et al. (1989), points to a primary alkaline magma with a dominant potassic character.The low Al 2 O 3 contents (< 10wt%) are unusual in the shoshonitic series as described by Morrison (1980) and, in the same way, K 2 O concentrations below  3wt% are in disagreement with the ultrapotassic series as proposed by Foley et al. (1987).However, Gameleira lamprophyres have most chemical characteristics similar to the shoshonitic rocks in the sense of Morrison (1980).According to the criteria of Morrison (1980) and Nardi (1986), the host monzonites (Table V) have also chemical affinity with the shoshonitic series, as deduced of its alkaline (Figure 9) and metaluminous character, moderate Al 2 O 3 (15wt%) and P 2 O 5 (< 0.6wt%), low TiO 2 (0.7wt%) and high Rb, Sr and Ba.The classification diagram involving trace elements developed by Muller et al. (1992) also confirms that Gameleira lamprophyres are compositionally close to typical shoshonitic rocks (Figure 10).and clinopyroxene.The incompatibility of K points to a minor participation of mica in the fractionation processes, and may suggest that lamprophyres and the monzonitic host are not genetically related.The primary character of lamprophyre magmas is also recognized by the trace element contents.High concentrations of Cr (> 500 ppm) and moderate to low of Ni (41 -159 ppm) are in agreement with a mantle with high proportions of pyroxene and olivine-free.Gameleira lamprophyres are also enriched in Ba and Sr, and show moderate contents of Rb (Table V).The high concentrations of High Field Strengths Elements (HFSE), commonly observed in alkaline rocks of within-plate settings, are not observed in Gameleira lamprophyres that show moderate concentrations of Y and Zr, and low Hf, Nb and Ta.Low contents of HFSE in potassic and ultrapotassic magmatism have been associated with a metasomatic mantle-source at subduction-related settings (e.g.Peccerillo 1985, Foley andPeccerillo 1992).
(Ce/Yb)N chondritic ratios, normalized by Evensen et al. (1980) values, are between 45 and 71, pointing to the strong enrichment of LREE and extremely fractionated REE-patterns (Figure 11).Such highly fractionated patterns are a consequence of the extreme enrichment of LREE, with Ce rea-  Middlemost (1994).Open circles correspond to Gameleira lamprophyres and filled circles to host granites.
The very high contents of MgO, above 10.9 wt%, as well as the very low SiO 2 concentrations, point out to the primary composition of Gameleira lamprophyres.These rocks are also characterized by high P 2 O 5 values (1.4wt% -2wt%), whereas TiO 2 shows moderate values (1wt% -1.5wt%).FeO T , CaO and P 2 O 5 show a compatible behavior with SiO 2 , whereas K 2 O and K 2 O/Na 2 O ratios increase with differentiation, suggesting that fractional crystallization was dominated by apatite  V).Similar high amounts of LREE are observed in typical ultrapotassic rocks from within-plate (i.e.lamproites) and in lamprophyre magmas of post-collisional settings (i.e.minettes) (Foley 1992, Gibson et al. 1992), and are, therefore, correlated with the metasomatic process at the source and not necessarily with the tectonic setting.Eu-negative anomalies are not present in Gameleira Lamprophyres.REE-patterns from Morro do Afonso lamprophyres, which show a strong similarity with the Gameleira rocks, were plotted for comparison in Figure 11.

Mineralogy
The crystallization history of Paleoproterozoic lamprophyres in NE Brazil, associated to the syenitic intrusions from Cara Suja and Morro do Afonso (Rios 1997, Paim et al. 2002, Plá Cid et al. 2006), as well as, the minettes from Piquiri Syenite Massif (Plá Cid et al. 2002, 2003) in south Brazil, have shown similar near-liquidus paragenesis.Clinopyroxene-apatite-mica are the main mineral fractionated phases.However, in Piquiri and Cara Suja lamprophyres, a pargasitic amphibole was also identified as an early magmatic phase, as reported from inclusions in clinopyroxenes (Paim et al. 2002, PETROLOGY OF GAMELEIRA LAMPROPHYRES Plá Cid et al. 2003, Nardi et al. 2007).Although such inclusions in clinopyroxenes were not observed in Gameleira lamprophyres, cores of pargasitic composition in some amphibole grains may suggest that the near-liquidus mineralogy is similar to that found in potassic/ultrapotassic lamprophyres.
