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Agenor Faria 
  
Luana Oliveira 
  
Maria Cristina De Souza 
  
Kazutoshi Matsugano 
  
Aos Professores Do 
  
Carlos Eduardo De Mesquita Barros 
  
José Manoel 
  
Dos Reis 
  
Eleonora Maria Gouvêa Vasconcellos 
  
Cristina Valle Pinto-Coelho 
  
José Nadalin 
  
Secchi E Keiji 
  
Leonardo Professores 
  
Cury 
  
Eleonora 
  
Alain Vauchez 
  
Michel Lopez 
  
Jean-Jacques Cornee 
  
Bernard Boyer 
  
Christophe Nevado 
  
Anne À Delplanque 
  
Carolina Professora 
  
Cavalcante 
  
Aos Amigos Geólogos 
  
Daniela Zaramella 
  
José Eduardo Morais 
  
Pela Amizade 
  
  
  
  
  
  
  
  
  
  
  
  
  
  
  
  
  
  
  
  
  
  
  
Keywords: magmatismo alcalino, carbonatito, magma parental, isótopos, idades argônio alkaline magmatism, carbonatite, parental magma, isotopes, Ar ages magmatisme alcalin, carbonatite, magma parental, géochimie isotopiques, géochronologie Ar-

doutoramento no país e

INTRODUCTION

La plupart des carbonatites connues à travers le monde sont spatialement et temporellement associés à des complexes mafiques alcalins. Ceci sous-entend des liens pétrogénétiques possibles et, par conséquent, et que la relation entre les roches silicatées et carbonatitiques est essentielle dans les études petrologique et métallogénique dédiées à explorer leur genèse. Cependant bien qu'un lien de génétique plus ou moins direct des carbonatites depuis un magma silicaté soit souvent supposé (e.g. [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF][START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF], des études expérimentales et certains cas naturels suggèrent la possibilité d'autres scénarios. [START_REF] Gittins | Myth and reality in the carbonatite -silicate rock "association[END_REF] attribuent la popularité du modèle de genèse des carbonatites depuis les roches silicatées à l'évolution de notre connaissance des carbonatites. Selon ces auteurs, l'origine magmatique de carbonatites n'a pas été largement acceptée jusqu'à la fin des années 1950, une époque où on savait peu sur la composition du manteau et sur l'origine mantellique des magmas. Ainsi, la relation spatiale avec les roches silicatées a conduit les pétrologues à supposer un lien génétique entre ces roches (un « axiome », selon Harmers et [START_REF] Gittins | Myth and reality in the carbonatite -silicate rock "association[END_REF]. Les études expérimentales et l'analyse des systèmes naturels qui ont suivi (et qui appuient les modèles de relation génétique) seraient, selon ces auteurs, sélectives et tendancieuses: pour expliquer l'origine de carbonatites, on requiert la présence des roches silicatées souvent associées, sans tenir compte de l'existence de plus de 70 occurrences de carbonatite isolé [START_REF] Woolley | Igneous silicate rocks associated with carbonatites: their diversity, relative abundances and implications for carbonatite genesis[END_REF]. Ceci suggère que l'on doit tenir compte de tous les modèles possibles de pétrogenèse pour les carbonatites comme pour les autres roches magmatiques [START_REF] Bell | Carbonatitesinto the twenty-first century[END_REF][START_REF] Mitchell | Carbonatites and carbonatites and carbonatites[END_REF]. À cet égard, trois modèles sont classiquement mentionnés: (1) la fusion directe du manteau [START_REF] Wallace | An experimental determination of primary carbonatite magma composition[END_REF][START_REF] Thibault | Experimental investigation of melts from a carbonated phlogopite lherzolite: implications for metasomatism in the continental lithospheric mantle[END_REF][START_REF] Dalton | The compositions of primary carbonate melts and their evolution through wallrock reaction in the mantle[END_REF]Lee et Wyllie. 1998;Harmer et al, 1998;[START_REF] Harmer | The case for primary, mantle-derived carbonatite magma[END_REF][START_REF] Srivastava | Emplacement age and isotope geochemistry of Sung Valley alkalinecarbonatite complex, Shillong Plateau, northeastern India: implications for primary carbonate melt and genesis of the associated silicate rocks[END_REF] (2) la cristallisation fractionnée à partir d'un magma silicaté (e.g. [START_REF] Lee | Experimental data bearing on liquid immiscibility, crystal fractionation, and the origin of calciocarbonatites and natrocarbonatites[END_REF][START_REF] Brassinnes | Magmatic evolution of the differentiated ultramafic, alkaline and carbonatite intrusion of Vuoriyarvi (Kola Peninsula, Russia). A LA-ICP-MS study of apatite[END_REF] (3) l'immiscibilité entre liquides (e.g. [START_REF] Bas | Carbonatite-Nephelinite Volcanism[END_REF][START_REF] Hamilton | The behaviour of trace elements in the evolution of carbonatites[END_REF]Lee et Wyllie, 1998).

En ce qui concerne les roches alcalines et ultramafiques fréquemment associées aux carbonatites, les processus de genèse invoqués sont également variables. Alors que l'évolution d'un seul stock de magma parental est proposé pour certaines unités (e.g. [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF][START_REF] Brassinnes | Magmatic evolution of the differentiated ultramafic, alkaline and carbonatite intrusion of Vuoriyarvi (Kola Peninsula, Russia). A LA-ICP-MS study of apatite[END_REF], on voit aussi des modèles qui proposent plusieurs injections d'une même magma parent (e.g. [START_REF] Verhulst | Petrological and geochemical (trace elements and Sr-Nd isotopes) characteristics of the Paleozoic Kovdor ultramafic, alkaline and carbonatite intrusion (Kola Peninsula, NW Russia)[END_REF][START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF], ou de magmas avec des compositions différents (e.g. Melluso et al, 2014) et aussi le mélange de magmas plus ou moins évolués (e.g. [START_REF] Arzamastsev | Geochemical indicators of the evolution of the ultrabasic-alkaline series of Paleozoic massifs of the Fennoscandian shield[END_REF].

Cette diversité empêche la proposition d'un modèle général pour les unités de ce type, de sorte que chaque exemple doit être considéré individuellement, compte tenu de ses particularités.

CONTEXTE GEOLOGIQUE

Depuis l'ouverture de l'océan Atlantique, la dernière phase d'activation de la Plateforme Sud-Américaine (Jurassique supérieur - [START_REF] Almeida | The origin and evolution of the South American Platform[END_REF] comprend des épisodes magmatiques de compositions tholéiitiques et alcalines. Dans la partie sud de la plate-forme, l'activité basaltique tholéïtique a donné naissance à la Province Magmatique du Paraná (134,7 ± 1 Ma, [START_REF] Thiede | Parana flood basalts: Rapid extrusion hypothesis confirmed by new 40 Ar/ 39 Ar results[END_REF], l'une des plus importantes provinces de basaltes continentaux du monde. Son équivalent alcalin se présente sous la forme de plusieurs corps intrusifs (plugs, stocks et diques) avec une large gamme de compositions : saturées en SiO 2 ou non saturées, des roches ultrabasiques, carbonatites et / ou kimberlites.

Dans la partie centre-sud-est de la plate-forme, les affleurements alcalins sont situés aux bords du Bassin du Paraná (Gomes et Comin-Chiaramonti, 2005). Le cadre tectonique contrôlant cette répartition de l'activité alcaline reste controversé, bien qu'il soit clairement associé aux limites du bassin. Néanmoins, les intrusions du littoral méridional et central sont généralement liées à l'arche de Ponta Grossa [START_REF] Almeida | Relações tectônicas das rochas alcalinas Mesozoicas da região Meridional da Plataforma Sul-americana[END_REF][START_REF] Riccomini | Tectonic controls of the Mesozoic and Cenozoic alkaline magmatism in the central-southeastern Brazilian Platform[END_REF], une structure de direction NW-SE matérialisée par des essaims de filons basaltiques du PMP et actives depuis le Crétacé Inferieur. Parmi les quatre alignements de tendance N40-60W qui contrôlent le cadre structurel de l'arche de Ponta Grossa (Guapiara, São Jerônimo-Curiúva, Rio Alonso et Rio Piquiri), les secteurs sud des alignements Guapiara et São Jerônimo-Curiúva présentent certaines unités alcalines et carbonatites parallèles à leur axe (Ruberti et al., 2005). Deux principaux chronogroupes, du Crétacé Inférieur et du Crétacé Supérieur, sont individualisés [START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF]. Aucune donnée géochronologique de haute précision n'est actuellement disponible pour le chronogroupe le plus ancien (seuls des âges K/Ar ou Rb/Sr sont publiés) et l'extension de cet épisode alcalin n'est pas définie avec précision. Trois complexes du Crétacé Inférieur sont liés au linéament de Guapiara, et le Complexe de Jacupiranga (~ 65 km 2 ) est le plus grand d'entre eux.

LE COMPLEXE DE JACUPIRANGA

Le Complexe de Jacupiranga (Figure 1) est une unité ultrabasique alcaline et carbonatitique qui couvre une surface de 65 km 2 près de la ville de Cajati, située à environ 240 km au sud-ouest de la ville de São Paulo (État de São Paulo, Brésil). Il affleure au milieu de granites et de roches métasédimentaires Néoprotérozoïque. Pendant que sa moitié nord est constituée principalement de dunite, entourée par une zone de roches syénitique et dioritique, la partie sud est composée d'ijolites/melteigites, de clinopyroxenites et de carbonatites.

L'origine de cette unité est liée à des évènements magmatiques possiblement associés à la rupture de l'extrémité ouest du Gondwana et à l'ouverture de l'Océan Atlantique Sud [START_REF] Herz | Timing and spreading in the South Atlantic: Kimberlite Conference, Araxa. Brasilia, DF: CPRM, Special information from Brazilian alkaline rocks[END_REF]. Ces événements se caractérisent par l'éruption des basaltes de plateaux continentaux de la Province Magmatique du Paraná (Crétacé Inférieur) et peut-être aussi par l'intrusion de plusieurs unités alcalines (avec ou sans carbonatite).

Le Complexe de Jacupiranga est exploité depuis 70 ans, le minerai étant formé par les carbonatites, riches en apatite, dont on extrait le phosphate nécessaire aux engrais.

Comme le manteau latéritique carbonaté original a été épuisé dans les années 70, aujourd'hui la roche saine constitue le matériel exploité. De façon générale, la moitié sud du Complexe de Jacupiranga est formée principalement par des clinopyroxènites de texture grenue et cumulative. Les cristaux de clinopyroxène sont fortement orientés (phase cumulus) avec des minéraux opaques interstitiels (phase intercumulus). Dans l'ouest de cette unité un corps de roche ijolitique (texture micro grenue ou grenue) affleure en forme de demi-lune. Cette roche présente des niveaux alternéscomposés essentiellement de clinopyroxène ou de néphéline (cumulus) ou par l'association néphéline plus clinopyroxène (cumulus), déterminant un litage magmatique.

Les carbonatites forment un corps allongé qui intrude la clinopyroxenite. L'apatite se trouve sous la forme de poches, de niveaux plus ou moins continus ou disséminée dans la roche.

Autour des dunites, il y a une zone hétérogène que [START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF] désignent de « transition/assimilation ». Elle est formée par des roches syénitiques (syénite à feldspath alcalin et melasyenite), des roches dioritiques (meladiorite et diorite), des lamprophyres et des dykes de phonolite. Par rapport au reste du complexe, cette zone diffère par sa considérable diversité des lithotypes affleurants dans une surface relativement petite. En comparaison, alors que l'unité clinopyroxènitique (~20 km²) est formée seulement de clinopyroxènite et de melteigite, il y a sept lithotypes dans la zone hétérogène (~9 km²). Audelà de la relation variété lithologique/surface d'affleurement élevée, les roches dans cette zone ont une continuité latérale limitée (décamétrique ou hectométrique). En ce qui concerne les dunites, la pénurie d'affleurement de roche saine (qui est observée seulement dans les forages) liée à la très forte latérisation, la grande épaisseur du manteau d'altération et le grand niveau de serpentinisation entravent l'obtention des informations petrologiques précises sur ces roches.

OBJECTIFS DE CETTE RECHERCHE

Bien que les premièrs travaux de repérage du complexe remontent au XIXe siècle, de nombreux aspects restent mal connus à Jacupiranga. La principale explication en est la quasi absence d'études pétrogénétiques couvrant tous les types de roches constituant l'unité et notamment les roches silicatées. A cause de leur minéralisation, les études se sont jusqu'ici concentrées sur les carbonatites, alors que cette roche représente seulement ~1% de la surface d'affleurement du Complexe de Jacupiranga. La grande majorité des roches, silicatée, a été très peu étudiée alors même que seule une vision globale de ce massif dans toute sa diversité pétrologique permettra de comprendre sa genèse.

Ce sont précisément les travaux pionniers de cartographie [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF][START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF][START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] qui englobent la plus grande variété de types de roches et proposent les modèles pétrologiques les plus complets pour l'unité. Cependant, peut-être en raison des limitations techniques de l'époque, l'absence de données géochimiques et isotopiques ne permet pas une étude pétrogénétique approfondie. Le Complexe de Jacupiranga est aussi abordé dans sa totalité au travers de quelques travaux régionaux ou qui concernent plusieurs unités alcalines d'une région particulière, tels que l'Arche de Ponta Grossa ou du Sud-Est Plate-forme en Amérique du Sud (e.g. [START_REF] Morbidelli | The Pariquera Açu K-alkaline complex and southern Brazil lithospheric mantle source characteristics[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF][START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF]. Aucun de ces études n'est consacrée spécifiquement à Jacupiranga.

Il n'y a pas, de plus, de données géochronologiques robustes disponibles pour les complexes du Crétacé inférieur liés à la région de l'Arche de Ponta Grossa, parmi lesquels le Complexe Jacupiranga. Par conséquent, l'extension du magmatisme dans la région manque d'une définition plus précise [START_REF] Amaral | Potassium-argon ages of alkaline rocks from southern Brazil[END_REF][START_REF] Amaral | Potassium-argon age studies on the Jacupiranga alkaline district, State of São Paulo, Brazil[END_REF][START_REF] Roden | Sr and Nd Isotopic Composition of the Jacupiranga Carbonatite[END_REF].

Mon travail vise à proposer une vision globale et intégrée de l'ensemble du complexe pour en comprendre la génèse à travers plusieurs objectifs :

• Définir les relations temporelles entre les différents roches qui composent le Complexe Jacupiranga, sur la base de données géochronologiques robustes, pour tenter d'en établir une chronologie relative et l'ordre de mise en place des différentes unités;

• Réaliser la caractérisation petrologique du Complexe de Jacupiranga, prenant en compte les roches silicatées et les carbonatites. Les objectifs spécifiques de ce point sont l'identification des magmas parents potentiels, des sources manteliques et la détermination des processus évolutifs qui ont formé les roches silicatées et les carbonatites.

MÉTHODES UTILISÉES

Pour répondre à ces questions, six fronts d'étude ont été développés: 1) campagnes de terrain; 2) analyses pétrographiques; 3) chimie minérale (clinopyroxène, olivine, amphibole, micas et feldspath); 4) géochimie des roches totales (majeurs et traces); 5) géochimie isotopique (Sr-Nd-Pb-Hf); et 6) analyses géochronologiques ( 40 Ar/ 39 Ar et U-Pb SHRIMP).

DISCUSSION

GEOCHRONOLOGIE

Les datations 40 Ar/ 39 Ar sur micas et U-Pb sur zircons sur de différentes lithologies permettent de déterminer l'intervalle de mise en place du Complexe de Jacupiranga. Les âges 40 Ar/ 39 Ar varient entre 133,7 ± 0,5 Ma et 131,9 ± 0,5 Ma, tandis que l'âge U/Pb concordia calculé pour la monzonite est de 134,9 ± 0,65 Ma. La similitude entre les valeurs obtenues par ces deux méthodes différentes (U-Pb: 134,9 ± 0,65 Ma et 40 Ar/ 39 Ar: 133,7 ± 0,5 Ma) sur la monzonite indiquent que la mise en place de la monzonite a eu lieu à faible profondeur et son refroidissement a été assez rapide suggérant que les âges 40 Ar/ 39 Ar signent la mise en place des roches et non leur refroidissement. Bien qu'il ne soit pas possible de définir une séquence précise de mise en place entre les différentes lithologies compte tenu du recouvrement entre les âges 40 Ar/ 39 Ar, la monzonite présente clairement l'âge 40 Ar/ 39 Ar et U-Pb le plus ancien, et toute l'évolution de l'unité a eu lieu dans un temps relativement court (environ 4 Ma).. Dans le contexte régional, la mise en place du complexe Jacupiranga a été remarquablement contemporaine de l'extrusion de basaltes tholéiitiques de Province Paraná magmatique ( 40 Ar/ 39 Ar: 134,7 ± 1 Ma, [START_REF] Thiede | Parana flood basalts: Rapid extrusion hypothesis confirmed by new 40 Ar/ 39 Ar results[END_REF].

SÉRIES MAGMATIQUES

Sur la base de la géochimie des roches silicatées de Jacupiranga et de leurs minéraux, deux séries magmatiques sont proposées (Figure 2): (1) une série fortement soussaturée en silice, éventuellement liée à un magma parental de composition néphélinitique et

(2) une deuxième série modérément sous-saturée, liée à un magma basanitique dont les lamprophyres du complexes sont les plus proches équivalents. À la série fortement soussaturé se rapportent les roches ijolitiques et certaines clinopyroxénites (en particulier celles qui présentent de la néphéline modale), tandis que la série modérément sous-saturée est formée des roches à feldspaths, des lamprophyres et d'une partie des clinopyroxénites. La cristallisation de clinopyroxène (formant à présent des roches cumulatives), d'olivine et de Timagnétite a joué un rôle majeur dans l'évolution des deux séries. Dans la série fortement sous-saturée, ce fractionnement a déclenché l'apparition de néphéline dans le système, produisant les melteigites et, selon l'augmentation de la proportion néphéline/clinopyroxène, les ijolites et urtites. Dans le cas de la série modérément sous-saturés, la cristallisation de plagioclase a permis la genèse des roches à feldspath. Si cette dernière série semble dériver essentiellement par fractionnement progressif, elle montre aussi une certaine hétérogénéité de détail et les modèles peinent à reconstituer une lignée de différenciation unique.

La forte altération des dunites entrave l'identification de leurs textures primaires.

Cependant, la composition des cristaux d'olivine (Fo 83-84 , CaO 0,13-0,31 wt.% et NiO 0,19-0,33 wt.%) indique que cette phase a été générée par processus de cristallisation fractionnée. Cette interprétation diffère de celle proposée par [START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF] qui, sur la base des données de roches totales, ont considéré une origine mantelique pour les dunites. Les modèles thermodynamiques MELTS indiquent que les cristaux d'olivine Fo 83-84 peuvent être fractionné soit à partir des magmas basanitiques soit depuis des magmas néphélinitique. Donc les dunites peuvent être liées à l'une ou l'autre des deux séries silicatées proposées pour le complexe.

Figure 2 -Diagrammes de classification pour les roches silicatées du Complexe de Jacupiranga. Les champs rosés representent les données compilées pour les roches encaissantes [START_REF] Faleiros | Geologia e Recursos Minerais da Folha Eldorado Paulista -SG-22-X-B-XI, estado de São Paulo[END_REF]. Données de Jacupiranga compilées selon [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF]. (A) Diagramme alcalins totaux vs. SiO 2 (Le [START_REF] Le Bas | The construction of the Total Alkali-Silica chemical classification of volcanic rocks[END_REF]. (B) Diagramme R1-R2 [START_REF] De La Roche | A classification of volcanic and plutonic rocks using R1-R2 diagram and major-element analyses. Its relationships with current nomenclature[END_REF]. En gris, sont representées les compositions moyennes des principales phases minerales de Jacupiranga.

MAGMAS PARENTAUX DES ROCHES SILICATEES

Les lamprophyres, classés chimiquement dans le champs des téphrites ou basanites, sont considérés représentatifs de la composition du magma parental de la série modérément sous-saturée en silice. De fait, les diagrammes d'éléments de terres rares (ETR) des lamprophyres s'apparentent fortement aux roches avec feldspath et aux phonolites du complexe. Parmi celles-ci, les roches les plus évoluées sont les plus appauvries en ETR, indiquant que la Zone Heterogène s'est formée par la cristallisation fractionnée d'un magma basanitique. Pour les clinopyroxénites, les valeurs du Mg# du liquide en équilibre avec les coeurs de clinopyroxène sont identiques au Mg# (roche totale) des lamprophyres. En outre, la composition ETR des liquides calculés en équilibre avec ces pyroxènites sont similaire aux lamprophyres.

Ainsi, le modèle pétrologique proposé pour les roches avec feldspath ainsi qu'une partie des clinopyroxénites suggère des intrusions de magma basanitique, dont les phases fractionnées ont été déposées dans des chambres magmatiques de faible profondeur. Des filons de lamprophyres recoupant les syenites cela suggère une récurrence de ces injections, en accord avec les variations de composition observées sur les liquides calculés en équilibre.

Les caractéristiques du magma parental néphélinitique sont difficiles à définir car il ne semble subsister aucun équivalent actuellement à l'affleurement dans le complexe.

Cependant, un liquide néphélinitique est classiquement associé à de nombreuses unités ultramafiques alcalines dans différentes provinces à travers le monde. De plus des roches de cette composition ont été trouvées dans le Complexe Anitápolis, qui partage de nombreuses similitudes avec Jacupiranga (e.g. l'âge du Cretacé Inferieur, composition, contexte tectonique), et où elles sont considérées comme représentatives du magma parental.

EVIDENCES DE CONTAMINATION CRUSTALE MODEREE

Les échantillons de monzonite et de meladiorite présentent des caractéristiques pétrographiques, compositionnelles et isotopiques (monzonite : 87 Sr/ 86 Sri de 0,706086 meldiorite : 143 Nd/ 144 Ndi de 0.511867) qui suggérent que des processus d'assimilation crustale ont exercé un rôle actif dans la genèse de ces roches. Les rapports isotopiques de Nd et Sr de la monzonite et de la meladiorite sont compatibles avec une courbe de mélange calculée à partir de la composition d'un lamprophyre et des roches métasédimentaires de la région (Figure 3). Cependant, ces processus ont un caractère local, et limité à quelques intrusions de magma basanitique. Bien qu'il ne soit pas possible d'exclure complètement la possibilité de contamination pour les roches syénitiques, cela peu probable compte tenu de l'absence de témoins pétrographiques et des rapports isotopiques similaires à ceux des clinopyroxénites et carbonatites qui n'ont pas été affectées par les processus de contamination crustale selon [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF].

L'ORIGINE DES CARBONATITES

Classiquement, les études sur l'origine des carbonatites considèrent trois modèles possibles différents: (1) l'origine directe depuis la fusion partielle d'un manteau metasomatisé ou dérivation par (2) cristallisation fractionnée ou (3) immiscibilité de liquides depuis un unique magma parental silicaté.

Les magmas parentaux des deux series silicatées proposées à Jacupiranga peuvent produire des carbonatites par immiscibilité de liquide. Toutefois, malgré des similitudes entre les rapports initiaux de 87 Sr/ 86 Sr, les carbonatites ont des compositions isotopiques de Nd et Pb différentes de celles des roches silicatées. Les lamprophyres, phonolite et nephelinesyenites présentent des rapports Ba/La plus élevés que les carbonatites (Figure 4), ce qui empêcherait une origine par immiscibilité de liquide depuis les magmas parentaux des séries silicateés, si on prend en compte les critères expérimentaux de Hamilton et al. (1989) et petrologique de Harmer (1999) et [START_REF] Srivastava | Emplacement age and isotope geochemistry of Sung Valley alkalinecarbonatite complex, Shillong Plateau, northeastern India: implications for primary carbonate melt and genesis of the associated silicate rocks[END_REF]. Les carbonatites dolomitiques montrent néanmoins des rapports Zr/Hf subcondritiques, en accord avec à la composition des carbonatites considérées comme issues de processus d'immiscibilité (e.g. [START_REF] Thompson | Ankerite carbonatite from Swartbooisdrif, Namibia: the first evidence for magmatic ferrocarbonatite[END_REF]. Mais il faut pour cela spéculer de l'existence d'un magma silicaté qui ne serait pas actuellement reconnu dans l'unité. 86 Sr i vs. 143 Nd/ 144 Nd i pour les roches du Complexe de Jacupiranga. Une courbe de mélange (depuis les formules d [START_REF] Albarède | Introduction to Geochemical Modeling[END_REF] a été proposée pour évaluer les processus d'assimilation crustale (depuis la composition du lamprophyre JAC46.2). Le contaminant représentatif est une roche métasédimentaire de Siga Jr. et al. (2011) -87 Sr / 86 Sr 0,91788 et 143 Nd/ 144 Ndi 0,511390. Les champs indiquent les données compilées pour les carbonatites de Jacupiranga (CARB, de Roden et al., 1987[START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF], les clinopyroxénites (CPX, de Huang et al., 1995) et les syénites (SYE, de Ruberti et al. 2005).

Figure 4 -Variation Ba/La vs. Mg# pour les roches du Complexe de Jacupiranga. Données compilées depuis [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF].

Comme les carbonatites de Jacupiranga ne sont pas dérivés depuis les magmas parental proposés pour les roches silicatées, une origine primaire doit être envisagée. Ceci suggère que leur signature isotopique sont des caractères primitifs qui reflètent, par conséquent, les sources mantelliques dont ces roches dérivent. Un magma carbonatitique avec Ca/Mg <1 peut être généré par fusion partielle aux profondeurs supérieures à 70 km et, pendant son ascension, interagir avec le manteau lherzolitique, ce qui aboutit à une composition plus enrichie en calcium du liquide. [START_REF] Srivastava | Emplacement age and isotope geochemistry of Sung Valley alkalinecarbonatite complex, Shillong Plateau, northeastern India: implications for primary carbonate melt and genesis of the associated silicate rocks[END_REF] proposent par ailleurs que les différences isotopiques entre les roches alcalines et les carbonatites du Complexe de Sung Valley (Inde) sont reliées à l'ordre de mise en place des magmas parentaux. Le magma silicaté, généré et mis en place avant les carbonatites, possède alors la signature isotopique la plus enrichie. Cette relation pourrait être une explication pour les différences isotopiques en Nd entre les roches silicatées et les carbonatites de Jacupiranga.

SOURCE MANTELLIQUE

Bien que certains échantillons (monzonite et meladiorite) présentent des preuves de contamination crustale, les compositions isotopiques et trace de la majorité des roches du complexe reflétent vraisemblablement les caractéristiques des sources mantelliques.

Un mécanisme de fusion « vein-plus-wall-rock » [START_REF] Foley | Vein-plus-wall-rock melting mechanisms in the lithosphere and the origin of potassic alkaline magmas[END_REF] est généralement proposé pour expliquer le large spectre compositionel des associations alcalines. La composition chimique des lamprophyres (CaO/Al 2 O 3 : 0,74-1,72) et des liquides calculés en équilibre avec le clinopyroxene des clinopyroxénites (rapports La N /Zr N élevés et Ti N /Eu N faibles) indiquent des événements métasomatiques de caractère carbonaté dans la source mantellique. Ce metasomatisme a conduit à la formation de veines wehrlitiques dans le manteau peridotitique. La prédominance de la composante enrichie est aussi indiquée par les faibles rapports initiaux de Nd et Hf. De plus les variations du rapport Hf/Y, suggèrent une variation de la proportion cpx/grenat à la source. Toutes ces différences ne peuvent pas être expliquées par un modèle simple qui ne tiendrait en compte que des taux de fusion partielle différents (Figure 5). Ces variations sont interprétées comme le résultatdu mélange (en différentes proportions) d'un liquide généré par la fusion des filons wehrlitiques (plus enrichis) et par la fusion de la péridotite encaissante (plus appauvrie).

Les lamprophyres sont chimiquement similaires aux basaltes riches en Ti de la Province Magmatique du Paraná : ils se caractérisent par un appauvrissement en Nb-Yb, et un enrichissement en ETR léger par rapport aux ETR lourdes, ainsi que par un enrichissement en Cs, Rb et Sr. Ces caractéristiques suggèrent que la source mantellique a été metasomatisée par les fluides liées à des processus de subduction, tel que proposé par Rocha-junior et al. (2013) pour la source des roches tholéitiques.

Ces hyptohèses sont renforcées par les données isotopiques Nd-Sr-Pb-Hf qui indiquent une contribution importante du manteau sous-continental lithosphérique (SCLM) dans la genèse des roches du Complexe de Jacupiranga. Dans leur ensemble, les échantillons analysés se trouvent dans le domaine de magmatisme alcalin-carbonatitique du sud-est de la Plate-forme Sud-Américaine [START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF] et se rapprochent du pôle du mantle enrichi du type 1 (EM1), avec une faible contribution du pôle HIMU (Figure 6). Cette signature implique un manteau lithosphérique sous-continental avec des caractéristiques hétérogènes, résultant de différents degrés de métasomatisme (e.g. [START_REF] Gibson | The Late Cretaceus impact of the Trindade Mantle Plume: Evidence from largevolume mafic, potassic magmatism in SE, Brazil[END_REF][START_REF] Gibson | The limited extent of plume-lithosphere interactions during continental flood-basalt genesis: Geochemical evidence from Cretaceous magmatism in southern Brazil[END_REF][START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF].

De plus les roches de la série modérément sous-saturée sont caractérisées par des valeurs négatives de ΔεHf généralement interprétées comme une indication de SCLM métasomatisé, tandis que les clinopyroxénites et ijolite (série fortement-saturée) ont des ΔεHf positifs, suggérant une contribution plus forte de grenat à la source de ces roches (les grenats et clinopyroxènes des péridotites mantelliques présentent un rapport 176 Hf/ 177 Hf plus radiogénique que le clinopyroxéne de la wehrlite). Ces faits peuvent être rapprochés du modèle de source présenté ci-dessus, où le basanite a été formée depuis une contribution plus importante des filons wehrlitiques, alors que le magma néphélinitique a été généré à partir de contributions un peu plus importantes des peridotites encaissantes.

Figure 5 -Diagrammes La N /Zr N vs. Hf N /Y N (normalisé au manteau primitif, [START_REF] Sun | Chemical and isotopic systematics of oceanic basalts: implications for mantle composition and processes[END_REF] pour les liquidds calculés en équilibre avec le coeur du clinopyroxène des clinopyroxenites. Ligne en pointillés : dykes de lamprophyre de la région de L'Arche de Ponta Grossa (Jacupiranga inclu) compilés depuis [START_REF] Menezes | The antecryst compositional influence on Cretaceous alkaline lamprophyre dykes, SE Brazil[END_REF]. Les modèles de fusion pour différentes sources mantelliques sont présentés [START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF]. Carré noir: veine metasomatique; Carré gris: roche encaissante. Résidus de la source: triangle inversé (gt-lherzolite hors-craton); diamants (manteau primitive gt-lherzolite); cercles (wehrlite théorique). Les chiffres indiquent le degré de fusion partielle. Données compilées à partir de [START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF]: champ vert clair, mesocumulats du Complexe de Juquiá; champ vert foncé, adcumulats du Complexe de Juquiá. Les âges modèle T DM indiquent l'hétérogénéité de la source mantellique et sont compatibles avec les valeurs obtenues pour les roches alcalines du Sud-Est de la Plate-forme Sud-américaine.

Les valeurs moyennes pour les âges modèles Nd (971 Ma ± 198) et Hf (1,1 ± 0,3 Ga) tombent dans la moyenne des unités liées au linéament de Guapiara. Ces âges sont donc interprétés comme indiquant que la source mantellique a été metasomatisée par les fluides associés à des événements de subduction d'âge Néoprotérozoïque (le cycle Brasiliano/Pan-africain), avec une certaine hétérogénéité régionale. Ces hétérogénéités dans les sources des unités alcalines brésiliennes à l'échelle régionale sont également visibles dans les rapports isotopiques de Hf, qui sont similaires à Jacupiranga et Catalão I [START_REF] Guarino | U-Pb ages, geochemistry, C-O-Nd-Sr-Hf isotopes and petrogenesis of the Catalão II carbonatitic complex (Alto Paranaíba Igneous Province, Brazil): implications for regional-scale heterogeneities in the Brazilian carbonatite associations[END_REF]) mais sont plus radiogéniques dans les peridotites de Goiás [START_REF] Carlson | Chemical and isotopic relationships between peridotite xenoliths and mafic-ultrapotassic rocks from Southern Brazil[END_REF].

En ce qui concerne le contexte géodynamique, les compositions isotopiques et traces des roches du Complexe de Jacupiranga suggèrent la contribution essentielle du manteau sous continental, sans besoin d'impliquer un composant asthénospherique tel qu'il pourrait être trouvé dans un panache mantellique de type « hot spot ».

LISTA DE ILUSTRAÇÕES

Figura 1 -Mapa rodoviário simplificado destacando o acesso a Cajati a partir de Curitiba, pela BR-116. Modificado a partir de [START_REF] Dnit | Mapa multimodal[END_REF] Figura 3 -Ocorrências alcalinas ao longo das margens da Bacia do Paraná, na região centro-sudeste da Plataforma Sul-Americana (modificado de [START_REF] Riccomini | Tectonic controls of the Mesozoic and Cenozoic alkaline magmatism in the central-southeastern Brazilian Platform[END_REF]: 1) Bacia Bauru (Cretáceo Superior); 2) Província Magmática do Paraná (Cretáceo Inferior); 3) Bacia do Paraná (Ordoviciano Superior ao Cretáceo Inferior); 4) Unidades alcalinas (losangos, Permiano-Triássico; quadrados, Cretáceo Inferior; triângulos, Cretáceo Inferior; círculos, Paleógeno); 5) Eixo dos principais arcos; 6) Principais zonas de fratura (Lineamentos Guapiara (GP), São Jerônimo-Curiúva (JC), Rio Alonso (RA) e Rio Piquiri (RP); 7) Lineamento Lancinha-Cubatão. . Rochas alcalinas e ultramáficas se associam espacial e temporalmente a carbonatitos em várias unidades intrusivas em diversas províncias ígneas ao redor do mundo (e.g. [START_REF] Le Bas | Nephelinites and carbonatites[END_REF][START_REF] Woolley | Igneous silicate rocks associated with carbonatites: their diversity, relative abundances and implications for carbonatite genesis[END_REF][START_REF] Downes | Petrogenetic processes in the ultramafic, alkaline and carbonatitic magmatism in the Kola Alkaline Province: A review[END_REF][START_REF] Srivastava | Emplacement age and isotope geochemistry of Sung Valley alkalinecarbonatite complex, Shillong Plateau, northeastern India: implications for primary carbonate melt and genesis of the associated silicate rocks[END_REF].

Dentre as rochas silicáticas mais comuns nestas unidades figuram clinopiroxenitos, rochas da série ijolítica e álcali-sienitos, além de peridotitos, dunitos e, por vezes, turjaitosmelilitolitos, em geral menos expressivos.

Contudo, as relações genéticas entre estes litotipos são complexas e ainda bastante discutidas. Apesar de um vínculo derivativo entre o magma silicático e os carbonatitos ser frequentemente assumido (e.g. [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF][START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF], estudos experimentais e alguns sistemas naturais sugerem cenários diferentes, nos quais a relação entre carbonatitos e rochas silicáticas reflete tão somente a justaposição de dois pulsos de magmas distintos. ocorrências isoladas de carbonatito [START_REF] Woolley | Igneous silicate rocks associated with carbonatites: their diversity, relative abundances and implications for carbonatite genesis[END_REF]. Portanto, o reconhecimento de que carbonatitos podem apresentar diferentes gêneses deve anteceder qualquer estudo petrológico que abranja estes litotipos [START_REF] Bell | Carbonatitesinto the twenty-first century[END_REF][START_REF] Mitchell | Carbonatites and carbonatites and carbonatites[END_REF]. Neste sentido, três modelos são classicamente invocados: (1) origem primária do magma carbonatítico, a partir da fusão direta do manto (e.g. [START_REF] Wallace | An experimental determination of primary carbonatite magma composition[END_REF][START_REF] Thibault | Experimental investigation of melts from a carbonated phlogopite lherzolite: implications for metasomatism in the continental lithospheric mantle[END_REF]Dalton e Wood, 1993;Lee e Wyllie, 1998;Harmer et al., 1998;Harmer e Gittins, 1998;[START_REF] Srivastava | Emplacement age and isotope geochemistry of Sung Valley alkalinecarbonatite complex, Shillong Plateau, northeastern India: implications for primary carbonate melt and genesis of the associated silicate rocks[END_REF]; (2) cristalização fracionada a partir de um magma silicático (e.g. Lee e Wyllie, 1994;[START_REF] Brassinnes | Magmatic evolution of the differentiated ultramafic, alkaline and carbonatite intrusion of Vuoriyarvi (Kola Peninsula, Russia). A LA-ICP-MS study of apatite[END_REF]; e (3) imiscibilidade de líquidos (e.g. e.g. [START_REF] Bas | Carbonatite-Nephelinite Volcanism[END_REF][START_REF] Hamilton | The behaviour of trace elements in the evolution of carbonatites[END_REF]Wyllie e Lee, 1998).

A despeito dos processos que lhes deram origem, em casos em que carbonatitos ocorrem espacialmente relacionados a rochas silicáticas, estudos petrológicos devem também abranger estes litotipos. No que concerne às rochas alcalinas e ultramáficas, seus processos de gênese são igualmente variáveis. Enquanto a evolução de um único pulso de magma parental é proposta para algumas unidades (e.g. [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF][START_REF] Brassinnes | Magmatic evolution of the differentiated ultramafic, alkaline and carbonatite intrusion of Vuoriyarvi (Kola Peninsula, Russia). A LA-ICP-MS study of apatite[END_REF], a outras é atribuída a recorrência de diversos pulsos de um magma parental de mesma composição (e.g. [START_REF] Verhulst | Petrological and geochemical (trace elements and Sr-Nd isotopes) characteristics of the Paleozoic Kovdor ultramafic, alkaline and carbonatite intrusion (Kola Peninsula, NW Russia)[END_REF][START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF], pulsos de magmas de diferentes composições [START_REF] Melluso | Mineral compositions and petrogenetic evolution of the ultramafic-alkaline -carbonatitic complex of Sung Valley, Northeastern India[END_REF] ou ainda mistura de magmas mais primitivos com pulsos mais evoluídos (e.g. Arzamastsev e Arzamastseva, 2013). Este panorama impede a proposição de modelos generalistas para unidades deste tipo, de modo a cada ocorrência dever ser considerada individualmente, considerando suas particularidades.

O Complexo de Jacupiranga (Cajati, SP) é uma unidade intrusiva mesozóica que abrange uma grande gama de litotipos, incluindo dunitos, clinopiroxenitos, ijolitos, rochas com feldspato, lamprófiros e carbonatitos. Estes, mineralizados em fosfato, foram extensamente investigados nas últimas décadas [START_REF] Mitchell | Manganoan magnesian ilmenite and titanian clinohumite from the Jacupiranga carbonatite, São Paulo, Brazil[END_REF]Gaspar e Wyllie, 1983;[START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF][START_REF] Costanzo | Fluid inclusions in apatite from Jacupiranga calcite carbonatites: Evidence for a fluid-stratified carbonatite magma chamber[END_REF], apesar de poucos estudos também abrangerem os litotipos silicáticos (e.g. [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF][START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF].

Consequentemente, a ausência de estudos petrológicos que considerem todos os litotipos do complexo confere uma compreensão compartimentada da sua origem, em geral restrita aos carbonatitos e clinopiroxenitos. [START_REF] Almeida | Relações tectônicas das rochas alcalinas Mesozoicas da região Meridional da Plataforma Sul-americana[END_REF][START_REF] Costanzo | Fluid inclusions in apatite from Jacupiranga calcite carbonatites: Evidence for a fluid-stratified carbonatite magma chamber[END_REF][START_REF] Salvioli-Mariani | Late veins of C3 carbonatite intrusion from Jacupiranga complex (Southern Brazil): fluid and melt inclusions and mineralogy[END_REF], justamente por este constituir o corpo mineralizado.

São justamente os trabalhos pioneiros de mapeamento da unidade [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF][START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF][START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] Grossa ou a região centro-sudeste da Plataforma Sul Americana (e.g. [START_REF] Morbidelli | The Pariquera Açu K-alkaline complex and southern Brazil lithospheric mantle source characteristics[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF][START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF], não focados exclusivamente neste complexo.

Não há dados geocronológicos robustos disponíveis para as ocorrências do

Cretáceo Inferior relacionadas à região do Arco de Ponta Grossa, dentre as quais o Complexo de Jacupiranga se inclui. Logo, a extensão do magmatismo na região ainda carece de uma definição mais precisa. As rochas do complexo foram analisadas pelos métodos K-Ar [START_REF] Amaral | Potassium-argon ages of alkaline rocks from southern Brazil[END_REF][START_REF] Amaral | Potassium-argon age studies on the Jacupiranga alkaline district, State of São Paulo, Brazil[END_REF] e Rb-Sr [START_REF] Roden | Sr and Nd Isotopic Composition of the Jacupiranga Carbonatite[END_REF], o último aplicado somente a amostras de carbonatito. -Fo (forsterita): Mg 2 SiO 4 ;

OBJETIVOS

MATERIAIS E MÉTODOS

I M 2-3 □ 1-0 T 2 O 10 A 2 ,
-Fa (faialita): Fe 2 SiO 4 .

Anfibólio

Foram realizadas 20 análises em cristais de anfibólio (Tabela A4 dos Anexos) em amostras de monzonito (JAC25) e de álcali-feldspato sienito (JAC32). O cálculo da fórmula estrutura seguiu as recomendações de [START_REF] Leake | Nomenclature of amphiboles. Report of the subcommittee on amphiboles of the International Mineralogical Association Commission on New Minerals and Mineral Names[END_REF], conforme a fórmula padrão:

AB 2 C VI 5 T IV 8 O 22 (OH) 2 .

Os componentes desta fórmula correspondem aos sítios cristalográficos:

A: 1 sítio por fórmula unitária B: dois sítios M4 por fórmula unitária C: 2 sítios M1, 2 M2 e 1 M3 por fórmula unitária; T: 8 sítios, em dois grupos de 4; "OH" dois sítios por fórmula unitária.

O cálculo foi realizado por meio da planilha de [START_REF] Locock | An Excel spreadsheet to classify chemical analyses of amphiboles following the IMA 2012 recommendations[END_REF] 

ISÓTOPOS RADIOGÊNICOS EM ROCHA TOTAL

Tendo por base os dados petrográficos e geoquímicos, 16 amostras de diferentes litotipos e 2 duplicatas foram selecionadas para análises de isótopos de Pb, Sr, Nd e Hf em rocha total. Após terem sido britadas e pulverizadas, 100 a 200 mg destas amostras foram lixiviados durante 1 hora em uma solução de HCl 6N à 95°C (exceto os carbonatitos). Em seguida, os resíduos foram purificados três vezes em água ultrapura e então dissolvidos em uma mistura de HF-HNO 3 (1:1) por 72 horas em uma placa de aquecimento. Após completamente secos, 1 ml de HNO 3 foi adicionada a estes resíduos, que foram mantidos em temperaturas de, em média, 110°C, por 48 horas.

A separação química dos vários isótopos foi desenvolvida seguindo diferentes etapas, conforme descrito por [START_REF] Bosch | Pb, Hf and Nd isotope compositions of the two Réunion volcanoes (Indian Ocean): a tale of two small-scale mantle "blobs[END_REF]. As composições isotópicas de Sr foram obtidas em um espectrômetro de massa Triton Finnigan Mat no Labogis, Universidade de Nîmes, na França. Durante as análises, foram realizadas medidas sistemáticas no padrão NBS987, que indicaram um valor médio de 87 Sr/ 86 Sr de 0,710242 (n=5) (normalizado para 86 Sr/ 88 Sr = 0,1194).

As composições isotópicas de Nd, Pb e Hf foram obtidas por meio de um espectrômetro de massa com plasma indutivamente acoplado (ThermoFisher Scientific Neptune Plus) na École Normale Supérieure de Lyon (ENSL). Para as análises de Nd, o padrão AMES-Rennes, analisado durante o desenvolvimento do trabalho, apresenta uma razão 143 Nd/ 144 Nd média de 0,511961 ± 23 (n=17 = 0,512638 [START_REF] Hamilton | Sm-Nd studies of Archean metasediments and metavolcanics from West Greenland and their implications for the Earth's early history[END_REF]. As idades modelo Nd T DM foram calculadas considerando a constante de decaimento (λ) 6,54 × 10 [START_REF] Almeida | Relações tectônicas das rochas alcalinas Mesozoicas da região Meridional da Plataforma Sul-americana[END_REF][START_REF] Riccomini | Tectonic controls of the Mesozoic and Cenozoic alkaline magmatism in the central-southeastern Brazilian Platform[END_REF], uma elevação continental NW-SE ativa desde o Paleozóico e definida por um enxame de diques de diabásio da PMP. Figura 3 -Ocorrências alcalinas ao longo das margens da Bacia do Paraná, na região centro-sudeste da Plataforma Sul-Americana (modificado de [START_REF] Riccomini | Tectonic controls of the Mesozoic and Cenozoic alkaline magmatism in the central-southeastern Brazilian Platform[END_REF]: 1) Bacia Bauru (Cretáceo Superior); 2) Província Magmática do Paraná (Cretáceo Inferior); 3) Bacia do Paraná (Ordoviciano Superior ao Cretáceo Inferior); 4) Unidades alcalinas (losangos, Permiano-Triássico; quadrados, Cretáceo Inferior; triângulos, Cretáceo Inferior; círculos, Paleógeno); 5) Eixo dos principais arcos; 6) Principais zonas de fratura: Lineamentos Guapiara (GP), São Jerônimo-Curiúva (JC), Rio Alonso (RA) e Rio Piquiri (RP); 7) Lineamento Lancinha-Cubatão.