MacKenzie and Zusmann (1972) demonstrated that reverse zoning in feldspars was induced in supercooled magmas that suffered elevated mineral growth rate, and, in such conditions, some elements follow an 'effective distribution coefficient', rather than the equilibrium distribution coefficient.Such effective distribution coefficient induced in the melt/magma gradients of some elements only in the interface of crystallizing minerals/magma cause the disequilibrium between feldspars and liquid.In Gameleira lamprophyres, the high growth rate of the amphibole was induced by the emplacement of lamprophyric magma into narrow fractures in the host shoshonitic monzonite, establishing, in this way, a strong temperature gradient.At the moment of the emplacement, the lamprophyric magma was in the initial crystallization stage, with diopside, apatite, mica, and, probably, pargasite crystals.A considerable temperature contrast between the hotter lamprophyric magma and the host monzonite promoted, in a water-buffered system, the high rate of amphibole crystallization.Such "undercooling" induced in the lamprophyre magma a substantial growth rate of amphibole crystals, inducing a gradient of elements as Ca, Na and K similar to that defined by MacKenzie and Zusmann (1972).As described previously, some feldspar grains were found as inclusions in amphibole phenocrysts close to the borders.This shows that syncrystallization between amphibole and feldspar occurred during the disequilibrium caused by high growth rates of the amphibole.
The crystallization of plagioclase and alkali feldspar occurred at the same time, and evidences of resorption were not observed.As pointed out by Nekvasil (1990), the re-sorption field in the Ab-An-Or system contract with the increase of water and silica in the magma.The water-saturation of Gameleira lamprophyric magmas is corroborated by the large crystallization of mineral phases such as amphibole and apatite and, in minor scale, mica, since the earlier magmatic stages.As previously described, plagioclase and alkali feldspar crystallized together with later amphibole and apatite, showing that the crystallization of Gameleira lamprophyric magmas started under water-saturated conditions.Ba and Sr distribution in Gameleira lamprophyres is controlled by alkali feldspar and plagioclase crystallization, and the incompatibility of these elements was pointed out.Ba partition coefficient for plagioclase varies from 10 to 17, whereas for alkali feldspar this value is below the unity.Sr distribution is preferentially controlled by plagioclase, with values between 6.6 and 9.5, against 2 to 6.6 for alkali feldspar.According to Rock (1991), feldspar of lamprophyres is normally enriched in Ba and Sr.The crystallization order of Gameleira lamprophyres shows that the fractionation of the near liquidus mineral phases plus some pargasitic amphibole would produce monzonitic derived magmas enriched in Ba and Sr.
Low modal percentage of titanium-bearing phases restricted to some late-magmatic titanite and Fe-Ti oxides is a consequence of the Ti-poor original composition of the magma.In Cara Suja (Paim et al. 2002) and Morro do Afonso lamprophyres (Plá Cid et al. 2006) the same characteristic was described, as well as in the Piquiri lamprophyres (Plá Cid et al. 2003).
The pressure dependence of IV Al in the amphibole is suggested for these lamprophyres, by decreasing of 2.16 apfu (pargasite) to 1.32 apfu (more evolved edenite), although, its use as a geobarometer is hardly admitted, since the paragenesis and rock chemistry are different from those used in the proposition of Hollister et al. (1987) and Schmidt (1992).Such chemical evolution of the amphibole is also controlled by increasing fO 2 -conditions.This is corroborated by the increase in the Mg/(Mg+Fe) ratio due to coupled substitution Mg-Fe +3 (Figure 13), and crystallization in the later magmatic stages of iron oxides.A similar behavior has been observed in other alkaline lamprophyres in NE Brazil (i.e.Cara Suja and Morro do Afonso lamprophyres) and spessartites from Volcanic Association of Lavras do Sul, Brazil (Lima and Nardi 1998).
A two-feldspar equilibrium geothermometer was developed by Stormer (1975).Using the curves proposed by this author, between 5 and 10 kb, and compositions of alkali feldspar and plagioclase rims in contact with each other, nearsolidus temperatures were determined for these lamprophyres as close to 600°C.The liquidus temperature of Gameleira lamprophyre magma can be estimated using the experimental determinations of Esperança and Holloway (1987) for minette lamprophyres.These authors found olivine-free near-liquidus paragenesis, dominated by diopside and phlogopite, as now reported in the Gameleira lamprophyres, in systems with temperatures around 1070°C and pressures of 10 kb.Taking into account the similarity between magma compositions and liquidus mineralogy, such temperatures and pressures may be assumed to the Gameleira lamprophyre magma.Then, a range around 450°C can be estimated between liquidus and solidus temperatures of Gameleira lamprophyres, and a similar temperature contrast existed between lamprophyric magma and the host monzonite at the time of the intrusive event.