DESCOBERTA E MAPEAMENTO DO COMPLEXO DE JACUPIRANGA

O Complexo de Jacupiranga foi descoberto em 1877 por Bauer e investigado preliminarmente por [START_REF] Hussak | UeberBrazilit, einneus. Tantal (Niob) Mineral von der Eisenmine Jacupiranga: Neues[END_REF][START_REF] Hussak | Ueber den Baddelit (syn. Brazilit) von der Eisenmine in Jacupiranga in São Paulo[END_REF]Hussak ( , 1904) ) e [START_REF] Derby | The magnetite ore districts of Jacupiranga and Ipanema, São Paulo, Brazil[END_REF]. Este autor foi o responsável pela primeira descrição da unidade, além de ter cunhado o termo jacupiranguito para se referir a litotipos com a presença de piroxênio titanífero, comuns no complexo. [START_REF] Derby | The magnetite ore districts of Jacupiranga and Ipanema, São Paulo, Brazil[END_REF] descreve a área de afloramento dos carbonatitos como uma ocorrência de minério de ferro, dado o elevado conteúdo de magnetita nestas rochas.

A descoberta do depósito de fosfato por [START_REF] Knecht | Os minerais não metálicos do Estado de São Paulo[END_REF][START_REF] Knecht | Novas ocorrências nos municípios do extremo sudoeste paulista[END_REF], o desmatamento regional para fins de cultivo e a lavra do manto regolítico auxiliaram na exposição de toda a área de afloramento do carbonatito, permitindo a observação detalhada e amostragem desta rocha. [START_REF] Melcher | Nota sobre os distrito Alcalino de Jacpiranga[END_REF][START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF] ,1988). Em seguida, [START_REF] Amaral | Potassium-argon age studies on the Jacupiranga alkaline district, State of São Paulo, Brazil[END_REF] apresenta novos dados K-Ar, expandindo o total de amostras analisadas para 45, com uma média de idade de 130 ± 5 Ma. [START_REF] Roden | Sr and Nd Isotopic Composition of the Jacupiranga Carbonatite[END_REF] apresentam uma idade isócrona Rb-Sr para os carbonatitos de 131 ± 3 Ma.

Atualmente, há um único dado Ar-Ar publicado para o Complexo de Jacupiranga [START_REF] Basu | Alkaline igneous rocks of the Deccan and Paraná: implications for the origin of continental flood basalts (CFB)[END_REF], mas nenhum detalhe quanto a qual litotipo foi analisado é fornecido. Segundo os autores, a presença de uma câmara inferior é indicada pela presença de diques intrudidos na zona de transição, cujas composições variam de rochas gabróicas de alto Na, essexitos, teralitos, sienitos e granitos alcalinos com excesso de K. Esta complexa diferenciação a partir de um magma alcalino rico em Na (assumido como o magma primário) seria incompatível em uma câmara superior, com porções já solidificadas. Suprimento de calor a partir de uma fonte mantélica, assimilação de encaixantes e diferenciação magmática seriam os aspectos necessários, segundo [START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF], para a gênese de todas estas rochas. Estas condições seriam mais prováveis de ocorrer em um reservatório magmático secundário, mais profundo. Os diques se concentrariam na zona de transição por ser relacionarem à reativação de um antigo conduto. [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF], baseado em um extenso estudo de química mineral, propõe que a evolução do complexo não deva ser encarada como a história de uma câmara magmática, mas sim como a de um conduto central ao redor do qual condutos menores (no mínimo dois) se desenvolveram. Diferentes magmas parentais, de composições próximas, ascenderam por um complexo sistema de condutos e câmaras magmáticas, e, após processos de diferenciação e contaminação crustal, deram origem à associação alcalina, ultramáfica e aos carbonatitos. O autor propõe um sistema magmático com múltiplos estágios para as rochas ultramáficas e alcalinas, iniciado pela acumulação de cristais de olivina, a norte, e clinopiroxênio, a sul, gerando os dunitos e clinopiroxenitos, respectivamente. Cada corpo cumulático foi gerado a partir de um magma parental diferente, conforme o autor. Uma segunda fase intrusiva gerou os clinopiroxenitos com nefelina, sendo que este magma, a partir de processos de imiscibilidade, gerou os carbonatitos e ijolitos. As rochas com feldspato (sienito, diorito, monzonito etc) representariam, cada uma, um pulso de magma diferente. [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] sugere que estes magmas apresentariam a mesma composição do líquido parental formador das rochas com nefelina. Diferentes graus de contaminação crustal determinariam a grande variabilidade composicional das rochas com feldspato. [START_REF] Gomes | Carbonatite complexes from Brazil: a review[END_REF] afirmam que a constante associação dos complexos carbonatíticos brasileiros com rochas silicáticas sugere uma sequência de atividades magmáticas que evoluíram a partir de magmas ultramáficos e ultrabásicos, gradando progressivamente para estágios mais ricos em álcalis (ijolítico). Deste modo, os autores apontam que os jacupiranguitos e dunitos presentes em vários complexos brasileiros têm sua origem relacionada a processos de cumulados, enquanto que os demais litotipos (ijolitos, melteigitos, sienitos e nefelina sienitos) aparentemente foram gerados pelo fracionamento de magmas basaníticos ou álcali-gabróicos.

Conforme [START_REF] Morikiyo | Carbon and oxygen isotopic composition of the carbonatites from Jacupiranga and Catalão I carbonatite complexes. Brazil[END_REF], [START_REF] Nelson | Geochemical and isotopic systematics in carbonatites and implications for the evolution of oceanisland sources[END_REF]) e Comin-Chiaramonti et al. (2007), os carbonatitos de Jacupiranga têm composições isotópicas (δ 13 C = -5,6 a -6,4‰ e δ 18 O = +7,1 a +8,1‰) consideravelmente uniformes e condizentes com uma origem primária de carbonatos. No entanto, no que diz respeito a isótopos radiogênicos, a partir de razões isotópicas de Sr em minerais, [START_REF] Roden | Sr and Nd Isotopic Composition of the Jacupiranga Carbonatite[END_REF] consideram os carbonatitos isotopicamente heterogêneos. Deste modo, estes autores sugerem que um magma parental alcalino, isotopicamente similar a alguns basaltos de Walvis Rigde, teria sido contaminado pela crosta continental durante seus processos de diferenciação, que, por sua vez, culminaram na cristalização dos carbonatitos. [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF], a partir de dados isotópicos (Sr, Nd e Pb) e análises químicas (elementos maiores e traço) de amostras de carbonatitos e piroxenitos, estabelecem um modelo petrogenético para estas rochas. Conforme os autores, as razões isotópicas iniciais de Sr e Pb são diferentes nos carbonatitos e nos piroxenitos (razões de 208 Pb/ 204 Pb e 87 Sr/ 86 Sr, respectivamente, mais elevadas e mais baixas nos piroxenitos com relação aos valores obtidos em amostras de carbonatito). Esta diferença impossibilitaria que os dois magmas tivessem uma origem comum, descartando hipóteses de imiscibilidade de líquidos.

Esta variação nas razões seria decorrente, segundo os autores, de características primárias dos magmas, relacionadas às regiões do manto que lhe deram origem. Além disso, os autores afirmam que variações no conteúdo de elementos terras raras (ETR) entre estes dois litotipos não poderiam ser atribuídas à cristalização fracionada ou segregação por imiscibilidade de líquidos. Logo, estes dados seriam um indicativo de que os carbonatitos do Complexo de Jacupiranga não teriam sido formados a partir do mesmo magma que deu origem aos piroxenitos. Os autores admitem que o complexo seria o produto de múltiplos episódios intrusivos. [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF] afirmam, ainda, que as razões isotópicas iniciais de Sr, Nd e Pb do complexo em questão são similares àquelas dos basaltos da Província Magmática do Paraná (alto titânio), de Walvis Ridge e Tristan da Cunha. Aparentemente, estes líquidos foram formados a partir de fontes mantélicas similares e não foram afetados significativamente por processos de contaminação crustal. [START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF] sugerem que os dois litotipos menos evoluídos descritos em Jacupiranga, o álcali gabro e o ankaratrito (classificados conforme sua composição química), poderiam representar dois magmas parentais que evoluíram para nefelina sienitos e fonolitos peralcalinos, respectivamente. Considerando esta hipótese, [START_REF] Morbidelli | The Pariquera Açu K-alkaline complex and southern Brazil lithospheric mantle source characteristics[END_REF] calculam a composição do manto residual a partir da extração do ankaratrito de diferentes fontes (i.e. GP, granada peridotito; GPP, granada peridotito com flogopita e PP, flogopita peridotito), sendo que o grau de fusão parcial obtido varia entre 5,11 (para GPP) e 6,20% (para PP).

A partir da análise da distribuição de inclusões fluidas em cristais de apatita nos carbonatitos, [START_REF] Costanzo | Fluid inclusions in apatite from Jacupiranga calcite carbonatites: Evidence for a fluid-stratified carbonatite magma chamber[END_REF] propõem um modelo de câmara magmática na qual estas rochas se cristalizaram. Segundo os autores, há uma descontinuidade entre o núcleo dos cristais de apatita, ricos em inclusões fluidas primárias e com elevada concentração de Sr e ETR, e suas bordas, com poucas inclusões e baixa quantidade desses elementos. Os autores consideram que a causa mais provável para as bordas sem inclusões é a separação da fase fluida do magma antes do término da cristalização da apatita, além da remoção do cristal de uma área da câmara rica em fluidos para uma área com pouca fase fluida. Para explicar esta distribuição, os autores propõem uma câmara magmática estratificada, com concentração de fluidos na zona superior e com pouco fluido na base. Conforme os cristais de apatita iniciam a cristalização na zona superior, as inclusões fluidas são aprisionadas, formando o núcleo rico em inclusões. Dada à ação da gravidade, os cristais migram para as zonas inferiores da câmara, onde eles continuam a cristalizar. Como há pouca quantidade de fluidos nesta área, as novas zonas formadas nos cristais não terão inclusões fluidas, explicando então a distribuição de inclusões nos cristais de apatita.

Na área de contato entre o clinopiroxenito e o carbonatito, ocorrem bandas de reação constituídas alternadamente por níveis silicáticos e carbonáticos. Elas são formadas ou por níveis predominantemente de anfibólio, ou predominantemente de biotita ou pela associação olivina + flogopita + calcita. [START_REF] Morbidelli | Petrological and geochemical studies of alkaline rocks from continental Brazil, 3. Fenitization of jacupirangite by carbonatite magmas in the Jacupiranga Complex[END_REF], a partir de dados petrográficos, afirmam que o anfibólio e a flogopita derivam da interação do fluido carbonatítico com o protólito de clinopiroxenito. Segundo estes autores, a flogopitização e anfibolitização, tais como observadas nesta unidade, podem ser classificadas como processos de fenitização. O termo fenito foi inicialmente utilizado por [START_REF] Brögger | Die Eruptivgesteine des Kristianiagebietes: Vidensk[END_REF] para designar rochas alteradas metassomaticamente nas proximidades do Complexo de Fen (Noruega), sendo que as soluções metassomáticas teriam sido emanadas a partir de um magma ijolítico-melteigítico. Posteriormente, o termo fenitização passou a ser empregado para definir processos metassomáticos cujos efeitos se concentram nas proximidades de corpos carbonatíticos e ijolíticos.

Assim, baseados em cálculos de balanço de massa, [START_REF] Morbidelli | Petrological and geochemical studies of alkaline rocks from continental Brazil, 3. Fenitization of jacupirangite by carbonatite magmas in the Jacupiranga Complex[END_REF] concluem que o magma carbonatítico, possivelmente devido ao baixo conteúdo em sílica e alumina, não foi capaz de manter todos os álcalis presentes durante a cristalização do líquido. Dados mineralógicos e petrográficos indicam que as primeiras transformações que geraram os fenitos se associaram a uma elevada atividade de álcalis (Na, K e Rb) e de H 2 O.

Os autores obtêm, então, valores de Na, K e Rb nos carbonatitos relativamente baixos quando comparados aos do magma parental, de maneira a se concluir que estes componentes migraram para as encaixantes e geraram os fenitos.

ATIVIDADES DE LAVRA NO COMPLEXO

O carbonatito de Jacupiranga constitui um corpo mineralizado em fosfato cujas atividades de lavra se iniciaram em 1943. A princípio, o minério lavrado era de origem supergênica, com teores elevados (> 20% de P 2 O 5 ) e formado por apatita, magnetita e argilominerais, produtos oriundos da dissolução e lixiviação do carbonatito [START_REF] Ruberti | O Complexo Carbonatítico de Jacupiranga, SP: informações gerais[END_REF]). Menezes Jr. e Martins (1984) afirmam que o elevado teor de fosfato no manto intempérico da unidade já era de conhecimento desde o início do século XX, apesar de sua origem ser então atribuída a processos metamórficos entre o carbonatito e clinopiroxenito.

Exaurido o minério residual, a lavra do carbonatito são foi iniciada em 1969, quando foi implementado o parque industrial da mina de Cajati. Desde então, a apatita deixou de constituir a base econômica da mina, uma vez que subprodutos do carbonatito (tais como a magnetita e "calcário") passaram a ser também aproveitados [START_REF] Ruberti | O Complexo Carbonatítico de Jacupiranga, SP: informações gerais[END_REF][START_REF] Faria | Aprimoramento do controle de qualidade do minério no planejamento de lavra de curto prazo: estudo de caso[END_REF].

Como a rocha fresca apresenta teores de P 2 O 5 na ordem de 5,5% [START_REF] Ruberti | O Complexo Carbonatítico de Jacupiranga, SP: informações gerais[END_REF], produz-se um concentrado de apatita que é submetido a processos químicos e convertido para ácido fosfórico por meio de uma rota de ácido sulfúrico. O ácido fosfórico é usado na manufatura de fertilizantes, apesar da maior parte da produção da mina ser destinada à alimentação animal. O baixo teor de minério exigiu o desenvolvimento de procedimentos industriais específicos, permitindo o melhor uso de todo o material e resultando em vários produtos secundários (entre eles, matéria-prima carbonática e ferro para a indústria do cimento, dolomita para calcário agrícola e fosfogipso).

Conforme [START_REF] Alves | The carbonatite-hosted apatite deposit of Jacupiranga, SE Brazil: styles of mineralization, ore characterization, and association with mineral processing[END_REF], comparativamente a outros depósitos de apatita em carbonatito sendo lavrados no Brasil, o minério de apatita exposto no Complexo de Jacupiranga pode, a princípio, ser considerado mais homogêneo, já que não foi afetado pro processos de laterização. Em termos gerais, um depósito que contém predominantemente apatita primária, como é o caso de Jacupiranga atualmente, tende a ter baixa concentração de fosfato, predomínio de cristais de apatita prismática e uma variação menos significativa no teor de CaO/P 2 O 5 quando comparados a depósitos residuais de apatita (i.e. Araxá, Catalão, Tapira). [START_REF] Alves | The carbonatite-hosted apatite deposit of Jacupiranga, SE Brazil: styles of mineralization, ore characterization, and association with mineral processing[END_REF] utiliza análises microscópicas (luz refletida, transmitida, catodoluminescência e microscópio eletrônico de varredura) com o objetivo de definir os tipos de mineralização de apatita presentes no carbonatito. A autora descreve quatro estilos de mineralização: a) venulares, geralmente intensamente orientados conforme o fluxo magmático; b) pequenos pods, que podem tanto se associar a veios quanto serem formados por aglomerados individuais de cristais finos aciculares; c) cristais disseminados; d) agregados massivos de cristais de apatita de granulação média a grossa, desenvolvida na intrusão carbonatítica mais antiga. Segundo a autora, a apatita de Jacupiranga apresenta padrões geoquímicos e características texturais particulares em cada uma das cinco intrusões carbonatíticas definidas por Gaspar e [START_REF] Gaspar | Magnetite in the carbonatites from the Jacupiranga Complex, Brazil[END_REF], como, por exemplo, um aumento nos teores totais de elementos terras raras em direção ao norte do corpo carbonatítico.

Além do carbonatito, o espesso manto de alteração (superior a 40 m) sobre os dunitos também já foi alvo de pesquisa para níquel laterítico, apesar de nunca lavrados [START_REF] Oliveira | Lateritic evolution of the Jacupiranga alkaline complex[END_REF][START_REF] Oliveira | Os depósitos de níquel laterítico do Brasil[END_REF]. Conforme [START_REF] Vasconcelos | Projeto Jacupiranga-Rio Guaraú: mapeamento geológico na escala 1:50.000. Relatório final[END_REF], estas pesquisas indicaram possíveis jazimentos, além de indícios para cromo, ouro,ferro e outros bens minerais.

JACUPIRANGUITO

O termo jacupiranguito foi cunhado a partir de rochas ultramáficas que ocorrem a sul do Complexo de Jacupiranga, sendo que algumas mudanças no seu significado ocorreram com o passar do tempo.

Inicialmente proposto por [START_REF] Derby | The magnetite ore districts of Jacupiranga and Ipanema, São Paulo, Brazil[END_REF], o nome jacupiranguito era utilizado para designar rochas de séries com nefelina e que englobam fácies de magnetita pura, magnetita com piroxênio acessório, piroxênio com magnetita acessória e piroxênio com biotita e olivina como acessórios. [START_REF] Johansen | A descriptive petrography of igneous rocks[END_REF], em contrapartida, recomenda que este termo seja utilizado para rochas compostas por augita e minério de ferro e sem nefelina ou somente traços dela. Le [START_REF] Bas | Carbonatite-Nephelinite Volcanism[END_REF] usou o termo para rochas que contém cerca de 80% de titanoaugita e 20% de magnetita e ilmenita.

No glossário de Sorensen (1974) o jacupiranguito é descrito como um alcálipiroxenito contendo titanoaugita, titanomagnetita, nefelina, apatita, perovskita e melanita. Esta orientação é seguida por [START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF], que incluem nefelina como constituinte que pode atingir até 10% em volume da rocha, exceto para a rocha pura em magnetita descrita por [START_REF] Derby | The magnetite ore districts of Jacupiranga and Ipanema, São Paulo, Brazil[END_REF]. A descrição que este autor dá para jacupiranguito corresponde à sequência de rochas que ocorre na porção noroeste do principal corpo de piroxenito, onde todas as variações petrográficas ocorrem, e devido à ausência de afloramentos, não é sempre possível verificar a relação entre elas. Entretanto, conforme o autor, elas são rochas diferentes, com características químicas distintas e deveriam ter nomes diferentes.

Segundo o glossário de termos em Le Maitre (2002), jacupiranguito define uma variedade de piroxenito alcalino que consiste em augita titanífera com menores quantidades de titanoaugita, nefelina, apatita, perovskita e granada (melanita). No entanto, atualmente, sugere-se a utilização do termo clinopiroxenito para designar estas rochas, conforme as recomendações da IUGS. Esta orientação é utilizada neste trabalho. 

ASPECTOS DE CAMPO E PETROGRÁFICOS

DUNITOS E WEHRLITOS

O estudo das rochas duníticas é dificultado pelo espesso manto de alteração (Figura 10A) e a ausência de afloramentos sãos, produto das condições climáticas da região que favorecem processos intempéricos (umidade acima de 80% e temperaturas subtropicais - et al., 1999). As únicas amostras obtidas para o presente estudo são oriundas de furos de sondagem feitos pela Serrana S.A. Mineração, durante campanha de pesquisa de níquel laterítico no complexo. A rocha menos alterada só aparece nos furos de sondagem a profundidades superiores a 40 m.

Vasconcelos

A principal fase mineral destes litotipos é a olivina, parcialmente alterada para serpentina. Espinélio e carbonatos também podem estar presentes, mas em pequena quantidade (<5%). Três amostras de furo de sondagem foram selecionadas: um dunito de granulação fina (JAC248), constituído essencialmente por olivina subédrica e traços de espinélio, e dois wehrlitos de granulação média (JAC220 e JAC243), formados por olivina, diopsídio (<15%) e espinélio. O intemperismo e o elevado grau de serpentinização destas rochas (30-70%) dificultam a identificação de suas texturas e estruturas primárias. A serpentina forma um retículo intrincado cujos núcleos são as porções dos cristais de olivina e diopsídio que resistiram à alteração (Figura 10B). Apesar de a serpentina ser a fase secundária predominante, ocorre também iddingsita e talco, este tanto disseminado na rocha quanto na forma de veios.

CLINOPIROXENITOS

A porção sul do Complexo de Jacupiranga é formada majoritariamente por clinopiroxenitos de granulação média a grossa. São adcumulados a mesocumulados caracterizados pela orientação dos cristais de diopsídio. Magnetita clinopiroxenito é o principal litotipo desta unidade (Figura 11A), formado predominantemente por diopsídio cumulus (>80 vol.%) e Ti-magnetita intersticial (10-20 vol.%). O diopsídio pode se apresentar zonado (zonamento normal ou reverso -Figura 11B) ou com finas lamelas de exsolução para opacos e flogopita. Apesar de geralmente equigranulares (média a grossa, com dimensões máximas de 2 cm), algumas amostras são formadas por duas fases de diopsídio:

fenocristal (de até 1,5 cm) e matriz (0,5 a 2 mm). Traços de perovskita (bordejando cristais de Ti-magnetita), flogopita e apatita também ocorrem.

Outras variantes do clinopiroxenito também são observadas: flogopita clinopiroxenitos (com ou sem nefelina), clinopiroxenitos com nefelina (JAC18, JAC82 -Figura 11C), olivina clinopiroxenitos (JAC13, JAC73 -Figura 12A) e flogopita clinopiroxenitos com andesina (descrito por [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF]. Nestas variantes, enquanto a olivina ocorre como fase cumulus, a nefelina, a flogopita e a andesina são intercumulus (Figura 11D). As variantes com nefelina ocorrem sempre nas proximidades do corpo ijolítico.

Diques de clinopiroxenito são encontrados intrudidos nas encaixantes metassedimentares [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] e no magnetita clinopiroxenito a norte da unidade (Figura 12B). Na última ocorrência, os diques são magnetita clinopiroxenitos de granulação fina (JAC34), com uma proporção Ti-magnetita/diopsídio maior que a observada nos magnetita clinopiroxenito.

É comum a presença de veios constituídos por feldspato alcalino, magnetita, granada e biotita cortando o clinopiroxenito (Figura 7D). Estas estruturas não apresentam direção preferencial e ocorrem somente em afloramentos situados na região leste do corpo clinopiroxenítico. 

ROCHAS DA SÉRIE IJOLÍTICA

Também na região sul do complexo afloram rochas formadas predominantemente por nefelina e diopsídio, pertencentes à série ijolítica. No Complexo de Jacupiranga, esta série consiste principalmente de ijolitos com melteigitos subordinados, apesar de raros urtitos terem sido descritos por alguns autores [START_REF] Herz | Timing and spreading in the South Atlantic: Kimberlite Conference, Araxa. Brasilia, DF: CPRM, Special information from Brazilian alkaline rocks[END_REF][START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF]Ruberti et al., 2005).

As rochas da série ijolítica formam um corpo em meia-lua que atinge cotas de até 290 m, destacando-se em relação ao restante da unidade, que tem altitude máxima de 130 m; localmente, essa elevação é conhecida como Morro Grande. Texturalmente heterogêneos, os ijolitos são equigranulares finos, equigranulares médios, inequigranular fino a médio ou inequigranular médio a grosso.

Os ijolitos são formados por 40 a 55% de nefelina anédrica a subédrica e 25 a 35% Considerando esta distribuição, duas ocorrências de monzonito foram selecionadas para este estudo: um olivina monzonito (JAC26.2, constituído por diopsídio, andesina, feldspato potássico, biotita, olivina, magnetita e apatita -Figura 15A, B) e um monzonito (JAC25).

Aflorante ao norte do corpo dunítico (ponto 25), o monzonito (Figura 15C) tem estrutura maciça e textura porfirítica inequigranular com matriz fina. Sua principal particularidade é a presença de fenocristais prismáticos de andesina com margens de albita.

Esses cristais são zonados e estão em meio a uma matriz formada por andesina, feldspato alcalino pertitizado, hornblenda, biotita, titanita e minerais opacos. Todas essas fases têm hábito subédrico, exceto a titanita que por vezes é euédrica navicular. Alguns cristais de biotita tem as bordas cloritizadas, enquanto a hornblenda encontra-se pontualmente substituída por biotita e opacos. Apatita e zircão são os acessórios. Associado a esta rocha há enclaves alongados decimétricos e com textura xistosa (Figura 15D).

Rochas sieníticas

A leste e a norte da unidade dunítica (pontos 31, 32, 46, 55, 56, 58, 59, 60, 61, 63) ocorrem rochas cuja principal fase mineral é o feldspato alcalino, classificadas no diagrama QAPF de [START_REF] Streckeisen | Classification of the common igneous rocks by means of their chemical composition[END_REF] como álcali-feldspato sienitos. Conforme variações composicionais menores, essas rochas são classificadas nas fácies melassienito (textura inequigranular porfirítica) e álcali-fedspato sienito (textura equigranular média).

No melassienito (JAC31 -Figura 16A), o feldspato alcalino ocorre como fenocristais

(1 a 2 cm) e microfenocristais (de até 5 mm) euédricos prismáticos em meio a uma matriz submilimétrica a milimétrica, mas com dimensões de no máximo 2 mm. A matriz é predominantemente máfica, formada por biotita, diopsídio, opacos e titanita. Outra característica desta fácies é a presença de enclaves máficos arredondados e de diâmetro variável (2 mm até 7 cm). São constituídos por cristais submilimétricos arredondados de diopsídio e de minerais opacos, apesar de que em alguns fragmentos são observados cristais euédricos de feldspato alcalino. Macroscopicamente, os enclaves, de cor cinza escuro (Figura 16B), se destacam com relação à rocha sienítica, de cor cinza médio a claro.

No entanto, em lâmina delgada, os limites dos enclaves não são bem marcados: não há bordas de reação e sua assembleia mineral se confunde com a da matriz da rocha sienítica (Figura 16C), apesar de diferenças no hábito dos cristais. É principalmente a concentração de opacos e a granulação muito fina do diopsídio que diferencia esses fragmentos do restante da rocha. Já a principal característica do álcali-feldspato sienito (JAC32, JAC46.3 -Figura 16D) é a presença de agregados de minerais máficos (Figura 16E) em meio a cristais subédricos prismáticos de feldspato alcalino (em média 3 mm). Esses agregados são formados por diopsídio, magnésio-hastingsita, titanita, opacos e, ocasionalmente, biotita (0,2 a 1 mm). O diopsídio é castanho pálido esverdeado, em contraste àquele presente nos demais litotipos do complexo. Outro componente dos agregados máficos são cristais de titanita euédrica navicular ou subédrica. Inclusos no diopsídio ou na hornblenda há minerais opacos arredondados, apatita e, menos frequentemente, biotita.

No contato entre os cristais de magnésio-hastingsita (Figura 16F) ou diopsídio com o feldspato alcalino há uma borda de reação formada por minerais opacos e uma fase muito fina, que se assemelha ao diopsídio. Esta borda não ocorre nos cristais de titanita, também em contato direto com a fase félsica. Os cristais de opacos inclusos em diopsídio ou magnésio-hastingsita também são totalmente envoltos por bordas de reação de mesma composição. Já a biotita, em geral, está em contato direto com o feldspato alcalino, apesar de alguns cristais apresentarem alguns trechos dos seus limites também margeados por bordas de reação. O primeiro deles ocorre como diques de contatos sinuosos e espessuras entre 5 e 40 cm, sem orientação preferencial, intrudidos na Suíte Intrusiva Itapeúna (ponto 39 -Figura 18A), próximo ao contato nordeste do complexo, e também nos álcali-feldspato sienitos (ponto 46 -Figura 18B). São rochas de textura inequigranular porfirítica, com macrocristais máficos de granulação fina em meio a uma matriz muito fina. Os macrocristais são de olivina e de diopsídio euédricos com dimensões entre 1 e 2,5 mm. A olivina, em particular, apresenta feições de corrosão e preenchimento por opacos e biotita, além de estar envolta por um manto de microcristais de biotita e minerais opacos (Figura 18C), sugerindo condições de desequilíbrio entre esta fase e a matriz [START_REF] Menezes | The antecryst compositional influence on Cretaceous alkaline lamprophyre dykes, SE Brazil[END_REF]. Por conta disso, o termo macrocristal foi preferido em detrimento a "fenocristal", dada a conotação genética do segundo. Há microcristais de diopsídio, biotita e opacos euédricos com dimensões entre 0,1 e 0,3 mm. Há também estruturas globulares e ameboides submilimétricas formadas por feldspato alcalino e plagioclásio. A matriz é constituída por diopsídio, feldspato alcalino, plagioclásio, opacos e biotita de granulação muito fina O segundo tipo de lamprófiro se diferencia do anterior pela granulação mais grossa (JAC46.1 -Figura 18D). Ocorre como blocos dispersos no mesmo afloramento em que o lamprófiro fino está intrudido no álcali-feldspato sienito (ponto 46). É constituído por macrocristais de biotita e diopsídio em meio a uma matriz formada por diopsídio, biotita, magnetita, titanita, feldspato alcalino, mesóstase félsica, vidro vulcânico e apatita. Apresenta três tipos de cristais de diopsídio: 1) cristais límpidos submilimétricos, euédricos e subédricos, castanho pálido a castanho esverdeado; 2) cristais submilimétricos euédricos com núcleo extremamente "sujo" e borda aparentemente formada por sobrecrescimento, com cor e propriedades óticas similares às dos cristas límpidos; e 3) cristais límpidos milimétricos (até 2 mm) subédricos castanho pálido com linhas escuras concêntricas sugerindo marcas de crescimento ou sobrecrescimento. Do mesmo modo que o lamprófiro fino, a presença de vidro classifica o lamprófiro grosso como um monchiquito. Além dos carbonatos, outras fases descritas nestas rochas são apatita, magnetita, forsterita, serpentina, clinohumita, flogopita, pirrotita, galena, ilmenita, espinélio, pirocloro, baddeleíta, barita e perovskita [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF]. Dentre elas, apatita é a fase acessória mais importante (5-35 vol.%) e faz de Jacupiranga um dos mais importantes depósitos de fosfato do Brasil. Fases acessórios menos comuns são carbocernaíta, ancilita-(Ce), baritocalcita, norsetita, pirofanita, zircolita, bubanquita, siderita magnesiana e alanita [START_REF] Costanzo | Fluid inclusions in apatite from Jacupiranga calcite carbonatites: Evidence for a fluid-stratified carbonatite magma chamber[END_REF].

Enquanto [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF] • Lamprophyres are considered as representatives of a basanite parental magma.

• Local crustal assimilation processes are constrained for some lithotypes.

• Basanite melts were generated from a source with variable degrees of CO 2 -rich metasomatism.

ABSTRACT

The Jacupiranga Complex is one of several Meso-Cenozoic alkaline intrusive complexes along the margins of the intracratonic Paraná Basin in southern Brazil. The complex encompasses a wide range of rock-types, including dunites, wehrlites, clinopyroxenites, melteigites-ijolites, feldspar-bearing rocks (diorites, syenites, and monzonites), lamprophyres and apatite-rich carbonatites. While carbonatites have been extensively investigated over the last decades, little attention has been paid to the silicate rocks. This study presents new geochonological and geochemical data on the Jacupiranga Complex, with particular emphasis on the silicate lithotypes. 40 Ar/ 39 Ar ages for different lithotypes range from 133.7 ± 0.5 Ma to 131.9 ± 0.5 Ma, while monzonite zircon analyzed by SHRIMP yields a U-Pb concordia age of 134.9 ± 1.3 Ma. These ages indicate a narrow time frame for the Jacupiranga Complex emplacement, contemporaneous with the Paraná Magmatic Province. Most of the Jacupiranga rocks are SiO 2 -undersaturated, except for a quartz-normative monzonite. Based on geochemical compositions, the Jacupiranga silicate lithotypes may be separated into two magmaevolution trends: (1) a strongly silica-undersaturated series, comprising part of the clinopyroxenites and the ijolitic rocks, probably related to nephelinite melts and (2) a mildly silica-undersaturated series, related to basanite parental magmas and comprising the feldspar-bearing rocks, phonolites, lamprophyres, and part of the clinopyroxenites. Dunites and wehrlites are characterized by olivine compositionally restricted to the Fo 83-84 interval and concentrations of CaO (0.13-0.54 wt.%) and NiO (0.19-0.33 wt.%) consistent with derivation by fractional crystallization, although it is not clear whether these rocks belong to the nephelinite or basanite series. Lamprophyre dikes within the complex are considered as good representatives of the basanite parental magma. Compositions of calculated melts in equilibrium with diopside cores from clinopyroxenites are quite similar to those of the lamprophyres, suggesting that at least a part of the clinopyroxenites is related to the basanite series. Some feldspar-bearing rocks (i.e. meladiorite and monzonite) show petrographic features and geochemical and isotope compositions ( 87 Sr/ 86 Sr i : 0.705979-0.706086 and 143 Nd/ 144 Nd i : 0.511945-0.512089) indicative of crustal assimilation, although this may be relegated to a local process. Relatively high CaO/Al 2 O 3 and La/Zr and low Ti/Eu ratios from the lamprophyres and calculated melts in equilibrium with cumulus clinopyroxene point to a lithospheric mantle metasomatized by CO 2 -rich fluids, suggesting vein-plus-wall-rock melting mechanisms. The chemical differences among those liquids are thought to reflect both variable contributions of melting resulting from veins and variable clinopyroxene/garnet proportions of the source.

INTRODUCTION

Alkaline and ultramafic rocks are spatially and temporally associated with carbonatites in several intrusive units from different igneous provinces worldwide (Le [START_REF] Le Bas | Nephelinites and carbonatites[END_REF][START_REF] Woolley | Igneous silicate rocks associated with carbonatites: their diversity, relative abundances and implications for carbonatite genesis[END_REF][START_REF] Downes | Petrogenetic processes in the ultramafic, alkaline and carbonatitic magmatism in the Kola Alkaline Province: A review[END_REF]. Associated silicates are most commonly clinopyroxenites, rocks from the ijolite-series and, alkali-syenites with minor peridotites, dunites, and sometimes, turjaites-melilitolites (e.g., [START_REF] Downes | Petrogenetic processes in the ultramafic, alkaline and carbonatitic magmatism in the Kola Alkaline Province: A review[END_REF][START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF]. However, the petrogenetic links among these rocks are rather complex and still under discussion [START_REF] Gittins | Myth and reality in the carbonatite -silicate rock "association[END_REF].

Parental magmas with basanite composition have been attributed to several alkaline occurrences, either encompassing carbonatites [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF] or only silicate rocks (e.g. [START_REF] Brotzu | Petrology and geochemistry of the Passa Quatro alkaline complex, southeastern Brazil[END_REF][START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF][START_REF] Melluso | Mineral compositions and petrogenetic evolution of the ultramafic-alkaline -carbonatitic complex of Sung Valley, Northeastern India[END_REF]. These investigations indicate that basanite melts can differentiate either under nearly closed system conditions [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF] or with significant modification via crustal assimilation [START_REF] Azzone | Petrographic, geochemical and isotopic evidence of crustal assimilation processes in the Ponte Nova alkaline mafic-ultramafic massif, SE Brazil[END_REF]. However, mantle source heterogeneities are able to produce small variations on isotopic signatures, particularly when multiple pulses of parental magma are involved [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF][START_REF] Verhulst | Petrological and geochemical (trace elements and Sr-Nd isotopes) characteristics of the Paleozoic Kovdor ultramafic, alkaline and carbonatite intrusion (Kola Peninsula, NW Russia)[END_REF][START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF].

In the Early and Late Cretaceous, the southern part of the Brazilian Platform was the site of extensive alkaline and alkaline-carbonatite magmatism and several occurrences are found associated with the Ponta Grossa Arch region [START_REF] Almeida | Relações tectônicas das rochas alcalinas Mesozoicas da região Meridional da Plataforma Sul-americana[END_REF][START_REF] Riccomini | Tectonic controls of the Mesozoic and Cenozoic alkaline magmatism in the central-southeastern Brazilian Platform[END_REF].

Basanite parental magmas have been proposed for some alkaline occurrences related to the Ponta Grossa Arch (Juquiá, Pariquera-Açu and Tunas complexes - [START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF][START_REF] Morbidelli | The Pariquera Açu K-alkaline complex and southern Brazil lithospheric mantle source characteristics[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF] and are inferred to derive from a lithospheric garnet peridotite mantle source metasomatized by carbonated fluids (e.g. [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF][START_REF] Morbidelli | The Pariquera Açu K-alkaline complex and southern Brazil lithospheric mantle source characteristics[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF][START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF][START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF]. In some massifs, restricted crustal contamination is reported [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF][START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF].

The Jacupiranga Complex is a Mesozoic Brazilian intrusive unit that comprises a large sequence of rocks, including dunites, clinopyroxenites, ijolites, diorites, syenites, lamprophyres, and carbonatites. The apatite-rich carbonatite mined at Jacupiranga has been extensively investigated over the last decades [START_REF] Mitchell | Manganoan magnesian ilmenite and titanian clinohumite from the Jacupiranga carbonatite, São Paulo, Brazil[END_REF][START_REF] Gaspar | Magnetite in the carbonatites from the Jacupiranga Complex, Brazil[END_REF][START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF][START_REF] Costanzo | Fluid inclusions in apatite from Jacupiranga calcite carbonatites: Evidence for a fluid-stratified carbonatite magma chamber[END_REF], but only a few studies cover the silicate rocks (~90% of its outcropping surface [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF][START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF][START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF][START_REF] Morbidelli | Petrological and geochemical studies of alkaline rocks from continental Brazil, 3. Fenitization of jacupirangite by carbonatite magmas in the Jacupiranga Complex[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF][START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF]. In this way, not only is the knowledge about the complex still very fragmented, but there is also a lack of petrological and geochronological studies providing a comprehensive view of the Jacupiranga Complex, particularly regarding the silicate rocks.

The idea addressed in the current paper is to investigate how the different Jacupiranga rocks are related to each other, based on mineralogical, geochemical, isotopic, and geochronological data. As very little attention has been paid to the feldspar-bearing rocks, so we will put particular emphasis on them. This study focuses on (1) the isotopic composition of some silicate rocks that have never been analyzed; (2) high-precision 40 Ar/ 39 Ar and U-Pb measurements to better constrain the time span of the magmatism; (3) estimating the parental melt composition of the mildly silica-undersaturated rocks and some of the cumulates; (4) the source characteristics of those melts; and (5) constraining crustal assimilation processes.

GEOLOGICAL SETTING

Mainly driven by the Atlantic Ocean opening, the last activation stage of the South American Platform (Upper Jurassic onwards - [START_REF] Almeida | The origin and evolution of the South American Platform[END_REF] comprises episodes of both tholeiitic and alkaline magmatism. In the southern part of the platform, the tholeiitic basaltic activity gave rise to the Paraná Magmatic Province (PMP: 134.7 ± 1 Ma, [START_REF] Thiede | Parana flood basalts: Rapid extrusion hypothesis confirmed by new 40 Ar/ 39 Ar results[END_REF], one of the largest continental flood basalts in the world, accompanied by minor intrusive activity. Its alkaline counterpart occurs as intrusive bodies (plugs, stocks, and dikes) with a wide range of compositions (SiO 2 -saturated or undersaturated, down to ultrabasic rocks, carbonatites and/or kimberlites), yielding Early to Late Cretaceous ages [START_REF] Gomes | An introduction to the alkaline and alkaline-carbonatitic magmatism in and around the Paraná-Basin[END_REF]).

In the central-southeastern part of the platform (Fig. 1A), the alkaline occurrences are distributed along the margins of the intracratonic Paraná Basin [START_REF] Gomes | An introduction to the alkaline and alkaline-carbonatitic magmatism in and around the Paraná-Basin[END_REF]. The detailed tectonic framework controlling the distribution of the alkaline activity in the eastern margin of the basin is still controversial, despite being clearly associated with the basin boundaries. It is noteworthy that these igneous bodies are aligned along the Lancinha-Cubatão Shear Zone [START_REF] Biondi | Brazilian mineral deposits associated with alkaline and alkalinecarbonatite complexes[END_REF], which represents a NE-SW suture zone (Fig. 1A) formed during the Gondwana amalgamation and possibly reactivated during the Atlantic Ocean opening. There is no general agreement on neither the mechanical nor the petrogenetic relations between these tectonic features and the genesis of the alkaline complexes.

Nonetheless, the southern and central coastal intrusions are usually related to the Ponta Grossa Arch [START_REF] Almeida | Relações tectônicas das rochas alcalinas Mesozoicas da região Meridional da Plataforma Sul-americana[END_REF][START_REF] Riccomini | Tectonic controls of the Mesozoic and Cenozoic alkaline magmatism in the central-southeastern Brazilian Platform[END_REF], a NW-SE trending structure enhanced by swarms of basaltic dikes from the PMP. Among the four N40-60W-trending lineaments controlling the Ponta Grossa Arch structural framework (Fig. 1A, B -Guapiara, São Jerônimo-Curiúva, Rio Alonso, and Rio Piquiri), the southern sectors of the Guapiara and São Jerônimo-Curiúva lineaments present some alkaline and alkaline-carbonatite intrusions aligned parallel to their axis [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF]. Two major chronogroups, Early and Late Cretaceous [START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF], are distinguished for these occurrences. High-precision geochronological data are currently unavailable for the older chronogroup (only K/Ar or Rb/Sr ages are published) and the extension of this alkaline episode is not accurately defined.

Three Early Cretaceous complexes are related to the Guapiara lineament, and the Jacupiranga Complex (~65 km 2 ) is the largest of them.

THE JACUPIRANGA COMPLEX

The Jacupiranga Complex is a NNW elongated body [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF] intrusive into the Neoproterozoic Itapeúna granodiorites and micaschists from the Turvo-Cajati Formation (Fig. 1C). The northern portion of the unit mostly consists of dunites and rare wehrlites. This ultrabasic body is surrounded by an annular zone composed of rocks of widely varying composition (syenites, gabbros, diorites, monzonites, lamprophyres, and phonolites) and restricted lateral continuity (decametric at most). Due to these features, we rather use the term "Heterogeneous Zone" to designate this unit. The southern part of Jacupiranga consists of a clinopyroxenite unit (~22 km 2 ) with cumulative features associated with a crescentshaped body of banded ijolites. In the central clinopyroxenite, a carbonatite body (1.5 km²) hosts a phosphate ore deposit that has been mined for several decades. [START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF] suggested that mantle blocks of dunites caused a pluggingup of the Jacupiranga magma conduit, leading to the formation of two magma chambers. In this scenario, one chamber would have generated the ijolites and clinopyroxenites, while the other formed the syenites and diorites. This model, however, lacks a geochemical foundation as only some isolated data are reported. Mainly based on mineral chemistry, [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF][START_REF] Gaspar | The Magmatic Evolution of the Jacupiranga Complex[END_REF] proposed that a multi-stage magmatic system driven by crystal accumulation led to the formation of the ultramafic rocks, whereas diorites, monzonites, and syenites may represent each a different magma batch. [START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF] suggested that alkali gabbro and ankaratrite dikes from the Heterogeneous Zone could be representative of two distinct parental magmas for the Jacupiranga Complex. [START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF] proposed that two silicate intrusions, generated by different parental magmas, evolved under nearly closed system conditions and gave rise to (a) the clinopyroxenites and ijolitic rocks and to (b) the dunites, gabbros and syenites. [START_REF] Amaral | Potassium-argon ages of alkaline rocks from southern Brazil[END_REF] have led a pioneer geochronological study about the Jacupiranga Complex with a K-Ar dataset comprising five samples of different lithotypes that yield ages from 191.6 ± 14.6 to 134.1 ± 4.6 Ma (recalculated according to the updated decay constant by [START_REF] Sonoki | Idades K-Ar de rochas alcalinas do Brasil meridional e Paraguai oriental: compilação e adaptação às novas constantes de decaimento[END_REF]. Later on, [START_REF] Amaral | Potassium-argon age studies on the Jacupiranga alkaline district, State of São Paulo, Brazil[END_REF] presented new K-Ar results, bringing the total analyzed samples to 45 (mean age of 130 ± 5 Ma). [START_REF] Roden | Sr and Nd Isotopic Composition of the Jacupiranga Carbonatite[END_REF] present a Rb-Sr isochronic age for carbonatites of 131 ± 3 Ma. There is currently only one published 40 Ar/ 39 Ar plateau age for Jacupiranga (132.79 Ma - [START_REF] Basu | Alkaline igneous rocks of the Deccan and Paraná: implications for the origin of continental flood basalts (CFB)[END_REF], but no details regarding which lithotype was analyzed are provided.

PETROGRAPHY

The general geology of Jacupiranga has been described by [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF], [START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF], [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] and more recently summarized by [START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF] and [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF]. In this section, we describe the samples selected for geochronological and geochemical investigation and present the general features of each Jacupiranga rock-group. In this paper, we follow the IUGS recommendations for the classification of igneous rocks [START_REF] Le Maitre | Igneous Rocks: A Classification and Glossary of Terms[END_REF].

DUNITES

Investigations of the dunites and wehrlites are hampered by the absence of fresh outcrops and regolith thickness due to the local prevailing climatic conditions (humidity over 80% and subtropical temperatures - [START_REF] Vasconcelos | Projeto Jacupiranga-Rio Guaraú: mapeamento geológico na escala 1:50.000. Relatório final[END_REF], which facilitates intense rock weathering. Lateritic covers exceeding 40 m over the dunites have drawn interest as potential Ni ore deposits, although never significantly mined [START_REF] Oliveira | Lateritic evolution of the Jacupiranga alkaline complex[END_REF][START_REF] Oliveira | Os depósitos de níquel laterítico do Brasil[END_REF]. Olivine partially altered to serpentine dominates the mineral assemblage in dunites.

Scarce amounts of Al-and Ti-bearing ferrochromian spinels, iron hydroxides and carbonates may be also present [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF]. Three short drill hole samples were selected for this study: a fine-grained dunite (JAC248), essentially with subhedral olivine and minor spinel, and two medium-grained wehrlites (JAC220 and JAC243), with olivine, minor subhedral diopside (<15 vol.%), and spinel. Weathering and the high degree of serpentinization (30-70%) prevented us from accurately retrieving the primary rock textures, and serpentine now forms an intense network (Fig. 2A) surrounding the relict olivine edges [START_REF] Oliveira | Lateritic evolution of the Jacupiranga alkaline complex[END_REF].

CLINOPYROXENITES

Jacupiranga clinopyroxenites are typically layered adcumulates to mesocumulates, medium to coarse-grained rocks. Magnetite clinopyroxenites (JAC 45, JAC50, JAC53, JC105) are by far the dominant lithotype and form the largest part of the unit. They mainly consist of cumulus diopside (>80 vol.%), either reversely (Fig. 2B) or normally zoned, and interstitial Ti-magnetite (10-20 vol.%). Scarce perovskite (mantling the Ti-magnetite), phlogopite, apatite, kaersutite, and interstitial carbonate are also present. Other clinopyroxenite variants are found along the northwestern zone of the main body: phlogopite clinopyroxenites (with or without nepheline), nepheline-bearing clinopyroxenites (JAC18, JAC82), olivine-bearing clinopyroxenites (JAC13, JAC73, JC127) and andesine-bearing phlogopite clinopyroxenites [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF]. Diopside and olivine form the cumulus assemblage while the other phases are interstitial to them. The nepheline-bearing types occur mainly in the middle and south portions of the northwestern zone [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF], usually nearby the ijolite body. Pyroxenite dikes are found crosscutting the meta-sedimentary country rocks [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] and the northeast portion of the pyroxenite unit. In the latter, the dikes are fine-grained magnetite clinopyroxenites (JAC34) with higher amounts of interstitial Ti-magnetite than usually described in the magnetite clinopyroxenites.

IJOLITE ROCKS

The highest hill of the Jacupiranga Complex (Morro Grande: ~290m) reflects the outcrop of ijolite series rocks and stands out among the lower lands (130 m max) of the clinopyroxenites. That series consists mainly of ijolites and minor melteigites, although some authors have reported less common urtites [START_REF] Herz | Timing and spreading in the South Atlantic: Kimberlite Conference, Araxa. Brasilia, DF: CPRM, Special information from Brazilian alkaline rocks[END_REF][START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF], Ruberti et al., 2005). [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] describes rare melilite ijolites. Ijolites vary widely in grain size, ranging from fine (JAC84, JAC30) to coarse-grained (JAC29.2). They are composed of subhedral diopside (20-40 vol.%), nepheline (40-60 vol.%), phlogopite, Ti-magnetite (5-10 vol.%), kalsilite, apatite, and perovskite. The ijolite main feature is a subhorizontal banding defined by variations in the amounts of nepheline and diopside (Fig. 2C). Near the edges of the ijolite body, some rocks show an increase in clinopyroxene content and are classified as melteigites (JAC29.1, JAC88). From melteigites to ijolites, nepheline changes from interstitial to idiomorphic grains, as already pointed out by [START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF].

FELDSPAR-BEARING ROCKS

Except for the andesine-bearing phlogopite clinopyroxenite, all feldspar-bearing rocks from Jacupiranga occur as veins, dike swarms, or minor intrusions in the Heterogeneous Zone. They can be classified into three major groups: dioritic, monzonitic, and syenitic. [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] describes a large variety of monzonites in Jacupiranga: olivine monzonites, melamonzonites, porphyritic monzonites, monzonites, and quartz monzonites.

According to this author, olivine monzonite (classified as alkali gabbro by [START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF] based on chemical composition) occurs as an intrusion in northern Jacupiranga and shows variations in amount of potassic feldspar (some samples classified as monzodiorites or monzosyenites), while the other monzonites have a more restricted occurrence.

Considering this fact, we selected two monzonitic-types for this study: an olivine monzonite (JAC26.2, composed of clinopyroxene, andesine, potassic feldspar, biotite, olivine, magnetite, and apatite) and a monzonite (JAC25). The latter is a medium-grained rock found in only one outcrop, located in the northern part of the Heterogeneous Zone. It is composed of zoned plagioclase phenocrysts mantled by alkali-feldspar rims (Fig. 2D) set in an andesine, alkali-feldspar, sieve-textured hornblende (Fig. 2E), biotite, titanite, and magnetite groundmass. There is also accessory zircon and acicular apatite. Hornblende is the main mafic phase, unlike all other Jacupiranga lithotypes.

Diorites (JAC20) and meladiorites (JAC22, JAC63) are medium-to coarse-grained rocks, with diopside (20-35 vol.%) and zoned plagioclase (An<50%, 30-60 vol.%) as cumulus phases. Intercumulus phases are biotite, magnetite, and minor apatite. In some samples, diopside cores are partially corroded and are replaced by biotite (Fig. 2F). According to [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF], most of the "gabbroic" rocks already described in Jacupiranga show plagioclase with An<50% and should therefore be classified as diorites.

Syenitic rocks feature a large compositional and textural variation and comprise melasyenites, porphyritic syenites, syenites, quartz syenites, and alkali-feldspar syenites [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF]. The alkali-feldspar syenites (JAC32, JAC46.3) are the dominant type and consist of alkali-feldspar and aggregates of subhedral to anhedral clinopyroxene, hastingsite, titanite, biotite, and magnetite (Fig. 2G). The hastingsite exhibits pleochroism from yellowish brown to dark brown, and occurs in close association with the clinopyroxene. Besides the usual pale-brown clinopyroxene, alkali feldspar syenites also show rare, isolated green clinopyroxene. Melasyenites (JAC31) are medium-to coarse-grained porphyritic rocks and consist of alkali-feldspar phenocrysts within a groundmass mainly composed of alkali feldspar, clinopyroxene, biotite, and rare nepheline and apatite. Both lithotypes compose a small intrusion in the eastern part of the Heterogenous Zone. Nepheline syenites occur as pegmatitic veins that crosscut all Jacupiranga rocks. They consist of orthoclase, nepheline, clinopyroxene, titanite, and biotite [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF].

FINE-GRAINED ROCKS

Phonolites are associated with olivine monzonites in the northern Heterogeneous Zone. Phonolites (JAC26.1) show alkali feldspar phenocrysts within a groundmass composed of alkali feldspar, amphibole, nepheline, plagioclase, biotite, and titanite.

Lamprophyres are medium-to fine-grained dikes crosscutting alkali-feldspar syenites (JAC46.1 and JAC46.2) or basement rocks (JAC39). They are classified as monchiquite according to Le Maitre (2002) classification. They all feature biotite and clinopyroxene macrocrysts included in a fine-grained matrix made of volcanic glass, clinopyroxene, biotite, alkali feldspar, plagioclase, magnetite, titanite, and apatite. Clinopyroxene shows a wide textural variety: unzoned microcrysts, zoned and unzoned macrocrysts, macrocrysts with overgrowths, and dusty core macrocrysts (Fig. 2H). Lamprophyre JAC46.2 includes corroded olivine macrocrysts in its assemblage, mantled by biotite crystals. Lamprophyres were classified as ankaratrites by [START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF] based on chemical composition (i.e. R1-R2 diagram). However, as these rocks do not fit the definition of ankaratrite recommended by Le Maitre ( 2002) (e.g. normative nepheline>20%, olivine as essential phase), we favor the petrographic classification.

CARBONATITES

Jacupiranga carbonatites form a small elongated body intruded into the clinopyroxenites. Apart of the carbonates (mainly calcite with subordinate dolomite), minerals as apatite, magnetite, forsterite, serpentine, clinohumite, phlogopite, pyrite, pyrrotite, galena, ilmenite, spinel, pyrochlore, baddeleyite, barite, and perovskite also occur [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF].

Apatite is the most important accessory phase (sometimes as a main phase, 5 to 35 vol.%.)

and makes Jacupiranga one of the most significant Brazilian carbonatite-hosted phosphate ores. Much less common accessory phases are carbocernaite, ancylite-(Ce), barytocalcite, norsethite, pyrophanite, zirconolite, bubankite, magnesian siderite, and allanite [START_REF] Costanzo | Fluid inclusions in apatite from Jacupiranga calcite carbonatites: Evidence for a fluid-stratified carbonatite magma chamber[END_REF]. Melcher (1966) identifies two independent plugs (a northern and a southern body)

whereas [START_REF] Gaspar | Magnetite in the carbonatites from the Jacupiranga Complex, Brazil[END_REF] symplectites), although olivine-bearing clinopyroxenites also show fractures filling veins mainly comprising potassic feldspar and phlogopite. In the Neoproterozoic basement, fenitized rocks are predominantly bluish green and their new mineralogical assemblage include albite and sodic amphibole/clinopyroxene [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF], denoting a sodic character for this process.

ANALYTICAL PROCEDURES

Thirty-one samples were submitted to Acme Analytical Laboratories Ltd., Vancouver, Canada, for whole-rock analysis. Major and trace elements were determined by inductively coupled plasma emission spectrometry (ICP-OES) and laser ablation inductively coupled mass spectrometry (LA-ICP-MS), respectively. The data include weight loss on ignition (LOI) in the total. Dunite and wehrlite samples were analyzed for whole-rock major elements using a Panalytical AXIOS Max Advanced X-ray fluorescence spectrometer at the GeoAnalítica-USP facility of the Instituto de Geociências of the University of São Paulo, Brazil, following standard methods described by [START_REF] Mori | Development of a fused glass disc XRF facility and comparison with the pressed powder pellet technique at Instituto de Geociências, São Paulo University[END_REF]. LOI was evaluated using standard gravimetric techniques. For bulk trace element concentrations, those rocks were analyzed at the AETE technical platform (Trace Element Analysis in the Environment, Université de Montpellier) using a ThermoFinnigan ELEMENT XR (HR-ICP-MS: high resolution inductively coupled plasma mass spectrometer) after acid digestion with HNO 3 -HF-HClO 4 , as described by [START_REF] Ionov | Application of the ICP-MS technique to trace element analysis of peridotites and their minerals[END_REF].

Electron microprobe measurements were systematically made on selected olivine, clinopyroxene, biotite, amphibole, and feldspar crystals. The analyses were performed by a Cameca SX100 electron microprobe at the Géosciences Montpellier facilities (University of Montpellier, France) using an acceleration voltage and a beam current of 20 kV and of 10 nA, respectively. Counting time was 12 or 18 s for peak.

In order to better constraint parental magma compositions, trace element concentrations of clinopyroxene cores from clinopyroxenites were measured in-situ by LA ICP-MS at GeoAnalítica-USP facility using a Perkin Elmer ELAN 6100DRC ICP-MS instrument coupled with a Nd: YAG laser (New Wave UP 213 AF) operating at a frequency of 213 nm in a He+Ar atmosphere. The laser ablation operating conditions were a RF potential of 1400 W, a laser energy of 0.2-0.3 mJ, and beam diameter of ca. 60 µm (spot analyses).

The analytical time was of 120", with the first 60" used as blank, and 8.3" of integration time for each element. Synthetic glasses were employed as standards: BHVO-2G (USGS) for Five samples from different lithotypes were selected for 40 Ar/ 39 Ar geochronology. For each one, biotite was preferred for dating. Biotite crystals were separated using conventional techniques (crushing, sieving, Frantz magnetic separation and hand picking) then irradiated at Pavia TRIGA Nuclear Reactor for 50h with an approximate neutrons flux of 10 18 cm -2 s -1 .

Irradiation interferences on K, Ca and Cl were corrected from data acquired earlier by irradiating and analyzing KCl and CaF 2 pure salts. J factors were estimated using duplicates of the Fish Canyon sanidine standard, with an age of 28.02 Ma [START_REF] Renne | Intercalibration of standards, absolute ages and uncertainties in 40 Ar/ 39 Ar dating[END_REF].

Although debated, this value is used as a conservative estimate in the laboratory. For the present analyses, a J value of 0.00541900 ± 9.75 x 10 -6 was determined and used with a relative error of ca. 1%. The samples were analyzed at the Géosciences Montpellier facilities, using a Thermo-Argus IV multi-collection apparatus fitted with 4 faraday cups and a central ion counting system. Samples were loaded in holes of a Cu holder and step heated with an infrared laser until melting was achieved. For each step, the gas was purified through passage on Al-Zr getters. Once cleaned, the gas was introduced into the Argus IV apparatus with 1 min equilibration time before 10 analytical cycles were performed on all of the 5 Ar peaks simultaneously with 36 Ar on the ion counting. All errors are quoted at 2σ.

Zircon crystals were separated from a monzonite sample (JAC25) for U-Pb analysis. (n=17). Age corrected values were based on the argon ages reported in Table 2.

GEOCHRONOLOGY

6.1 U/Pb SHRIMP DATING Zircon crystals within the Jacupiranga monzonite are euhedral to subhedral.

Scanning electron microscope (SEM) cathodoluminescence (CL) imaging reveals primary igneous oscillatory growth or sector zoning for these grains (Fig. 3A). The analyzed spots (Table 1) show U and Th contents of 174-1338 and 54-1576 ppm respectively, and Th/U ranging from 0.11 to 2.21. All spots are distributed along or very near the concordia (Fig. 3B).

Point #15.1 shows a large error, being therefore not included in the age calculation. Eleven out of thirteen spots cluster around 141.0 ± 4.4 to 130.8 ± 4.4 Ma (2σ), which provide the concordia age of 134.9 ± 1.3Ma. The other two spots yield older, yet concordant ages of 178.9 ± 6.4 and 175.8 ± 5.6 Ma.

6.2 40 Ar/ 39 Ar GEOCHRONOLOGY Four out of the five analyzed biotite samples produce relatively undisturbed spectra and well-defined plateau ages (Fig. 4, Table 2), ranging from 131.9 ± 0.5 to 133.7 ± 0.5 Ma (2σ). The plateaus are defined by the release of at least 71% of 39 Ar gas in fifteen or more consecutive steps. Anomalously old apparent ages, probably due to excess argon in some of the low-temperature steps, yield a general decreasing trend to these spectra. Minor disturbances also occur in high temperature steps from two samples, with both older (JAC25)

and younger ages (JAC22), suggesting degassing from high temperature resilient impurities.

When cast in inverse isotope correlation diagrams, these four samples yield very good isochrones (MSWD<1.45) for the plateau steps, with ages from 133.7 ± 0.5 to 131.4 ± 0.7

Ma. 40 Ar/ 36 Ar ratio intercepts range from 305 to 350, and supports the idea of slight contamination through all the age spectra and not only restricted to the low temperature steps. Consequently, inverse isochron ages are preferred over the plateau ones. Besides these samples, the JAC42 also shows an undisturbed spectrum with a plateau age (132.1 ± 0.6 Ma; 39 Ar: 91.2) but defined only by four steps, as the sample melted at anomalous low temperatures. This age is therefore considered as only a weighed mean age. A1).

Overall, Jacupiranga clinopyroxenes are marked by a continuous Na and Fe 3+ enrichment with decreasing Mg, as seen in other Brazilian alkaline units (Fig. 5). The acmite component increases from the cumulate rocks, through ijolites and diorites and finally to syenites. The crystals with the highest Fe 3+ and Na concentrations are olive green diopsides from alkali feldspar syenite. Pale brown diopside is also present in JAC32 and shows Na, REE concentrations for clinopyroxenite diopsides (Supplementary material, Table A2) are 3 to 100 times higher than chondritic values (Fig. 6A). Crystal cores from magnetite et al., 1992); 3. Anitápolis [START_REF] Furtado | Caracterização química dos clinopiroxênios do maciço maciço alcalino de Anitápolis[END_REF]; 4. Itapirapuã [START_REF] Gomes | Petrologia do maciço alcalino de Itapirapuã[END_REF]; 5. Banhadão [START_REF] Ruberti | The Banhadão alkaline complex, southeastern Brazil: source and evolution of potassic SiO 2 -undersaturated high-Ca and low-Ca magmatic series[END_REF]; 6. Tunas [START_REF] Gomes | Petrological and geochemical studies of alkaline rocks from continental Brazil. 2. The Tunas massif, state of Paraná[END_REF]; 7. Cananeia [START_REF] Spinelli | A ocorrência alcalina de Cananéia, litoral sul do estado de São Paulo: química mineral[END_REF]. Bold line: obtained trend for the Jacupiranga Complex. [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] demonstrated that Mg is assigned to the tetrahedral site of Jacupiranga mica through the substitution (VI) Mg+ (IV) Si⇔ (IV) Mg+ (VI) Ti.

For the silicate rocks, the Fe/Mg and Fe/Al ratios increase from clinopyroxenites to monzonites towards the annite end member (Fig. 7). From nepheline-bearing clinopyroxenite to ijolite, the phlogopite shows increasing 

AMPHIBOLE

Amphibole is a rare mineral in the Jacupiranga rocks and was only found in the monzonite JAC25 and in an alkali-feldspar syenite (JAC32). In the monzonite, this phase is olive green in thin section, occurs as a groundmass compound and is mainly classified as edenite (using the spreadsheet of [START_REF] Locock | An Excel spreadsheet to classify chemical analyses of amphiboles following the IMA 2012 recommendations[END_REF] (Fig. 8). In syenites, the alkali feldspar is mainly sanidine with a homogeneous composition 

GEOCHEMISTRY

WHOLE-ROCK MAJOR AND TRACE ELEMENTS

Most rocks from the Jacupiranga Complex are SiO 2 -undersaturated with normative nepheline, except for a SiO 2 -oversaturated monzonite (Table 3). In the TAS diagram (Fig. carbonatites [START_REF] Woolley | Carbonatites: nomenclature, average chemical compositions, and element distribution[END_REF].

The chondrite-normalized REE patterns (Fig. 11A-D Clinopyroxenites, melteigites, and ijolites show irregular patterns in extended multielement diagrams normalized to primitive mantle (Fig. 11E). Almost all analyzed samples either have P content below detection limit or show P negative anomalies coupled with Ti peaks. Rb and K ratios smoothly increase from clinopyroxenites to ijolites. Dunites and wehrlites yield the lowest trace elements concentrations among all Jacupiranga lithotypes. All analyzed samples display pronounced Rb and Zr negative anomalies coupled with Ba and La peaks. From Sm to Lu, patterns show smoothly decreasing enrichment factors, with small ranges.

The rocks from the Heterogeneous Zone (Fig. 11F,G) show more regular patterns with LILE enrichment and, as seen in the cumulate rocks, pronounced troughs at P coupled with Ba and Sr peaks. Monzonite JAC25 differs from the other rocks by the absence of Sr and Ba anomalies. Carbonatites yield regular patterns with a decrease in the enrichment factors from Nd to Lu, marked by Zr and Ti negative anomalies (Fig. 11H). Sr/ 86 Sr i ratios extending from 0.51187 to 0.51251 and from 0.70473 to 0.70609, respectively (Table 4). In the 87 Sr/ 86 Sr i vs. 143 Nd/ 144 Nd i diagram (Fig. 12), the Jacupiranga rocks plot close to the fields defined for the other Cretaceous rocks of the Ponta Grossa Arch Province, particularly those from the Juquiá and Banhadão complexes. Carbonatites and clinopyroxenites show Sr-and Nd-ratios similar to those from previous studies [START_REF] Roden | Sr and Nd Isotopic Composition of the Jacupiranga Carbonatite[END_REF][START_REF] Nelson | Geochemical and isotopic systematics in carbonatites and implications for the evolution of oceanisland sources[END_REF][START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF][START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF] (Roden et al., 1987;[START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF][START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF], clinopyroxenites [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF][START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF], ijolitic rocks [START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF], syenites [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF][START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF] and gabbros [START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF]. Full line fields: Cretaceous alkaline units of the Ponta Grossa Arch Province [START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF][START_REF] Ruberti | The Banhadão alkaline complex, southeastern Brazil: source and evolution of potassic SiO 2 -undersaturated high-Ca and low-Ca magmatic series[END_REF]. Complex occurred over a relatively short time interval (ca. 4 Ma, all errors considered -Fig. 13). The argon ages obtained for the biotites from various lithotypes range from 133.7 ± 0.5 Ma to 131.4 ± 0.7 Ma (2σ). Those data refine the previous K-Ar whole rock ages of ca.130 ± 5 Ma provided by [START_REF] Amaral | Potassium-argon ages of alkaline rocks from southern Brazil[END_REF] and [START_REF] Amaral | Potassium-argon age studies on the Jacupiranga alkaline district, State of São Paulo, Brazil[END_REF] and the Rb-Sr ages presented by [START_REF] Roden | Sr and Nd Isotopic Composition of the Jacupiranga Carbonatite[END_REF]. The only Ar-Ar age previously available for the Jacupiranga Complex (132.79 Ma - [START_REF] Basu | Alkaline igneous rocks of the Deccan and Paraná: implications for the origin of continental flood basalts (CFB)[END_REF] falls within the obtained range.

Additional age constraints are given by the U-Pb zircon age determined for the monzonite. As the zircon population yields analyses from both cores and rims, the concordia age of 134.9 ± 1.3 Ma (2σ) reflects the crystallization age of the monzonite JAC25. The biotite from JAC25 provides an Ar age of 133.7 ± 0.5 Ma, which is within error identical to the U-Pb zircon of the same sample. This similarity in age is taken as evidence of both rather shallow emplacement (<10 km with a geothermal gradient of ca. 30 °C/Km) and rather rapid cooling. The first scenario is in agreement with the low-pressure context indicated by the clinopyroxene composition (Supplementary material, Table A1). Ar/Ar ages are thus considered as emplacement ages, precisely dating the time of intrusion.

The obtained ages also imply that the monzonite cooled before the other rocks, even when compared to other feldspar-bearing rocks (e.g. meladiorite JAC22 -Fig. 13).

There seems to be no obvious age progression for clinopyroxenites, diorites, or lamprophyres since their argon ages fail to show any significant contrast, but this is difficult to decipher within analytical errors. Although [START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF] inferred that the clinopyroxenites and the ijolitic rocks would have emplaced after the dunites and the rocks from the Heterogeneous Zone, our new ages do not allow to reliable assess an emplacement sequence. Since the carbonatite sample did not yield satisfactory plateau or inverse isochron ages, the clear intrusive relation between these rocks and the clinopyroxenites remains the main evidence for the carbonatites representing the final phase of the Jacupiranga magmatic event.

Previously published K/Ar, Ar/Ar, Rb/Sr, and U/Pb data for 14 alkaline occurrences related to the Ponta Grossa Arch region were compiled by [START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF]. According to this data compilation, high-precision ages (Ar/Ar or U/Pb) are only available for two units (Tunas and Cananéia complexes), both yielding Late Cretaceous ages. Early Cretaceous units were dated only by the K/Ar or Rb/Sr methods. Among them, Juquiá, Itanhaém, and Anitápolis complexes show K/Ar ages within our obtained time interval for Jacupiranga. In this sense, [START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF] propose a reference age of ~130 Ma for the Early Cretaceous assemblage, mainly based on the K/Ar and Rb/Sr analyses available from the Jacupiranga rocks [START_REF] Amaral | Potassium-argon age studies on the Jacupiranga alkaline district, State of São Paulo, Brazil[END_REF][START_REF] Roden | Sr and Nd Isotopic Composition of the Jacupiranga Carbonatite[END_REF]. Hence, based on our high precision Ar/Ar and U-Pb ages, we can now better define the extent of the Jacupiranga magmatism, which took place between ca. 134.9 and 131.9 Ma. In a regional context, the age of emplacement of the Jacupiranga Complex is coeval to the tholeiitic basalts from the Paraná Magmatic Province (Ar/Ar: 134.7±1 Ma, [START_REF] Thiede | Parana flood basalts: Rapid extrusion hypothesis confirmed by new 40 Ar/ 39 Ar results[END_REF]. 

JACUPIRANGA MAGMATIC SERIES

Geochemical and isotopic compositions of the silicate rocks from the Jacupiranga Complex are used to evaluate two main magma-evolution trends for that unit: (1) a strongly silica-undersaturated series, probably related to nephelinite melts and (2) a mildly silicaundersaturated series related to basanite melts. That proposal is consistent with previous suggestions made by [START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF], [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF][START_REF] Gaspar | The Magmatic Evolution of the Jacupiranga Complex[END_REF] Evidence for magmas of basanite composition is given by the presence of the lamprophyres dikes in the Jacupiranga Complex (see later sections), whereas the nephelinite melt is more difficult to constrain. Petrological and experimental data point to a parental magma with nephelinite composition for several ultrabasic-alkaline associations around the world (e.g. [START_REF] Le Bas | Nephelinites and carbonatites[END_REF][START_REF] Veksler | Trace element partitioning in immiscible silicate-carbonate liquid systems: an initial experimental study using a centrifuge autoclave[END_REF][START_REF] Verhulst | Petrological and geochemical (trace elements and Sr-Nd isotopes) characteristics of the Paleozoic Kovdor ultramafic, alkaline and carbonatite intrusion (Kola Peninsula, NW Russia)[END_REF][START_REF] Arzamastsev | Geochemical indicators of the evolution of the ultrabasic-alkaline series of Paleozoic massifs of the Fennoscandian shield[END_REF]. Nephelinites occur as dikes in the Anitápolis Complex and they could be considered as representative compositions of the parental magma for this unit [START_REF] Furtado | Petrologia do maciço alcalino de Anitápolis, SC. Tese de doutorado[END_REF]. The Anitápolis Complex shares some similarities with Jacupiranga: Early Cretaceous ages (~132 Ma) and a rock assemblage consisting of pyroxenites, melteigites, ijolites, syenites, and carbonatites [START_REF] Gibson | The limited extent of plume-lithosphere interactions during continental flood-basalt genesis: Geochemical evidence from Cretaceous magmatism in southern Brazil[END_REF]. The Anitápolis Complex can be equally well associated with the Ponta Grossa Arch [START_REF] Riccomini | Tectonic controls of the Mesozoic and Cenozoic alkaline magmatism in the central-southeastern Brazilian Platform[END_REF] and the Lancinha-Cubatão Shear Zone [START_REF] Biondi | Brazilian mineral deposits associated with alkaline and alkalinecarbonatite complexes[END_REF]. A nephelinite melt as parental magma for the strongly silicaundersaturated series could hint at a carbonatite origin, since nephelenite melts have long been related to carbonatite magmas generated by liquid immiscibility, fractional melting, or fractional crystallization (Le [START_REF] Le Bas | Nephelinites and carbonatites[END_REF][START_REF] Freestone | The role of liquid immiscibility in the genesis of carbonatites -an experimental study[END_REF][START_REF] Lee | Liquid immiscibility between nephelinite and carbonatite from 1.0 to 2.5 GPa compared with mantle melt compositions[END_REF][START_REF] Mitchell | Carbonatites and carbonatites and carbonatites[END_REF].

Clinopyroxene fractionation is the main process leading to the evolution of both series (Fig. 9). For the clinopyroxenites, the trace element abundances are controlled by the proportions of cumulus phases, which is emphasized by the similarities between chondritenormalized REE patterns yielded by diopside cores and bulk-rock (Fig. 6A). Crystallization of clinopyroxene, olivine, and Ti-magnetite played a major role at the beginning of the process for both series (generating the clinopyroxenites), causing the depletion in MgO, TiO 2 , Fe 2 O 3tot and CaO. For the strongly silica-undersaturated series, this evolution leads to the early appearance of the nepheline in the system, producing the melteigites and, as its proportion rises, ijolites and urtites. For the mildly silica-undersaturated series, this evolution leads to the early appearance of the plagioclase as a cumulus phase.

For the dunites, the high degree of alteration makes it difficult to distinguish primary textures. Nonetheless, ultramafic rocks containing olivine crystals with less than Fo 90 in their composition, CaO>0.1 wt.% and NiO<0.3 wt.% are typically interpreted to be derived from fractional crystallization processes rather than presenting a mantle origin (e.g. [START_REF] Stormer | Calcium zoning in olivine and its relationship to silica activity and pressure[END_REF][START_REF] Pearson | Mantle sample included in volcanic rocks: xenoliths and diamonds[END_REF][START_REF] Pál-Molnár | Origin of mafic and ultramafic cumulates from the Ditrău Alkaline Massif, Romania[END_REF]. As the Jacupiranga dunites comprise Fo 83-84 , CaO 0.13-0.54 wt.%, and NiO between 0.19-0.33 wt.%, a cumulate origin is assumed. This interpretation differs from the one proposed by [START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF], which suggested a mantle origin for these rocks based on whole-rock Mg#. However, we consider that the olivine in situ analysis is a more accurate indication of their origin, since lowtemperature serpentinization (as assumed for Jacupiranga dunites and wehrlites) does not affect olivine composition [START_REF] Evans | Lizardite versus antigorite serpentinite: Magnetite, hydrogen, and life(?)[END_REF]. In addition, the calculated pressure for the clinopyroxene from wehrlites indicates low-pressure conditions (Supplementary material -A1), consistent with a cumulate origin rather than a mantle one. [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] came to the same conclusion based on olivine enrichment in Fe and Mn from pyroxene-bearing dunites to wehlites, as expected in rocks produced by fractional crystallization and accumulation.

It is difficult to assess whether the dunites belong to the nephelinite or to the basanite series. MELTS thermodynamic modeling was carried out [START_REF] Ghiorso | Chemical mass transfer in magmatic processes. IV. A revised and internally consistent thermodynamic model for the interpolation and extrapolation of liquid-solid equilibria in magmatic systems at elevated temperatures and pressures[END_REF][START_REF] Asimow | Algorithmic modifications extending MELTS to calculate subsolidus phase relations[END_REF] in order to define the early predicted phases to fractionate from each melt (Supplementary material, Table A4). One nephelinite from a nearby alkaline occurrence (i.e. Anitápolis Complex) was selected as representative of the initial liquid for the strongly silica-undersaturated series, whereas a basanitic lamprophyre was used to constrain the mildly silica-undersaturated series evolution. Both models are consistent with the dunites composition, as olivine with Fo 84-80 is the liquidus phase in both tested melts. [START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF], in turn, relate the Jacupiranga dunites to a parental magma with alkaline to mildly alkaline composition, the same as that implied for the gabbro-syenite rocks.

Parental melts for the mildly silica-undersaturated series

Classified as basanites to tephrites, lamprophyres correspond to the least evolved liquids found within the Jacupiranga Complex. Moreover, fine-grained lamprophyre sample JAC46.2 shows a clinopyroxene population with variable textural and chemical features. This sample belongs to the same dike studied by [START_REF] Menezes | The antecryst compositional influence on Cretaceous alkaline lamprophyre dykes, SE Brazil[END_REF], who point out a significant antecryst cargo within that rock (~9 vol.%, composed of clinopyroxene, olivine, and Ti-magnetite) and highlight modifications caused by that antecryst assemblage in the bulk-rock composition. JAC46.1 is considered to be a good representative of a parental melt, since it yields the most primitive composition among analyzed lamprophyres and a minimum antecryst assemblage (diopside with dusty core, <2 vol.%), although it cannot be considered as a primary mantle melt with a pristine composition.

Chondrite-normalized REE patterns of lamprophyres are remarkably similar to those of diorites, syenites, monzonites, and phonolite (Fig. 11B,C). The most evolved rocks actually have lower REE contents, particularly when compared to JAC46.1 (the most REErich lamprophyre), which confirms that fractional crystallization and accumulation played an important role in the formation of the Heterogeneous Zone.

Compositions of early-crystallized minerals of ultramafic cumulates can be used to assess the equilibrium melt composition, particularly the mg# ([MgO/(MgO+FeO T )mol.%]*100). Therefore, the most primitive composition obtained could be considered as potential representative of the parental magma. The mg# of the equilibrium melt was estimated using the equation K D Mineral/melt = (X Fe /X Mg ) Mineral /(X Fe /X Mg ) Melt . Applying the thermodynamic formulas proposed by [START_REF] Putirka | Clinopyroxene + liquid equilibria to 100 kbar and 2450 K[END_REF], we obtain values for the Mg-Fe clinopyroxene/lamprophyre partitioning close to the suggested by [START_REF] Akinin | Clinopyroxene megacrysts from Enmelen melanephelinitic volcanoes (Chukchi Peninsula, Russia): application to composition and evolution of mantle melts[END_REF] (Kd Fe- Mg =0.26). For this investigation, magnetite clinopyroxenite JAC45 was disregarded, as its diopside is characterized by reverse zoning. For the magnetite clinopyroxenite JC105, the calculated mg# for the liquid in equilibrium with clinopyroxene cores varies from 50 to 55, exactly as those of the Jacupiranga lamprophyres (Mg# 50-55). For the olivine-bearing clinopyroxenite JC127, the calculated liquid in equilibrium with clinopyroxene cores yield lower mg# values (46-50) and therefore should represent slightly more evolved melts.

Trace element abundances of the liquids in equilibrium with the diopside cores were calculated using Kd values determined for alkaline lamprophyres [START_REF] Arzamastsev | Trace elements in minerals as indicators of the evolution of alkaline ultrabasic dike series: LA-ICP-MS data for the magmatic provinces of northeastern Fennoscandia and Germany[END_REF][START_REF] Foley | Trace element partition coefficients for clinopyroxene and phlogopite in an alkaline lamprophyre from Newfoundland by LAM-ICP-MS[END_REF]Debosi and Jenner, 1999 -Supplementary material, Table A5). There is a close similarity between the chondrite-normalized REE patterns of the calculated melts and those of the Jacupiranga lamprophyres (Fig. 6B), suggesting that the dike compositions are suitable representatives of the parental magma from which those cumulates crystallized.

Compositional correspondences between alkaline lamprophyre dikes and calculated equilibrium liquids from relict cores of the most primitive cumulus phases from ultramafic cumulates are also seen in the Juquiá alkaline-carbonatite Complex [START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF], nearby the Jacupiranga Complex. For Juquiá, those dikes were considered suitable parental magmas [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF][START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF].

The preferred petrological model for the feldspar-bearing series for the Jacupiranga complex, including important part of the clinopyroxenite cumulates, could be summarized as repeated influxes of antecryst-laden basanite magmas (lamprophyres) that deposited most of their suspended crystals mainly on the floor of the upper-crust magma chamber. Basanitic dikes crosscutting the feldspar-bearing rocks are a further indication of the recurrence of those batches. Similarly, a large volume of cumulates produced by the recurrence of basanite parental magma batches is also suggested for the Juquiá Complex [START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF]. Also, the early predicted phases to fractionate from the basanite melt (Supplementary material, Table A4) are consistent with the formation of clinopyroxenites. Our proposed model differs from that of [START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF], who consider that the entire clinopyroxenite unit was exclusively derived from nephelinitic parental melts, which would have evolved in nearly closed system conditions. 9.2.2 Evidence of crustal assimilation processes in the mildly silica-undersaturated series Concurrent wall-rock assimilation and fractional crystallization (AFC) processes are responsible for trace elements and isotope variations in many continental igneous rocks [START_REF] Depaolo | Trace element and isotopic effects of combined wall rock assimilation and fractional crystallization[END_REF] and proposed for some alkaline units related to the Ponta Grossa Arch region [START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF]. Those processes were envisaged for the Jacupiranga carbonatites by [START_REF] Roden | Sr and Nd Isotopic Composition of the Jacupiranga Carbonatite[END_REF], who attributed the isotopic heterogeneities in those rocks to contamination by crustal material during their differentiation. Based on mineral chemistry, [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] proposed crustal contamination as an important process in the evolution of the feldspar-bearing rocks and andesine-bearing clinopyroxenites of the Jacupiranga Complex. On the other hand, based on isotopic data, [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF] dismiss any significant contribution of contamination processes affecting the isotopic compositions of carbonatites and clinopyroxenites, favoring mantle source heterogeneities.

Our new isotopic data (Fig. 12), including a large variety of the Jacupiranga rocks, extend the known range of Sr and Nd ratios to, respectively, lower 143 Nd/ 144 Nd i and higher 87 Sr/ 86 Sr i values (0.511867 and 0.706086, respectively from meladiorite JAC22 and monzonite JAC25). Sr initial ratios higher than 0.706 are rather unusual among the lithotypes from alkaline-carbonatite units associated to the Ponta Grossa Arch and, if present, [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF] suggest that they are probably associated to crustal contamination or AFC processes.

Together with the highest 87 Sr/ 86 Sr i values, monzonite shows distinctive petrographic and compositional features: (1) absence of clinopyroxene;

(2) zircon among its accessory phases;

(3) disequilibrium textures and (4) a silica-oversaturated composition, unique among the Jacupiranga rocks. The presence of zircon is presumably related to a higher silica activity in the melt [START_REF] Heaman | Paragenesis and U-Pb systematics of baddeleyite (ZrO 2 )[END_REF][START_REF] Lewerentz | Experimental zircon alteration and baddeleyite formation in silica saturated systems: implications for dating hydrothermal events[END_REF]. Disequilibrium textures such as mantled plagioclase phenocrysts, sieve-textured edenite, and acicular apatite hint at open-system conditions and reaction processes during the monzonite crystallization [START_REF] Streck | Mineral textures and Zoning as evidence for Open System Processes[END_REF]. The monzonite sample plots slightly out of the Heterogeneous Zone trend and tends towards the composition field of the Precambrian basement rocks (Fig. 9). Meladiorite yields the lowest 143 Nd/ 144 Ndi values among the analyzed samples and comparatively high 87 Sr/ 86 Sr i . This rock also shows petrographic features suggestive of open system conditions and reaction processes, such as acicular apatite and diopside crystals with partially corroded cores and replaced by biotite. All these features highlight the influence of crustal contamination processes for both monzonite and meladiorite samples. Similar isotopic compositions are also reported on Jacupiranga gabbros and syenites by Beccaluva et al.

(2017), who do not exclude the possibility of crustal contamination processes on the genesis of the northern part of the Jacupiranga Complex.

Positive correlation between a fractionation index (e.g. SiO 2 ) and 87 Sr/ 86 Sr i ratios within a magmatic unit is generally interpreted as reflecting crustal contamination and/or AFC processes, as seen in a few alkaline districts related to the Ponta Grossa Arch (e.g. [START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF]. Some analyzed rocks from the Heterogeneous Zone have a broad positive correlation between 87 Sr/ 86 Sr i and SiO 2 (Fig. 14A), from lamprophyres to monzonites.

However, this trend is not continuous, as the diorite shows 87 Sr/ 86 Sr i values higher than those of the syenites. That fact could be suggestive of more than one differentiation sequence for the Heterogeneous Zone instead of a classical AFC process encompassing all lithotypes.

This proposition agrees with that of [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF], who argues that Jacupiranga syenites cannot have been derived by differentiation from monzonites or diorites because they show overlapping mineral compositions.

Even if we cannot entirely exclude the possibility of crustal assimilation for the syenite types, we consider this possibility an unlikely one because of the lack of petrographic

features suggestive of open-system processes and because those rocks display Nd and Sr isotopic signatures similar to those of clinopyroxenites and carbonatites (Fig. 12), lithotypes not affected by crustal contamination processes [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF]. Furthermore, if assimilation was a significant process in the evolution of the syenites, a straight line connecting these rocks and the contaminant should be seen in the 87 Sr/ 86 Sr i vs. 1/Sr diagram (Fig. 14B). Even though there is no isotopic data available for the Turvo-Cajati rocks or for the Itapeúna granodiorites, these rocks are likely to have high initial 87 Sr/ 86 Sr [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF] and low Sr contents [START_REF] Faleiros | Geologia e Recursos Minerais da Folha Eldorado Paulista -SG-22-X-B-XI, estado de São Paulo[END_REF] in comparison with the Jacupiranga rocks. Monzonite and meladiorite display a positive trend towards the hypothetical contaminant pole, suggesting mixing between parental melts and crustal components, whereas the syenites plot far away from the contaminant pole and tend towards lower 1/Sr values. [START_REF] Peate | Temporal variations in crustal assimilation of magma suites in the East Greenland flood basalt province: tracking the evolution of magmatic plumbing systems[END_REF] pointed out that the persistent use of a magma conduit system is expected to lead to a continuous decrease in the extent of assimilation. As monzonite predates the other rocks by at least 1 Ma (Fig. 13) and presents the strongest evidence of crustal assimilation, this rock-type could have differentiated from a magma batch slightly predating the other ones and therefore would have undergone more extensive crustal interaction. As xenoliths of host rocks were found into the monzonite, this batch ascent probably involved bulk incorporation and partial digestion of crustal rocks that may have helped to create room for the magma ascent [START_REF] Beard | Reactive bulk assimilation: A model for crust-mantle mixing in silicic magmas[END_REF].

To provide further constraint on the crustal assimilation processes, we have attempted to estimate the melt/assimilant ratios using mixing-model isotope curves [START_REF] Albarède | Introduction to Geochemical Modeling[END_REF]. Due to the lack of isotopic data for the surrounding host rocks, we used the Sr and Nd ratios of a representative of the regional basement for the contaminant pole [START_REF] Siga Jr | Calymmian (1.50-1.45 Ga) magmatic records in Votuverava and Perau sequences, south-southeastern Brazil: Zircon ages and Nd-Sr isotopic geochemistry[END_REF]. A hypothetical signature for the parental magma was obtained from the lamprophyre JAC46.2. The diorite and monzonite samples plot along the mixing line (Fig. 12), implying mixing processes between their parental magma and the partial melts from the host rocks, as supported by above-mentioned petrographic and geochemical data.

Our data on the carbonatites (Fig. 12) yield initial Nd and Sr ratios in the same range as those presented by [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF]. Our analyzed clinopyroxenites, ijolite, dunite, wehrlites, lamprophyres, and syenites define a second group close to the clinopyroxenites from [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF] and the syenites from [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF]. Isotopic differences between clinopyroxenites and carbonatites from Jacupiranga have been previously attributed by [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF] to primary features related to their mantle source regions. These authors argue that crustal assimilation processes (within realistic assimilation rates) cannot explain those isotopic variations even when considering suitable isotopic ratios for the host rocks. Therefore, generally, the relatively wide range of isotopic composition within the Jacupiranga lithotypes is best explained by mantle source heterogeneities. However, petrographic features and slightly more radiogenic compositions yielded by the monzonite and by the meladiorite suggest that crustal assimilation processes also played an active role during the evolution of some lithotypes from the mildly silica-undersaturated series. The crustal rock assimilation may be relegated to a local process though, restricted to some of the batches of basanite parental magma from which the rocks from the Heterogeneous Zone originated. Such conclusion only partially agrees with the model constrained by [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] for the feldspar-bearing rocks, as this author proposed crustal contamination processes affecting all of these rocks, which is not entirely consistent with our data.

However, a rather similar scenario is proposed for the Juquiá Complex, as only syenodiorites and some dikes show evidence of wall-rock contamination [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF].

Characteristics of the mantle sources for the basanite melts

Although some samples (i.e. meladiorite and monzonite) show evidence of crustal contamination, overall, the Jacupiranga rocks do not appear significantly contaminated by crustal materials. Therefore, their isotopic and trace elements compositions should reflect their mantle sources. Experiments indicate that alkali basalts and basanite melts, such as that proposed for the Jacupiranga mildly silica-undersaturated series, may be produced at small degrees of partial melting from garnet peridotites with 0.1-0.25 wt.% CO 2 [START_REF] Dasgupta | Partial melting experiments of peridotite þ CO 2 at 3 GPa and genesis of alkalic ocean island basalts[END_REF]. Parental magmas of alkaline occurrences related to the Ponta Grossa Arch (e.g.