Whole Rock Geochemistry
Morro do Afonso lamprophyres have lower concentrations of MgO (6.8 to 7.7wt.%)and P 2 O 5 (1.5wt.%), and higher K 2 O (4.1 to 4.9wt.%),Al 2 O 3 (10.6 to 11.2wt.%),and K 2 O/Na 2 O ratios (3 -4) relative to Gameleira lamprophyres (Table V).According to several authors (Loyd et al. 1985, Foley 1992, Foley and Peccerillo 1992, Ionov et al. 1997, and references therein), pyroxene, apatite, phlogopite and amphibole are the usual phases found in the upper mantle metasomatized zones.As emphasized by Foley (1992), different proportions of these minerals and, to a lesser extent, of typical mantle phases (garnet, olivine, spinel) participating in the melting processes may explain the diversity of alkaline potassium-enriched magmas.The comparison between Gameleira and Morro do Afonso primary magmas puts in evidence the presence of higher proportions of potassium-rich phases in the source of these lamprophyres.The main carriers of potassium in the upper mantle are phlogopite and amphiboles (pargasite and richterite), and mica seems to be dominant in the metasomatic source of Morro do Afonso magmas, whereas relatively lower amounts of potassium in Gameleira lamprophyres may be related to higher proportions of amphibole at the source.This is also supported by the lower Al 2 O 3 values in Gameleira lamprophyres, suggesting lower amounts of phlogopite at the source.Apatite is an abundant phase in both sources, as attested by high P 2 O 5 in both lamprophyres; and, clinopyroxene is dominant in the source of Gameleira, as deduced from its higher MgO content.Experimental data of Conceição and Green (2000) have shown the importance of phlogopite and pargasite melting in the upper-mantle, for the production of potassic liquids.Different melting rates of the same source could be an alternative hypothesis to explain some geochemical differences between Gameleira and Morro do Afonso lamprophyres.
The Cr concentrations of Gameleira lamprophyre, compared to Morro do Afonso rocks, confirm the supposition of higher proportions of clinopyroxene at its source.Low to moderate Ni concentrations in both indicates an olivine-free source.Ba contents are similar in both associations, and are probably concentrated by different K-rich phases (mica and amphibole) at the source of both primary magmas.O' Reilly and Griffin (2000) suggested that apatite is the main carrier of LREE in the mantle.Slightly higher contents of P 2 O 5 in Gameleira magmas (Table V) are in agreement with the higher concentrations of elements such as La, Ce and Nd when compared to Morro do Afonso lamprophyres (Table V; Figure 11).Considering the concentrations of compatible elements in Morro do Afonso and Gameleira lamprophyres, a higher melting rate would be expected for the source of Gameleira magma.This can explain the lower amounts of K and Al in Gameleira rocks, but not the concentrations of LREE and P, higher in these rocks than in the ultrapotassic Morro do Afonso lamprophyres.In this way, slight mineralogical differences at the source and different melting rates can explain the differences in geochemical patterns of both lamprophyre magmas.
Gameleira lamprophyres represent potassic liquids, with a geochemical signature typically related to a mantle-source affected by metasomatic process related to dehydration and/or melting of subductedslab.Very high concentrations of MgO, P 2 O 5 , Cr, Ba, Cs and LREE are indicative of a mantle-source enriched in apatite and clinopyroxene, whereas the moderate amounts of K 2 O when compared with the contemporaneous ultrapotassic liquids from Morro do Afonso Massif suggest higher proportions of amphibole relative to mica.The water-saturated primary magmas of Gameleira lamprophyres is another evidence of the presence of amphibole and mica in the mantle source.
The comparison of both primary magmas from Gameleira and Morro do Afonso lamprophyre associations forming bodies separated just by a few kilometers on the field and, probably contemporaneous, is a strong argument for mantle heterogeneity as the main cause of different types of alkaline liquids.The identification of different mineral paragenesis in the source of ultrapotassic and potassic lamprophyres from São Francisco Craton constitutes a useful approach for understanding the mantle and crustal evolution in northeastern Brazil.

Figure 4 .
Figure 4. Si+Na+K vs. Al+Ba diagram showing the substitutional scheme observed in alkali feldspars evolution of Gameleira lamprophyres.

Figure 10 .
Figure 10.Discriminatory diagram among shoshonitic, tholeitic and calc-alkaline series using trace and rare earth elements, proposed by Muller et al. 1992.Gameleira rocks are into the shoshonitic compositional field.
380JORGE PLÁ CID, CRISTIANI S. CAMPOS, LAURO V.S. NARDI and LUANA FLORISBAL the monzonite with straight and non-reactive contacts.These dykes are tabular intrusions, less than 0.5 m wide and more than 50 m long.These rocks are mafic, fine-grained, with black and dark green color.
03mm.Euhedral apatite, mica and colorless clinopyroxene grains are included in the amphibole and are also oriented by the magmatic flow.The paragenesis formed by clinopyroxene-apatite-mica constitutes the near-liquidus assemblage.Subhedral apatite crystals are also associated with the latemagmatic interstitial minerals.Pyroxene and mica are limited to the near-liquidus stages.Subhedral yellowish allanite grains are included in amphibole and are therefore interpreted also as a nearliquidus mineral, pointing to a rare earth elements (REE) enriched liquid.Titanite occurs as anhedral crystals included in the amphibole, with sinuous contacts suggesting late-magmatic exsolution from the amphibole.Felsic minerals are interstitial, consisting of alkali feldspar and plagioclase.