Juquiá, Jacupiranga, and Pariquera-Açu complexes) are inferred to derive from a lithospheric garnet peridotite mantle source metasomatized by carbonated fluids [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF][START_REF] Gibson | The limited extent of plume-lithosphere interactions during continental flood-basalt genesis: Geochemical evidence from Cretaceous magmatism in southern Brazil[END_REF][START_REF] Morbidelli | The Pariquera Açu K-alkaline complex and southern Brazil lithospheric mantle source characteristics[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF][START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF][START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF]. The high LREE/HREE ratios (Fig. 6B) and high abundances of incompatible elements yielded by the calculated basanite liquid are characteristic of the primary melts in the region and imply enriched mantle sources [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF]. According to these authors, although the local Brazilian granitic crust shows similar εNd (ca. -7), lower La/Nb ratios in the Anitápolis nephelinites (0.72-0.98, whereas the granitic crust is > 2.5) rule out the continental crust as a source region.

Vein-plus-wall-rock melting mechanism [START_REF] Foley | Vein-plus-wall-rock melting mechanisms in the lithosphere and the origin of potassic alkaline magmas[END_REF] explains the wide chemical spectrum seen in alkaline associations. Alkaline magmas are considered as partial melts of metasomatic veins hybridized with variable amounts of partial melts from the peridotite wall rock. At pressures below 1.5-2.0 GPa, dolomite will react with peridotite to produce clinopyroxene and a CO 2 rich fluid (CaMg(CO 3 ) 2 + 4MgSiO 3 = CaMgSi 2 O 6 + 2MgSiO 4 + 2CO 2fluid -Dalton and Wood, 1993), creating a clinopyroxene-veined network (enriched in incompatible elements) within a peridotite matrix. High CaO/Al 2 O 3 ratio, high La/Yb, and low Ti/Eu values are commonly interpreted as signatures of CO 2 -rich metasomatism [START_REF] Rudnick | Carbonatite metasomatism in the northern Tanzanian mantle: petrographic and geochemical characteristics[END_REF][START_REF] Klemme | Experimentally determined trace and minor element partitioning between clinopyroxene and carbonatite melt under upper mantle conditions[END_REF][START_REF] Coltorti | Carbonatite metasomatism of the oceanic upper mantle: evidence from clinopyroxenes and glasses in ultramafic xenoliths of Grande Comore, Indian Ocean[END_REF]. Element ratios were employed to investigate the sources of the calculated melts and lamprophyres, following the criteria of [START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF].

Experimental liquids produced from carbonate-bearing lherzolite that underwent small degrees of partial melting show CaO/Al 2 O 3 ratios from 1-11 [START_REF] Dasgupta | Partial melting experiments of peridotite þ CO 2 at 3 GPa and genesis of alkalic ocean island basalts[END_REF] Lamprophyres exhibit extremely low ratios (0.06-0.08).

Bulk partition coefficients estimated for mantle mineral assemblage in equilibrium with carbonatitic melt indicate that La is highly incompatible under these conditions, whereas

Zr has a more moderately incompatible behavior [START_REF] Dasgupta | Trace element partitioning between garnet lherzolite and carbonatite at 6.6 and 8.6 GPa with applications to the geochemistry of the mantle and of mantle-derived melts[END_REF][START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF]. The La N /Zr N values for the calculated parental melts of the Jacupiranga clinopyroxenites are greater than 3.8 and JC105 yields higher ratios (8.3-11.3) compared to JC127 (3.8-4.9). For the lamprophyres, JAC46.1 shows a La N /Zr N ratio close to the JC105 range, whereas the other analysed samples together with dike studies by [START_REF] Menezes | The antecryst compositional influence on Cretaceous alkaline lamprophyre dykes, SE Brazil[END_REF] yield ratios close to those of JC127.

Accordingly, major and trace element ratios favor a mantle source with variable degrees of CO 2 -rich metasomatism for the basanite parental melts of the Jacupiranga Complex. However, other mineralogical controls related to the source (e.g. amounts of olivine and garnet) may affect the composition of the calculated melts and should also be considered. As Hf and Y are moderately incompatible in peridotite and pyroxenite mantle assemblages in equilibrium with carbonatitic liquid [START_REF] Dasgupta | Trace element partitioning between garnet lherzolite and carbonatite at 6.6 and 8.6 GPa with applications to the geochemistry of the mantle and of mantle-derived melts[END_REF] and Y is compatible with garnets [START_REF] Green | SIMS determination of trace element partition coefficients between garnet, clinopyroxene and hydrous basaltic liquids at 2-7.5 GPa and 1080-1200[END_REF], variations in the Hf/Y ratios are controlled by the garnet content in the source. The calculated parental melts of the Jacupiranga clinopyroxenites have relatively high Hf N /Y N ratios. JC127 yields greater values (7.6-9.4) than JC105 (3.9-5.9). For the lamprophyres, JAC39 shows Hf N /Y N ratio close to the JC127 range, whereas the other analysed samples together with dikes studies by [START_REF] Menezes | The antecryst compositional influence on Cretaceous alkaline lamprophyre dykes, SE Brazil[END_REF] yield ratios close to those of JC105.

When applying the non-modal batch melting models developed by [START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF] in our data, different degrees of partial melting of a homogeneous source alone cannot explain the differences in trace elements ratios (Fig. 15). In consequence, the variations in the La N /Zr N ratios between the calculated liquids of JC127 and JAC105 and between the lamprophyre samples (particularly JAC46.1 and JAC39) are most probably due to differences in degree of CO 2 -rich metasomatism of the source. The models suggest that JAC46.1 and the calculated liquid of JC105 have a larger component of melting resulting from veins than JAC39 and the calculated parental magma of JC127. Besides, Hf/Y ratios suggest a modal heterogeneity in the source residues, with the source of JAC46.1 and JC105 yielding higher cpx/gt values than those of JAC39 and JC127.

A comparison between the equilibrium liquids of Jacupiranga and those found for the Juquiá Complex [START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF] indicate that these are derived from sources with similar degrees of CO 2 -rich metasomatism (e.g. similar La N /Zr N ratios). On the other hand, those rocks yield slightly different Hf N /Y N ratios, which suggest either variable degrees of partial melting or garnet peridotite sources with variable cpx/gt proportions. The latter option agrees with the model proposed by [START_REF] Stracke | Earth's heterogeneous mantle: a product of convection-driven interaction between crust and mantle[END_REF], which advocates small-scale heterogeneities (i.e. kilometer scale) in the melting region of mantle sources (Juquiá and Jacupiranga complexes are ca. 50 km apart).

Additionally, the aforementioned data make clear that more than one batch of parental melt of basanite composition is needed to explain the differences in calculated parental melts compositions of clinopyroxenites JC105 and JC127, in agreement with the proposed idea of recurrence of basanite parental magma pulses. That scenario diverges from the petrological model proposed by [START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF], in which closed system conditions are considered. Also, the reverse zoning seen in the clinopyroxene crystals of some magnetite clinopyroxenite (JAC45) can be suggestive of open system conditions, such as magma recharge [START_REF] Streck | Mineral textures and Zoning as evidence for Open System Processes[END_REF]. Under these processes, layered intrusions usually present some compositional reversals within the rock sequence [START_REF] Eales | Crustally contaminated komatiite: Primary source of the chromitites and marginal, Lower, and Critical zone magmas in a staging chamber beneath the Bushveld Complex[END_REF], which are not recognized in Jacupiranga, probably due to the lack of continuous exposures. 3. Rather than of mantle origin, dunites and wehrlites are cumulates mainly composed of cumulus olivine with Fo 83-84 . It is difficult to assess whether the dunites belong to the nephelinite or to the basanite series, as both parental magmas show olivine with coherent forsterite contents as liquidus phase.

4. Multiples batches of basanite parental magma evolving mainly by fractional crystallization gave rise to the mildly silica-undersaturated series. Lamprophyres are considered as good representative compositions for those melts.

5. Calculated melts in equilibrium with cumulus diopside cores from clinopyroxenites are considered representative of parental magmas. Those melts yield mg# and trace element contents similar to those of lamprophyres. Therefore, at least parts of the clinopyroxenites are probably genetically related to the basanite melts and belong to the mildly silica-saturated series.

6. Some feldspar-bearing rocks yield petrographic, geochemical, and isotopic features indicative of crustal assimilation, although it may be relegated to a local process.

Monzonite has undergone more extensive crustal contamination than the other mildly silica-undersaturated rocks, as indicated by the presence of zircon, disequilibrium textures, silica-oversaturated composition, and the highest 87 Sr/ 86 Sr i values within the Jacupiranga Complex. As monzonite slightly predates the other lithotypes, the ascent of the magma batch from which monzonite crystallized may have involved intense bulk incorporation and partial digestion of crustal rocks that helped to create room for the magma ascent. 0.048 0.005 0.017 0.060 0.000 0.207 0.025 0.231 0.161 0.089 0.108 0.209 0.000 0.000 0.000 0.000 0.000 Al VI 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.000 0.071 0.052 0.157 0.000 0.000 0.000 0.000 0.000 0.087 0.150 0.260 0.000 0.091 0.021 0. [START_REF] Dobosi | Petrologic implications of trace element variation in clinopyroxene megacrysts from the Nógrád volcanic province, north Hungary: a study by laser ablation microprobe-inductively coupled plasma-mass spectrometry[END_REF]. c Partition coefficients compiled from [START_REF] Foley | Trace element partition coefficients for clinopyroxene and phlogopite in an alkaline lamprophyre from Newfoundland by LAM-ICP-MS[END_REF]. d Partition coefficients obtained from interpolated data [START_REF] Azzone | Trace element composition of parental magmas from mafic-ultramafic cumulates determined by in situ mineral analyses: The Juquiá mafic-ultramafic alkaline-carbonatite massif, SE Brazil[END_REF].

INTRODUCTION

During the Mesozoic and Cenozoic times, the central-southeastern region of the South American Platform was the scenario of an extensive magmatic activity of tholeiitic and alkaline-carbonatite affinity (e.g. [START_REF] Almeida | Relações tectônicas das rochas alcalinas Mesozoicas da região Meridional da Plataforma Sul-americana[END_REF][START_REF] Piccirillo | The Mesozoic flood volcanism of the Paraná basin: petrogenetic and geophysical aspects[END_REF]Comin-Chiaramonti and Gomes, 2005). Notably, the alkaline occurrences were emplaced along the margins of the intracratonic Paraná Basin. Among them, the Jacupiranga Complex is a vastly known ultramafic-alkaline carbonatite unit (e.g. [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF][START_REF] Gaspar | Magnetite in the carbonatites from the Jacupiranga Complex, Brazil[END_REF][START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF][START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF][START_REF] Costanzo | Fluid inclusions in apatite from Jacupiranga calcite carbonatites: Evidence for a fluid-stratified carbonatite magma chamber[END_REF], mainly due to its important phosphate deposit related to the carbonatite body but also because of the particularities of some ultramafic cumulates (i.e. jacupirangites, [START_REF] Derby | The magnetite ore districts of Jacupiranga and Ipanema, São Paulo, Brazil[END_REF]. However, only a few studies cover the silicate rocks (> 90% of its outcropping surface [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF][START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF][START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF][START_REF] Morbidelli | Mineralogical, petrological and geochemical aspects of alkaline and alkaline-carbonatite associations from Brazil[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF]. Therefore, any attempt to propose a petrological model or an origin for the carbonatite rocks has been done without a

proper and comprehensive view of the Jacupiranga Complex.

The origin of carbonatites has long been a subject of debate (e.g. [START_REF] Freestone | The role of liquid immiscibility in the genesis of carbonatites -an experimental study[END_REF][START_REF] Le Bas | Nephelinites and carbonatites[END_REF]Lee andWyllie, 1997, Harmer and[START_REF] Harmer | The case for primary, mantle-derived carbonatite magma[END_REF]. Broadly speaking, the models consider two scenarios: (1) carbonatites derived from a primary carbonate magma directly generated from peridotite mantle and (2) derivative carbonatite melts related to primary silicate parental magmas (through fractional crystallization or liquid immiscibility). For this reason, in cases where carbonatites are spatially and temporally associated with alkaline and ultramafic rocks, as in the Jacupiranga Complex, the origin of the carbonatites cannot be properly constrained without taking into account the silicate lithotypes.

Although alkaline rocks and carbonatites are well established as mantle-derived, there is still no consensus on the nature and location of their mantle sources. Whereas some authors consider heterogeneous subcontinental mantle as suitable sources (e.g. [START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF][START_REF] Omarini | An overview of the Mesozoic-Cenozoic magmatism and tectonics in Eastern Paraguay and central Andes (Western Gondwana): Implications for the composition of mantle sources[END_REF][START_REF] Ashwal | Isotopic evidence for a lithospheric origin of alkaline rocks and carbonatites: an example from southern Africa[END_REF], other workers favor a derivation from sub-lithospheric sources (e.g. [START_REF] Bell | Source of parental melts to carbonatites: critical isotopic constraints[END_REF]. According to [START_REF] Pearson | Mantle sample included in volcanic rocks: xenoliths and diamonds[END_REF], of the incompatible element isotope systems, the Lu-Hf isotope is the most robust to metasomatic overprinting. The immobility of the refractory Lu-Hf system during metasomatic processes thus provides a powerful tool for evaluating the mantle source characteristics, particularly when dealing with the subcontinental lithospheric mantle. To date, only two Brazilian alkaline occurrences were studied on the basis of Hf isotope composition: Goiás peridodites [START_REF] Carlson | Chemical and isotopic relationships between peridotite xenoliths and mafic-ultrapotassic rocks from Southern Brazil[END_REF] and Catalão I [START_REF] Guarino | U-Pb ages, geochemistry, C-O-Nd-Sr-Hf isotopes and petrogenesis of the Catalão II carbonatitic complex (Alto Paranaíba Igneous Province, Brazil): implications for regional-scale heterogeneities in the Brazilian carbonatite associations[END_REF], both from Late Cretaceous.

The idea addressed in the current manuscript, still in preparation, is to contribute to the understanding of the Jacupiranga Complex petrogenesis, mainly based on the enhanced resolution provided by the Hf and Pb isotopes. This study offers the first Hf isotope analyses for the alkaline magmatism that occurred in Southeastern Brazil from during Early Cretaceous times, as well as 10 new Pb isotope analyses for the Jacupiranga Complex, including the first analyses for dunite, wehrlite, ijolite, feldspar-bearing rocks, and lamprophyre. For the origin of the carbonatites, we also used trace element data from our previous work. This study focuses on (1) the Hf isotopic composition of the Jacupiranga rocks;

(2) better constraints of the mantle sources; and (3) the petrogenetical relationship, if any, between the carbonatites, the mildly silica-undersaturated and strongly silicaundersaturated series.

GEOLOGICAL SETTING

Mainly driven by the Atlantic Ocean opening, the last activation stage of the South American Platform (Upper Jurassic onwards - [START_REF] Almeida | The origin and evolution of the South American Platform[END_REF] comprises episodes of both tholeiitic and alkaline magmatism. In the southern part of the platform, the tholeiitic basaltic activity gave rise to the Paraná Magmatic Province (PMP: 134.7 ± 1 Ma, [START_REF] Thiede | Parana flood basalts: Rapid extrusion hypothesis confirmed by new 40 Ar/ 39 Ar results[END_REF], one of the largest continental flood basalts in the world, accompanied by minor intrusive activity. Its alkaline counterpart occurs as intrusive bodies (plugs, stocks, and dikes) with a wide range of compositions (SiO 2 -saturated or unsaturated, down to ultrabasic rocks, carbonatites and/or kimberlites), all yielding Early to Late Cretaceous ages [START_REF] Gomes | An introduction to the alkaline and alkaline-carbonatitic magmatism in and around the Paraná-Basin[END_REF]).

In the central-southeastern part of the platform (Fig. 1A), the alkaline occurrences are distributed along the margins of the intracratonic Paraná Basin [START_REF] Gomes | An introduction to the alkaline and alkaline-carbonatitic magmatism in and around the Paraná-Basin[END_REF]. The detailed tectonic framework controlling the distribution of the alkaline activity in the eastern margin of the basin is still controversial, despite being clearly associated with the basin boundaries. It is noteworthy that these igneous bodies are aligned along the Lancinha-Cubatão Shear Zone [START_REF] Biondi | Brazilian mineral deposits associated with alkaline and alkalinecarbonatite complexes[END_REF], which represents a NE-SW suture zone (Fig. 1A) formed during the Gondwana amalgamation and possibly reactivated during the Atlantic Ocean opening.

There is no general agreement on neither the mechanical nor the petrogenetic relations between these tectonic features and the genesis of the alkaline complexes.

Nonetheless, the southern and central coastal intrusions are usually related to the Ponta Grossa Arch [START_REF] Almeida | Relações tectônicas das rochas alcalinas Mesozoicas da região Meridional da Plataforma Sul-americana[END_REF][START_REF] Riccomini | Tectonic controls of the Mesozoic and Cenozoic alkaline magmatism in the central-southeastern Brazilian Platform[END_REF], a NW-SE trending structure enhanced by swarms of basaltic dikes from the PMP. Among the four N40-60W-trending lineaments controlling the Ponta Grossa Arch structural framework (Fig. 1A-Guapiara, São Jerônimo-Curiúva, Rio Alonso, and Rio Piquiri), the southern sectors of the Guapiara and São

Jerônimo-Curiúva lineaments present some alkaline and alkaline-carbonatite intrusions aligned parallel to their axis [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF]. Three Early Cretaceous complexes are related to the Guapiara lineament, and the Jacupiranga Complex (~65 km2) is the largest of them.

The Jacupiranga Complex is a NNW elongated body [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF] intrusive into the Neoproterozoic Itapeúna granodiorites and micaschists from the Turvo-Cajati Formation (Fig. 1B). The northern portion of the unit mostly consists of dunites and rare wehrlites. This ultrabasic body is surrounded by an annular zone composed of rocks of widely varying composition (syenites, gabbros, diorites, monzonites, and fine-grained rocks) and restricted lateral continuity (decametric at most). Due to these features, we rather use the term "heterogeneous zone" to designate this unit. The southern part of Jacupiranga consists of a clinopyroxenite unit (~22 km 2 ) with cumulative features associated with a crescent-shaped body of banded ijolites. In the central clinopyroxenite, a carbonatite body (1.5 km²) hosts a phosphate ore deposit that has been mined for several decades. In our previous work (Chmyz et al., 2016, submitted manuscript), we propose two distinct magmatic series for the Jacupiranga silicate rocks: (1) a strongly silica-undersaturated series, comprising part of the clinopyroxenites and the ijolitic rocks, probably related to nephelinite melts and (2) a mildly silica-undersaturated series, related to basanite parental magmas and comprising the feldspar-bearing rocks, phonolites, lamprophyres, and part of the clinopyroxenites.

MAIN PETROGRAPHIC ASPECTS

The general geology of Jacupiranga has been extensively described by [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF][START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF], [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF], and more recently summarized by Ruberti et al. (2005). A brief description of each analyzed sample is given below. For a more detailed description, see Chmyz et al. (2016, submitted manuscript), where all these samples have previously been characterized in terms of major and trace elements, Sr-Nd isotopes and Ar/Ar ages.

Magnetite clinopyroxenite JAC45 is a coarse-grained layered mesocumulate mainly composed of subhedral cumulus diopside (>80 vol.%), either normally or reversely zoned. Timagnetite (10-20 vol.%) is the main interstitial phase. Although scarce, there is also phlogopite, apatite, and perovskite (mantling the Ti-magnetite). In comparison with the magnetite clinopyroxenite, the nepheline-bearing clinopyroxenite (JAC18) differ by the presence of interstitial nepheline and by the higher and lower amounts of phlogopite and Timagnetite, respectively. Ijolite JAC29.2 is a coarse-grained rock composed of subhedral diopside (40 vol.%), nepheline (55 vol.%), phlogopite (<5% vol.%), Ti-magnetite (5 vol.%), apatite, and perovskite. The ijolite main feature is a subhorizontal banding defined by variations in the amounts of nepheline and clinopyroxene.

The Jacupiranga dunites are hindered by the absence of fresh outcrops and regolith thickness, so their primary features are scarcely known. Three short drill holes samples were selected for this study: a fine-grained dunite (JAC248) essentially with subhedral olivine, and two medium-grained wehrlites (JAC220 and JAC243), with olivine and minor subhedral diopside (<15 vol.%). Nonetheless, weathering and the high serpentinization degree (30-70%) prevent to accurately retrieve the primary textures or minerals proportion and satisfactorily classify this rock.

We selected a representative sample of each group of feldspar-bearing rocks that constitute the Heterogeneous Zone (i.e. dioritic, syenitic, and monzonitic rocks), except for the syenites, for which two samples were selected. Melasyenite JAC31 is a medium-to coarse-grained porphyritic rock, presenting alkali feldspar phenocrysts within a matrix mainly composed of alkali feldspar, clinopyroxene, biotite, and minor nepheline and apatite. Alkalifeldspar syenite JAC32 is characterized by mafic aggregates (i.e. subhedral to anhedral clinopyroxene, hastingsite, titanite, biotite, and magnetite) associated with alkali feldspar euhedral crystals. Monzonite (JAC25) is a medium-grained rock outcropping in the northern part of the heterogeneous zone. It is composed of zoned plagioclase phenocrysts mantled by alkali-feldspar rims set in an andesine, alkali-feldspar, sieve-textured hornblende, biotite, titanite, magnetite matrix, and accessory zircon. Meladiorite JAC22 is a medium-grained rock composed of diopside and Ca-plagioclase, with minor biotite, apatite, and magnetite.

Lamprophyres are coarse-to fine-grained rocks that occur as dikes crosscutting alkali-feldspar syenites. Two lamprophyre samples were selected for Pb and Hf isotopic investigations: a coarse-(JAC46.1) and a fine-grained (JAC46.2) samples, both related to the same outcrop. They both feature biotite and clinopyroxene macrocrysts included in a finer-grained matrix made of volcanic glass, clinopyroxene, biotite, alkali feldspar, plagioclase, magnetite, titanite, and apatite.

For the carbonatites, we selected four samples: two apatite calcite carbonatites (CCap), one outcropping in the southern part of the intrusion (JAC04) and the other in the north (JAC44); one dolomite carbonatite (DC -JAC09) and a magnetite calcite carbonatite (CCmg -JAC08). All samples present apatite, magnetite and phlogopite as essential phases, although in different proportions. Additionally, as the carbonatite ore mineral, the apatite occurs in different forms: small aggregates (JAC44), pockets (JAC09), layers (JAC08), or disseminated throughout the rock (JAC04). 

RESULTS

Pb ISOTOPE COMPOSITION

Whole-rock Th contents are extremely low in the clinopyroxenites (<0.5 ppm) and rather low in the carbonatites (0.6 -3.5 ppm). As noted by [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF], samples of these lithotypes with low Th values also yield low P 2 O 5 , suggesting apatite as an important Th carrier. Additionally, most of the Jacupiranga analyzed rocks show low to extremely low whole-rock U contents. Similar results were obtained for the carbonatites and clinopyroxenites by [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF]. Four analyzed samples (JAC08, JAC09, JAC29.2, and JAC45) are below the detection limit of 0.1 ppm.

Considering the dataset presented by [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF], the Jacupiranga rocks show rather low Pb (< 24 ppm). Unfortunately, we have detected a possible analytical error regarding our measurements of common Pb concentrations for the feldspar-bearing rocks and lamprophyres. Our Pb concentrations for these rocks are systematically lower than those presented by [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF] and [START_REF] Menezes | The antecryst compositional influence on Cretaceous alkaline lamprophyre dykes, SE Brazil[END_REF]. Lamprophyre JAC46.2 yields almost identical major and trace elements compositions than those obtained by [START_REF] Menezes | The antecryst compositional influence on Cretaceous alkaline lamprophyre dykes, SE Brazil[END_REF] for the same dike, except for Pb (four times higher than our data). For carbonatites and clinopyroxenites, our Pb measurements are coherent with those from [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF]. However, in order to minimize further misinterpretations, we have decided to present the measured Pb isotopic ratios for the entire dataset, which should be considered with some caution. These analyses will be redone for further publication.

Pb isotope data are presented in Overall, the analyzed carbonatites show measured Pb-isotope values similar to those obtained by [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF] and they have the lowest Pb ratios among the analyzed lithotypes. Despite their overall distinct major and trace element compositions, the rocks from the strongly and mildly silica-undersaturated series have quite similar Pb ratios and do not yield any organized distribution. [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF]. The parameters EM1, EM2, HIMU, and DMM are approximations of mantle end-members as in [START_REF] Bell | Nd, Pb and Sr isotopic compositions of east African carbonatites: evidence for mantle mixing and plume inhomogeneity[END_REF], taken after [START_REF] Hart | A possible new Sr-Nd-Pb mantle array and consequences for mantle mixing[END_REF][START_REF] Hart | Mantle plumes and entrainment: isotopic evidence[END_REF] 

Hf ISOTOPE COMPOSITION

The Hf isotope data are given in Table 2 and presented in Fig. 3. The data span a rather large range of 176 Hf/ 177 Hf i values: 0.28227-0.28277 (-16.48< εHf i < 1.47).

Clinopyroxenites and ijolites display higher Hf isotope ratios (0.28265-0.28276) than the feldspar-bearing rocks and the lamprophyres (0.28227-0.28253), with a small gap of 0.00012 separating both groups. Monzonite and meladiorite are the least radiogenic rocks. Dunite yield an initial Hf isotopic ratio (0.282771) similar with clinopyroxenites-ijolites, whereas wehrlite yields a composition (0.282526) close to the feldspar bearing rocks. The εHf and εNd correlate well, giving a linear expression of εHf = 0.895εNd -0.176 with R 2 = 0.99 for clinopyroxenites-ijolites and εHf = 0.619εNd -0.034 with R 2 = 0.94 for the rocks from the Heterogeneous Zone. Most samples lie on, or close to, the mantle array, a linear regression (εHf = 1.33εNd + 3.19) through MORB to OIB (data from [START_REF] Vervoort | Relationships between Lu-Hf and Sm-Nd isotopic systems in the global sedimentary system[END_REF]. Departure from the mantle array can be expressed in terms of the parameter ΔεHf [START_REF] Beard | Hf isotope composition of late Cenozoic basaltic rocks from northwestern Colorado, USA: new constraints on mantle enrichment processes[END_REF], with data plotting above the reference live having positive values. The Jacupiranga clinopiroxenites-ijolites have positive ΔεHf values (+3.48 to +4.13), whereas the rocks from the Heterogeneous Zone show negative to slightly positive values (-2.27 to 0.67). Dunite yields the highest ΔεHf among the analyzed samples (4.71) and wehrlite JAC243 has a slightly negative ΔεHf (-0.19). [START_REF] Salters | Domains of depleted mantle: New evidence from hafnium and neodymium isotopes[END_REF], Goiás peridotite xenoliths [START_REF] Carlson | Chemical and isotopic relationships between peridotite xenoliths and mafic-ultrapotassic rocks from Southern Brazil[END_REF] and Catalão rocks [START_REF] Guarino | U-Pb ages, geochemistry, C-O-Nd-Sr-Hf isotopes and petrogenesis of the Catalão II carbonatitic complex (Alto Paranaíba Igneous Province, Brazil): implications for regional-scale heterogeneities in the Brazilian carbonatite associations[END_REF] are shown for comparison. Other fields were compiled from [START_REF] Guarino | U-Pb ages, geochemistry, C-O-Nd-Sr-Hf isotopes and petrogenesis of the Catalão II carbonatitic complex (Alto Paranaíba Igneous Province, Brazil): implications for regional-scale heterogeneities in the Brazilian carbonatite associations[END_REF] and references therein.

Table 2 -Hf isotopic ratios for the Jacupiranga samples. Abbreviations: CPX, magnetite clinopyroxenite ; Ne-CPX, nepheline-bearing clinopyroxenite ; IJL, ijolite ; WEH, wehrlite ; DUN, dunite ; LAM, lamprophyre ; MDIO, meladiorite ; AFS, alkali feldspar syenite ; MSY, melasyenite; MON, monzonite. Isotopic ratios were corrected for in situ radioactive decay using Ar-Ar ages obtained on the same samples (Chmyz et al., 2016, submitted manuscript) 

DISCUSSION

CONSTRAINTS ON THE ORIGIN OF THE JACUPIRANGA CARBONATITES

Experimental data suggest that calcite carbonatites may be products of crystal accumulation, rather than representatives of melts (e.g. [START_REF] Bas | Carbonatite-Nephelinite Volcanism[END_REF]Veskler et al., 1998;[START_REF] Lee | Petrologic and geochemical investigation of carbonates in peridotite xenoliths from northeastern Tanzania[END_REF]. The Jacupiranga carbonatites show a pronouncing layering defined by the variation in the amounts of non-carbonate phases (apatite, olivine, magnetite, phlogopite, and sulfides). However, according to [START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF], this mineral layering is usually vertical (i.e. intrusions C2 and C4) or steeply dipping (i.e. C1 and C5) and only C3 shows layers with lower angles of dip (i.e. between 20 and 40°). Although steep dips are commonly found in the lateral zones of cumulative intrusions, it is unlikely here considering how widespread those vertical/subvertical layers are. Moreover, considering the density of magnetite crystals (5.1-5.2 g/cm³), it would be expected that in an accumulation dominated process the magnetite occurred (at least locally) as conspicuous magnetite-enriched levels. Therefore, we consider that those layers shall be interpreted as flow structures (as already proposed by [START_REF] Melcher | The carbonatites of Jacupiranga, São Paulo, Brazil[END_REF], rather than of cumulative origin.

Based on petrological and experimental studies, three different models are classically invoked to explain the genesis of carbonatites: (1) direct partial melting of a metasomatized mantle source (e.g. Harmer et al., 1998;[START_REF] Harmer | The case for primary, mantle-derived carbonatite magma[END_REF][START_REF] Srivastava | Emplacement age and isotope geochemistry of Sung Valley alkalinecarbonatite complex, Shillong Plateau, northeastern India: implications for primary carbonate melt and genesis of the associated silicate rocks[END_REF]; (2) fractional crystallization of a parental magma with carbonated silicate composition (e.g. [START_REF] Lee | Experimental data bearing on liquid immiscibility, crystal fractionation, and the origin of calciocarbonatites and natrocarbonatites[END_REF][START_REF] Brassinnes | Magmatic evolution of the differentiated ultramafic, alkaline and carbonatite intrusion of Vuoriyarvi (Kola Peninsula, Russia). A LA-ICP-MS study of apatite[END_REF] or (3) derivation by liquid immiscibility from a carbonated silicate melt such as carbonated nephelinite (e.g. Le [START_REF] Bas | Carbonatite-Nephelinite Volcanism[END_REF][START_REF] Hamilton | The behaviour of trace elements in the evolution of carbonatites[END_REF][START_REF] Wyllie | Model system controls on conditions for formation of magnesiocarbonatite and calciocarbonatite magmas from the mantle[END_REF].

Generally, liquid immiscibility from silicate liquids is believed to have generated most of the Brazilian carbonatites [START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF][START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF]. Such hypothesis is based on either mass-balance calculations [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF] or geochemical constraints (e.g. [START_REF] Guarino | Magmatism and fenitization in the Cretaceous potassium-alkaline-carbonatitic complex of Ipanema São Paulo State, Brazil[END_REF][START_REF] Ruberti | The geochemistry of the Barra do Itapirapuã carbonatite (Ponta Grossa Arch, Brazil): a multiple stockwork[END_REF][START_REF] Brod | Decoupling of paired elements, crossover REE patterns, and mirrored spider diagrams: fingerprinting liquid immiscibility in the Tapira alkaline carbonatite complex, SE Brazil[END_REF].

For the Juquiá Complex, [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF] argue that the crystallization of mafic cumulates have led a basanitic parental magma to fractionate to a melt with nepheline syenite composition from which a carbonatite melt separated by immiscibility. The silicate counterpart would have been represented by rocks of the ijolite series. [START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF] suggest that the Juquiá model may represent a suitable picture for the other Mesozoic to Cenozoic Brazilian carbonatites. Therefore, alkaline and carbonatite associations would have been generated by a combination of fractional crystallization and immiscibility processes [START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF].

Indeed, liquid immiscibility is regarded by [START_REF] Germann | The alkaline complex of Jacupiranga, São Paulo, Brazil -petrology and genetic considerations[END_REF] and [START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF] as the mechanism generating the Jacupiranga carbonatites. The latter suggest that alkali gabbro melts evolved by fractionation of clinopyroxene and olivine (i.e. dunites and clinopyroxenites) to phonolite melts, from which the carbonatite liquid would have separated (the silicate conjugate would be represented by peralkaline phonolites).

Based on mineral compositions, Gaspar (1989) also invoked liquid immiscibility for the unit, although considering two different events: a first leading to the formation of C1 and ijolites, and a second event generating C2 to C5 and melilite ijolites. Later on, [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF] came to an opposite conclusion by comparing isotope and trace elements compositions and concluded that the Jacupiranga carbonatites and clinopyroxenites derived from different parental magmas. Moreover, calculations made by [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF] indicate that the trace-element patterns of the Jacupiranga carbonatite can be reproduced by small degrees of partial melting of phlogopite garnet peridotites.

Both silicate series defined for Jacupiranga may generate carbonatites by liquid immiscibility. Parental magmas with nephelinite composition, such as that suggested for the strongly silica-undersaturated series, have long been proposed to relate to carbonatite magmas generated by liquid immiscibility, (Le [START_REF] Le Bas | Nephelinites and carbonatites[END_REF][START_REF] Freestone | The role of liquid immiscibility in the genesis of carbonatites -an experimental study[END_REF][START_REF] Lee | Liquid immiscibility between nephelinite and carbonatite from 1.0 to 2.5 GPa compared with mantle melt compositions[END_REF][START_REF] Mitchell | Carbonatites and carbonatites and carbonatites[END_REF]. Similarly, basanite parental magmas, such as those of the mildly silica-undersaturated series, could originate carbonatite melts following the same evolution path proposed for Juquiá by [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF].

MELTS thermodynamic modeling [START_REF] Ghiorso | Chemical mass transfer in magmatic processes. IV. A revised and internally consistent thermodynamic model for the interpolation and extrapolation of liquid-solid equilibria in magmatic systems at elevated temperatures and pressures[END_REF][START_REF] Asimow | Algorithmic modifications extending MELTS to calculate subsolidus phase relations[END_REF] was carried out to further evaluate the possibility of a Jacupiranga lamprophyres (proposed as representatives of the parental magma of the mildly silica-undersaturated rocks) fractionate to phonolite compositions, as suggested by [START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF]. Fractional crystallization conditions (FC) were evaluated and the initial composition selected is that of the lamprophyre JAC46.1 (M1), the best representative of a basanite melt in the complex. The calculations have been carried out at low-pressure condition (P = 1 kbar, based on clinopyroxene geobarometer results), with ƒO 2 =QFM buffer and an initial temperature of ca. 1,200°C. Theoretical liquid line of descent indicates that a basanite melt may produce phonolites by fractional crystallization (Fig. 4). The models predict olivine as liquidus phase, followed by spinel and clinopyroxene, consistent with the main phases of the dunites and/or the magnetite clinopyroxenites.

Harmer and Gittins (1998) argue that although immiscibility that goes to completion destroys much of the petrographic evidence of it having ever occurred, isotopic and geochemical evidences should remain in the conjugate liquids and in the carbonatite and silicate rocks that crystallize from them. Those authors also point out that the two conjugate immiscible liquids must have the same isotopic compositions. However, this is not the case for the Jacupiranga Complex. Although most of silicate rocks and carbonatites span a similar range in initial 87 Sr/ 86 Sr ratios, carbonatites exhibit distinctly higher 143 Nd/ 144 Nd i ratios (Fig. 5), except for a clinopyroxenite from [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF]. As carbonatites generally contain Sr and Nd concentrations higher than those of common crustal rocks, it has been argued that this elevated contents would "buffer" the carbonatite isotopic compositions against crustal interaction, whereas the silicate conjugate would be more readily affect by such process.

Even if it were the case and assimilation processes did affect the silicate conjugate more strongly than the carbonatite liquid [START_REF] Ray | Trace element and isotope evolution during concurrent assimilation, fractional crystallization, and liquid immiscibility of a carbonated silicate magma[END_REF], the Jacupiranga rocks do not appear significantly contaminated by crustal materials [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF] as only some lithotypes (i.e. meladiorite and monzonite) show evidences of crustal contamination (Chmyz et al., submitted manuscript, 2016). Therefore, the differences of initial Nd ratios between carbonatites and silicate rocks are regarded as a primary feature. Similarly, the Jacupiranga carbonatites show lower Pb isotopic ratios than those of the silicate rocks, which Huang et al.

(1995) consider as reflecting differences in their mantle source regions. Sr isotopic ratios for the analyzed Jacupiranga rocks. Compiled Jacupiranga samples are from [START_REF] Roden | Sr and Nd Isotopic Composition of the Jacupiranga Carbonatite[END_REF], [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF]. Symbols and fields are as in Fig. 2.

To further constrain the petrological relationship, if any, between the carbonatites and silicate rocks, we consider the partition coefficients (D carbonate/silicate melts at ca. 1 kbar) obtained by [START_REF] Veksler | Trace element partitioning in immiscible silicate-carbonate liquid systems: an initial experimental study using a centrifuge autoclave[END_REF] to assess the eventual effects of liquid immiscibility in the Jacupiranga rocks. Those partition coefficients were obtained by experimental studies and reflect the trace elements partitioning between carbonate and silicate liquids generated by liquid immiscibility. Considering the proposition of [START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF], Jacupiranga phonolites (e.g. JAC26.1) may represent the parental melt from which carbonatites would have derived from liquid immiscibility, whereas peralkaline phonolites would represent their conjugate silicate liquid. As we did not sample the latter lithotype, a peralkaline phonolite compiled from [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF] was selected for this evaluation.

Considering the idea that Jacupiranga carbonatites emplaced from South to North [START_REF] Gaspar | Magnetite in the carbonatites from the Jacupiranga Complex, Brazil[END_REF], two carbonatites samples were selected: CCap JAC04, our southernmost analyzed sample, and the DC JAC09, representative of the youngest intrusive episode of carbonatite composition in the complex (i.e. C5 of [START_REF] Gaspar | Magnetite in the carbonatites from the Jacupiranga Complex, Brazil[END_REF].

According to several experimental studies [START_REF] Hamilton | The behaviour of trace elements in the evolution of carbonatites[END_REF][START_REF] Jones | Experimental investigations of the partitioning of Nb, Mo, Ba, Ce, Pb, Ra, Th, Pa, and U between immiscible carbonate and silicate liquids[END_REF][START_REF] Veksler | Trace element partitioning in immiscible silicate-carbonate liquid systems: an initial experimental study using a centrifuge autoclave[END_REF], Sr and Ba partition preferentially into the carbonate liquid. In Jacupiranga (Fig. 6), even though these elements decrease from phonolite to peralkaline phonolite, only Sr would have partitioned into the carbonatite, as Ba contents are higher in the phonolites (carbonate/silicate < 1).

According to [START_REF] Veksler | Trace element partitioning in immiscible silicate-carbonate liquid systems: an initial experimental study using a centrifuge autoclave[END_REF], although HFSE partition into the silicate liquid, Hf partition into the silicate compound more than Zr does, and Ta partitions into the silicate liquid more than Nb does. That decoupling is considered as a fingerprint for immiscibility process (e.g. [START_REF] Brod | Decoupling of paired elements, crossover REE patterns, and mirrored spider diagrams: fingerprinting liquid immiscibility in the Tapira alkaline carbonatite complex, SE Brazil[END_REF]. Jacupiranga phonolites indeed have higher Zr, Hf, Ti, Nb, and Ta than the carbonatites, as predicted by the experimental data. However, all the tested pairs of Jacupiranga rocks yield considerably higher ratios of Ta in comparison with Nb ratios and only the pair CCap/phonolite shows the Zr-Hf depletion. In the Nb vs. Ta diagram (Fig. 7) from [START_REF] Thompson | Ankerite carbonatite from Swartbooisdrif, Namibia: the first evidence for magmatic ferrocarbonatite[END_REF], the partitioning experiments from [START_REF] Veksler | Trace element partitioning in immiscible silicate-carbonate liquid systems: an initial experimental study using a centrifuge autoclave[END_REF] are also plotted. Both starting material and silicate conjugate have lower Nb/Ta ratios than that of the separated carbonatite melt. These experimental relationships are well constrained by the carbonatites, silicate rocks and parental magma from the Tapira alkaline-silicate carbonatite Complex (Late Cretaceous, Alto Paranaíba Igneous Province, Brazil -Brod et al., 2013) (Fig. 7). In this unit, carbonatites generated by liquid immiscibility show considerably higher Nb/Ta than those of the parental magma and silicate rocks, whereas carbonatites attributed to fractional crystallization yield lower ratios, sometimes similar to that of the parental magma. In comparison, Jacupiranga lamprophyres (representatives of the basanite parental magma of the mildly silica-undersaturated series) and phonolite yield Nb/Ta values (15.5-16.4 and 19.35, respectively) higher than most carbonatites (1.6-16.3), precluding the latter to be generated by immiscibility processes from any of those melts.

The studies of [START_REF] Veksler | Trace element partitioning in immiscible silicate-carbonate liquid systems: an initial experimental study using a centrifuge autoclave[END_REF] indicate that all REE but La partition into the silicate liquid. Only the pairs composed with the CCap present the behavior expected for La (Fig. 6). Conversely, all pairs show Nd, Sm, and Tb partitioning into the carbonate compound. Therefore, our tests indicate that carbonatite-silicate liquid immiscibility processes are unlikely to produce the Jacupiranga carbonatites with phonolites as conjugate silicate liquid. [START_REF] Thompson | Ankerite carbonatite from Swartbooisdrif, Namibia: the first evidence for magmatic ferrocarbonatite[END_REF] for the Jacupiranga carbonatites. Jacupiranga compiled data are from [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF]. Green and grey fields represent the silicate rocks from the highly and mildly silicaundersaturated series, respectively. Dashed fields: a, Tapira parental melt and b, Tapira bebedorites and syenite. Data for Tapira carbonatites and silicate rocks are from [START_REF] Brod | Decoupling of paired elements, crossover REE patterns, and mirrored spider diagrams: fingerprinting liquid immiscibility in the Tapira alkaline carbonatite complex, SE Brazil[END_REF], whereas those for Barra do Itapirapuã carbonatites are from [START_REF] Ruberti | The geochemistry of the Barra do Itapirapuã carbonatite (Ponta Grossa Arch, Brazil): a multiple stockwork[END_REF].

The results of partitioning experiments of [START_REF] Hamilton | The behaviour of trace elements in the evolution of carbonatites[END_REF] indicate that, during immiscibility processes, Ba/La ratios should be higher in the carbonatite melt relative to its silicate conjugate under almost all pressure and temperature conditions. Due to this behavior, those elements are used as evidence for the origin mechanisms of carbonatites (e.g. Harmer, 1999;[START_REF] Srivastava | Emplacement age and isotope geochemistry of Sung Valley alkalinecarbonatite complex, Shillong Plateau, northeastern India: implications for primary carbonate melt and genesis of the associated silicate rocks[END_REF]. The Jacupiranga carbonatites have lower Ba/La ratios than most silicate rocks (Fig. 8). Therefore, according to the constraints of [START_REF] Hamilton | The behaviour of trace elements in the evolution of carbonatites[END_REF], the higher Ba/La values showed by lamprophyres and phonolites would preclude an origin by liquid immiscibility from the mildly silica-undersaturated series. Nepheline syenites (data from [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF] and the rocks from the ijolite series show respectively, higher and similar ratios than those of carbonatites, and hence it is also unlikely that the latter were generated from immiscibility processes related to the strongly silicaundersaturated series (i.e. nephelinite parental magma).

Although our data on the Jacupiranga carbonatites appear not to support a link by liquid immiscibility with neither the highly nor the mildly silica-undersaturated series, we could nevertheless speculate an origin by immiscibility from a hypothetical silicate magma currently unknown in the complex. As mentioned before, Zr and Hf partition very strongly into the silicate melt during immiscibility processes, thus low ratios in carbonatites are coherent with a derivative origin by these mechanisms (Veskler et al., 1998). Subchondritic Zr/Hf ratios, such as those of JAC09 (Zr/Hf CN =0.9), are seen in rhyolites and granites which fractionated zircon and also in carbonate melt generated by silicate-carbonate immiscibility experiments [START_REF] Veksler | Trace element partitioning in immiscible silicate-carbonate liquid systems: an initial experimental study using a centrifuge autoclave[END_REF][START_REF] Thompson | Ankerite carbonatite from Swartbooisdrif, Namibia: the first evidence for magmatic ferrocarbonatite[END_REF]. As our previous considerations show that the dolomite carbonatite cannot be related to the Jacupiranga silicate parental magmas, that could hint an origin by liquid immiscibility from unknown silicate magma. However, further data are needed to better constrain this scenario. Additionally, most analyzed carbonatites show Nb/Ta ratios lower than 17.7 (Fig. 7), considered as enigmatic by [START_REF] Thompson | Ankerite carbonatite from Swartbooisdrif, Namibia: the first evidence for magmatic ferrocarbonatite[END_REF]. These authors suggest two hypothesis to explain such values: (1) Nb (but not Ta) becoming trivalent [START_REF] Thompson | An assessment of the relative roles of crust and mantle in magma genesis: an elemental approach[END_REF] and, as Nb 3+ shows ionic radius very close to that of Hf 4+ , Nb and Ta would substitute into different mineral phases during magma differentiation; or (2) Nd and Ta are lost differently during fenitization processes. Jacupiranga fenitization products are mainly composed of amphibole (Mg-arfvedsonite, pargasite, Mg-hastingsite and richterite), phlogopite and olivine. According to [START_REF] Salvioli-Mariani | Late veins of C3 carbonatite intrusion from Jacupiranga complex (Southern Brazil): fluid and melt inclusions and mineralogy[END_REF], one effect of the metasomatic fluids/liquids in Jacupiranga is a progressive Nb-depletion and a Ta-enrichment, coherent with the second proposition of [START_REF] Thompson | Ankerite carbonatite from Swartbooisdrif, Namibia: the first evidence for magmatic ferrocarbonatite[END_REF]. Barra do Itapirapuã carbonatites (Early Cretaceous, Ponta Grossa Arch Province, Brazil), to which an origin by liquid immiscibility is proposed by [START_REF] Ruberti | The geochemistry of the Barra do Itapirapuã carbonatite (Ponta Grossa Arch, Brazil): a multiple stockwork[END_REF], also show Nb/Ta ratios> 17.7, similar to those of Jacupiranga.

If the Jacupiranga carbonatites were not derived from liquid immiscibility from any of the two silicate parental magmas considered for this unit, a primary origin by direct partial melting of a metasomatized mantle source should be accepted as a more probable origin. Such model is supported by both experimental [START_REF] Wallace | An experimental determination of primary carbonatite magma composition[END_REF][START_REF] Thibault | Experimental investigation of melts from a carbonated phlogopite lherzolite: implications for metasomatism in the continental lithospheric mantle[END_REF][START_REF] Dalton | The compositions of primary carbonate melts and their evolution through wallrock reaction in the mantle[END_REF][START_REF] Lee | Processes of crustal carbonatite formation by liquid immiscibility and differentiation, elucidated by model systems[END_REF] and natural systems (e.g. Harmer, 1999;[START_REF] Srivastava | Early Cretaceous Sung Valley ultramafic-alkalinecarbonatite complex, Shillong Plateau, Northeastern India: petrological and genetic significance[END_REF][START_REF] Srivastava | Emplacement age and isotope geochemistry of Sung Valley alkalinecarbonatite complex, Shillong Plateau, northeastern India: implications for primary carbonate melt and genesis of the associated silicate rocks[END_REF]. Primary carbonatite melts may be generated at depths greater than 70 km (ca. 25 kbar), according to the experimental data of [START_REF] Lee | Processes of crustal carbonatite formation by liquid immiscibility and differentiation, elucidated by model systems[END_REF]. Those liquids show a magnesian composition (Ca/Mg<1), high mg# and between 5 and 7 wt.% of total alkalis. During their ascent, those melts will react with mantle lherzolite, crystallize and release CO 2 vapor at depths of ca. 70 km and increase the mantle clinopyroxene amounts at expense of orthopyroxene, changing lherzolite to wehrlite in a metosomatic process [START_REF] Dalton | The compositions of primary carbonate melts and their evolution through wallrock reaction in the mantle[END_REF]. The reaction between the magnesian carbonate melts with wehrlite shifts the composition of the liquid to calcic-carbonatite melts [START_REF] Dalton | The compositions of primary carbonate melts and their evolution through wallrock reaction in the mantle[END_REF][START_REF] Sweeney | Carbonatite Melt Compositions in the Earth's Mantle[END_REF]. [START_REF] Harmer | The origin of dolomitic carbonatites: field and experimental constraints[END_REF] argue that such liquids are able to produce the complete range of carbonatite compositions recognized at the surface.

THE MANTLE SOURCE OF THE JACUPIRANGA ROCKS

Although some samples (i.e. meladiorite and monzonite) show evidences of crustal contamination, overall, the Jacupiranga rocks do not appear significantly contaminated by crustal materials. Therefore, their isotopic and trace elements compositions should reflect their mantle sources. Sr, Nd, and Pb isotopic ratios (Fig. 9) define a domain largely overlapping the field of the Early Cretaceous alkaline-carbonatite magmatism of the southeastern part of the South American Platform [START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF], except for a lamprophyre and the two contaminated samples. Jacupiranga carbonatites (Fig. 5) and some silicate rocks (Fig. 9) also present a good correspondence with the high-Ti basalts of the Paraná Magmatic Province. Overall, the Jacupiranga rocks plot close to the composition of the EM1 (enriched mantle type 1) reservoir with some contribution of HIMU. These components are in agreement with the well-defined array involving depleted and enriched mantle components proposed by [START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF] for the alkaline-carbonatite complexes from the Paraná-Angola-Namíbia System. That signature is largely interpreted as indicative of a heterogeneously enriched subcontinental lithospheric mantle (SCLM) related to variable degrees of metasomatism (e.g. [START_REF] Gibson | The Late Cretaceus impact of the Trindade Mantle Plume: Evidence from largevolume mafic, potassic magmatism in SE, Brazil[END_REF][START_REF] Gibson | The limited extent of plume-lithosphere interactions during continental flood-basalt genesis: Geochemical evidence from Cretaceous magmatism in southern Brazil[END_REF][START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF]. Parental magmas of alkaline occurrences related to the Ponta Grossa Arch (e.g. Juquiá, Jacupiranga, and Pariquera-Açu complexes) are inferred to derive from a lithospheric garnet peridotite mantle source metasomatized by carbonated fluids [START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF][START_REF] Gibson | The limited extent of plume-lithosphere interactions during continental flood-basalt genesis: Geochemical evidence from Cretaceous magmatism in southern Brazil[END_REF][START_REF] Morbidelli | The Pariquera Açu K-alkaline complex and southern Brazil lithospheric mantle source characteristics[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF][START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF]Azzone Overall, Jacupiranga Hf-Nd range (Fig. 3) is comparable with the Canadian carbonatite-lamprophyre and Group II kimberlites fields to more unradiogenic values. The isotopic signature of the Group II kimberlites is believed to represent extensive contribution of the lithospheric mantle [START_REF] Nowell | High precision Hf isotope measurements of MORB and OIB by thermal ionization mass spectrometry: insights into the depleted mantle[END_REF], whereas the Canadian lamprophyres are mainly related to CO 2 -rich fluids interacting with a veined lithospheric mantle [START_REF] Tappe | Between carbonatite and lamproite -Diamondiferous Torngat ultramafic lamprophyres formed by carbonate-fluxed melting of cratonic MARID-type metasomes[END_REF].

Jacupiranga parental melts and mantle sources

The lamprophyres, proposed to be representative of the parental magmas of the mildly silica-rocks, show low ε Nd values (from -10.4 to -7.5) and high Ba (from 1478 to 2573 ppm), Rb (from 70.8 to 144.2 ppm), and K contents (3.71-3.95 %). Similar compositions are found in the nephelinites of Anitápolis Complex, to which [START_REF] Gibson | The limited extent of plume-lithosphere interactions during continental flood-basalt genesis: Geochemical evidence from Cretaceous magmatism in southern Brazil[END_REF] propose subcontinental lithospheric mantle (SCLM) as the predominant melt source region. According to these authors, although the local Brazilian granitic crust shows similar εNd (ca. -7), a lower La/Nb ratios in the Anitápolis nephelinites (0.72-0.98, whereas the granitic crust is > 2.5) rule out the continental crust as a source region. Similarly, the Jacupiranga lamprophyres show La/Nb ratios between 1.2 and 1.6.

The origin of parental magma of the strongly silica-undersaturated series is harder to constrain, as no direct representative is found within the complex, although a nephelinitic composition is suggested (Chmyz et al., 2016, submitted paper). As ijolite and nephelinebearing clinopyroxenites show isotopic compositions close to those of the rocks from the mildly silica-undersaturated rocks, both series may have originated from similar mantle sources. Nephelinites related to the Asunción-Sapucai graben (Eartern Paraguay) are proposed to be generated by 4 to 6% degrees of partial melting from garnet peridotite sources [START_REF] Comin-Chiaramonti | Tertiary nephelinitic magmatism in Eastern Paraguay: Petrology, Sr-Nd isotopes and genetic relationships with associated spinel-peridotite xenoliths[END_REF][START_REF] Comin-Chiaramonti | Potassic and sodic igneous rocks from Eastern Paraguay: their origin from the lithospheric mantle and genetic relationships with the associated Paraná flood tholeiites[END_REF]. Two magmatic series are also attributed by [START_REF] Ruberti | The Banhadão alkaline complex, southeastern Brazil: source and evolution of potassic SiO 2 -undersaturated high-Ca and low-Ca magmatic series[END_REF] to the Banhadão alkaline Complex (Ponta Grossa Arch Province): one generated from a kamafugite-like parental magma and another from a nephelinitic melt. Those authors proposed that both parental melts of Banhadão Complex were generated from a CO 2 -rich metasomatized lithosphere mantle, but while the kamafugite-like melt has a major contributions coming from the melting of the veins (enriched component), the nephelinitic liquid have a major component from the wall-rocks (depleted component). Therefore, a similar situation can be expected for the Jacupiranga basanite and nephelinitic parental magmas. The ΔεHf positive values yielded by the analyzed clinopyroxenites and ijolite can be a hint for a slightly higher contribution of the peridodite matrix. However, as all Jacupiranga lithotypes show low Sm/Nd and Lu/Hf ratios, the source for all those rocks is still LREE and HFSE enriched.

Causes of the mantle metasomatism

Mantle metasomatism may be caused by (1) slab-derived fluids (e.g. [START_REF] Maury | Metasomatism of the sub-arc mantle inferred from trace elements in Philippine xenoliths[END_REF] or (2) by the migration of low-density, small melt fractions from the asthenosphere [START_REF] Mckenzie | Some remarks on the movement of small melt fractions in the mantle[END_REF]. The Jacupiranga lamprophyres have La/Th (9.46 to 11.71) and Nb/La (0.61 to 0.81) ratios similar to those reported by [START_REF] Marques | Petrology, geochemistry and Sr-Nd isotopes of the Trindade and Martin Vaz volcanic rocks (Southern Atlantic Ocean)[END_REF] for the high-Ti basalts of the PMP (9-12 and 0.51 to 0.72). Additionally, in the primitive mantle-normalized trace element diagram, the lamprophyres show a slight depletion of Nb and Ta relative to La (Fig. 10). Although with different magnitudes, these signatures were described in the High-Ti tholeiites from Northern PMP by [START_REF] Rocha-Júnior E | Sr-Nd-Pb isotopic constraints on the nature of the mantle sources involved in the genesis of the high-Ti tholeiites from Northern Paraná Continental Flood Basalts (Brazil)[END_REF]. These authors favored the influence of subduction-related fluids in the origin of the metasomatic processes to affect those basalts mantle sources, based on their (1) enrichment of LREE relative to HREE, (2) enrichment in mobile LILE (e.g. Cs, Rb, U, Sr) and (3) strong negative anomalies of Nb-Ta.

All these features are also seen in the lamprophyres (Fig. 10), and, therefore, we favor slabderived fluids as the cause of enrichment of the Jacupiranga mantle sources. On the other hand, the absence of depletion in high-field-strength elements (e.g. Nb, Ta) has led [START_REF] Gibson | The Late Cretaceus impact of the Trindade Mantle Plume: Evidence from largevolume mafic, potassic magmatism in SE, Brazil[END_REF] to propose that the metasomatic enrichment of the mantle source of the Alto Parnaíba Igneous Province (also located around the margin of the Paraná Basin) was caused by migration of melts from the asthenosphere. 

Mantle heterogeneities and other Brazilian alkaline occurrences

The heterogeneous nature of the mantle source of the carbonatite-alkaline occurrences in the southeastern part of the Brazillian Platform are stressed by their large range of T DM model ages, varying from 0.6 to 1.5 Ga [START_REF] Gibson | The Late Cretaceus impact of the Trindade Mantle Plume: Evidence from largevolume mafic, potassic magmatism in SE, Brazil[END_REF][START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF]Comin-Chiaramonti and Gomes, 2005;[START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF][START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF]. Although these values should only be taken as reference values, [START_REF] Comin-Chiaramonti | Potassic and sodic igneous rocks from Eastern Paraguay: their origin from the lithospheric mantle and genetic relationships with the associated Paraná flood tholeiites[END_REF], 1999) interpreted those ages as implying that the parental magmas of those unites were derived from a SCLM modified by metasomatic processes since Middle to Late Proterozoic times. Our 143 Nd/ 144 Nd ratios give T DM model ages of 681-1402 Ma (Supplementary materialtable A1) with a mean value of 971 Ma (±198), coherent with the mean T DM model age of 0.9 Ga obtained by [START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF] for the alkaline occurrences related to the Guapiara lineament. Analyzed carbonatites systematically yield lower T DM model ages (681-858 Ma), whereas the silicate rocks show a more dispersive range (777 to 1402 Ma). Both lithotypes with evidences of crustal contamination processes (i.e. meladiorite JAC22 and monzonite JAC25) yield the highest model ages (1.4 and 1.2 Ga, respectively), which may suggest a contaminant source older than the Jacupiranga host rocks (Turvo-Cajati Formation and the Itapeúna Granodiorite, both with Neoproterozoic ages). Therefore, a contamination at depth, during the magma ascent, may also be a possibility. Overall, the large range of the fractionation factor (ƒ Sm/Nd from -0.33 to -0.61) is consistent with a heterogeneous source. The hafnium model ages (Table 2) range from 0.7 to 2.0 Ga. If we exclude the two samples with crustal contamination evidences, the T DM Hf interval will be reduced to 0.7 to 1.6 Ga, with a mean value of 1.1 Ga ± 0.3, still coherent with the Guapiara lineament model ages. Considering the assumptions of [START_REF] Comin-Chiaramonti | Potassic and sodic igneous rocks from Eastern Paraguay: their origin from the lithospheric mantle and genetic relationships with the associated Paraná flood tholeiites[END_REF], 1999), the average model ages (both T DM Hf and T DM Nd) together with the trace element distribution suggest that the Jacupiranga mantle source was metasomatized by fluids probably related to Neoproterozoic subduction processes (e.g. Brasiliano/Pan-African orogenic cycle), the same scenario proposed by Rocha-Júnior for the high-Ti tholeiites.

Hf isotope data on Brazilian alkaline occurrences remain limited; however, the available data [START_REF] Carlson | Chemical and isotopic relationships between peridotite xenoliths and mafic-ultrapotassic rocks from Southern Brazil[END_REF][START_REF] Guarino | U-Pb ages, geochemistry, C-O-Nd-Sr-Hf isotopes and petrogenesis of the Catalão II carbonatitic complex (Alto Paranaíba Igneous Province, Brazil): implications for regional-scale heterogeneities in the Brazilian carbonatite associations[END_REF]and this work) consistently reveal markedly mantle source heterogeneities: Jacupiranga Hf-Nd range (Fig. 3) is comparable with the Catalão I magnetite and apatitite to more unradiogenic values, whereas Goiás peridodites show a more radiogenic composition.

Insights on the geodynamic context

Several competing models have been put forward concerning the geodynamic context in which the Meso-Cenozoic alkaline magmatism in the Brazilian Platform was originated. [START_REF] Thompson | Migrating Cretaceous-Eocene magmatism in the Serra do Mar Alkaline Province, SE Brazil: melts from the deflected Trindade mantle plume[END_REF] and [START_REF] Gibson | The Late Cretaceus impact of the Trindade Mantle Plume: Evidence from largevolume mafic, potassic magmatism in SE, Brazil[END_REF][START_REF] Gibson | The limited extent of plume-lithosphere interactions during continental flood-basalt genesis: Geochemical evidence from Cretaceous magmatism in southern Brazil[END_REF][START_REF] Gibson | Meltgeneration processes associated with the Tristan mantle plume: Constraints on the origin of EM-1[END_REF] suggested that the origin of the alkaline and tholeiitic magmatism was related to assimilation of melts derived from SCLM by plume-related melts (i.e. Tristan da Cunha and Trindade). On the other hand, [START_REF] Comin-Chiaramonti | Potassic and sodic igneous rocks from Eastern Paraguay: their origin from the lithospheric mantle and genetic relationships with the associated Paraná flood tholeiites[END_REF], 1999, 2004, 2005, 2007), [START_REF] Castorina | Carbonatites from Eastern Paraguay and genetic relationships with potassic magmatism: C, O, Sr and Nd isotopes[END_REF] and [START_REF] Alberti | Geochemical characteristics of Cretaceous carbonatites from Angola[END_REF] proposed that the alkaline-carbonatite events in the Paraná-Angola-Namibia system originated from lithospheric mantle sources without appreciable participation of plume-derived materials. Based on petrological and geophysical evidences, Ernesto et al. (2002) proposed an alternate non-plume related heat source in which the magmatism was triggered by a regional thermal anomaly. According to those authors, the similarity among Rio Grande Rise basalts, Walvis Ridge and the Paraná analogues is suggestive of a delaminated lithospheric mantle.

Overall, the Jacupiranga trace and isotope compositions suggest that an asthenospheric or a mantle plume component is not required for the genesis of the complex.

It should be noted that the εHf-εNd isotopic array of the Jacupiranga rocks is displaced from the fields of global OIB and Hawaii islands, indicating the absence of an asthenospheric contribution. The trace-elements distribution patterns in the lamprophyres (Fig. 10), the sole representative of parental magma found within Jacupiranga, are not similar to that found in Tristan da Cunha least evolved alkaline volcanic. Moreover, according to [START_REF] Gibson | The limited extent of plume-lithosphere interactions during continental flood-basalt genesis: Geochemical evidence from Cretaceous magmatism in southern Brazil[END_REF], it is not possible to establish whether or not melts derived from the Tristan da Cunha plume contributed to the Anitápolis nephelinites, which yield isotope and trace element compositions similar to those of the Jacupiranga lamprophyres. Additionally, Pb and Hf isotope compositions on the present day products of the Tristan da Cunha plume are different from those of the Jacupiranga rocks (Fig. 2, 3), even though some carbonatite samples yield Sr-Nd isotope ratios that partly overlap the Tristan da Cunha field (Fig. 5).

CONCLUSIONS

Several lines of evidence indicate that Jacupiranga carbonatites are not directly related to neither highly nor mildly silica-undersaturated series. We favor an origin by direct partial melting of a mantle source, although a derivation by liquid immiscibility from an unknown magmatic precursor is also a possibility. In any case, whatever model is proposed to explain the origin of carbonatites, it has to account not only for their association with ultramafic and alkaline silicate rocks, but also their trace element and isotopic signatures.

Overall, the Nd-Sr-Pb-Hf isotope systematic of the Jacupiranga Complex implies an important contribution of the metasomatized subcontinental lithospheric mantle (SCLM) for the genesis of these rocks. Our data overlap those on the alkaline-carbonatite occurrences in Southern Brazil and imply an important contribution of the EM1 component with some HIMU input. The enhanced resolution provided by the Hf isotope data helps to assess the important contribution of metasomatic pyroxenitic clinopyroxene on the Jacupiranga source. Besides, the ΔεHf signatures are suggestive of a slightly higher role of the wall-rock peridotite as a source component for the strongly silica-undersaturated series, whereas the mildly silicaundersaturated parental magma is mainly related to the pyroxenitic veins. Lamprophyres, the sole parental magma representative found within the complex, yield trace element compositions coherent with slab-related fluids as the main agent of metasomatism to affect the SCLM. Finally, considering the long-standing debate about the geodynamic context of the alkaline and tholiitic magmatism in Southeastern/Southern Brazil, the Jacupiranga traceelement and isotopic data suggest that an asthenospheric or a mantle plume component is not required for the genesis of the complex.

CONSIDERAÇÕES FINAIS

Dentre as várias ocorrências alcalinas localizadas no centro-sudeste da Plataforma Sul-Americana, o Complexo de Jacupiranga se destaca tanto por se tratar de um exemplo clássico de unidade ultramáfica alcalina com carbonatitos quanto por sua grande importância econômica. Apesar da extensa bibliografia disponível sobre a unidade, com trabalhos pioneiros que remontam ao final do século XIX, somente alguns estudos incluem as rochas silicáticas (mais de 90% da área aflorante da unidade). Este panorama faz com que as tentativas de desenvolvimento de modelos petrológicos ou de definição da origem das rochas carbonatíticas (se gerada por magmas carbonatíticos primários, por imiscibilidade de líquidos ou cristalização fracionada) esbarrem justamente no conhecimento ainda compartimentado acerca do complexo. Além disso, a ausência de dados geocronológicos robustos impede a determinação da duração do magmatismo Jacupiranga.

A seguir, é apresentada uma síntese dos principais resultados atingidos durante o desenvolvimento desta tese e que permitem o melhor entendimento da origem e evolução do Complexo de Jacupiranga.

GEOCRONOLOGIA

Os dados 40 Ar/ 39 Ar e U-Pb, obtidos, respectivamente, em cristais de mica e zircão de diferentes litotipos (Capítulo 5), permitem refinar o intervalo de tempo de colocação do Complexo de Jacupiranga. As idades 40 Ar/ 39 Ar variam entre 133,7 ± 0,5 Ma e 131,9 ± 0,5 Ma, enquanto que a idade concórdia calculada para o monzonito é de 134,9 ± 1,3 Ma. Em linhas gerais, estes dados indicam que toda a evolução da unidade ocorreu dentro de um intervalo de tempo relativamente curto (cerca de 4 Ma, ao se considerar os erros). Apesar de não ser possível definir uma sequência de colocação entre clinopiroxenito, diorito e lamprófiro, dada a ausência de contrastes entre suas idades 40 Ar/ 39 Ar, o monzonito apresenta tanto idades 40 Ar/ 39 Ar quanto U-Pb mais antigas que as demais rochas analisadas. Além disso, a similaridade entre os valores obtidos pelos diferentes métodos (U-Pb: 134,9 ± 1,3 Ma e 40 Ar/ 39 Ar: 133,7 ± 0,5 Ma) indica que a colocação do monzonito ocorreu em profundidades rasas e que o seu resfriamento foi razoavelmente rápido. No contexto regional, a colocação do Complexo de Jacupiranga foi contemporânea à extrusão dos basaltos toleíticos da Província Magmática do Paraná (Ar/Ar: 134,7± 1 Ma, Thiede e Vasconcelos, 2010).

SÉRIES MAGMÁTICAS

A evolução magmática das rochas silicáticas de Jacupiranga é discutida no Capítulo 5. Tendo em vista a composição destes litotipos, duas séries magmáticas são propostas: (1) uma série fortemente insaturada em sílica, possivelmente relacionada a um magma de composição nefelinítica e (2) uma segunda série, moderadamente insaturada em sílica, relacionada a magmas parentais basaníticos. À série fortemente insaturada em sílica se relacionam as rochas da série ijolítica e alguns clinopiroxenitos (em particular aqueles com nefelina modal), enquanto que a série moderadamente insaturada é representada pelas rochas com feldspato, lamprófiros e parte dos clinopiroxenitos. A cristalização de clinopiroxênio cumulus, olivina e Ti-magnetita desempenharam um importante papel no início da evolução de ambas as séries (gerando os clinopiroxenitos). Na série fortemente insaturada em sílica, este fracionamento desencadeou no aparecimento de nefelina no sistema, gerando melteigitos e, conforme o aumento da proporção nefelina/clinopiroxênio, ijolitos e urtitos. No caso da série moderadamente insaturada, ocorreu a cristalização de plagioclásio cumulus.

O elevado grau de alteração das rochas duníticas dificulta a identificação de suas texturas primárias. No entanto, a composição dos cristais de olivina (Fo 83-84 , CaO 0.13-0.31 wt.%, e NiO entre 0.19-0.33 wt.%) indica que esta fase foi gerada por processos de cristalização fracionada. Esta interpretação difere da proposta de Germann et al. (1987), com base em dados de rocha total, de uma origem mantélica para os dunitos. Modelos termodinâmicos indicam que cristais de olivina com Fo 83-84 podem ser fracionados tanto a partir de magmas de composição basanítica quanto nefelinítica, de modo às rochas duníticas poderem estar relacionadas a qualquer uma das duas séries silicáticas propostas para o complexo.

MAGMAS PARENTAIS DAS ROCHAS SILICÁTICAS

A composição dos magmas parentais das rochas silicáticas é discutida no Capítulo 5. Os lamprófiros, quimicamente classificados como tefritos e basanitos, são considerados representativos da composição do magma parental da série moderadamente insaturada em sílica. Padrões de elementos terras raras (ETR) dos lamprófiros são similares aos das rochas com feldspato e fonolito, sendo que as rochas mais evoluídas são mais empobrecidas nesses elementos, o que indica processos de cristalização fracionada e acumulação a partir de um magma basanítico para a gênese das rochas da Zona Heterogênea. Para os clinopiroxenitos, valores de mg# do líquido em equilíbrio com os núcleos de clinopiroxênio são idênticos ao Mg# dos lamprófiros. Além disso, os padrões de ETR dos líquidos calculados são igualmente similares aos padrões das amostras de lamprófiro. Deste modo, o modelo petrológico proposto para as rochas com feldspato e parte dos clinopiroxenitos envolve repetidos pulsos de magma basanítico, sendo que as fases deles fracionadas se depositaram em câmaras magmáticas rasas. A ocorrência de diques basaníticos cortando álcali-feldspato sienitos é indicativa da recorrência destes pulsos. Esta hipótese é também favorecida pelas variações composicionais observadas nos líquidos em equilíbrio com os núcleos de clinopiroxênio dos clinopiroxenitos.

Enquanto evidências da composição do magma basanítico são obtidas a partir análise dos lamprófiros, as características do magma parental nefelinítico são de difícil definição. No entanto, líquidos de composição nefelinítica são atribuídos como magmas parentais de diversas unidades ultrabásicas alcalinas em diferentes províncias ao redor do mundo. Rochas desta composição são encontradas no Complexo de Anitápolis, que compartilha várias similaridades com Jacupiranga (e.g. idades do Cretáceo Inferior, associação de litotipos, contexto tectônico), e são consideradas como representativas do magma parental de Anitápolis.

EVIDÊNCIAS DE ASSIMILAÇÃO CRUSTAL

Uma discussão acerca da contribuição de processos de contaminação crustal na gênese das rochas de Jacupiranga é realizada no Capítulo 5. Amostras de monzonito e meladiorito apresentam características petrográficas, composicionais e isotópicas (razões 87 Sr/ 86 Sr i de 0,706086 para o monzonito e 143 Nd/ 144 Nd i de 0,511867 para o meladiorito) que sugerem que processos de assimilação crustal exerceram papel ativo na gênese destas rochas. No entanto, esses processos têm um caráter local, restritos a alguns pulsos de magma basanítico a partir dos quais as rochas da Zona Heterogênea se formaram. As razões isotópicas de Nd e Sr do monzonito e do meladiorito são compatíveis com a curva de mistura calculada a partir da composição de um lamprófiro e das rochas metassedimentares da região. Apesar de não ser possível descartar totalmente a possibilidade de contaminação para as rochas sieníticas, ela é considerada pouco provável uma vez que feições petrográficas indicativas desses processos não são observadas, além de estes litotipos apresentarem razões isotópicas similares aos clinopiroxenitos e carbonatitos (os quais não sustentam indícios de processos de contaminação, conforme [START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF].

ORIGEM DOS CARBONATITOS

Considerações quanto à origem dos carbonatitos são desenvolvidas no Capítulo 6. O estudo da origem destas rochas considera, classicamente, três diferentes modelos: (1) origem direta por fusão parcial de uma fonte mantélica metassomatizada e derivação por (2) cristalização fracionada ou (3) imiscibilidade de líquidos a partir de um magma parental silicático carbonatado.

Os magmas parentais de ambas as séries silicáticas propostas para o Complexo de Jacupiranga podem gerar carbonatitos por imiscibilidade de líquidos. Apesar das similaridades entre as razões iniciais de 87 Sr/ 86 Sr, os carbonatitos apresentam composições isotópicas de Nd e Pb diferentes daquelas das rochas silicáticas. Estas variações são interpretadas como características primárias, refletindo, portanto, diferenças nas fontes mantélicas dos magmas que geraram estes litotipos. Razões dos teores de elementos traço apresentados por rochas carbonatíticas e seus eventuais pares conjugados silicáticos (i.e. carbonatito/fonolitos peralcalinos) foram utilizados para avaliar processos de imiscibilidade de líquidos. Enquanto que os teores de Zr, Hf, Ti e Nb são de fato superiores nos fonolitos, como previsto em processos de imiscibilidade, os pares conjugados testados apresentam razões de Ta maiores que os de Nb e somente o par CCap/fonolito é depletado em Zr-Hf.

Lamprófiros, fonolitos e nefelina sienitos apresentam razões Ba/La superiores às dos carbonatitos, o que, seguindo os critérios experimentais de Hamilton et al. (1989) e petrológicos de Harmer (1999) e [START_REF] Srivastava | Emplacement age and isotope geochemistry of Sung Valley alkalinecarbonatite complex, Shillong Plateau, northeastern India: implications for primary carbonate melt and genesis of the associated silicate rocks[END_REF], impediria uma origem por imiscibilidade de líquidos a partir dos magmas parentais das séries silicáticas descritas.

Aventa-se ainda a possibilidade de um magma silicático não reconhecido atualmente na unidade ter gerado os carbonatitos, uma vez que o dolomita carbonatito apresenta razões Zr/Hf subcondríticas, relacionadas a carbonatitos gerados por processos de imiscibilidade (e.g. [START_REF] Thompson | Ankerite carbonatite from Swartbooisdrif, Namibia: the first evidence for magmatic ferrocarbonatite[END_REF]. No entanto, esta hipótese carece de maiores evidências.

Como os carbonatitos de Jacupiranga não derivam por processos de imiscibilidade a partir de nenhum dos magmas parentais silicáticos previamente definidos, uma origem primária deve ser considerada. Conforme este modelo, magmas carbonatíticos com Ca/Mg<1 e gerados a profundidades superiores a 70 km interagiriam, durante a sua ascensão, com o manto lherzolítico, tornando a composição desses líquidos mais cálcica.

FONTE MANTÉLICA

As características das fontes mantélicas às quais os magmas parentais de Jacupiranga se associam são discutidas nos capítulos 5 e 6. Apesar de algumas amostras (monzonito e meladiorito) apresentarem evidências de interação crustal, em geral as rochas de Jacupiranga não apresentam indícios significativos de contaminação.

Consequentemente, as composições isotópicas e de elementos traço devem refletir características das fontes mantélicas.

Mecanismos de fusão de veios-mais-encaixantes (vein-plus-wall-rock, Foley, 1992) são et al., 1995;[START_REF] Gibson | The limited extent of plume-lithosphere interactions during continental flood-basalt genesis: Geochemical evidence from Cretaceous magmatism in southern Brazil[END_REF][START_REF] Comin-Chiaramonti | A review of carbonatitic magmatism in the Paraná-Angola-Namibia (PAN) system[END_REF].

As rochas da Zona Heterogênea são caracterizadas por valores negativos de ΔεHf, similares, os peridotitos de Goiás são mais radiogênicos [START_REF] Carlson | Chemical and isotopic relationships between peridotite xenoliths and mafic-ultrapotassic rocks from Southern Brazil[END_REF].

No que se refere ao contexto geodinâmico, as composições traço e isotópica das rochas do Complexo de Jacupiranga sugerem que uma componente astenosférica ou relacionada a uma pluma não são necessárias para a geração da unidade.

Tabela A1 -Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: WEHwehrlitos; Nnúcleo do cristal. Amostra JAC220 JAC220 JAC243 JAC220 JAC220 JAC220 JAC220 JAC220 JAC243 JAC220 JAC220 JAC220 JAC220 JAC220 JAC220 JAC243 JAC220 0,001 0,000 0,000 0,008 0,005 0,013 0,007 0,001 0,000 0,003 Fe 3+ M1 0,043 0,057 0,068 0,030 0,037 0,048 0,056 0,022 0,045 0,027 0,046 0,053 0,045 0,050 0,043 0,071 0,040 Ti M1 0,020 0,018 0,018 0,021 0,020 0,034 0,020 0,019 0,020 0,020 0,022 0,019 0,019 0,019 0,020 0,022 0,017 Cr M1 0,020 0,020 0,021 0,020 0,021 0,017 0,020 0,020 0,021 0,022 0,020 0,022 0,021 0,021 0,021 0,021 0,018 Mg M1 0,852 0,858 0,855 0,844 0,842 0,830 0,856 0,848 0,866 0,850 0,848 0,852 0,850 0,862 0,857 0,842 0,848 Fe 2+ M1 0,054 0,035 0,021 0,068 0,065 0,064 0,041 0,077 0,048 0,073 0,046 0,035 0,048 0,044 0,060 0,031 0,061 Mn M1 0,001 0,001 0,002 0,002 0,002 0,002 0,002 0,002 0,002 0,001 0,002 0,001 0,002 0,002 0,002 M1 subtotal 0,991 0,990 0,985 0,993 0,994 0,994 0,996 1,000 0,021 0,000 0,001 0,000 0,001 0,000 0,001 0,000 0,000 0,001 0,000 0,001 0,000 0,000 0,000 0,000 0,000 Mg M1 0,858 0,715 0,755 0,724 0,758 0,739 0,721 0,772 0,725 0,742 0,717 0,757 0,764 0,751 0,729 0,735 0,739 Fe 2+ M1 0,058 0,037 0,050 0,038 0,039 0,039 0,044 0,020 0,038 0,048 0,046 0,028 0,037 0,031 0,048 0,032 0,046 Mn M1 0,002 0,003 0,002 0,002 0,002 0,002 0,003 0,002 0,002 0,002 0,003 0,002 0,002 0,002 0,002 0,002 0,002 M1 subtotal 1,000 0,068 0,083 0,070 0,084 0,074 0,078 0,077 0,080 0,080 0,080 0,081 0,081 0,079 0,078 0,072 0,076 0,067 Cr M1 0,000 0,000 0,001 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,001 0,001 0,001 0,002 Mg M1 0,749 0,713 0,746 0,710 0,741 0,727 0,734 0,714 0,715 0,722 0,715 0,737 0,730 0,741 0,753 0,749 0,754 Fe 2+ M1 0,034 0,039 0,051 0,052 0,046 0,056 0,039 0,057 0,059 0,043 0,075 0,036 0,043 0,026 0,024 0,028 0,052 Mn M1 0,002 0,003 0,002 0,002 0,002 0,002 0,003 0,002 0,003 0,003 0,002 0,002 0,002 0,002 0,002 0,002 0,001 0,001 0,001 0,000 0,000 0,001 0,000 0,000 0,001 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Mg M1 0,756 0,720 0,754 0,733 0,738 0,723 0,738 0,722 0,717 0,733 0,718 0,732 0,721 0,717 0,717 0,736 0,727 Fe 0,000 0,000 0,016 0,006 0,007 0,000 0,011 0,015 0,018 0,016 0,000 0,011 0,011 0,009 0,009 0,000 0,022 Fe 3+ M1 0,095 0,091 0,086 0,081 0,082 0,087 0,058 0,060 0,084 0,154 0,110 0,131 0,128 0,147 0,142 0,174 0,105 Ti M1 0,016 0,018 0,020 0,022 0,019 0,017 0,018 0,018 0,020 0,022 0,050 0,032 0,031 0,029 0,024 0,033 0,029 Cr M1 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,001 0,000 M2 subtotal 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 0,030 0,018 0,017 0,032 0,015 0,021 0,009 0,016 0,027 0,020 0,020 0,014 0,029 0,031 0,030 0,017 0,042 Cr M1 0,001 0,001 0,004 0,001 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,001 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 M2 subtotal 1,000 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 3,4 CaTs 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 2,2 0,5 0,4 0,4 5,1 CaTs 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,1 0,0 0,0 4,4 0,0 0,0 0,0 0,0 0,052 0,024 0,025 0,052 0,021 0,002 0,019 0,011 0,006 0,023 0,020 0,022 0,022 0,030 0,024 Fe 3+ M1 0,073 0,093 0,137 0,133 0,175 0,085 0,101 0,107 0,092 0,148 0,061 0,148 0,140 0,105 0,126 Ti M1 0,061 0,053 0,075 0,052 0,080 0,049 0,087 0,061 0,063 0,097 0,044 0,053 0,076 0,046 0,046 Cr M1 0,014 0,016 0,000 0,011 0,013 0,001 0,004 0,009 0,000 0,005 0,001 0,000 0,003 0,001 0,001 Mg M1 0,742 0,753 0,672 0,690 0,659 0,778 0,690 0,733 0,721 0,648 0,801 0,703 0,681 0,753 0,746 Fe 2+ M1 0,059 0,060 0,090 0,062 0,052 0,086 0,098 0,079 0,117 0,079 0,073 0,075 0,079 0,066 0,057 Mn M1 M1 subtotal 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 Mg M2 Fe 2+ M2 0,103 0,077 0,046 0,025 0,006 0,068 0,062 0,057 0,064 0,038 0,122 0,014 0,015 0,056 0,035 Mn M2 0,004 0,004 0,005 0,005 0,006 0,005 0,004 0,004 0,005 0,004 0,006 0,007 0,005 0,006 0,007 Ca M2 0,848 0,885 0,903 0,873 0,893 0,900 0,904 0,908 0,904 0,899 0,843 0,871 0,911 0,862 0,869 Na M2 0,044 0,034 0,046 0,097 0,096 0,026 0,030 0,031 0,027 0,058 0,029 0,108 0,069 0,076 0,089 K M2 M2 subtotal 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 Tabela A3 -Composição química (porcentagem peso) de cristais de olivina das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 4 oxigênios e 3 cátions. Abreviações: WEH, wehrlito; DUN, dunito.

Amostra JAC243 JAC243 JAC243 JAC243 JAC243 JAC243 JAC243 JAC243 JAC220 JAC220 JAC220 JAC220 JAC220 JAC220 JAC220 JAC220 JAC220 0,01 0,01 0,02 0,01 0,04 0,02 0,00 0,04 0,00 0,03 0,00 0,00 0,01 0,02 0,00 0,00 0,01 0,02 0,00 Al 2 O 3 0,01 0,01 0,00 0,00 0,01 0,02 0,03 0,01 0,00 0,01 0,01 0,01 0,00 0,00 0,00 0,01 0,01 0,02 0,00 0,26 0,17 0,25 0,14 0,26 0,25 0,27 0,22 0,27 0,29 0,18 0,14 0,24 0,24 0,25 0,08 0,27 0,37 0,41 Na 2 O 0,00 0,01 0,01 0,00 0,00 0,03 0,00 0,00 0,02 0,00 0,01 0,00 0,01 0,00 0,00 0,01 0,00 0,00 0,02 K 2 O 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,00 1,009 Ti 0,000 0,000 0,000 0,000 0,001 0,000 0,000 0,001 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Al 0,000 0,000 0,000 0,000 0,000 0,000 0,001 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Cr 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Fe 2+ 0,312 0,314 0,317 0,311 0,315 0,309 0,311 0,313 0,318 0,316 0,316 0,310 0,317 0,309 0,314 0,318 0,314 0,314 0,312 Mn 0,005 0,006 0,006 0,005 0,005 0,005 0,005 0,005 0,005 0,006 0,006 0,005 0,005 0,006 0,005 0,006 0,005 0,006 0,006 0,007 0,005 0,007 0,004 0,007 0,007 0,007 0,006 0,007 0,008 0,005 0,004 0,006 0,006 0,007 0,002 0,007 0,010 0,011 Ni 0,006 0,006 0,006 0,006 0,007 0,006 0,007 0,006 0,006 0,006 0,006 0,006 0,007 0,006 0,006 0,006 0,005 0,005 0,004 Na 0,000 0,001 0,001 0,000 0,000 0,001 0,000 0,000 0,001 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,001 K 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 1,009 Ti 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,001 0,000 0,000 0,000 Al 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Cr 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Fe 2+ 0,312 0,313 0,313 0,310 0,316 0,316 0,316 0,318 0,316 0,315 0,315 0,311 Mn 0,006 0,006 0,005 0,005 0,006 0,006 0,006 0,006 0,006 0,006 0,006 0,006 Mg 1,656 1,651 1,650 1,653 1,656 1,662 1,651 1,659 1,640 1,650 1,651 1,647 Ca 0,009 0,013 0,013 0,011 0,013 0,011 0,012 0,013 0,015 0,012 0,013 0,013 Ni 0,005 0,005 0,005 0,005 0,004 0,004 0,004 0,004 0,004 0,004 0,004 0,004 Na 0,000 0,000 0,000 0,001 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 K 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,03 0,09 0,06 0,10 0,06 0,01 0,09 0,05 0,02 0,02 0,07 0,02 0,02 0,02 0,06 0,05 0,01 FeO 0,13 0,19 0,17 0,19 0,12 0,09 0,11 0,13 0,17 0,09 0,13 0,13 0,17 0,09 0,16 0,10 0,07 MnO 0,00 0,01 0,00 0,00 0,01 0,01 0,01 0,00 0,00 0,00 0,00 0,00 0,01 0,00 0,01 0,00 0,00 MgO 0,00 0,00 0,00 0,00 0,00 0,01 0,00 0,02 0,00 0,004 0,012 0,009 0,013 0,008 0,001 0,012 0,007 0,003 0,002 0,009 0,002 0,003 0,002 0,008 0,007 0,001 Fe 2+ 0,020 0,028 0,026 0,029 0,018 0,014 0,017 0,020 0,026 0,014 0,019 0,020 0,026 0,014 0,024 0,015 0,011 Mn 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Mg 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,004 0,000 0,007 0,000 0,001 0,000 0,000 0,000 0,000 0,000 0,030 0,014 0,027 0,022 0,024 0,000 0,023 0,000 0,000 0,000 0,011 0,000 0,000 0,002 0,027 0,008 0,000 Ba 0,001 0,001 0,001 0,000 0,001 0,003 0,001 0,001 0,001 0,002 0,001 0,001 0,000 0,001 0,001 0,001 0,001 0,03 0,02 0,03 0,01 0,03 0,01 0,05 0,30 0,02 0,04 0,01 0,02 0,02 0,04 0,00 0,11 0,11 FeO 0,13 0,14 0,17 0,19 0,15 0,01 0,09 12,38 0,15 0,13 0,12 0,14 0,13 0,27 0,07 0,12 0,13 MnO 0,00 0,00 0,00 0,00 0,01 0,00 0,01 0,34 0,00 0,01 0,02 0,00 0,00 0,01 0,00 0,02 0,01 MgO 0,00 0,01 0,00 0,00 0,00 10,38 0,00 0,02 0,00 0,01 0,00 0,01 0,00 0,00 0,00 0,004 0,002 0,004 0,001 0,004 0,001 0,007 0,046 0,003 0,005 0,002 0,002 0,002 0,006 0,000 0,015 0,014 Fe 2+ 0,020 0,021 0,026 0,029 0,023 0,001 0,014 2,106 0,023 0,019 0,019 0,021 0,021 0,042 0,010 0,018 0,019 Mn 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,007 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Mg 0,000 0,000 0,000 0,003 0,000 0,000 0,001 3,150 0,000 0,005 0,000 0,004 0,000 0,002 0,000 0,000 0,01 0,08 0,09 0,11 0,07 0,10 0,10 0,10 0,12 0,02 0,01 FeO 0,06 0,11 0,13 0,56 0,12 0,29 0,15 0,20 0,22 0,12 0,13 MnO 0,00 0,00 0,00 0,00 0,00 0,01 0,00 0,01 0,00 0,00 0,00 MgO 0,00 0,00 0,00 0,00 0,00 0,00 0,00 0,01 0,00 0,02 0,00 CaO 0,20 0,008 0,017 0,020 0,085 0,018 0,044 0,023 0,029 0,033 0,018 0,021 Mn 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 0,000 Mg 0,000 0,000 0,000 0,001 0,001 0,001 0,000 0,003 0,001 0,005 0,000 Ca 0,038 0,361 0,328 0,579 

Figure 1 -

 1 Figure 1 -Carte géologique et de localisation du Complexe de Jacupiranga. Adaptée de Faleiros et Pavan (2013).

Figure 3 -

 3 Figure 3 -Variation de 87 Sr/ 86 Sr i vs. 143 Nd/ 144 Nd i pour les roches du Complexe de Jacupiranga. Une courbe de mélange (depuis les formules d'Albarède, 1995) a été proposée pour évaluer les processus d'assimilation crustale (depuis la composition du lamprophyre JAC46.2). Le contaminant représentatif est une roche métasédimentaire de Siga Jr. et al. (2011) -87 Sr / 86 Sr 0,91788 et 143 Nd/ 144 Ndi 0,511390.Les champs indiquent les données compilées pour les carbonatites de Jacupiranga (CARB,de Roden et al., 1987[START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF], les clinopyroxénites (CPX,de Huang et al., 1995) et les syénites (SYE,de Ruberti et al. 2005).

Figure 6 -

 6 Figure 6 -Comparaison entre les données Nd-Sr pour les roches du Complexe de Jacupiranga et les unité alcalines du sudest de la Plate-forme Sud-Américaine.

Figura 2 -

 2 Figura 1 -Mapa rodoviário simplificado destacando o acesso a Cajati a partir de Curitiba, pela BR-116. Modificado a partir de DNIT (2013). ................................................................ 27 Figura 2 -Localização dos principais unidades de rochas alcalinas conhecidas no Brasil. Adaptado de Biondi, 2005. .................................................................................................... 39

Figura 8 -

 8 Figura 3 -Ocorrências alcalinas ao longo das margens da Bacia do Paraná, na região centro-sudeste da Plataforma Sul-Americana (modificado de[START_REF] Riccomini | Tectonic controls of the Mesozoic and Cenozoic alkaline magmatism in the central-southeastern Brazilian Platform[END_REF]: 1) Bacia Bauru (Cretáceo Superior); 2) Província Magmática do Paraná (Cretáceo Inferior); 3) Bacia do Paraná (Ordoviciano Superior ao Cretáceo Inferior); 4) Unidades alcalinas (losangos, Permiano-Triássico; quadrados, Cretáceo Inferior; triângulos, Cretáceo Inferior; círculos, Paleógeno); 5) Eixo dos principais arcos; 6) Principais zonas de fratura (Lineamentos Guapiara (GP), São Jerônimo-Curiúva (JC), Rio Alonso (RA) e Rio Piquiri (RP); 7) Lineamento Lancinha-Cubatão. ............................................................................................. 41 Figura 4 -Mapa geológico das cinco intrusões carbonatíticas do Complexo de Jacupiranga e suas respectivas características. Adaptado de Gaspar e Wyllie (1983). ............................ 43 Figura 5 -Mapa geológico do Complexo de Jacupiranga que inclui o Gabro Itapuvuçu no Complexo de Jacupiranga. Adaptado de Faleiros e Pavan (2013). ...................................... 44 Figura 6-Mapa geológico das diferentes unidades presentes no carbonatito do Complexo de Jacupiranga conforme classificação de Saito et al. (1994): CPS -Carbonatito Sul Periférico; CCS -Carbonatito Central Sul; COX -Carbonatito oxidado; FCS -Áreas com Foskorito Sul; ZFA -Zona de Falha; CBI -Carbonatito Intermediário; CBF -Carbonatito Foliado; CBRcarbonatito branco; CBNcarbonatito norte; FCN -Áreas com foscorito Norte; DOL_N -Carbonatito dolomítico; XEN, XEE, XESáreas com xenólitos; JAC -Jacupiranguito. DLM_F: Carbonatito dolomítico fino Mesquita Sampaio; DLM_G: Carbonatitodolomítico grosso Mesquita Sampaio. FONTE: Lee e Ferreira (2007). .............. 45 Figura 7 -(A) Bloco métrico de rocha sienítica em meio a pasto (ponto 61); (B) Blocos e matacões de meladiorito em leito de rio (ponto 63); (C) Detalhe das bancadas da mina de carbonatito (Morro da Mina); (D) Afloramento de clinopiroxenito moderadamente alterado (ponto 34). ............................................................................................................................. 52 Figura 8 -Mapa de pontos descritos no Complexo de Jacupiranga. Base cartográfica: carta topográfica de Jacupiranga (1:50.000; IBGE, 1987). ............................................................ 53 Figura 9 -Mapa geológico do Complexo de Jacupiranga. Alterado de Faleiros e Pavan (2013). ................................................................................................................................... 54 Figura 10 -(A) Manto intempérico formado a partir da alteração das rochas duníticas (ponto 19); (B) Fotomicrografia de wehrlito (JAC220), com serpentina formando um retículo em torno dos cristais de olivina (polarizadores cruzados). .......................................................... 56 Figura 11 -(A) Amostra de magnetita clinopiroxenito (JAC50); (B) Fotomicrografia do magnetita clinopiroxenito JAC45 com cristais de diopsídio com zonamento inverso (polarizadores paralelos); (C) Amostra de clinopiroxenito com nefelina (intersticial) de granulação grossa (JAC18); (D) Fotomicrografia de clinopiroxenito com nefelina JAC18, com diopsídio cumulus e flogopita e nefelina intersticiais (polarizadores paralelos). Abreviações: Di, diopsídio; Mag, magnetita; Ne, nefelina; Phl, flogopita. ................................................... 56 Figura 12 -(A) Fotomicrografia do olivina clinopiroxenito JAC13 (polarizadores paralelos); (B) Diques de magnetita clinopiroxenito (granulação fina) intrudido em magnetita clinopiroxenito alterado (ponto 34). Abreviações: Di, diopsídio; Mag, magnetita; Ol, olivina. 57 Figura 13 -(a) Bloco de ijolito acamadado em meio a propriedade rural (ponto 29); (B) Amostra de ijolito acamadado, caracterizado por níveis alternados contituídos ora

3

  GEOLOGIA REGIONAL ................................................................................................................ 3.1 OCORRÊNCIAS ALCALINAS NO CENTRO-SUDESTE DA PLATAFORMA SUL-AMERICANA ...................................................................................................................................... 3.2 A PROVÍNCIA DO ARCO DE PONTA GROSSA ................................................................. 3.3 DESCOBERTA E MAPEAMENTO DO COMPLEXO DE JACUPIRANGA ........................... 3.4 GEOCRONOLOGIA .............................................................................................................. 3.5 PETROGÊNESE DO COMPLEXO DE JACUPIRANGA ...................................................... 3.6 ATIVIDADES DE LAVRA NO COMPLEXO .......................................................................... 3.7 JACUPIRANGUITO ............................................................................................................... .................................................................................................... 4.2 CLINOPIROXENITOS ........................................................................................................... 4.3 ROCHAS DA SÉRIE IJOLÍTICA ........................................................................................... 4.4 ZONA HETEROGÊNEA ........................................................................................................ 4.4.1 Rochas dioríticas ............................................................................................................... 4.4.2 Rochas monzoníticas ........................................................................................................ 4.4.3 Rochas sieníticas .............................................................................................................. 4.4.4 Fonolitos ............................................................................................................................ 4.4.5 Lamprófiros ........................................................................................................................ 4.5 CARBONATITOS .................................................................................................................. .......................................................................................................... 7.2 SÉRIES MAGMÁTICAS ...................................................................................................... 7.3 MAGMAS PARENTAIS DAS ROCHAS SILICÁTICAS ....................................................... 7.4 EVIDÊNCIAS DE ASSIMILAÇÃO CRUSTAL ..................................................................... 7.5 ORIGEM DOS CARBONATITOS ........................................................................................ 7.6 FONTE MANTÉLICA ........................................................................................................... 8 REFERÊNCIAS ........................................................................................................................... ANEXOS.............................................................................................................................................

Figura 1 -

 1 Figura 1 -Mapa rodoviário simplificado destacando o acesso a Cajati a partir de Curitiba, pela BR-116. Modificado a partir de DNIT (2013).

  na qual: I é ocupado por K, Na ou Ca (podendo também apresentar Ba, Cs, NH 4 , Rb) ; M por Fe (di-e trivalente), Mg, Mn, Al, Ti (Li, Zn. Cr, V) □ é uma vacância T é ocupado por Al, Fe (trivalente), Si A é ocupado por Cl, F ou OH (O).O recálculo dos dados da microssonda foram realizados em base anidra, considerando 22 oxigênios. Para as análises em que Si+Al<8, o Mg ocupa o sítio tetraédrico das micas de Jacupiranga conforme a substituição (VI) Mg+ (IV) Si⇔ (IV) Mg+(VI) Ti[START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] 2.4.3 OlivinaO cálculo das fórmulas estruturais das 31 análises de olivina (Tabela A3 dos Anexos) foi feito na base de 4 átomos de oxigênio e todo o Fe analisado foi considerado como Fe 2+ . A classificação dessa fase considerou os componentes moleculares:

  superiores do manto. Quando o magma atinge a posição atual do complexo, teria sido formada uma câmara magmática superior (CMS). A presença dos blocos de dunito teria causado o entupimento do conduto e levado à formação de uma segunda câmara magmática, abaixo da primeira (câmara magmática inferior -CMI). Como resultado de cristalização fracionada, o magma sódico na CMS se diferenciaria em uma sequência cumulática de dunitos, melteigitos e jacupiranguitos. Os autores consideram os carbonatitos como uma fase decorrente da imiscibilidade de líquidos silicáticos e carbonáticos.

  Intrudido em rochas metassedimentares da Formação Turvo-Cajati e na Suíte Intrusiva Itapeúna, ambos do Neoproterozóico, o Complexo de Jacupiranga apresenta forma ovalada, com direção NNW, cerca de 65 km² de área aflorante e altitudes que variam de 30 a 290 m. Dos 89 pontos descritos em campo, a maior parte se trata de blocos métricos (Figura 7A, B), aparentemente não in situ, apesar de a topografia suave sugerir que eles se mantêm consideravelmente próximos de sua origem. Fora da área da mina (Figura 7C), os poucos afloramentos encontrados são de clinopiroxenitos (Figura 7D), com grau de alteração moderado a muito elevado. O mapa de todos os pontos descritos é apresentado na Figura 8.

Figura 7 -

 7 Figura 7 -(A) Bloco métrico de rocha sienítica em meio a pasto (ponto 61); (B) Blocos e matacões de meladiorito em leito de rio (ponto 63); (C) Detalhe das bancadas da mina de carbonatito (Morro da Mina); (D) Afloramento de clinopiroxenito moderadamente alterado (ponto 34).

Figura 8 -

 8 Figura 8 -Mapa de pontos descritos no Complexo de Jacupiranga. Base cartográfica: carta topográfica de Jacupiranga (1:50.000; IBGE, 1987).

Figura 9 -

 9 Figura 9 -Mapa geológico do Complexo de Jacupiranga. Alterado de Faleiros e Pavan (2013).

Figura 10 -

 10 Figura 10 -(A) Manto intempérico formado a partir da alteração das rochas duníticas (ponto 19); (B) Fotomicrografia de wehrlito (JAC220), com serpentina formando um retículo em torno dos cristais de olivina (polarizadores cruzados).

  Figura 12 -(A) Fotomicrografia do olivina clinopiroxenito JAC13 (polarizadores paralelos); (B) Diques de magnetita clinopiroxenito (granulação fina) intrudido em magnetita clinopiroxenito alterado (ponto 34). Abreviações: Di, diopsídio; Mag, magnetita; Ol, olivina.

  Figura 14 -(A) Amostra de diorito JAC20; (B) Amostra de meladiorito JAC63;

Figura 15 -

 15 Figura 15 -(A) Amostra de olivina monzonito (JAC26.2); (B) Fotomicrografia de olivina monzonito (JAC26.2); (C) Amostra de monzonito (JAC25); (D) Afloramento de monzonito com enclave decimétrico alongado (ponto 25).

Figura 16 -

 16 Figura 16 -(A) Melassienito com fenocristais de feldspato alcalino em meio a matriz máfica (JAC31); (B) Enclaves máficos arredondados em melassienito (ponto 31); (C) Fotomicrografia de enclave máfico arredondado no melassienito JAC31 (polarizadores paralelos); (D) Amostra de álcali-feldspato sienito em contato com lamprófiro (JAC46.4); (E) Álcali feldspato sienito com agregados máficos constituídos por hastingsita, titanita, magnetita e biotita (JAC32 -polarizadores paralelos); (F) Agregado máfico em álcali feldspato sienito com borda de reação (JAC32 -polarizadores paralelos). Abreviações: Afs, feldspato alcalino; Bt, biotita; Di, diopsídio; Hs, hastingsita; Mag, magnetita; Ttn, titanita.

(

  submilimétricos) associado a vidro vulcânico e mesóstase félsica e a relação microcristais/matriz é cerca de 1:5. Há níveis descontínuos com maior e menor concentração de vidro, indicando fluxo magmático. Devido à presença de vidro vulcânico, esse lamprófiro é classificado como monchiquito conforme a classificação de Le Maitre (2002).

Figura 18 -

 18 Figura 18 -(A) Diques de lamprófiro sem direção preferencial intrudidos no Granodiorito Itapeúna (ponto 39); (B) Diques de lamprófiro intrudidos em álcali-feldspato sienito (ponto 46); (C) Fotomicrografia de lamprófiro de granulação fina com macrocristais de olivina corroídos, circundados por biotita (JAC46.2 -polarizadores paralelos); (D) Fotomicrografia de lamprófiro de granulação grossa com macrocristais de biotita e diopsídio (JAC46.1 -polarizadores paralelos). Abreviações: Bt, biotita; Di, diopsídio; Mag, magnetita; Mes, mesóstase félsica; Ol, olivina; Ttn, titanita.

  identifica duas intrusões carbonatíticas distintas em Jacupiranga, uma a sul e outra a norte, Gaspar e[START_REF] Gaspar | Magnetite in the carbonatites from the Jacupiranga Complex, Brazil[END_REF] descrevem cinco episódios intrusivos sucessivos (C1, C2, C3, C4 e C5). Baseado em critérios mineralógicos,Hirano et al. (1987) definem quatro classes composicionais para a unidade: calcita carbonatito (CC), calcita carbonatito rico em magnetita (CCmt), apatita-calcita carbonatito (CCap) e dolomita carbonatito (DC). A porção sul da unidade é constituída predominantemente por CC, com CCap e CCmt nas zonas de borda. Já a norte, predomina DC com CC e algumas bandas constituídas por CCmt. Tendo em vista o seu caráter descritivo e sem conotações genéticas, a classificaçãode Hirano et al. (1987) foi a adotada neste trabalho.Em alguns pontos da unidade carbonatítica, são observados níveis centimétricos e descontínuos definidos por uma concentração de fases não-carbonatíticas (principalmente níveis de apatita ou magnetita -Figura 19B). De acordo com o minucioso estudo estrutural realizado por[START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF] na unidade, estes níveis são verticais (no caso das intrusões C2 e C4 -Figura 19C) ou de alto ângulo (C1 e C5). Somente em C3 o autor descreve níveis com menores ângulos de mergulho (20-40°).Da porção norte da unidade, foram coletadas amostras representativas de CC (JAC07), CCmt (JAC08) e DC (JAC09), enquanto que, a sul, foram coletadas CCap (JAC04, JAC42) e CCmt (JAC11). Tratam-se de rochas de granulação média a grossa constituídas predominantemente por calcita, exceto JAC09, na qual dolomita é a fase carbonática mais abundante. JAC07 é um calcita carbonatito (Figura 20A, B) de granulação média, textura granular e constituído unicamente por calcita. JAC08 é um magnetita calcita carbonatito de granulação média (Figura 20C, D), formado predominantemente por calcita, magnetita e apatita, com dolomita, olivina, sulfetos e badelleíta subordinados. Este litotipo é caracterizado por um bandamento composicional (milimétrico a centimétrico) definido por variações nas proporções de apatita e magnetita, que se apresentam orientados paralelamente a estas bandas. O dolomita carbonatito JAC09 (Figura 20E, F) apresenta granulação média e cristais alongados, de granulação fina, de apatita como fase acessória, que ocorrem como bolsões irregulares em meio à dolomita. Outras fases subordinadas são magnetita, calcita, flogopita e rara olivina. JAC04 e JAC42 são apatita calcita carbonatitos de granulação média e textura granular (Figura 21A, B). São constituídos por cristais de apatita prismáticos disseminados, geralmente fraturados. JAC11 apresenta granulação grossa e é constituído por calcita, magnetita e apatita Figura 21C, D), com dolomita, olivina, flogopita e sulfetos subordinados. Assim como JAC08, variações nas proporções modais de apatita/magnetita e a orientação preferencial dos cristais de apatita definem um bandamento composicional neste litotipo.

Figura 19 -

 19 Figura 19 -(A) Vista da zona de xenólitos de clinopiroxenito em meio a carbonatito; (B) Níveis descontínuos com concentração de magnetita em dolomita carbonatito (ponto 09); (C) Magnetita calcita carbonatito com bandamento verticalizado (ponto 08).

Fig. 1 .

 1 Fig. 1. (A) Alkaline occurrences along the Paraná Basin margins at the central-southeastern part of the South America platform (after Riccomini et al., 2005): 1) Late Cretaceous Bauru Basin; 2) Early Cretaceous Paraná Magmatic Province; 3) Late Ordovician to Early Cretaceous Paraná Basin; 4) Alkaline units (diamonds, Permian-Triassic; squares, Early Cretaceous; triangles, Late Cretaceous; circles, Paleogene); 5) Axes of main archs; 6) Major fracture zones (GP, Guapiara; JC, São Jerônimo-Curiúva; RA, Rio Alonzo; RP, Rio Piquiri); 7) Lancinha-Cubatão Shear Zone. (B) Detailed tectonic setting of Cretaceous alkaline magmatism in the Ponta Grossa Arch (after Ruberti et al. 2012): (A) and (B) dikes as inferred by field geology and remote sensing and aeromagnetic survey, respectively; (C) alkaline complexes: BIT-Barra do Itapirapuã, BN-Banhadão, BT-Barra do Teixeira, CN-Cananéia, IP-Ipanema, IT-Itapirapuã, JAC-Jacupiranga, JQ-Juquiá, MP-Mato Preto, PAR-Pariquera-Açu and TU-Tunas. (C) Schematic geological map of the Jacupiranga Complex (compiled and modified from Faleiros and Pavan, 2013) with the location of all samples collected for this study (diamonds, core sample; circles, outcrop samples).

Fig. 2 .

 2 Fig. 2. Petrographic features of the Jacupiranga rocks. (A) Relict olivine surrounded by serpentine network in wehrlite JAC220. (B) Cumulus diopside with reverse zoning and interstitial Ti-magnetite in clinopyroxenite JAC45. (C) Banded ijolite JAC29.2 showing different proportions of nepheline and diopside. (D) Plagioclase phenocrysts mantled by alkali-feldspar rims in monzonite JAC25. (E) Sieve-texture hornblende in monzonite JAC25. (F) Partially corroded diopside cores replaced by biotite in meladiorite JAC22 (G) Aggregates of hastingsite and magnetite in alkali-feldspar syenite JAC32. (H) Diopside macrocryst with turbid core in coarse-grained lamprophyre JAC46.1. Plane-polarized light, except (D). Abbreviations: Afsalkali feldspar, Apapatite, Btbiotite, Cpxclinopyroxene, Hbhornblende, Hshastingsite, Magmagnetite, Mesmesostasis, Nenepheline, Phlphlogopite, Plplagioclase, Srpserpentine, Ttntitanite.

  quantification and drift control, and the BIR-2G and SRM-612 (NIST) for quality controls. For data integration and determination of concentrations, detection limits and analytical errors of the different elements, the Glitter 4.4.2 software[START_REF] Van Achterbergh | Data reduction software for LA-ICP-MS: appendix[END_REF] was used. As an internal standard for normalization and quantification purposes, CaO contents from the electron microprobe analyses were utilized. Linear adjustment was selected as interpolation method for drift control and quantification. Errors (1s) are around 5% for mostly trace elements analyzed. Average detection limits can be found inAndrade et al. (2014). For this investigation, we selected two samples from[START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF] (JC105 and JC127) as they show higher Mg# values (65 and 66, respectively) than those of our sampling (42-63).

  Separation and purification were carried out at the Mineral Separation Laboratory (MSL) from the Center for Geochronological Research (CPGeo-USP, University of São Paulo, Brazil) by conventional techniques (ring mill, sieving, washing, heavy liquids, magnetic separation and hand pick). Selected grains were mounted on epoxy and polished. The crystals were analyzed for U, Th, and Pb isotopic compositions using the sensitive high-resolution ion microprobe (SHRIMP) at the U-Pb Laboratory of CPGeo-USP, following the procedures stated by[START_REF] Sato | Sensitive High Resolution Ion Microprobe ( SHRIMP IIe / MC) of the Institute of Geosciences of the University of São Paulo, Brazil: analytical method and first results[END_REF].For the Sr-Nd isotope analyses, 100-200 mg of whole-rock powders were leached with 6 N HCl during one hour at 95°C (except for the carbonatites), rinsed three times in ultrapure water and then dissolved in a mixture of HF-HNO 3 during 72h on a hot plate. After evaporation to dryness, concentrated HNO 3 was added to the residue and kept at about 110 °C for 48h. Sr and Nd chemical separation was carried out using different chemical separation steps (seeBosch et al., 2008 for details). Sr concentrate was loaded into Re filaments adding a tantalum activator to the sample and its isotopic composition was measured using a Triton Finnigan Mat spectrometer from the Labogis (Nîmes University).During this study, measurements of the NBS987 standard gave an average 87 Sr/ 86 Sr ratio of 0.710242 (n=5) (normalized to 86 Sr/ 88 Sr = 0.1194). Nd isotopic composition was measured by multicollector inductively coupled plasma mass spectrometry (ThermoFisher Scientific Neptune Plus) at the École Normale Supérieure de Lyon. The AMES-Rennes standard analyzed during the course of this study gave an average 143 Nd/ 144 Nd value of 0.511961±23

Fig. 3 .

 3 Fig. 3. (A) CL SEM images of the analysed zircon grains. (B) SHRIMP zircon U-Pb concordia diagram for monzonite (sample JAC25) of the Jacupiranga Complex.

Fe

  3+ , and Mg contents similar to those of the melasyenite. Despite plotting close to clinopyroxenites and ijolite clinopyroxenes, diorite diopsides are comparatively depleted in Ca and enriched in Si. Within the lamprophyres, clinopyroxenes have strongly variable compositions that overlap those from all other lithotypes.

  clinopyroxenite JC105 yield well-defined convex-upwards patterns, near-constant abundances of LREE, and negative Eu anomalies. In comparison, diopside cores from olivine-bearing clinopyroxenite (JC127) display smoother REE normalized patterns with slightly more variable LREE contents (particularly La, Ce, Pr, and Sm). La N /Yb N values range from 7.12 to 15.76 (JC105) and from 9.32 to 12.43 (JC127). JC127 yields higher concentrations of Nb (1.72-2.24 ppm) and Sr (389-720 ppm) and lower than those in JC105 (<0.27 ppm, 149-271 ppm, and 129-206 ppm, respectively).

Fig. 5 .

 5 Fig. 5. Compositional variation in clinopyroxene crystals of the Jacupiranga Complex in the Na-Mg-Fe* (Fe*=Fe2++Fe3++Mn-Na) diagram and comparison with other Brazilian alkaline units. Field of Jacupiranga clinopyroxene data compiled from[START_REF] Gaspar | Geologie et mineralogie du complexe carbonatique de Jacupiranga, Brésil. Tese de doutorado[END_REF]. Trends: 1. Ipanema[START_REF] Guarino | Magmatism and fenitization in the Cretaceous potassium-alkaline-carbonatitic complex of Ipanema São Paulo State, Brazil[END_REF]; 2. Juquiá[START_REF] Beccaluva | Fractional crystallization and liquid immiscibility processes in the alkaline-carbonatite complex of Juquiá, São Paulo, Brazil[END_REF]; 3. Anitápolis[START_REF] Furtado | Caracterização química dos clinopiroxênios do maciço maciço alcalino de Anitápolis[END_REF]; 4. Itapirapuã[START_REF] Gomes | Petrologia do maciço alcalino de Itapirapuã[END_REF]; 5. Banhadão[START_REF] Ruberti | The Banhadão alkaline complex, southeastern Brazil: source and evolution of potassic SiO 2 -undersaturated high-Ca and low-Ca magmatic series[END_REF]; 6. Tunas[START_REF] Gomes | Petrological and geochemical studies of alkaline rocks from continental Brazil. 2. The Tunas massif, state of Paraná[END_REF]; 7. Cananeia[START_REF] Spinelli | A ocorrência alcalina de Cananéia, litoral sul do estado de São Paulo: química mineral[END_REF]. Bold line: obtained trend for the Jacupiranga Complex.

Fig. 6 .

 6 Fig. 6. (A) Chondrite-normalized[START_REF] Sun | Chemical and isotopic systematics of oceanic basalts: implications for mantle composition and processes[END_REF]) REE patterns diagram for cores of diopsides cumulus crystals from Jacupiranga clinopyroxenites. (B) Chondrite-normalized[START_REF] Sun | Chemical and isotopic systematics of oceanic basalts: implications for mantle composition and processes[END_REF]) REE pattern fields for calculated liquid in equilibrium with diopside cores from Jacupiranga clinopyroxenites. For comparison, lamprophyres compositional field is also shown (this work and[START_REF] Menezes | The antecryst compositional influence on Cretaceous alkaline lamprophyre dykes, SE Brazil[END_REF].

Fig. 7 .

 7 Fig. 7. Compositional variation in micas from the Jacupiranga Complex in the Mg-Al-Fe(T) diagram. Fe(T): total iron calculated as Fe2+ (apfu). TFP: tetra-ferriphlogopite. Fields for Jacupiranga micas compiled from Brod et al. (2001): green fieldmicas from carbonatites; pink fieldmicas from silicate rocks.

(

  Ab 52-55 Or 43-47 ) and subordinate perthite. Lamprophyres are composed of groundmass sanidine and mesostasis of anorthoclase.In monzonite, alkali feldspar occurs as groundmass sanidine and as perthite rims on andesine phenocrysts.The plagioclase in diorite, monzonite, and lamprophyre tends towards more Na-rich compositions (An<55). Diorite plagioclase is normally zoned andesine (An 31-48 ) with cores occasionally reaching labradorite compositions (An 55 ). The plagioclase in monzonite is mainly andesine (An 24-45 ) with subordinate oligoclase and labradorite. In lamprophyres, groundmass plagioclase is mainly oligoclase (Ab 73-97 An 1-22 ) with subordinate albite compositions.

Fig. 8 .

 8 Fig. 8. Compositional variation in feldspar from the Jacupiranga Complex in the Ab-Or-An diagram (mol.%).

  9A), the rocks from the Heterogeneous Zone show a continuous trend of alkalis and silica rising from basanites to trachyte/phonolites, whereas the clinopyroxenites and ijolitic rocks present increasing alkalis with almost constant silica. Those two silicate groups are also distinguished in the R1-R2 diagram (Fig.9B): clinopyroxenites and ijolitic rocks form an evolution trend mainly controlled by the fractionation of clinopyroxene with increasing nepheline, whereas the rocks from the Heterogeneous Zone plot near the SiO 2 -saturation plane. In variation diagrams, the latter group shows a systematic rise in Al 2 O 3 , Na 2 O, and K 2 O with increasing silica, while TiO 2 , CaO, and Mg# decrease (Fig.10). Clinopyroxenites and ijolitic rocks yield a strong increase of Mg# with SiO 2 , which mainly reflect variations in their amount of intercumulus phases (e.g. Ti-magnetite, phlogopite). Other Jacupiranga analyses compiled from[START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF] and[START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF] systematically follow these trends (Fig.9, 10). The carbonatites are poor in silica (< 2.38 wt.%) and show low Al 2 O 3 (<0.23 wt.%), K 2 O (<0.09 wt.%), and Na 2 O (<0.06wt.%), as seen in most plutonic

Fig. 9 .

 9 Fig. 9. Classification diagrams for the Jacupiranga silicate rocks. The pink field is representative of compiled data of the basement rocks (Faleiros and Pavan, 2013). Jacupiranga rocks compiled from Ruberti et al. (2005) and Beccaluva et al. (2017) are shown as small symbols. (A) Total alkalis vs. SiO2 (TAS) diagram (Le Bas et al., 1992). Light-gray line shows the divide between alkaline and subalkaline igneous rocks after Irvine and Baragar (1971); (B) R1-R2 diagram (De La Roche et al., 1980). Average mineral poles of the Jacupiranga main assemblage are shown as empty circles. Abbreviations: afs, alkali feldspar; cpx, clinopyroxene; mag, magnetite; ne, nepheline; ol, olivine; pl, plagioclase.

  close age-corrected Nd isotopic values (0.51232-0.51239 and 0.51224-0.51238, respectively). When considered separately, samples from the Heterogeneous Zone are widely scattered as meladiorite JAC22 and monzonite JAC25 yield unexpected low Nd (0.51187 and 0.51201) and high Sr ratios (0.70583 and 0.70609), similar to those from gabbros and syenites from[START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF].

Fig. 12 .

 12 Fig. 12. Variation of 87Sr/86Sri vs. 143Nd/144Ndi for analyzed rocks from the Jacupiranga Complex. Mixingmodel curve based on the formulae of Albarède (1995) was offered to evaluate crustal assimilation processes (from lamprophyre JAC46.2). Representative contaminant is a metasedimentar rock from Siga Jr. et al. (2011) -87Sr/86Sr 0.91788 and 144Nd/143Ndi 0.511390. Smaller symbols are compiled data for Jacupiranga arbonatites

Fig. 13 .

 13 Fig. 13. Age distribution chart for representative Jacupiranga samples. Error bars are 2σ. Black squares: isochron weighed mean age (with plateau age); black circle: isochron weighed mean age (without plateau age).

  ,[START_REF] Ruberti | The alkaline magmatism from the Ponta Grossa Arch[END_REF],[START_REF] Gomes | Alkaline magmatism in the Ponta Grossa Arch, SE Brazil: a review[END_REF][START_REF] Beccaluva | The alkaline-carbonatite complex of Jacupiranga (Brazil): Magma genesis and mode of emplacement[END_REF], who have considered that the Jacupiranga rocks were originated from distinct parental magmas. In our view, the nephelinite series comprises part of the clinopyroxenite unit (particularly nepheline-bearing clinopyroxenites) and the ijolitic rocks, whereas the basanite series encompasses the feldspar-bearing rocks, phonolites, lamprophyres and, possibly, part of the clinopyroxenites.

Fig. 14 .

 14 Fig. 14. Variation of (A) 87Sr/86Sri vs. SiO2 diagram and (B) 87Sr/86Sri vs. 1/Sr for the analyzed rocks from the Jacupiranga Complex. The symbols are as in Fig. 12.

  The lamprophyres show low εNd values (from -10.4 to -7.5) and high Ba (1478-2573 ppm), Rb (70.8-144.2 ppm), and K contents (3.71-3.95 %). Similar compositions are found in the nephelinites of Anitápolis Complex, to which[START_REF] Gibson | The limited extent of plume-lithosphere interactions during continental flood-basalt genesis: Geochemical evidence from Cretaceous magmatism in southern Brazil[END_REF] attributed a subcontinental lithospheric mantle (SCLM) as the predominant melt source region.

Fig. 15 .

 15 Fig. 15. LaN/ZrN vs. HfN/YN (primitive mantle-normalized, Sun and McDonough, 1989) for the calculated liquids in equilibrium with diopside cores from Jacupiranga clinopyroxenites. Dashed field: lamprophyres dikes related to the Ponta Grossa Arch region (Jacupiranga included) compiled from Menezes et al. (2015). Non-modal batch melting models for different mantle sources by Azzone et al. (2013) are presented. Black square: metasomatic vein; Grey square: wall rock. Mantle source residues: inverted triangle (off-craton gt-lherzolite); diamonds (primitive mantle gt-lherzolite); circles (theoretical wehrlite). Numbers indicate degree of partial melting. Compiled data from Azzone et al. (2013): light green field, Júquia mesocumulates; dark green field, Juquiá adcumulates.

Fig. 1 .

 1 Fig. 1. (A) Alkaline occurrences along the Paraná Basin margins at the central-southeastern part of the South America platform (after Riccomini et al., 2005): 1) Late Cretaceous Bauru Basin; 2) Early Cretaceous Paraná Magmatic Province; 3) Late Ordovician to Early Cretaceous Paraná Basin; 4) Alkaline units (diamonds, Permian-Triassic; squares, Early Cretaceous; triangles, Late Cretaceous; circles, Paleogene); 5) Axes of main archs; 6) Major fracture zones (GP, Guapiara; JC, São-Jerônimo-Curiúva; RA, Rio Alonzo; RP, Rio Piquiri); 7) Lancinha-Cubatão Shear Zone. (B) Schematic geological map of the Jacupiranga Complex (compiled and modified from Faleiros and Pavan, 2013). (C) Location of all samples collected for this study (red diamonds, core sample; red circles, outcrop samples).

  Fig. 2. Measured 206 Pb/ 204 Pb vs. measured 207 Pb/ 204 Pb and 208 Pb/ 204Pb for the analyzed Jacupiranga rocks. Compiled Jacupiranga data are from[START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF]. The parameters EM1, EM2, HIMU, and DMM are approximations of mantle end-members as in[START_REF] Bell | Nd, Pb and Sr isotopic compositions of east African carbonatites: evidence for mantle mixing and plume inhomogeneity[END_REF], taken after[START_REF] Hart | A possible new Sr-Nd-Pb mantle array and consequences for mantle mixing[END_REF][START_REF] Hart | Mantle plumes and entrainment: isotopic evidence[END_REF]. The fields of Early Cretaceous tholeiites from the Paraná Etendeka Province (Comin-Chiaramonti et al., 2005 and references therein), Brazilian alkaline-carbonatite complexes (Comin-Chiaramonti et al., 2005 and references therein) are plotted for comparison. Tristan da Cunha and Paraná Magmatic Province tholeiites are based on data from the GEOROC database (http://georoc.mpch-mainz.gwdg.de/georoc/).

Fig. 3 .

 3 Fig. 3. εHfi vs. εNdi diagram for the analyzed Jacupiranga samples. Field of Tristan da Cunha[START_REF] Salters | Domains of depleted mantle: New evidence from hafnium and neodymium isotopes[END_REF], Goiás peridotite xenoliths[START_REF] Carlson | Chemical and isotopic relationships between peridotite xenoliths and mafic-ultrapotassic rocks from Southern Brazil[END_REF] and Catalão rocks[START_REF] Guarino | U-Pb ages, geochemistry, C-O-Nd-Sr-Hf isotopes and petrogenesis of the Catalão II carbonatitic complex (Alto Paranaíba Igneous Province, Brazil): implications for regional-scale heterogeneities in the Brazilian carbonatite associations[END_REF] are shown for comparison. Other fields were compiled from[START_REF] Guarino | U-Pb ages, geochemistry, C-O-Nd-Sr-Hf isotopes and petrogenesis of the Catalão II carbonatitic complex (Alto Paranaíba Igneous Province, Brazil): implications for regional-scale heterogeneities in the Brazilian carbonatite associations[END_REF] and references therein.

Fig. 4 .

 4 Fig. 4. Classification diagrams for the Jacupiranga silicate rocks. The pink field is representative of compiled data of the basement rocks (Faleiros and Pavan, 2013). Black solid line: liquid line of descent obtained by model of fractional crystallization using the MELTS algorithm. Points a and b indicate the percentage mass of fractionation of 25% and 50% respectively. (A) Total alkalis vs. Silica (TAS) diagram (Le[START_REF] Le Bas | The construction of the Total Alkali-Silica chemical classification of volcanic rocks[END_REF]. Light-green line shows the divide between alkaline and subalkaline igneous rocks after[START_REF] Irvine | A Guide to the Chemical Classification of the Common Volcanic Rocks[END_REF]; (B) R1-R2 diagram[START_REF] De La Roche | A classification of volcanic and plutonic rocks using R1-R2 diagram and major-element analyses. Its relationships with current nomenclature[END_REF]. Average mineral poles of the Jacupiranga main assemblage are shown as red circles. Abbreviations: cpx, clinopyroxene; afs, alkali feldspar; mag, magnetite; ne, nepheline; pl, plagioclase.

Fig

  Fig. 5. Initial 143 Nd/ 144 Nd vs. Initial 87 Sr/ 86

Fig. 6 .

 6 Fig. 6. Concentration ratios between selected Jacupiranga carbonatites and phonolites. Partition coefficients of trace elements between immiscible carbonate and silicate liquids (represented by the grey fieldcompiled data from Veksler et al., 1998) are also plotted. *compiled data from Ruberti et al. (2005).

Fig. 7 .

 7 Fig. 7. Nb vs. Ta diagram[START_REF] Thompson | Ankerite carbonatite from Swartbooisdrif, Namibia: the first evidence for magmatic ferrocarbonatite[END_REF] for the Jacupiranga carbonatites. Jacupiranga compiled data are from[START_REF] Huang | Geochemical characteristics and origin of the Jacupiranga carbonatites, Brazil[END_REF]. Green and grey fields represent the silicate rocks from the highly and mildly silicaundersaturated series, respectively. Dashed fields: a, Tapira parental melt and b, Tapira bebedorites and syenite. Data for Tapira carbonatites and silicate rocks are from[START_REF] Brod | Decoupling of paired elements, crossover REE patterns, and mirrored spider diagrams: fingerprinting liquid immiscibility in the Tapira alkaline carbonatite complex, SE Brazil[END_REF], whereas those for Barra do Itapirapuã carbonatites are from[START_REF] Ruberti | The geochemistry of the Barra do Itapirapuã carbonatite (Ponta Grossa Arch, Brazil): a multiple stockwork[END_REF].

Fig. 8 .

 8 Fig. 8. Distribution of Ba/La compositions in carbonatites and silicate rocks in the Jacupiranga Complex.

Fig. 9 .

 9 Fig. 9. (A) Initial 87 Sr/ 86 Sr VS. measured 206 Pb/ 204 Pb isotopic ratios and (B) Initial 143 Nd/ 144 Nd VS. measured 206 Pb/ 204 Pb isotopic ratios for the analyzed Jacupiranga rocks. Symbols and fields are as in Fig, 2.

Fig. 10 .

 10 Fig. 10. Primitive-mantle normalized (McDonough and Sun, 1995) trace element diagrams for the Jacupiranga lamprophyres. High-Ti tholeiites (i.e. Pitanga and Paranapanema-types) similarly show Nb-Ta negative anomaly (grey field). On the other hand, Tristan da Cunha (TdC) volcanics yield Nb-Ta positive anomaly. Compiled data from Rocha-Júnior et al. (2013).

  tipicamente interpretados como indicativos de SCML metassomatizado, enquanto que os clinopiroxenitos, ijolito e dunito têm ΔεHf positivos, sugestivos de uma contribuição levemente maior de granada peridodito na fonte destas rochas, uma vez que granada e clinopiroxênio peridotíticos apresentam valores de 176 Hf/ 177 Hf radiogênicos. Logo, no que tange aos magmas parentais das duas séries silicáticas, supõe-se que enquanto o líquido basanítico resulta de uma maior contribuição dos veios wehrlíticos, o magma nefelinítico seria gerado a partir de contribuições um pouco mais significativa das encaixantes peridotíticas, apesar de ambos os líquidos serem enriquecidos. Os lamprófiros se assemelham quimicamente aos basaltos de alto titânio aflorantes a norte da Província Magmática do Paraná, caracterizados por depleção em Nb-Yb, enriquecimento em ETR leves em relação aos pesados e enriquecimento em Cs, Rb e Sr. Estas características sugerem que as reações metassomáticas na fonte mantélica do complexo associam-se a fluidos derivados de processos de subducção, tal como proposto por Rocha-Júnior et al. (2013) para a fonte das rochas toleíticas. As idades modelo T DM das rochas analisadas indicam o caráter heterogêneo da fonte mantélica e são coerentes com os valores geralmente obtidos para as ocorrências alcalinas do sudeste da Plataforma Sul Americana. Os valores médios obtidos tanto para as idades Nd (971 Ma ± 198) quanto para Hf (1,1 Ga ± 0,3) se enquadram nas médias encontradas nas unidades relacionadas ao lineamento Guapiara e sugerem que a fonte mantélica foi metassomatizada por fluidos possivelmente relacionados a eventos de subducção do Neoproterozóico (e.g. Ciclo Brasiliano/Pan-Africano). Heterogeneidades na fonte das ocorrências alcalinas brasileiras também são indicadas pelas razões isotópicas de Hf, uma vez que enquanto os dados de Jacupiranga e Catalão I (Guarino et al. 2016) são

  

  

  

  

  

  

  

  

  

  

  

  

  1.1 CONTEXTUALIZAÇÃO ......................................................................................................... 1.2 LOCALIZAÇÃO E VIAS DE ACESSO ................................................................................... 1.3 JUSTIFICATIVA .................................................................................................................... 1.4 OBJETIVOS .......................................................................................................................... 1.5 APRESENTAÇÃO E ESTRUTURAÇÃO DA TESE .............................................................. AMOSTRAGEM.............................................................................. 2.2 ANÁLISE PETROGRÁFICA .................................................................................................. 2.3 GEOQUÍMICA DE ROCHA TOTAL ...................................................................................... 2.4 QUÍMICA MINERAL .............................................................................................................. 2.4.1 Clinopiroxênio .................................................................................................................... 2.4.2 Micas ................................................................................................................................. 2.4.3 Olivina ................................................................................................................................ 2.4.4 Anfibólio ............................................................................................................................. 2.4.5 Feldspato ........................................................................................................................... Datação Ar-Ar .................................................................................................................... 2.6.2 Datação U-Pb SHRIMP .....................................................................................................

	2.1	ETAPAS DE CAMPO E

2 MATERIAIS E MÉTODOS ............................................................................................................. 2.5 ISÓTOPOS RADIOGÊNICOS EM ROCHA TOTAL ............................................................. 2.6 GEOCRONOLOGIA .............................................................................................................. 2.6.1

Sr-Nd isotope geochemistry, and implications for the origin of the silicate rocks of the Jacupiranga ultramafic-alkaline Complex (Brazil)", submetido

  ao Journal of South American Earth Sciences. No artigo, destacam-se dados geoquímicos de rocha total (elementos maiores e traço), dados de isótopos radiogênicos de Nd e Sr, química mineral (elementos maiores) e análises pontuais de elementos traço em clinopiroxênio, além das idades Ar-Ar e U-Pb SHRIMP. Esses dados serviram de base para a caracterização de duas séries magmáticas distintas para as rochas

	Tendo em vista este panorama, os objetivos gerais desta tese são:
	1.	Definir as relações temporais entre os diferentes litotipos que compõem o
	no Brasil.	
	A tese é dividida em oito capítulos, sendo que os dois primeiros abordam os
	aspectos introdutórios e as técnicas analíticas empregadas neste estudo.
	O capítulo 3 apresenta uma revisão bibliográfica acerca do magmatismo alcalino na
	Plataforma Sul Americana, com destaque às ocorrências associadas à região do Arco de
	Ponta Grossa, além de um levantamento sobre as principais propostas até então publicadas
	concernente à petrogênese do Complexo de Jacupiranga.

Complexo de Jacupiranga, com base em dados geocronológicos, na tentativa de se estabelecer uma cronologia relativa e a ordem de colocação das diferentes unidades;

2.

Caracterizar petrologicamente o Complexo de Jacupiranga, incluindo tanto as rochas silicáticas quanto os carbonatitos. Os objetivos específicos deste item incluem a identificação dos potenciais magmas parentais, características de fontes mantélicas e determinação dos processos evolutivos que culminaram na formação tanto das rochas silicáticas quanto dos carbonatitos. 1.5 APRESENTAÇÃO E ESTRUTURAÇÃO DA TESE O presente volume engloba os resultados obtidos nesta tese, iniciada em março de 2013 e desenvolvida em co-tutela entre a Universidade Federal do Paraná (UFPR -Programa de Pós-Graduação em Geologia) e a Université de Montpellier (UM -Géosciences Montpellier), na França, no âmbito do convênio estabelecido entre estas duas instituições. Foi acordado entre os representantes de cada universidade que, dos quatro anos de duração da tese, um seria desenvolvido na Université de Montpellier, e os demais, O capítulo 4 descreve a geologia e a petrografia das unidades que constituem o Complexo de Jacupiranga. Apesar de alguns desses aspectos serem retomados nos capítulos seguintes, optou-se por esta abordagem com a intenção de se apresentar feições de campo e algumas particularidades que não puderam ser adequadamente tratadas nos capítulos 5 e 6. No capítulo 5 discute-se a geocronologia do Complexo de Jacupiranga e alguns aspectos petrológicos das rochas silicáticas. Este capítulo é apresentado sob a forma de artigo científico, o qual se intitula: "Ar-Ar ages, silicáticas da unidade, envolvendo diferentes magmas parentais (basanítico e nefelinítico).

Os dados de elementos traço em clinopiroxênio, por sua vez, permitiram caracterizar em detalhe o magma basanítico, principalmente no que diz respeito à sua fonte mantélica. Os dados isotópicos foram empregados com o intuito de se investigar a contribuição dos processos de contaminação crustal na evolução da unidade, em particular das rochas com feldspato. As idades obtidas por métodos Ar-Ar e U-Pb, mais precisas que aquelas encontradas na literatura, permitiram melhor definir a duração do magmatismo Jacupiranga.

O capítulo 6 é destinado à caracterização da origem dos carbonatitos e da fonte mantélica dos magmas parentais do complexo. Estas discussões são sustentadas por dados de elementos traço (já apresentadas no capítulo anterior) e por dados de isótopos radiogênicos de Sr-Nd-Pb-Hf em rocha total. Destaca-se a apresentação de dados de Hf, uma vez que nenhuma unidade alcalina brasileira do Cretáceo Inferior foi até então analisada para este par isotópico. Este capítulo é apresentado na forma de um manuscrito, ainda em preparação, intitulado provisoriamente de "New

constraints on the petrogenesis of the Jacupiranga ultramafic-alkaline carbonatite Complex (BR) from Pb and Hf isotope

  

	Os trabalhos citados se encontram referenciados no Capítulo 8.
	Nos Anexos são apresentadas as tabelas com resultados analíticos obtidos por
	microssonda eletrônica em cristais de clinopiroxênio, olivina, anfibólio, micas e feldspato.

data", a ser submetido em breve.

Finalmente, o capítulo 7 proporciona uma discussão integrada dos principais itens explorados nos dois manuscritos científicos, de modo a se apresentar o fechamento da tese.

  Tabela 1 -Padrões analíticos e cristais utilizados nas análises de química mineral.

		M1 são os cátions em coordenação octaédrica regular;
	Elemento Collerson (1974). Cristal Linha de T são os cátions em coordenação tetraédrica. Padrão Composição do padrão Os membros finais foram calculados de acordo com o método de Cawthorn e emissão
	Si Sp1 TAP Ka	Wollastonita	O : 41.32%, Si : 23.9%, Ca : 34.5%
	Ti Sp4 PET Ka 2.4.2 Micas	TiO 2	Ti : 59.95%, O : 40.05%
	Al Sp1 TAP Ka	Al 2 O 3	Al : 52.9242%, O : 47.0758%
	Fe Sp3 LLIF Ka Para o cálculo das fórmulas estruturais das 85 análises pontuais de minerais do Fe 2 O 3 Fe 2 O 3 = Fe : 69.9426%, O : 30.0574%
	Mn Sp3 LLIF Ka K Sp2 LPET Ka grupo das micas (Tabela A2 dos Anexos) foram seguidas as recomendações propostas por Mn Mn : 100.% O : 45.75%, Na : 0.24%, Mg : 0.02%, Al : 8.99%, Si : 30.41%, K : 14.01%, Ca : Ortoclásio 0.02%, Fe : 1.33% Ca Sp4 PET Ka Wollastonita O : 41.32%, Si : 23.9%, Ca : 34.5% Rieder et al. (1999), aprovadas pela Commission on New Minerals and Mineral Names of the
	Sr Sp5 TAP International Mineralogical Association. A fórmula simplificada pode ser escrita como: La SrSO 4 Sr : 47.7026%, S : 17.4543%, O : 34.8431%
	Ba Sp2 LPET La	BaSO 4	Ba : 58.8415%, S : 13.7367%, O : 27.4218%
	Na Sp1 TAP Ka	Albita	Al : 10.08%, O : 48.86%, Na : 8.41%, Mg : 0.09%, Si : 31.81%, K : 0.18%, Ca : 0.45%, Fe : 0.05%
	Mg Sp5 TAP Ka	Forsterita modificada	O : 43.94%, Mg : 29.314%, Si : 19.06%, Fe : 7.3%, Ni : 0.276%, Mn : 0.11%
	Ni Sp3 LLIF Ka	Ni	Ni : 100.%
	Cr Sp2 LPET Ka	Cr 2 O 3	Cr : 68.4195%, O : 31.5805%
	F	Sp5 TAP Ka	CaF 2	Ca : 51.3341%, F : 48.6659%
	Cl Sp2 LPET Ka Cl = O : 37.F representa o número de íons Fe 3+ ; Apatita
		X é o número correto de oxigênios na fórmula mineral;
		T indica o número ideal de cátions por unidade de fórmula e
		S representa o número de cátions observados por X oxigênios calculados
	assumindo que todo o ferro ocorre como Fe 2+ .
		A utilização dessa fórmula requer assumir que o ferro é o único elemento presente
	com valência variável e que o oxigênio é o único ânion. Para a razão Fe 2+ / Fe 3+ , considera-
	se que X = 6 oxigênios e T = 4 cátions.
		O cálculo da fórmula estrutural seguiu as recomendações de Morimoto et al. (1988),
	conforme a fórmula química geral:
				M2M1T 2 O 6 , na qual:
		M2 refere-se aos cátions em coordenação octaédrica, geralmente distorcida;

%, P : 18.%, Ca : 37.%, Cl : 7.% 2.4.1 Clinopiroxênio Ao total, foram analisados 216 pontos em cristais de clinopiroxênio dos diversos litotipos que compõem o Complexo de Jacupiranga (Tabela A1 dos Anexos). Como as análises de microssonda eletrônica não são capazes de determinar separadamente o ferro em seus dois estados de oxidação, foi utilizada a equação de

[START_REF] Droop | A general equation for estimating Fe3+ concentrations in ferromagnesian silicates and oxides from microprobe analyses, using stoichiometric criteria[END_REF] 

para estimar a proporção Fe 2+ / Fe 3+ em piroxênio, definida por: F = 2X(1 -T/S), na qual:

  ). Valores εNd foram calculados a partir da equação ([ 143 Nd/ 144 Nd] amostra / [ 143 Nd/ 144 Nd] CHUR -1) × 10.000 , na qual [ 143 Nd/ 144 Nd] CHUR

  -12 e valores do manto depletado de 147 Sm/ 144 Nd = Toft e[START_REF] Blichert-Toft | The Lu-Hf isotope geochemistry of chondrites and the evolution of the mantle-crust system[END_REF]. O delta ε Hf (Δε Hf ) indica a diferença entre os valores (iniciais ou medidos) das razões isotópicas de Hf e aquela prevista para um basalto oceânico conforme a linha de correlaçãode Vervoort et al. (1999). Esta linha é definida pela equação

	magnético Frantz, variando-se a inclinação lateral da canaleta e a corrente conforme o IIe/MC. As composições isotópicas de U, Th e Pb foram medidas de acordo com os 3 GEOLOGIA REGIONAL
	comportamento de cada amostra. A separação fina foi feita manualmente, com auxílio de procedimentos indicados por Sato et al. (2014).
	pinças e agulhas. 3.1 OCORRÊNCIAS ALCALINAS NO CENTRO-SUDESTE DA PLATAFORMA SUL-
	0,22 e 143 Nd/ 144 Nd = 0,51313. O material selecionado foi então irradiado no Reator Nuclear TRIGA, no Laboratory AMERICANA
	As razões 176 Hf/ 177 Hf foram corrigidas usando a razão 179 Hf/ 177 Hf = 0,7325. Múltiplas of Applied Nuclear Energy, em Pavia (Itália), em dezembro de 2014, por um período de 14
	medidas efetuadas no padrão internacional JMC-475 durante a aquisição dos dados indicam horas com um fluxo de nêutrons de aproximadamente 10 18 cm -2 s -1 . Interferências A partir do Jurássico Superior (Almeida et al., 2000), a região meridional da
	valores de 0,282150 ± 11 (n = 17). Valores εHf foram calculados a partir da equação decorrentes da irradiação para K, Ca e Cl foram corrigidas a partir de dados obtidos Plataforma Sul-Americana foi cenário de um importante processo diastrófico, reflexo da
	([ 176 Hf/ 177 Hf] amostra / [ 176 Hf/ 177 Hf] CHUR -1) × 10.000, na qual anteriormente, pela irradiação e análise de sais puros de KCl e CaF 2 . Os fatores J foram [ 176 Hf/ 177 Hf] CHUR = 0,282772 abertura do Oceano Atlântico Sul. Este evento extensional foi denominado por Almeida
	estimados utilizando-se de duplicatas dos padrões de sanidina de Fish Canyon, com idade de 28,02 Ma, conforme Renne et al. (1998). Embora este valor seja debatido, ele é usado como uma estimativa conservadora. Para estas análises, um J de 0,00541900 ± 9,75 x 10 -6 foi determinado e usado com um erro relativo de aproximadamente 1%. As amostras foram analisadas no laboratório de geocronologia da Universidade de Montpellier, usando-se um aparato multicoletor Thermo-Argus IV com quatro faradays e um sistema de contagem de íon central. Elas foram colocadas em porta-amostras de cobre e aquecidas em etapas, até que a fusão fosse atingida. Para cada etapa, o gás emitido foi purificado ao ser passado por Al-Zr getters. Em seguida, o gás foi introduzido na Argus IV com 1 mn de tempo de equilíbrio antes que ciclos de 10 análises fossem efetuados em todos os cinco picos de argônio, simultaneamente. Regressões lineares conduziram a intensidade do sinal à entrada e o erro (1983) de Reativação Wealdeniana, caracterizada pela reativação de antigos falhamentos, surgimento de blocos de falha, soerguimento de arcos, abatimentos de bacias costeiras e por processos de subsidência na Bacia do Paraná. Episódios magmáticos associados a este estágio de ativação da Plataforma Sul-Americana compreendem tanto manifestações de natureza toleítica quanto alcalina. Na porção sul da plataforma, a atividade basáltica deu origem à Província Magmática do Paraná (PMP -134,7 ± 1 Ma, Thiede e Vasconcelos, 2010), um dos maiores derrames de basalto de platô continental do mundo, acompanhada por manifestações intrusivas de menor magnitude, como soleiras e diques. Sua contraparte alcalina ocorre como corpos isolados, de área restrita (plugs, stocks e diques), com composição variável (saturados ou insaturados em sílica, por vezes com rochas ultrabásicas, carbonatitos e/ou kimberlitos associados) e idade que vão do Permo-Triássico até o Oligoceno, apesar das unidades (Blichert-2.6 GEOCRONOLOGIA associado é incluído no cálculo de idade, do mesmo modo que erros analíticos são brasileiras serem, principalmente, do Cretáceo.
	Na porção centro-sudeste da plataforma, as ocorrências alcalinas estão distribuídas corrigidos pelos valores de branco, calibrados a cada três etapas de aquecimento de uma Para a determinação da duração do magmatismo, foram empregados dois métodos ao longo das margens da Bacia do Paraná (Gomes e Comin-Chiaramonti, 2005), amostra. A discriminação de massa é calculada a partir da análise do ar a cada manhã geocronológicos: Ar-Ar e U-Pb SHRIMP (Microssonda Iônica de Alta Resolução e de Alta principalmente intrudidas no embasamento. Detalhes do controle tectônico atuante na antes do início das análises. Todos os erros são calculados para 2 sigmas. Sensibilidade). Para a análise Ar-Ar, foram selecionadas 5 amostras representativas de distribuição da atividade alcalina na margem leste da sinéclise ainda são controversos,
	diferentes litotipos. Tendo em vista que a biotita/flogopita é uma fase mineral comum à 2.6.2 Datação U-Pb SHRIMP apesar de o magmatismo claramente se concentrar ao redor dos limites da bacia. É notável,
	maioria dos litotipos do complexo, optou-se pela análise desta fase. Datação U-Pb SHRIMP ainda, que estes corpos ígneos estejam alinhados com o Sistema de Cisalhamento
	foi realizada em somente uma amostra de monzonito (JAC25 -a única amostra na qual Cristais de zircão de uma amostra de monzonito foram separados para datação U-Lancinha-Cubatão (Biondi, 2005 -Figura 2), que representa zonas de sutura NE-SW
	zircão foi descrito) com fins comparativos. Pb SHRIMP. A separação e purificação dos cristais de zircão foram realizadas no formadas durante a concatenação do Gondwana e possivelmente reativadas durante a
	Laboratório de Separação do Centro de Pesquisas Geocronológicas (CPGeo) da USP, por abertura do Oceano Atlântico. Não há consenso sobre as relações mecânicas e 2.6.1 Datação Ar-Ar métodos convencionais (moinho de anel, peneiramento, lavagem, líquidos pesados, petrogenéticas entre essas feições tectônicas e a gênese dos complexos alcalinos. No
	Inicialmente, foi realizado um estudo microscópico a respeito da faixa separação magnética e catação). Os grãos selecionados foram montados em um disco de entanto, as intrusões a sul e na região central da costa são frequentemente relacionadas ao
	granulométrica apresentada pelos cristais de biotita em cada amostra selecionada para epoxy e polidos. Foram feitas imagens de catodoluminescência acoplada a MEV desses Arco de Ponta Grossa
	datação. Em seguida, as amostras foram quebradas com uma marreta e cominuídas em um cristais para facilitar a seleção dos pontos a serem analisados.
	pilão. Este material foi peneirado e separado em três frações: 24-60 Ty, 60-100 Ty e > 100 As análises pontuais dos cristais de zircão foram realizadas no Laboratório de
	Ty, sendo escolhida a fração mais adequada conforme a granulometria apresentada pela Geocronologia de Alta Resolução (GEOLAB), do CPGeo -USP e no equipamento SHRIMP
	biotita em cada amostra. As frações selecionadas foram então passadas no separador

ε Hf (OIB) = 1,33ε Nd + 3,19, na qual ε Hf OIB indica o valor do um basalto de ilha oceânica. As idades modelo Hf T DM foram calculadas considerando a constante de decaimento (λ) 1,865 × 10 -11 (Scherer et al. 2001) e valores do manto depletado de 176 Lu/ 177 Hf = 0.0384 e 176 Hf/ 177 Hf = 0,28325 (Blichert-Toft e Albarède, 1997). O padrão NBS981 para as análises de chumbo também foram rotineiramente analisadas e apresentam reprodutibilidade superior a 200 ppm para as três razões de 204 Pb.

As razões iniciais de cada um dos pares isotópicos foram recalculadas conforme as idades obtidas pelo método Ar-Ar.

PROVÍNCIA DO ARCO DE PONTA GROSSA As ocorrências alcalinas localizadas a sul do paralelo 15°S foram agrupadas por Almeida (1983) em 12 províncias alcalinas: Poços de Caldas, Alto Paranaíba, Rio Verde-

  

	estado de São Paulo e dispostas paralelamente ao lineamento Guapiara) e Anitápolis (Santa
	Catarina).
		Apesar dos primeiros sinais de soerguimento remontarem ao Paleozóico (Northfleet
	et al., 1969), foi durante o Triássico-Cretáceo que o Arco de Ponta Grossa desenvolveu sua
	atual feição em abóbada (Almeida, 1983), uma vez que o seu soerguimento foi intensificado
	pela reativação Wealdeniana. Um extenso enxame de diques de composição
	predominantemente basáltica e relacionado ao magmatismo toleítico da Província
	Magmática do Paraná encontra-se encaixado nas falhas e fraturas da região do arco.
		O arcabouço estrutural do Arco de Ponta Grossa é definido por quatro lineamentos
	de direção N40-60W: Guapiara, São Jerônimo-Curiúva, Rio Alonso e Rio Piquiri, que se
	abrem em leque em direção ao interior da bacia (Figura 3). As ocorrências alcalinas
	concentram-se no setor sul dos lineamentos Guapiara e São Jerônimo-Curiúva e suas
	imediações (Gomes et al., 2011). Durante o Mesozóico, o lineamento Guapiara, que delimita
	o limite norte do arco, atuou como uma extensa zona de fissura (ca. 600 km de comprimento
	e 20-60 km de largura) que, segundo modelagens realizadas por Ferreira et al. (1989), foi
	submetida a um afinamento crustal na ordem de 14% (ascensão do manto de 5 km) quando
	da intrusão dos diques básicos. Três unidades cretáceas com direção NW-SE se dispõem
	paralelamente ao lineamento Guapiara (complexos de Jacupiranga, Juquiá e Pariquera-Açu
	-Gomes et al. 2011), sendo o Complexo de Jacupiranga o maior deles, com uma área de
	Figura 2 -Localização das principais unidades de rochas alcalinas conhecidas no Brasil. Adaptado de Biondi, afloramento de 65 km².
	2005.	Trabalhos detalhados abrangendo a Província do Arco de Ponta Grossa (Ruberti et
	al., 2005; Gomes et al. 2011) indicam três diferentes associações de rochas nestas ocorrências alcalinas: máfica-ultramáfica, sienítica e carbonatítica. A primeira inclui uma larga gama de litotipos, em geral com origem cumulática: clinopiroxenitos, jacupiranguitos, dunitos, peridotitos, glimeritos, rochas de filiação gabroide (essexitos, álcali gabros, 3.2 A Iporá, Paraguai Oriental, Mariscala, Piratini, Santa Catarina, Arco de Ponta Grossa, sienogabbros e teralitos) e rochas da série ijolítica (melteigitos, ijolitos e urtitos). A
	Ipanema, Serra do Mar, Velasco e Candelária. Apesar de o critério inicial para esta divisão associação sienítica (que também pode apresentar origem cumulática) abrange sienitos,
	ser a disposição geográfica das unidades, o autor salienta as similaridades petrográficas e nefelina sienitos e sienodioritos, sendo que algumas ocorrências alcalinas (e.g. Tunas,
	geocronológicas apresentadas por cada um dos agrupamentos, justificando a denominação Banhadão) são constituídas predominantemente por estas rochas. Já as rochas de
	de "províncias". O avanço do conhecimento geológico da região, tendo em vista novos associação carbonatítica geralmente ocorrem relacionadas aos litotipos ultramáficos e, em
	dados geológicos, geocronológicos, geofísicos e estruturais, permitiu a Riccomini et al. menor abundância, a rochas fonolíticas. Além destas três associações, também são comuns
	(2005) revisarem esta divisão, que passou a contar com 15 províncias. A partir deste a presença de diques, veios e pequenos plugs de composições diversas.
	trabalho, a Província do Arco de Ponta Grossa passa a englobar somente unidades do
	Cretáceo Inferior, geocronologicamente relacionadas à Província Magmática do Paraná.
	Neste novo agrupamento, Riccomini et al. (2005) inserem na Província do Arco de Ponta
	Grossa as unidades de Ipanema, Salto de Pirapora, Piedade, Itanhaém (aflorantes no

Mapa geológico das cinco intrusões carbonatíticas do Complexo de Jacupiranga e suas respectivas características. Adaptado de Gaspar e Wyllie (1983). Figura 5 -Mapa geológico do Complexo de Jacupiranga que inclui o Gabro Itapuvuçu no Complexo de Jacupiranga. Adaptado de Faleiros e Pavan (2013).

  

	deu notoriedade mundial ao complexo, efetuando um estudo O progressivo avanço da lavra das rochas carbonatíticas tornou necessária a
	em detalhe da unidade como um todo, bem como sugerindo uma origem magmática para os obtenção de detalhes descritivos mais precisos da distribuição do minério. Saito et al. (2004)
	carbonatitos intrusivos nos jacupiranguitos. distinguem doze unidades geológicas compondo o carbonatito, conforme características
	Melcher (1966) descreve a unidade como rochas alcalinas leucocráticas composicionais, texturais, estruturais, de coloração e, principalmente, sua posição
	circundando litotipos básicos/ultrabásicos, que constituem dois corpos principais, um a sul e geográfica. Lee e Ferreira (2007) incluem um novo corpo à unidade, denominado de
	outro a norte. O autor descreve o corpo norte como sendo dunito de origem intrusiva, Mesquita Sampaio, localizado a norte do limite até então considerado para o carbonatito
	parcialmente alterado para serpentina. Em direção às bordas do corpo e, principalmente, (Figura 6). Ele é formado por carbonatitos dolomíticos (de granulação fina ou grossa) e por
	para o sul do complexo, a porcentagem de piroxênio aumenta, e o dunito grada para brechas magmáticas.
	membros da série ijolito-jacupiranguito e piroxenitos. Os jacupiranguitos típicos circundam o
	corpo carbonatítico e consistem quase que exclusivamente de titanoaugita e magnetita, com
	pequenas quantidades de nefelina e biotita.
	Baseados em um extenso mapeamento de detalhe, dados petrográficos e de
	química mineral, Gaspar e Wyllie (1983) dividem o carbonatitos em cinco intrusões (Figura
	4). As intrusões C1, C2 e C3 constituem a porção sul da unidade, enquanto os corpos C4 e
	C5, a porção norte. Os autores utilizam evidências de campo para propor que a sequência
	das intrusões se deu de sul para norte (da intrusão mais antiga para a mais recente,
	respectivamente, C1, C2, C3, C4 e C5). Petrograficamente, as intrusões se diferenciam em
	termos composicionais (porcentagem de calcita, dolomita e não-silicatos), texturais
	(granulação, que varia de fina a grossa) e estruturais (com ausência ou presença de
	bandamentos de diversas espessuras).
	Germann et al. (1987) descrevem ao redor do corpo dunítico uma zona de
	assimilação ou transição com diques peralcalinos. Estas rochas não se enquadrariam como
	fenitos, visto serem caracterizadas por processos metassomáticos de natureza potássica e
	cálcica, enquanto que os fenitos são gerados por processos metassomáticos sódicos. Os 3.4 GEOCRONOLOGIA
	autores também descrevem diques de diversas composições, como essexitos, teralitos,
	sienitos, alcaligranitos e gabros, distribuídos em várias partes do complexo. Amaral et al. (1967) desenvolveram um estudo geocronológico pioneiro englobando
	Em 2013, o Serviço Geológico Brasileiro (CPRM), a partir da integração de dados o Complexo de Jacupiranga, com análises pelo método K-Ar de cinco amostras de
	de mapeamento geológico, levantamento geoquímico e processamento aerogeofísico, diferentes litotipos (i.e. foram analisados cristais de flogopita para a datação do carbonatito,
	elabora a carta geológica e metalogenética/provisional da folha Eldorado Paulista (SG.22-X-de biotita e de feldspato alcalino para o nefelina sienito, rocha total para o jacupiranguito e
	B-VI), em escala 1:100.000, que abrange o Complexo de Jacupiranga (Figura 5 -Faleiros e feldspato para o clinopiroxenito), que apresentam idades entre 191,6 ± 14,6 e 134,1 ± 4,6
	Pavan, 2013). A principal mudança com relação aos mapas anteriores é a inclusão de um Ma (recalculadas conforme a constante de decaimento atualizada por Sonoki e
	corpo satélite adjacente detectado a partir de dados magnéticos e gamaespectométricos. Garda
	Segundo este trabalho, o corpo (denominado de Gabro Itapuvuçu) é formado por biotita-
	olivina gabro com hornblenda, no entanto somente uma amostra foi descrita
	petrograficamente, dada a escassez de afloramentos. Neste trabalho, o termo jacupiranguito
	é evitado, optando-se por termos mais descritivos, como magnetita clinopiroxenito e
	nefelina-flogopita clinopiroxenito, conforme a recomendação da IUGS.

Figura 4 -

Carbonatito dolomítico fino Mesquita Sampaio; DLM_G: Carbonatito dolomítico grosso Mesquita Sampaio. FONTE: Lee e Ferreira (2007).

  As idades até então apresentadas para o complexo têm boa correspondência com aquelas dos derrames básicos da Província Magmática do Paraná-Etendeka (dados geocronológicos de 40 Ar/ 39 Ar de Thiede e Vasconcelos, 2010 apontam uma idade de 134,7 ± 1 Ma para estas rochas).

	3.5 PETROGÊNESE DO COMPLEXO DE JACUPIRANGA
	Melcher (1966) sugere que dois eventos intrusivos tenham ocorrido e dado origem
	às rochas ultramáficas do complexo. Ao norte o corpo dunítico teria se colocado primeiro,
	sendo então englobado por piroxenitos. Em seguida, houve a intrusão do jacupiranguito,
	com formato quase circular, que se diferenciou parcialmente para rochas ijolíticas, gerando
	um corpo de formato concêntrico em forma de meia-lua. As zonas periféricas de composição
	leucocrática descritas pelo autor são definidas como fenitos.
	Germann et al. (1987) afirmam que a evolução do complexo se iniciou com a
	gênese, no manto superior, de um líquido carbonatado rico em sódio. Este magma teria
	intrudido ao longo de fraturas associadas aos estágios iniciais de abertura do Oceano
	Atlântico. Porções deste líquido teriam envolvido blocos de dunito (em estado sólido)

Figura 6-Mapa geológico das diferentes unidades presentes no carbonatito do Complexo de Jacupiranga conforme classificação de Saito et al. (1994): CPS -Carbonatito Sul Periférico; CCS -Carbonatito Central Sul; COX -Carbonatito oxidado; FCS -Áreas com Foscorito Sul; ZFA -Zona de Falha; CBI -Carbonatito Intermediário; CBF -Carbonatito Foliado; CBRcarbonatito branco; CBNcarbonatito norte; FCN -Áreas com foscorito Norte; DOL_N -Carbonatito dolomítico; XEN, XEE, XESáreas com xenólitos; JAC -Jacupiranguito. DLM_F:

  describe five successive intrusive episodes within the carbonatite body (C1 to C5). Based on mineralogical criteria,[START_REF] Hirano | Jacupiranga carbonatites in the São Paulo State, Brazil: their mode of occurrence[END_REF] define four compositional classes for the carbonatite unit: calcite carbonatite (CC), magnetite-rich calcite carbonatite (CCmt), apatite-calcite carbonatite (CCap), and dolomite carbonatite (DC). CC is the main constituent of the southern plug with CCap and CCmt in the marginal zones, the northern body consists of CC with a DC and some CCmt bands. Since this study focuses on a comprehensive view of the Jacupiranga Complex and a thorough discussion about the carbonatites would be out of the scope, we have followed the[START_REF] Hirano | Jacupiranga carbonatites in the São Paulo State, Brazil: their mode of occurrence[END_REF] criteria.

	Samples from northern CC (JAC07), CCMt (JAC08), and DC (JAC09) and southern
	CCAp (JAC04, JAC42) and CCMt (JAC11) were investigated. They are medium-to coarse-
	4.7 FENITES
	Fenitization processes occurred both internally to and around the Jacupiranga
	Complex. Mineralogical changes usually indicate potassic fenitization effects within the
	ijolites and clinopyroxenites (e.g. nepheline replaced by potassic feldspar or cancrinite;

grained rocks with, apart from JAC09, calcite as the main phase. Sample JAC07 is a medium-grained calcite carbonatite with granular texture and only composed of hypidiomorphic calcite. Sample JAC08 is a medium-grained magnetite calcite carbonatite consisting of calcite, magnetite, and apatite with subordinate dolomite, olivine, sulphides, and baddeleyite. Vertical, millimeter-to centimeter-scale compositional banding characterizes this rock and is given by the variation of apatite/magnetite ratios (between 90/10 and 60/40) and by the alignment of apatite and magnetite crystals. Sample JAC09 is a medium-grained dolomite carbonatite with small, elongated apatite as main accessory phase. Apatite forms irregular pockets amongst the dolomite. Subordinate phases are magnetite, calcite, phlogopite, and rare olivine. JAC04 is a medium-grained apatite carbonatite with granular texture and subordinate magnetite, phlogopite, and olivine. Prismatic apatite occurs disseminated through the rock and some crystals are oriented along their c-axes. Sample JAC11 is coarse-grained, consisting of calcite, magnetite, and apatite with subordinated dolomite, olivine, phlogopite, and sulfides. As for JAC08, variations in apatite/magnetite ratios and the preferred alignment of apatite crystals define a compositional banding.

Table 1 .

 1 SHRIMP U-Pb data for monzonite JAC25 from the Jacupiranga Complex.

		U	Th			206 Pb		%comm	Total	err	Total	err		err	Age	err
	Spot	(ppm) (ppm)	237 Th/	238 U	(ppm)	204/206	206	238/206 (%) 207/206 (%)	206/238	(%)	206 Pb/ U	238	2σ
	1.1	1338 1576	1.22	26.7 0.00350	6.56	43.1	1.3 0.1085 3.8 0.0217 1.5	138.1	4.0
	2.1	336	313	0.96	6.1 0.000098	0.18	47.07	1.4 0.0533 1.6 0.0212 1.4	135.3	3.6
	3.1	777	374	0.5	14.1 0.00016	0.29	47.44	1.3 0.0500 1.1 0.0210 1.3	134.1	3.6
	4.1	332	234	0.73	6.6	0.00260	4.83	43.00	1.4 0.0862 3.1 0.0221 1.6	141.0	4.4
	5.1	285	227	0.82	5.2	0.00019	0.36	46.75	1.4 0.0528 2.1 0.0213 1.5	135.9	4.0
	7.1	264	94	0.37	6.6	0.00190	3.43	34.3	1.6 0.0724 3.2 0.0281 1.8	178.9	6.4
	8.1	278	367	1.36	5.3	0.00360	6.75	45.45	1.4 0.1018 1.3 0.0205 1.7	130.8	4.4
	9.1	556	623	1.16	10.1 0.00013	0.24	47.2	1.3 0.0513 1.3 0.0211 1.4	134.8	3.6
	10.1	380	403	1.1	6.9	0.00061	1.13	47.33	1.4 0.0576 1.4 0.0209 1.4	133.3	3.6
	11.1	492	54	0.11	9.3	0.00037	0.68	45.49	1.3 0.0544 1.4 0.0218 1.4	139.2	3.8
	12.1	196	89	0.47	4.7	0.00056	1.03	35.79	1.5 0.0606 2.6 0.0277 1.6	175.8	5.6
	13.1	292	624	2.21	5.5	0.00190	3.57	45.81	1.6 0.0779 1.8	0.021	1.7	134.2	4.6
	14.1	436	177	0.42	8.1	0.00014	0.26	46.32	1.4 0.0535 1.4 0.0215 1.5	137.3	4.0
	15.1* 174	90	0.53	3.5	0.00610	11.25	42.7	1.6 0.1378 11.6 0.0208 3.4	132.4	9.0

Fig. 4. Argon-release age spectra for the Jacupiranga samples.

Table 2 .

 2 Clinopyroxenes are the main mafic phase in the silicate rocks. They are generally pale brown and broadly classified as diopside[START_REF] Morimoto | Nomenclature of pyroxenes[END_REF], with minor augite and hedenbergite (see table A1 of the Supplementary material). For the clinopyroxenites and ijolite, the diopside is characteristically zoned with a narrow range of Wo 50-53 En 37-41 Fs 8-12 and high mg# (83.6-75.8). Whereas ijolite and nepheline-bearing clinopyroxenite are composed of normally zoned diopside, magnetite clinopyroxenite can show reverse zoned diopsides with progressive increase of mg# towards crystal rims. Wehrlites have rather homogeneous diopsides with Wo 49-51 En 43-45 Fs 5-6 and high mg# (90-88). Clinopyroxenes from lamprophyres and feldspar-bearing rocks have a wider compositional range (Wo 40-51 En 32-46 Fs 4-18 and Wo 46-

		Sample	JAC18	JAC22	JAC25	JAC46.1	JAC42
		Rock type	Ne-cpx	MDi	Mon	Lam	CCAp
		Analyzed mineral	Phl	Bt	Bt	Bt	Phl
	Plateau	age	Statistical approach (Ma, ±2σ) N° of steps	WMP 132.1 ± 0.5 131.9 ± 0.5 133.7 ± 0.5 132.3 ± 0.5 132.1 ± 0.6 WMP WMP WMP WMA 23 18 23 15 4
	Isochron	age	(Ma, ±2σ) 40 Ar/ 36 Ar MSWD N° of steps	131.7 ± 0.5 131.4 ± 0.7 133.7 ± 0.5 131.8 ± 0.6 131.9 ± 0.6 350 ± 28 367 ± 63 305 ± 17 339 ± 27 301 ± 24 0.98 1.45 1.42 0.94 0.96 23 18 23 15 4
	Total Fusion Age	(Ma, ±2σ)	132.5 ± 2.0 131.4 ± 0.6 133.7 ± 0.5 132. ± 0.5 132.3 ± 0.6
	Chosen age	(Ma, ±2σ)	131.7 ± 0.5 131.4 ± 0.7 133.7 ± 0.5 131.8 ± 0.6 132.1 ± 0.6

40 

Ar/ 39 Ar ages determined on biotite/phlogopite and glassy matrix separated from Jacupiranga rocks. Abbreviations: Ne-cpxnepheline-bearing clinopyroxenite, MDimeladiorite, Monmonzonite, Lamlamprophyre, CCApapatite-calcite carbonatite. WMPweighed mean plateau, WMAweighed mean age. 50 En 13-34 Fs 3-40 respectively). All analyzed clinopyroxene crystals display calculated pressures <3.9 kbar, with an average error of ±1.7 kbar and no organized distribution regarding rock type (estimated applying the themobarometer of

Nimis and Ulmer, 1998 -Supplementary material, Table 

  7.3 MICASMicas from carbonatites, clinopyroxenites, and ijolites are classified as phlogopite, while those from Heterogeneous Zone are mostly biotite (see table A3 of the Supplementary material). Most carbonatite phlogopites show Al in excess and their tetrahedral sites are occupied by Si and Al only. For the cases in which Si+Al<8,

  TiO 2 (2.27 to 5.29 wt.%) and BaO (1.39 to 3.61 wt.%) and decreasing SiO 2 (37.22 to 35.34 wt.%) and MgO (19.04 to 15.36 wt.

%). Among the silicate rocks, the monzonite biotite yields the highest Fe/Mg ratios (FeO from 20.17 to 21.59 wt.% and MgO from 10.97 to 12.04 wt.%) and low SiO 2 (36.78-38.31 wt.%), while diorite and syenites contain biotite with the highest MgO contents. As seen in the clinopyroxenes, lamprophyre micas do not yield any conspicuous geochemical signature as their composition overlap those of the other micas from the Heterogeneous Zone.

  . Despite having similar Mg/(Mg+Fe 2+ ) ratio to the monzonite edenite, the SiO 2 content of the syenite amphibole is lower(39.95-40.94 wt.%), being therefore classified as Ti-rich Mg-hastingsite. This mineral has higher values of Na 2 O (2.9-3.16 wt.%), TiO 2 (2.87-3.07), and K 2 O (~1.75 wt.%) than the observed in the monzonite (0. 57-1.98 wt.%, <1.38 wt.%, <1.07 wt.%, respectively).

7.5 FELDSPAR

Alkali feldspar in syenites, lamprophyres, and monzonite ranges from Or 24 to Or 93

  La N /Yb N > 9.8). Silicate rocks from the northern part of Jacupiranga have similar La N /Gd N ratios (dunites: 6.22-28.09, Heterogeneous Zone: 6.38-22.2) while the rocks from the Southern part present lower values (2.97-8.67 for silicate rocks and 4.23-7.43 for carbonatites). There is an overall LREE enrichment in the sequence nepheline-bearing clinopyroxenitemelteigiteijolite.

) are similar for all Jacupiranga rocks and show LREE enrichment over HREE without pronounced anomalies (only some diorite and syenite samples display slightly positive Eu anomalies). Rocks from the Heterogeneous Zone and carbonatites show the highest REE contents. Enrichment of LREE with respect to HREE is extremely low for dunites (La N /Yb N : 0.11-0.46) whereas the other rocks show steeper distribution patterns (

Table 3 .

 3 Whole-rock geochemical analyses for the Jacupiranga rocks. Mg# = MgO mol. /(MgO mol. +FeO Tmol. )*100.

	Sample JAC45 JAC50 JAC53 JAC34 JAC73 JAC13 JAC18 JAC82 JAC29.1 JAC88 JAC84 JAC29.2 JAC30
	wt.%	Magnetite clinopyroxenite	Olivine-bearing clinopyroxenite	Nepheline-clinopyroxenite bearing	Melteigite		Ijolite	
	SiO 2	39.70	38.17 40.14	31.96 43.20	44.00 46.37	46.50	40.48	37.22 40.01	38.10	42.20
	TiO 2	3.56	4.04	5.12	7.81	2.83	2.89	2.08	1.42	1.31	2.75	2.04	2.82	1.74
	Al 2 O 3	5.49	5.26	2.26	5.45	5.58	6.07	4.85	7.62	19.37	9.32	17.10	9.45	14.14
	Fe 2 O 3T	15.45	18.66 18.85	23.76	9.58	12.97	7.62	6.62	6.15	14.46	9.17	14.77	8.08
	MnO	0.14	0.14	0.23	0.30	0.11	0.17	0.11	0.09	0.08	0.18	0.11	0.19	0.10
	MgO	12.61	12.03 14.43	8.69	12.81	11.29 12.93	11.75	5.28	8.15	6.32	8.49	7.63
	CaO	20.47	19.41 16.92	17.46 22.37	18.72 22.24	21.06	10.44	18.16 12.75	18.57	15.62
	Na 2 O	0.38	0.30	0.34	0.41	0.47	0.91	0.68	1.92	7.75	3.24	6.73	3.44	4.68
	K 2 O	0.07	0.01	0.01	0.02	0.04	1.13	0.38	0.79	4.76	1.94	3.35	2.13	4.17
	P 2 O 5	< 0.01 < 0.01	0.13	2.15	< 0.01	0.08	0.03	< 0.01	0.92	0.40	0.91	0.44	0.02
	LOI	1.70	1.60	0.90	1.5	2.40	1.20	2.30	1.80	3.20	3.70	1.20	1.20	1.20
	TOTAL	99.60	99.65 99.50	99.53 99.49	99.56 99.62	99.67	99.56	99.57 99.66	99.70	99.61
	Mg#	61.79	56.09 60.27	42.02 72.60	63.30 77.08	77.86	62.98	52.76 57.73	53.25	65.17
	ppm													
	Rb	2.3	0.3	0.4	2.4	0.4	46.5	10.9	14.3	31.9	33.7	57.3	69.5	71.8
	Sr	289.9	254.9 372.1	510.7 359.9	511.0 420.6	598.8	1249.5 1208.3 873.4	777.1	1090.5
	Y	6.9	6.4	14.3	31.2	12.0	12.9	8.3	6.6	9.0	8.5	9.4	8.2	5.7
	Zr	140.6	108.4	92.9	164.2 200.9	119.0 100.9	74.1	65.3	61.8	55.8	53.3	66.5
	Nb	4.7	2.7	8.8	20.6	23.2	9.7	7.3	0.9	4.2	4.1	12.8	1.6	4.9
	Cs	< 0.1	< 0.1	< 0.1	< 0.1	< 0.1	0.6	< 0.1	< 0.1	< 0.1	0.2	0.2	0.2	0.7
	Ba	82	38	33	58	57	262	264	65	149	99	141	215	249
	La	11.3	9.2	25.0	66.2	31.2	20	12.6	8.4	26.8	24.1	45.2	31.4	14.5
	Ce	30.6	24.8	76.6	151.6	79.0	46.6	27.2	21.2	52.3	51.7	87.7	62.0	28.9
	Pr	4.60	3.73	11.51	19.45 10.00	6.22	3.74	3.09	6.51	6.07	10.41	7.18	3.79
	Nd	20.7	16.3	48.7	86.6	39.5	25.3	15.4	14.3	25.8	25.3	39.1	28.3	15.3
	Sm	3.97	3.15	8.65	15.51	6.81	4.96	3.35	2.87	4.56	4.25	5.73	4.34	2.66
	Eu	1.17	0.99	2.10	4.43	1.96	1.49	1.01	0.87	1.37	1.26	1.63	1.27	0.86
	Gd	3.24	2.66	5.97	12.85	5.43	4.32	2.92	2.45	3.80	3.55	4.52	3.60	2.24
	Tb	0.41	0.34	0.76	1.56	0.67	0.59	0.38	0.33	0.45	0.42	0.51	0.42	0.28
	Dy	1.89	1.65	3.58	7.53	3.16	2.94	1.94	1.62	2.22	1.96	2.38	1.81	1.36
	Ho	0.27	0.23	0.54	1.18	0.44	0.48	0.29	0.26	0.34	0.30	0.35	0.29	0.22
	Er	0.61	0.61	1.31	2.69	1.04	1.24	0.74	0.62	0.72	0.66	0.83	0.68	0.53
	Tm	0.08	0.08	0.17	0.33	0.14	0.17	0.10	0.10	0.10	0.09	0.09	0.09	0.07
	Yb	0.50	0.46	0.97	1.83	0.82	0.98	0.64	0.61	0.54	0.54	0.57	0.47	0.40
	Lu	0.08	0.08	0.16	0.26	0.14	0.15	0.10	0.10	0.09	0.09	0.09	0.08	0.06
	Hf	6.0	4.9	4.1	6.6	7.0	4.1	4.1	2.9	2.3	2.3	2.2	1.9	2.2
	Pb	8.1	< 0.1	0.2	0.4	115.9	1.7	0.3	0.2	1.3	1.5	0.2	0.2	0.7
	Th	0.3	< 0.2	< 0.2	1.3	10.8	0.6	0.5	< 0.2	0.4	0.4	3.6	0.5	0.2
	U	< 0.1	< 0.1	< 0.1	< 0.1	0.4	< 0.1	0.2	< 0.1	< 0.1	< 0.1	0.1	< 0.1	< 0.1
	V	257	384	668	868	173	620	216	165	426	433	329	205	305
	Co	70.1	85.1	135.5	50.8	58.1	76.7	54.0	48.1	81.4	86.4	70.9	59.0	69.3
	Ni	181.0	179.5 345.0	12.8	187.0	111.8	88.7	13.1	46.2	49.4	21.2	10.5	33.3
	Cu	468.0	10.4	21.1	22.2 1205.9	61.4	46.2	0.9	111.9	103.8	3.5	4.0	6.9
	Sc	80	71	55	29	68	58	78	66	35	33	18	14	34
	Zn	37	48	50	57	18	52	10	7	93	89	16	10	58
	Ga	14.1	15.0	10.6	21.1	10.8	11.9	9.1	9.2	15.5	14.8	14.4	14.8	13.7

Table 3 .

 3 Continuation. 

	Sample JAC26-2	JAC25	JAC20 JAC63 JAC22 JAC31 JAC32 JAC46.3 JAC61 JAC26.1 JAC46.1 JAC46.2
	wt.%	Olivine monzonite	Monzonite		Diorite		Mela-syenite	Alkali-feldspar syenite	Phonolite	Lamprophyre
	SiO 2	44.20	62.96	49.08	48.24 46.35	52.52	58.05	56.65	59.08	55.52	41.51	44.90
	TiO 2	4.24	1.05	2.60	2.79	2.96	2.20	1.15	1.48	0.82	1.02	4.24	2.93
	Al 2 O 3	9.86	16.15	16.93	14.57 16.53	14.76	18.01	17.10	18.43	20.49	8.87	13.05
	Fe 2 O 3T	15.92	4.39	9.76	11.08 10.91	7.66	4.24	5.11	3.44	4.08	14.62	12.77
	MnO	0.23	0.09	0.20	0.17	0.21	0.17	0.09	0.10	0.08	0.15	0.28	0.20
	MgO	9.57	1.20	3.27	4.70	4.37	4.40	1.21	1.40	0.88	0.79	9.29	7.32
	CaO	11.03	2.49	6.35	7.47	8.32	5.56	2.71	3.16	2.31	2.56	12.12	9.72
	Na 2 O	1.97	4.69	4.51	4.08	3.82	4.25	5.90	4.92	6.02	7.14	2.19	3.97
	K 2 O	1.83	5.50	3.93	3.94	2.60	5.66	6.22	7.26	6.46	6.61	3.08	3.28
	P 2 O 5	0.37	0.26	0.84	0.72	1.22	0.34	0.25	0.25	0.19	0.18	0.68	0.53
	LOI	0.20	0.80	1.80	1.30	1.90	1.50	1.20	1.20	1.20	0.90	2.20	0.70
	TOTAL	99.46	99.60	99.25	99.08 99.22	99.07	99.00	98.62	98.87	99.41	99.16	99.37
	Mg#	54.36	35.13	39.90	45.67 44.25	53.23	36.12	35.19	33.64	27.73	55.73	53.18
	ppm												
	Rb	41.1	153.4	75.0	70.0	55.8	162.6	122.2	135.4	144.5	169.9	107.9	70.8
	Sr	959.9	591.5	1791.1 2311.1 2088.9 2947.0 3391.6 6207.9 3965.5 1428.7	1472.4	1259.9
	Y	17.8	23.6	26.7	18.7	25.2	32.1	21.3	18.3	13.7	17.8	38.1	18.6
	Zr	203.2	287.8	80.7	247.9	91.1	373.2	333.8	300.8	237.3	341.2	384.2	270.0
	Nb	35.1	52.6	53.4	65.6	34.8	143.9	98.8	88.5	66.7	89.0	130.3	61.9
	Cs	0.5	2.9	0.4	0.7	0.4	2.6	2.0	2.1	1.9	1.2	1.5	0.6
	Ba	805	1427	3374	3558	2891	2289	3579	3857	4467	2404	1888	1478
	La	50.6	81.8	74.8	107.2	84.0	218.0	161.7	127.9	126.5	87.7	213.3	76.7
	Ce	105.0	153.4	149.2	206.0 164.1	389.4	268.3	237.3	188.7	134.3	403.1	149.0
	Pr	12.41	15.72	17.06	21.30 19.31	37.79	25.79	22.93	17.68	12.66	42.26	16.82
	Nd	49.9	53.9	63.5	71.3	76.7	121.3	81.0	75.0	55.7	38.6	140.7	61.9
	Sm	8.46	8.13	10.57	9.62	11.62	15.33	10.05	9.71	6.87	5.08	19.14	9.82
	Eu	2.44	2.01	3.82	3.13	3.83	3.97	3.45	3.19	2.98	1.51	4.93	2.80
	Gd	6.87	6.18	9.02	7.02	9.70	10.72	7.09	7.11	4.94	4.05	13.42	7.11
	Tb	0.84	0.90	1.11	0.83	1.17	1.34	0.88	0.83	0.60	0.56	1.65	0.88
	Dy	3.91	4.74	5.64	4.29	5.96	6.57	4.43	4.08	2.93	2.92	7.88	4.20
	Ho	0.66	0.82	0.90	0.67	0.94	1.06	0.72	0.64	0.47	0.58	1.27	0.65
	Er	1.59	2.26	2.24	1.65	2.30	2.66	1.80	1.68	1.24	1.65	3.27	1.64
	Tm	0.21	0.33	0.30	0.25	0.30	0.42	0.25	0.24	0.19	0.26	0.46	0.22
	Yb	1.74	1.98	1.65	1.45	1.29	2.40	1.53	1.38	1.12	1.77	2.91	1.34
	Lu	0.20	0.31	0.24	0.22	0.26	0.36	0.23	0.21	0.16	0.27	0.42	0.20
	Hf	6.1	7.8	2.1	6.7	2.5	9.5	7.6	6.7	5.3	6.5	11.0	6.6
	Pb	1.1	6.1	2.1	2.7	1.6	4.4	5.7	3.6	8.4	18.4	5.0	2.4
	Th	4.4	13.0	1.9	7.1	2.0	22.9	25.5	22.4	18.9	15.8	18.2	7.9
	U	0.9	2.7	0.4	1.1	0.3	3.5	4.5	4.2	3.4	3.1	2.8	1.6
	V	504	64	136	257	195	244	106	170	83	48	487	336
	Co	78.5	49.3	26.6	48.9	30.3	44.5	29.6	48.8	46.6	36.2	53.9	65.7
	Ni	84.5	7.5	2.8	44.4	5.1	108.1	4.6	29.4	4.6	3.3	161.9	92.1
	Cu	33.1	6.8	12.3	83.0	11.4	54.7	14.9	20.7	24.6	2.9	131.9	99.6
	Sc	39	5	13	17	17	11	3	4	3	1	33	28
	Zn	81	48	99	50	98	59	27	39	24	40	81	84
	Ga	15.9	20.4	21.3	17.2	19.9	19.5	19.6	18.4	19.9	22.1	18.0	18.0

Table 3 .

 3 Continuation. 

	Sample	JAC39	JAC04 JAC07 JAC09 JAC08 JAC11 JAC243 JAC220 JAC248
	wt.%	Lamprophyre CCAp	CC	DC	CCMg	Wehrlite	Dunite
	SiO 2	41.25	2.38	< 0.01	0.45	0.65	1.7	35.94	35.63	34.77
	TiO 2	5.18	0.21	< 0.01	0.03	0.02	0.75	0.174	0.182	0.305
	Al 2 O 3	7.41	0.18	< 0.01	0.23	0.09	0.19	0.25	0.22	0.17
	Fe 2 O 3T	15.95	6.73	0.97	6.68	6.77	13.5	15.26	15.16	16.24
	MnO	0.21	0.11	0.15	0.17	0.12	0.22	0.23	0.232	0.255
	MgO	8.23	3.47	4.02	16.98	3.58	5.72	38.51	38.75	39.08
	CaO	12.71	46.7	50.21 31.55	47.88 42.13	1.62	1.61	0.78
	Na 2 O	0.96	0.06	0.03	0.03	0.04	0.04	0.16	< 0.02	< 0.02
	K 2 O	3.12	0.09	< 0.01	0.09	0.02	0.08	0.02	0.01	< 0.01
	P 2 O 5	0.80	9.13	1.27	4.76	5.16	6.61	0.014	0.013	0.01
	LOI	3.20	30.1	42.3	38.3	34.8	28	6.42	6.98	4.54
	TOTAL	99.11	99.19	98.96 99.29	99.10 98.98	98.60	98.79	96.15
	Mg#	50.55	50.53	89.14 83.43	51.17 45.64	83.33	83.51	82.66
	ppm									
	Rb	144.2	2.5	< 0.1	2.0	< 0.1	1.7	0.25	0.18	0.73
	Sr	1394.1	4223.0 6453.6 2861.3 5170.7 4886.7	39.26	52.30	73.83
	Y	22.7	32.3	38.2	15.4	38.1	35.0	0.56	0.49	0.61
	Zr	476.1	267.2	0.5	3.3	331.6 885.8	2.04	1.74	2.89
	Nb	121.4	15.3	2.0	7.1	12.0	72.4	0.36	0.32	1.04
	Cs	1.4	< 0.1	< 0.1	< 0.1	< 0.1	< 0.1	< 0.1	< 0.1	0.06
	Ba	2573	696	1094	295	690	626	28.22	27.26	75.03
	La	158.0	150.3	123.0	38.0	124.4 125.9	1.12	0.83	3.39
	Ce	318.6	302.2	230.4	85.2	251.1 271.2	1.79	1.44	3.57
	Pr	34.41	37.05	26.35 10.72	28.41 32.33	0.21	0.18	0.30
	Nd	117.5	142.8	97.0	46.7	110.8 126.5	0.84	0.73	0.91
	Sm	16.41	23.89	16.52	8.45	19.94 22.42	0.16	0.14	0.13
	Eu	4.27	6.87	5.00	2.63	5.85	6.71	0.05	0.04	0.04
	Gd	11.03	18.81	14.34	7.78	16.74 18.34	0.13	0.12	0.10
	Tb	1.24	2.16	1.83	0.92	2.02	2.14	0.02	0.02	0.02
	Dy	5.45	9.28	8.87	4.17	9.43	9.42	0.10	0.09	0.09
	Ho	0.80	1.23	1.34	0.59	1.35	1.25	0.02	0.02	0.02
	Er	1.74	2.48	3.40	1.35	3.00	2.59	0.05	0.05	0.06
	Tm	0.23	0.28	0.42	0.14	0.37	0.30	0.01	0.01	0.01
	Yb	1.40	1.39	2.38	0.77	1.96	1.67	0.05	0.05	0.08
	Lu	0.19	0.17	0.32	0.09	0.27	0.22	0.01	0.01	0.01
	Hf	11.6	3.6	< 0.1	0.1	4.2	12.0	0.07	0.06	0.09
	Pb	8.3	4.4	10.4	3.2	6.0	4.5	0.49	0.69	0.30
	Th	16.7	3.5	1.1	0.6	1.2	10.5	0.10	0.03	0.40
	U	3.0	4.0	< 0.1	< 0.1	< 0.1	3.0	0.015	0.013	0.02
	V	463	90	0	71	51	208			
	Co	77.6	50.8	30.2	29.6	38.9	46.8			
	Ni	132.3	2.7	11.3	1.2	0.8	14.1			
	Cu	185.8	22.3	16.8	0.2	0.4	32.4			
	Sc	39	23	11	11	17	22			
	Zn	87	40	4	17	17	96			
	Ga	18.6	0.8	0.0	0.0	0.0	1.9			

  8.2 Sr-Nd ISOTOPE COMPOSITIONThe analyzed Jacupiranga samples yield a range of age-corrected 143 Nd/ 144 Nd i and 87

  . While carbonatites and cumulate rocks cluster in rather restricted Sr isotopic intervals, the lithotypes from the Heterogeneous Zone spread across the entire Jacupiranga 87 Sr/ 86 Sr i array, i.e. from 0.70476 to 0.70609. For the cumulate rocks, both clinopyroxenites and dunites yield high and very

Table 4 .

 4 87 Sr/ 86 Sr and 143 Nd/ 144 Nd whole-rock isotopic data determined for the Jacupiranga rocks. Age corrected values were based on the argon ages reported in Table1.

	Lithotype	Magnetite clinopyroxenite	Ne-clinopyroxenite	Ijolite	Wehrlite	Dunite	Lamprophyre
	Sample	JAC45	JAC45B	JAC18	JAC29.2	JAC220	JAC430	JAC248	JAC46.1
	Rb				2.3	2.3	10.9		69.5		0.2	0.2	0.7	107.9
	Sr				289.9	289.9	420.6		777.1	54.6	41.6	75.5	1472.4
	87 Rb/	86 Sr	0.023	0.023	0.075		0.259	0.010	0.017	0.028	0.212
	87 Sr/	86 Sr	0.704771	0.704798	0.704911	0.705519	0.705199	0.705281	0.704977	0.705350
	Error (±2σ)	0.000014	0.000012	0.000012	0.000011	0.000006	0.000007	0.000009	0.000007
	87 Sr/	86 Sr (i)	0.704729	0.704755	0.704771	0.705034	0.705181	0.705249	0.704924	0.704953
	εSr (i)			5.41	5.79	6.01		9.75		11.85	12.81	8.20	8.60
	Sm				3.97	3.97	3.35		4.34		0.14	0.16	0.13	19.14
	Nd				20.7	20.7	15.4		28.3		0.7	0.8	0.9	140.7
	147 Sm/ 144 Nd	0.116	0.116	0.131		0.093	0.113	0.115	0.088	0.082
	143 Nd/	144 Nd	0.512484	0.512493	0.512430	0.512350	0.512413	0.512339	0.512456	0.512306
	Error (±2σ)	0.000003	0.000003	0.000003	0.000005	0.000011	0.000007	0.000017	0.000003
	143 Nd/	144 Nd (i)	0.512385	0.512393	0.512317	0.512270	0.512315	0.512239	0.512380	0.512235
	εNd (i)		-4.6	-4.4	-5.9		-6.8		-6.0	-7.5	-4.7	-7.5
	Table 4. Continuation.						
	Lithotype	Lamprophyre Meladiorite AF Syenite Melasyenite Monzonite	CCMt	CCMt	DC	CC
	Sample	JAC46.2	JAC22	JAC46.3	JAC31	JAC25	JAC08	JAC08B	JAC09	JAC04
	Rb				70.8	55.8	135.4	162.6		153.4	< 0.1	< 0.1	2.0	2.5
	Sr				1259.9	2088.9	6207.9	2947.0	591.5	5170.7	5170.7	2861.3	4223.0
	87 Rb/	86 Sr	0.163	0.077	0.063	0.160		0.750	0.000	0.000	0.002	0.002
	87 Sr/	86 Sr	0.705062	0.705980	0.705782	0.705680	0.707512 0.705605 0.705631 0.705556 0.705116
	Error (±2σ)	0.000006	0.000003	0.000009	0.000008	0.000006 0.000005 0.000002 0.000002 0.000003
	87 Sr/	86 Sr (i)	0.704757	0.705835	0.705663	0.705379	0.706086 0.705605 0.705631 0.705552 0.705113
	εSr (i)			5.82	21.12	18.70	14.66		24.72	17.86	18.23	17.11	10.88
	Sm				9.82	11.62	9.71	15.33			8.13	19.94	19.94	8.45	23.89
	Nd				61.9	76.7	75.0	121.3			53.9	110.8	110.8	46.7	142.8
	147 Sm/ 144 Nd	0.096	0.091	0.078	0.076		0.091	0.109	0.109	0.109	0.101
	143 Nd/	144 Nd	0.512172	0.511945	0.512353	0.512296	0.512089 0.512532 0.512503 0.512590 0.512599
	Error (±2σ)	0.000003	0.000003	0.000005	0.000004	0.000005 0.000006 0.000004 0.000007 0.000004
	143 Nd/	144 Nd (i)	0.512089	0.511867	0.512285	0.512230	0.512009 0.512438 0.512409 0.512496 0.512511
	εNd (i)		-10.4	-14.7	-6.6	-7.6			-11.9	-3.6	-4.1	-2.4	-2.1

Table A2 .

 A2 Chemical analyses oftrace elements (ppm) of cores of clinopyroxene crystals from the Jacupiranga clinopyroxenes TableA3. Summary of chemical analyses of mica crystals from the Jacupiranga Complex TableA3. Summary of chemical analyses of mica crystals from the Jacupiranga Complex

	Sample analysis Supplementary material -Rock/Sample JAC08 Supplementary material -Rock/Sample JAC31 Supplementary material -Sample (ppm) 1 Biotite Phlogopite Biotite Biotite	2	JC127 JAC09 JAC32 3 4 Phlogopite Biotite	5	6	JAC18 JAC39 Phlogopite Biotite	JAC22 JAC46.1 Biotite Biotite	JAC25 JAC46d Biotite Biotite	JAC29 JAC43 Phlogopite Phlogopite
	7. Major and trace element ratios of calculated melts in equilibrium with clinopyroxenite %ferro 0.027 0.021 0.022 0.025 0.052 0.036 0.017 0.035 0.052 0.047 0.067 diopsides favor a garnet peridotite mantle source with variable degrees of CO 2 -rich rim core rim analysis JC105 Li 1.45 1.2 1.53 1.56 1.94 1.72 N. analysis 6 3 8 6 N. analysis 3 3 12 6 core SiO 2 52.45 52.45 46.15 47.82 51.471 49.54 49.28 48.44 49.72 48.41 (ppm) 1 2 3 4 5 6 7 8 9 10 11 P 50.48 44.15 47.47 38.08 61.51 Biotite AM 1σ Max Min AM 1σ Max Min AM 1σ Max Min AM 1σ Max Min Biotite AM 1σ Max Min AM 1σ Max Min AM 1σ Max Min AM 1σ Max Min 50.34 TiO 2 0.71 0.74 2.90 2.63 1.876 1.12 1.79 2.03 1.96 2.30 Li 2.82 2.56 2.76 2.4 3.19 1.9 2.83 2.58 2.03 2.89 2.74 Sc 94.51 75.06 83.99 90.2 95.88 85.09 SiO 2 40.76 1.08 41.90 38.72 38.84 0.67 39.58 38.27 36.44 0.51 37.22 35.70 36.45 0.27 36.92 36.14 37.40 11 3 AM AM SiO 2 36.94 0.20 37.15 36.77 36.46 0.42 36.87 36.03 35.99 0.67 37.72 34.98 36.41 0.44 36.87 35.71 36.56 1σ 1σ 0.92 38.31 34.91 35.96 6 11 Max Min AM Max Min AM 2.36 39.25 34.82 39.78 1σ 0.47 36.50 35.24 Max Min 1σ Max Min 0.48 40.36 38.82 1.48 A l2 O 3 1.72 1.68 5.87 5.60 2.158 3.21 3.90 4.39 3.43 4.04 P 24.68 36.24 27.34 50.63 63.64 45.25 59.98 33.54 38.03 62.41 V 277.49 283.8 262.5 273.7 255.02 301 Al 2 O 3 14.01 0.21 14.43 13.87 16.07 0.54 16.39 15.44 15.47 0.28 15.85 15.01 13.92 0.28 14.32 13.49 12.26 0.24 12.74 12.00 15.79 0.16 16.05 15.61 Al 2 O 3 13.54 0.19 13.76 13.41 13.37 0.21 13.57 13.15 14.00 0.39 14.61 13.38 13.99 0.22 14.21 13.57 14.75 0.42 15.20 14.37 14.37 0.17 14.59 14.01 3.02 FeO 3.15 3.47 6.55 4.78 6.126 7.16 5.41 6.66 7.09 7.37 Sc 97.56 80.78 97.05 87.7 90.99 90.45 87.14 87.17 82.18 81.83 81.58 Co 46.34 46.59 47.21 44.54 46.48 47.96 TiO 2 0.08 0.03 0.11 0.04 0.05 0.02 0.06 0.03 2.77 0.60 4.13 2.27 6.07 0.14 6.28 5.88 3.18 0.78 5.26 2.34 5.07 0.27 5.29 4.65 TiO 2 4.61 0.25 4.81 4.32 4.17 0.13 4.29 4.03 2.81 0.35 3.27 2.07 6.36 0.41 6.77 5.65 5.34 2.67 7.37 2.32 0.66 0.07 0.76 0.54 7.82 MnO 0.04 0.06 0.08 0.07 0.163 0.14 0.06 0.12 0.15 0.14 V 146.09 240.75 187.08 279.91 228.99 219.77 277.17 118.28 264.87 274.11 237.98 Ni 121.81 119.78 120.87 120.58 123.16 127.13 FeO 2.54 1.26 5.07 1.70 2.44 0.01 2.44 2.43 11.68 0.51 12.40 10.78 16.97 0.85 17.53 15.34 21.02 0.67 22.40 20.18 12.27 0.28 12.70 12.00 FeO 16.39 0.44 16.76 15.90 17.45 0.35 17.71 17.05 15.39 0.29 15.77 14.79 14.84 0.67 15.39 13.56 15.61 3.04 18.38 12.36 3.54 0.09 3.67 3.39 0.29 MgO 15.57 15.70 12.96 13.69 15.719 13.60 14.16 13.17 13.13 12.92 Co 46.45 42.94 42.91 44.63 44.26 44.18 44.98 39.95 42.07 42.57 42.76 Cu 0.292 0.258 0.35 0.25 MnO 0.01 0.01 0.03 0.00 0.02 0.01 0.03 0.01 0.13 0.01 0.15 0.11 0.19 0.02 0.23 0.17 0.41 0.05 0.53 0.34 0.09 0.01 0.11 0.08 MnO 0.38 0.01 0.39 0.37 0.49 0.01 0.50 0.48 0.29 0.03 0.35 0.26 0.27 0.01 0.28 0.26 0.18 0.01 0.19 0.16 0.05 0.01 0.07 0.03 13.14 CaO 24.90 24.68 24.61 24.81 23.11 23.97 24.92 24.32 24.40 24.15 Ni 206.38 141.6 149.44 151.44 151.9 150.41 149.63 142.75 129.73 147.9 153.48 Zn 29.1 30.05 31.48 26.48 29.15 31.58 MgO 26.82 0.09 26.89 26.71 25.60 0.27 25.80 25.28 18.25 0.64 19.04 17.16 12.74 0.29 13.06 12.19 11.41 0.61 12.04 9.94 16.08 0.44 16.73 15.37 MgO 13.90 0.59 14.41 13.25 13.36 0.52 13.88 12.84 15.47 0.70 16.85 14.47 14.20 0.73 15.44 13.21 13.63 2.59 16.59 11.72 25.03 0.25 25.27 24.36 22.11 Na 2 O 0.41 0.51 0.36 0.36 0.43 0.61 0.48 0.60 0.66 0.61 Cu 0.29 0.38 0.71 0.33 0.218 0.45 0.82 0.237 1 0.21 0.72 Ga 9.11 11.21 10.67 9.98 9.98 11.9 CaO 0.02 0.01 0.04 0.00 0.01 0.01 0.03 0.00 0.00 0.00 0.00 0.00 0.04 0.05 0.10 0.00 0.03 0.04 0.10 0.00 0.01 0.01 0.03 0.00 CaO 0.01 0.01 0.02 0.00 0.00 0.00 0.00 0.00 0.28 0.15 0.60 0.14 0.01 0.02 0.04 0.00 0.04 0.03 0.08 0.01 0.00 0.01 0.02 0.00 1.10 Cr 2 O 3 0.18 0.02 0.36 0.02 0 0.03 0.03 0.02 0.00 0.01 Zn 28.82 23.84 27.12 27 26.29 24.96 26.04 24.32 22.56 24.23 25 Sr 389.52 468.11 720.61 483.36 512 532.8 BaO 1.68 0.62 2.60 0.93 2.42 0.63 3.13 1.96 1.69 0.23 1.94 1.39 0.56 0.19 0.76 0.21 0.17 0.45 1.49 0.00 2.37 0.65 3.61 1.91 BaO 0.06 0.10 0.17 0.00 0.23 0.14 0.38 0.11 0.23 0.26 0.81 0.01 0.78 0.48 1.62 0.25 1.13 1.00 1.91 0.00 1.04 0.19 1.36 0.72 0.01 Total 100.16 100.37 100.16 99.84 101.067 99.39 100.03 99.75 99.73 99.46 Ga 5.12 5.79 5.59 7.32 6.25 6.3 6.77 3.99 6.75 7.18 6.37 Y 16.78 17.64 23.1 19.15 19.54 22.6 Na 2 O 1.48 0.14 1.64 1.32 0.25 0.03 0.27 0.22 0.14 0.04 0.19 0.09 0.48 0.27 0.89 0.21 0.12 0.04 0.19 0.07 0.06 0.04 0.12 0.02 Na 2 O 0.33 0.05 0.38 0.30 0.36 0.03 0.39 0.33 0.18 0.05 0.29 0.11 0.39 0.04 0.45 0.33 0.39 0.10 0.44 0.27 0.23 0.07 0.43 0.15 100.36 Sr 158.27 245.24 208.33 256.39 255.12 233.18 263.28 149.09 266.33 271.59 243.25 Zr 136.43 162.09 214.84 161.98 173.02 242.01 K 2 O 8.39 0.78 8.99 6.96 9.99 0.39 10.33 9.57 9.94 0.22 10.21 9.57 9.69 0.54 10.16 8.97 9.96 0.35 10.24 9.06 9.88 0.34 10.14 9.27 K 2 O 10.00 0.26 10.29 9.78 9.90 0.14 10.03 9.75 6.97 0.90 8.05 5.45 9.96 0.28 10.18 9.41 9.76 0.41 10.23 9.49 10.48 0.34 10.79 9.70 Formula units Si T 1.933 1.928 1.718 1.769 1.877 1.845 1.816 1.800 1.837 1.801 Y 5.94 15.39 10.32 18.16 17.55 16.24 17.06 6.15 14.47 15.65 13.87 Hf 5.12 5.1 7.5 6.12 6.58 8.08 Total 95.97 0.34 96.32 95.40 95.87 0.17 96.04 95.70 96.94 0.64 97.87 95.94 97.58 1.01 98.88 96.33 97.08 0.76 98.17 95.95 98.03 0.40 98.48 97.34 Total 96.84 0.43 97.18 96.36 96.42 0.51 96.94 95.91 92.01 1.33 95.24 89.93 97.71 0.26 97.96 97.27 97.78 1.20 98.62 96.41 95.41 0.81 96.30 93.26 1.877 Al T 0.067 0.072 0.257 0.231 0.093 0.141 0.169 0.192 0.149 0.177 0.123 Fe 3+ T 0.000 0.000 0.025 0.000 0.031 0.015 0.015 0.008 0.014 0.022 0.000 Al M1 0.008 0.001 0.000 0.013 0 0.000 0.000 0.000 0.000 0.000 0.010 Fe 3+ M1 0.043 0.065 0.135 0.098 0.051 0.135 0.119 0.130 0.102 0.114 Ti M1 0.020 0.021 0.081 0.073 0.051 0.031 0.050 0.057 0.054 0.064 0.041 Cr M1 0.005 0.001 0.011 0.000 0.000 0.001 0.001 0.001 0.000 0.000 Mg M1 0.855 0.860 0.719 0.755 0.854 0.755 0.778 0.729 0.723 0.717 Fe 2+ M1 0.054 0.041 0.044 0.050 0.044 0.073 0.033 0.069 0.103 0.093 Mn M1 0.001 0.002 0.002 0.002 0.000 0.000 0.000 0.009 Ca M2 0.984 0.972 0.981 0.983 0.903 0.956 0.984 0.968 0.966 0.963 Na M2 0.029 0.036 0.026 0.026 0.03 0.044 0.034 0.043 0.047 0.044 %Jad 0.024 0.027 0.020 0.023 0.022 0.033 0.026 0.032 0.035 0.033 %Acmit 0.011 0.018 0.013 0.007 0.015 0.022 0.017 0.022 0.024 0.022 %CaFeTsc 0.011 0.015 0.055 0.043 0.010 0.046 0.043 0.044 0.028 0.035 %CaTiTsc 0.020 0.021 0.081 0.073 0.051 0.031 0.050 0.057 0.054 0.064 %CaTsch 0.003 0.000 0.035 0.036 0.000 0.017 0.018 0.018 0.000 0.003 %woll 0.475 0.468 0.406 0.416 0.420 0.431 0.437 0.425 0.442 0.431 %enst 0.428 0.430 0.360 0.378 0.427 0.377 0.389 0.365 0.362 0.359 0.365 Th 0.057 0.118 0.099 0.111 0.102 0.143 0.132 0.053 0.017 0.169 0.099 0.411 Pb 0.235 0.287 0.187 0.2 0.187 0.198 0.21 0.137 0.14 0.233 0.288 0.000 Lu 0.046 0.094 0.106 0.199 0.19 0.115 0.171 0.083 0.173 0.153 0.164 Th 0.449 0.447 0.31 0.396 0.61 0.265 0.041 Yb 0.258 0.88 0.63 1.22 0.99 1.13 0.86 0.45 0.98 0.77 0.82 Pb 0.226 0.153 0.239 0.199 0.22 0.17 0.020 Tm 0.043 0.147 0.076 0.191 0.218 0.225 0.213 0.082 0.188 0.193 0.183 Lu 0.172 0.214 0.27 0.225 0.236 0.319 0.035 Er 0.632 1.55 0.91 1.79 1.8 1.7 1.45 0.598 1.74 1.6 1.11 Yb 1.1 1.22 1.74 1.03 1.4 1.36 0.063 Ho 0.204 0.545 0.352 0.607 0.657 0.645 0.697 0.283 0.5 0.615 0.593 Tm 0.173 0.192 0.309 0.231 0.23 0.289 End member Dy 1.19 3.11 2.44 4.42 3.87 3.86 4 1.51 3.17 3.78 3.16 Er 1.41 1.73 2.3 1.95 1.81 2.46 0.080 Tb 0.259 0.684 0.467 0.697 0.863 0.71 0.759 0.262 0.7 0.702 0.68 Ho 0.647 0.73 0.83 0.66 0.69 0.89 Cations on the basis of 22 O 0.883 Sm 2.85 7.11 4.87 8.12 7.44 7.38 7.44 2.7 7.01 7.1 6.62 Eu 0.623 1.84 1.08 1.63 1.81 1.59 1.62 0.721 1.75 1.91 1.49 Gd 2.53 5.63 3.78 6.06 6.22 5.76 6.27 2.66 6.11 6.61 5.89 Gd 5.19 6.09 6.65 6.08 5.59 6.65 Tb 0.622 0.659 0.888 0.681 0.67 0.94 Dy 3.3 3.77 4.63 4.23 4.37 4.73 Ba 0.093 0.035 0.144 0.050 0.135 0.036 0.176 0.109 0.097 0.014 0.112 0.079 0.032 0.011 0.044 0.012 0.010 0.027 0.090 0.000 0.136 0.038 0.209 0.109 Na 0.404 0.039 0.449 0.361 0.069 0.008 0.076 0.060 0.039 0.011 0.054 0.024 0.140 0.080 0.260 0.060 0.035 0.011 0.056 0.021 0.016 0.011 0.034 0.007 K 1.504 0.131 1.606 1.263 1.815 0.073 1.868 1.732 1.862 0.030 1.893 1.802 1.835 0.093 1.921 1.716 1.919 0.054 1.969 1.781 1.844 0.054 1.893 1.749 0.005 0.000 Nd 14.09 29.47 19.81 35.83 35.12 31.38 32.81 12.93 31.48 33.88 29.59 Eu 1.61 1.79 2.08 1.57 1.69 2.16 Ca 0.003 0.002 0.006 0.000 0.001 0.002 0.004 0.000 0.000 0.000 0.001 0.000 0.007 0.008 0.016 0.000 0.004 0.006 0.016 0.000 0.002 0.002 0.005 0.000 0.108 Pr 2.76 6.03 4.37 6.88 6.85 6.24 6.56 2.71 6.74 6.89 6.09 Sm 4.98 6.42 7.06 6.22 5.8 7.46 Mg 5.623 0.039 5.670 5.577 5.434 0.025 5.461 5.411 3.995 0.121 4.131 3.789 2.820 0.057 2.902 2.728 2.570 0.126 2.715 2.283 3.510 0.084 3.643 3.389 0.731 Ce 17.01 33.88 26.44 38.69 37.59 35.97 38.59 16.18 38.4 38.47 33.54 Nd 27.19 29.07 35.32 27.71 29.6 36.48 Mn 0.002 0.001 0.004 0.000 0.002 0.002 0.004 0.001 0.017 0.002 0.019 0.014 0.024 0.003 0.030 0.021 0.052 0.007 0.068 0.044 0.011 0.001 0.013 0.010 0.000 Ba 0.183 0.287 0.137 0.307 0.386 0.304 0.69 0.175 0.1 0.426 La 5.67 10.51 8.73 12.12 12.67 11.67 11.68 4.95 11.13 11.89 10.32 Pr 5.45 6.5 8.02 6.31 6.63 7.91 Fe 0.288 0.125 0.538 0.201 0.291 0.001 0.292 0.290 1.426 0.060 1.503 1.312 1.960 0.051 2.009 1.863 2.484 0.064 2.575 2.371 1.481 0.035 1.539 1.440 2+ 0.87 Ce 37.36 43.4 54.9 41.52 42.5 54.45 Ti 0.008 0.003 0.011 0.004 0.005 0.002 0.007 0.003 0.307 0.068 0.460 0.248 0.679 0.020 0.709 0.655 0.362 0.092 0.610 0.267 0.558 0.030 0.589 0.515 0.110 Zr 22.81 48.63 42.12 65.78 59.19 56.2 60 20.73 51.67 60.94 Nb 1.724 1.85 2.16 2.06 2.24 1.89 Si 5.730 0.111 5.829 5.513 5.531 0.070 5.611 5.488 5.352 0.032 5.409 5.317 5.415 0.025 5.437 5.379 5.649 0.105 5.804 5.379 5.264 0.036 5.307 5.213 Si 5.488 0.033 5.523 5.457 5.485 0.038 5.528 5.454 5.530 0.047 5.601 5.456 5.364 0.036 5.419 5.325 5.420 0.306 5.771 5.205 5.675 0.031 5.747 5.624 46.44 Hf 1.02 2.9 2.01 2.92 2.82 2.98 3.67 0.93 2.51 3.52 Sn 1.4 1.88 2.19 1.11 1.56 1.96 Al IV 2.259 0.085 2.422 2.171 2.469 0.070 2.512 2.389 2.639 0.030 2.676 2.591 2.438 0.042 2.514 2.387 2.179 0.044 2.273 2.119 2.714 0.023 2.755 2.693 Al IV 2.371 0.035 2.412 2.350 2.371 0.046 2.424 2.344 2.465 0.052 2.544 2.393 2.429 0.038 2.460 2.354 2.491 0.230 2.658 2.229 2.325 0.031 2.376 2.253 3 Nb 0.272 0.143 0.106 0.134 0.152 0.093 0.159 0.082 0.202 0.199 Sn 0.68 1.06 1.13 0.75 1.31 0.85 0.7 1.07 La 14.52 16.2 23.67 17.85 18.2 20.42 Al 0.063 0.035 0.103 0.000 0.227 0.036 0.262 0.190 0.039 0.035 0.085 0.000 0.000 0.000 0.000 0.000 0.004 0.015 0.049 0.000 0.010 0.024 0.058 0.000 VI 0.159 Ba 0.391 0.466 0.84 0.196 0.87 0.73 Mgl IV 0.011 0.027 0.066 0.000 0.000 0.000 0.000 0.000 0.009 0.022 0.062 0.000 0.147 0.056 0.195 0.049 0.172 0.092 0.392 0.000 0.021 0.018 0.047 0.000 Mgl IV 0.141 0.046 0.191 0.103 0.143 0.083 0.200
	Total mg# cpx	0.998 metasomatism for the basanite parental melts, as seen in other alkaline units related 0.999 0.990 0.999 0.997 0.993 0.995 0.996 0.996 0.992 1.003 0.898 0.890 0.779 0.836 0.820 0.772 0.823 0.779 0.768 0.758 0.750
	mg# liquid to the Ponta Grossa Arch. 0.696 0.678 0.478 P (kbar) -2.200 -2.130 -2.980	0.570 -1.900	0.542 -2.100	0.468 -1.900	0.548 -3.200	0.478 -2.500	0.462 -4.500	0.449 -4.200	0.438 -2.500
	Cations on the basis of 6 O				
	Fe	2+ /Fe	3+ ratio is estimated based on stoichiometric criteria as outlined by Droop (1987)	119 120
	mg# = 100*Mg/(Mg+Fe	2+ ), assuming all Fe as Fe	2+
	P crystallization conditions estimated applying the themobarometer of Nimis and Ulmer, 1998
	mg# liquid calculated considering Kd=0.26			
		Droop, G.T.R., 1987. A general equation for estimating Fe	3+ concentrations in ferromagnesian silicates and oxides
	from microprobe analyses, using stoichiometric criteria. Mineralogical Magazine 51, 431-435.
		Nimis, P., Ulmer, P., 1998. Clinopyroxene geobarometry of magmatic rocks Part 1: An expanded structural
	geobarometer for anhydrous and hydrous, basic and ultrabasic systems. Contributions to Mineralogy and Petrology 133,
	122-135.						

  Supplementary material -TableA5. Calculated mg# and trace element composition (ppm) of liquids in equilibrium with diopside cores from clinopyroxenites of the Jacupiranga Complex.

		Sample								JC105								JC127				
		Kd(s)		2	3		4		5	6	7	8	9	10	11	1	2	3	4	5	6	
	mg# (liq)		51	51		49	50	50	50	53	49	48	49	46	43	43	43	42	42	
	Sc	6	a	13	16		15	15	15	15	15	14	14	14	16	13	14	15	16	14	
	Ti	0.83	b	9474 9309 11402 9991 9664 11507 6609 10899 10831 9444	10445 11165 9455 9684 9372 11524	
	V	0.67	a	359	279	418	342	328	414	177	395	409	355	414	424 392 409 381	449	
	112 0.053 0.515 0.028 0.538 0.483 0.472 0.020 0.488 0.450 0.325 0.039 0.379 0.239 0.705 0.048 0.751 0.621 0.598 0.302 0.829 0.256 0.071 0.007 0.082 0.058 1.896 0.073 1.980 1.849 2.053 0.125 2.183 1.934 1.972 0.054 2.018 1.817 1.622 0.071 1.705 1.497 1.849 0.295 2.088 1.520 0.422 0.014 0.448 0.402 0.048 0.001 0.049 0.047 0.063 0.002 0.064 0.060 0.038 0.003 0.047 0.033 0.033 0.001 0.035 0.032 0.023 0.002 0.024 0.020 0.006 0.001 0.008 0.003 3.079 0.131 3.193 2.937 2.995 0.090 3.073 2.897 3.544 0.171 3.870 3.284 3.118 0.143 3.365 2.938 3.011 0.548 3.636 2.612 5.324 0.020 5.363 5.298 0.001 0.001 0.002 0.000 0.000 0.000 0.000 0.000 0.047 0.025 0.101 0.023 0.002 0.003 0.007 0.000 0.006 0.005 0.012 0.002 0.001 0.001 0.003 0.000 0.004 0.006 0.010 0.000 0.014 0.008 0.023 0.007 0.014 0.015 0.049 0.001 0.045 0.028 0.095 0.014 0.066 0.058 0.111 0.000 0.058 0.011 0.078 0.040 0.094 0.013 0.109 0.086 0.105 0.010 0.116 0.096 0.054 0.014 0.085 0.033 0.112 0.013 0.128 0.093 0.111 0.028 0.128 0.079 0.064 0.020 0.119 0.042 1.895 0.047 1.947 1.855 1.900 0.048 1.938 1.846 1.366 0.171 1.604 1.081 1.872 0.043 1.913 1.789 1.847 0.062 1.919 1.810 1.907 0.052 1.964 1.808 Cations on the basis of 22 O Ti Fe 2+ Mn Mg Ca Ba Na K Cr 3.29 a 35 438 33 293 281 35 715 35 31 45 38 41 61 38 111 37 fO2 (DFMQ) -8.42 -8.65 -8.89 -9.14 -9.39 -9.65 -9.92 -10.2 Co 0.85 a 51 50 53 52 52 53 47 49 50 50 55 55 56 52 55 56 -10.5 Liquid mass 100 98.28 96.52 94.88 93.33 100.14 100.22 100.25 100.27 Ni 3.56 a 40 42 43 43 42 42 40 36 42 43 34 34 34 34 35 36 Liquid mass 100 99.47 97.21 95.09 87.99 79.12 73.42 69.08 Zn 0.24 a 99 113 113 110 104 109 101 94 101 104 121 125 131 110 121 132 65.75 f (%) 0 1.72 3.47 5.12 6.67 26.65 41.37 47.86 f (%) 0.54 2.81 4.96 12.12 21.04 26.79 Ga 0.31 a 19 18 24 20 20 22 13 22 23 21 29 36 34 32 32 38 31.15 liq (%) 100.0 98.3 96.5 94.9 93.3 73.48 58.85 52.39 48.49 liq (%) 100.0 99.5 97.2 95.1 88.0 79.12 73.42 69.08 Sr 0.0963 c 2547 2163 2662 2649 2421 2734 1548 2766 2820 2526 4045 4861 7483 5019 5317 5533 65.75 SiO2 42.41 42.46 42.51 42.56 42.61 45.15 47.39 48.64 49.54 SiO2 41.36 41.39 41.89 42.41 42.95 43.39 43.72 44.16 Y 0.438 c 35 24 41 40 37 39 14 33 36 32 38 40 53 44 45 52 44.62 TiO2 4.33 4.41 4.49 4.57 4.64 3.57 2.67 2.17 1.8 TiO2 1.86 1.85 1.67 1.5 1.13 0.74 0.51 0.35 Zr 0.121 c 402 348 544 489 464 496 171 427 504 384 1128 1340 1776 1339 1430 2000 0.25 Al2O3 9.06 9.22 9.39 9.55 9.71 11.3 13.02 14 14.62 Al2O3 13.22 13.29 13.52 13.74 14.29 15.11 15.76 16.35 Hf 0.245 d 12 8 12 12 12 15 4 10 14 12 21 21 31 25 27 33 16.87 Fe2O3 2.57 2.61 2.65 2.7 2.74 2.28 1.78 1.48 1.29 Cr2O3 2.38 2.4 2.34 2.26 2.15 2.01 1.86 1.72 La 0.0435 c 242 201 279 291 268 269 114 256 273 237 334 372 544 410 418 469 1.58 FeO 11.13 11.09 11.02 10.94 10.85 8.29 6.03 4.83 4.05 FeO 8.28 8.22 7.69 7.13 6.5 5.78 5.15 4.58 Ce 0.0843 c 402 314 459 446 427 458 192 456 456 398 443 515 651 493 504 646 4.07 MnO 0.29 0.28 0.28 0.28 0.28 0.35 0.44 0.5 0.54 MnO 0.2 0.2 0.21 0.21 0.22 0.25 0.27 0.28 Pr 0.124 c 49 35 55 55 50 53 22 54 56 49 44 52 65 51 53 64 0.3 MgO 9.49 8.87 8.23 7.61 7.03 5.29 3.47 2.44 1.76 MgO 6.32 6.13 5.57 5.05 4.27 3.35 2.66 2.12 Nd 0.173 c 170 115 207 203 181 190 75 182 196 171 157 168 204 160 171 211 1.69 CaO 12.38 12.59 12.8 13.01 13.21 12.45 11.1 10.12 9.33 CaO 10.32 10.37 10.6 10.83 10.26 9.12 8.26 7.41 Sm 0.283 c 25 17 29 26 26 26 10 25 25 23 18 23 25 22 20 26 6.65 Na2O 2.24 2.28 2.32 2.36 2.4 3.02 3.75 4.19 4.52 Na2O 7.37 7.41 7.59 7.75 8.37 9.29 10 10.62 Eu 0.312 c 6 3 5 6 5 5 2 6 6 5 5 6 7 5 5 7 11.15 K2O 3.15 3.2 3.26 3.32 3.37 4.28 5.35 6.01 6.49 K2O 3.02 3.03 3.1 3.17 3.43 3.81 4.11 4.37 4.59 P2O5 0.69 0.71 0.72 0.73 0.74 0.95 1.18 1.33 1.43 P2O5 1.15 1.15 1.18 1.21 1.3 1.45 1.56 1.51 1.4 H2O 2.04 2.08 2.12 2.15 2.19 2.78 3.47 3.9 4.21 H2O 2.92 2.93 3 3.07 3.32 3.69 3.98 4.22 4.42 CO2 0.2 0.21 0.21 0.22 0.22 0.28 0.35 0.39 0.42 CO2 0.58 0.57 0.56 0.56 0.54 0.51 0.48 0.45 0.43 Solid phases (in equilibrium with each step) Solid phases (in equilibrium with each step) ol 1.72 1.76 1.65 1.55 ol 0.46 1.12 1.01 0.5 7.6 4.81 3.39 2.48 ol (Fo) 83.14 82.08 80.93 79.69 ol (Fo) 83.81 83.01 82.22 Gd 0.336 c 17 11 18 19 17 19 8 18 20 18 Yb 0.313 c 3 2 4 3 4 3 1 3 2 3 4 4 6 3 4 4 81.3 spinel 6.48 3.62 1.28 0.61 spinel 0.08 1.17 1.15 1.36 1.33 0.94 0.74 0.59 Lu 0.265 c 0 0 1 1 0 1 0 1 1 1 1 1 1 1 1 1
	cpx	La N /Yb N		62	72		51	66	13.51 53	11.1 70	5.21 57	3.31 59	cpx 80	65	68	69	70	89	67	5.29 78	7.6	4.81	3.39	2.48
	mass sol. Ti N /Eu N	1.72	1.76 0.21 0.35	1.65 0.28 0.22 0.25 1.55 19.99	14.72 0.29 0.37 6.49	3.92 0.25	mass sol. 0.23 0.26	0.26	0.54 0.25 0.18 0.25 0.22 2.28 2.15	7.16 0.22	8.93	5.75	4.37	3.37
		La N /Zr N		Summary of accumulation 10 9 8 10	9	9	11	10	9	10	5	5	Summary of accumulation 5 5 5 4	
	ol	Hf N /Y N		1.72 5	5	3.48	4	5.13	4	6.68 5	6	4	5	ol 6	6	8	8	0.46 9	8	1.58 9	2.59 9	3.09
	spinel										6.48	10.1	11.38	spinel				0.08		1.25	2.4	3.76	5.09	6.03	6.77
	cpx										13.51	24.61	29.82	cpx								0.5	8.1	12.91	16.3

a Partition coefficients compiled from Arzamastsev et al. (2009). b Partition coefficients compiled from

  Table 1 and illustrated in Fig.2. Measured isotope ratios range from 17.08 to 18.13, from 15.39 to 15.55, and from 37.67 to 39.52 for 206 Pb/ 204 Pb, 207 Pb/ 204 Pb, and 208 Pb/ 204 Pb, respectively. A well-defined positive correlation is displayed between 208 Pb/ 204 Pb, 207 Pb/ 204 Pb, and 206 Pb/ 204 Pb ratios encompassing all samples.

Table 1 -

 1 Present day Pb isotopic ratios for the Jacupiranga samples. Abbreviations: : CPX, magnetite clinopyroxenite; Ne-IJL, ijolite ; WEH, wehrlite; DUN, dunite; LAM, lamprophyre; MDIO, meladiorite; AFS, alkali feldspar syenite; MSY, melasyenite; MON, monzonite; CCmg, magnetite calcite carbonatite; DC, dolomite cabonatite; CCap, apatite calcite carbonatite.

	Sample	Lithotype	Th ppm	U ppm	206 Pb/	204 Pb (±2σ)	207 Pb/	204 Pb (±2σ)	208 Pb/	204 Pb (±2σ)
	JAC45	CPX	0.3	< 0.1	17.6304 ± 0.0004	15.4513 ± 0.0004	38.0609 ± 0.0011
	JAC29.2	IJL	0.5	< 0.1	17.8780 ± 0.0005	15.4934 ± 0.0005	38.5683 ± 0.0015
	JAC220	WEH	0.03	0.01	17.5975 ± 0.0003	15.4597 ± 0.0003	37.9526 ± 0.0010
	JAC243	DUN	0.10	0.01	17.6001 ± 0.0004	15.4585 ± 0.0005	38.0555 ± 0.0013
	JAC248	DUN	0.40	0.02	17.8341 ± 0.0004	15.4979 ± 0.0005	39.5236 ± 0.0015
	JAC46.1	LAM	18.2	2.8	18.1251 ± 0.0002	15.5463 ± 0.0003	38.9922 ± 0.0009
	JAC46.2	LAM	7.9	1.6	17.3192 ± 0.0002	15.4660 ± 0.0002	37.7026 ± 0.0006
	JAC22	MDIO	2.0	0.3	17.1917 ± 0.0003	15.4681 ± 0.0003	37.6709 ± 0.0012
	JAC46.3	AFS	22.4	4.2	17.8389 ± 0.0003	15.5321 ± 0.0003	38.3691 ± 0.0011
	JAC31	MSY	22.9	3.5	17.8370 ± 0.0004	15.5268 ± 0.0004	38.4558 ± 0.0012
	JAC25	MON	13.0	2.7	17.7285 ± 0.0003	15.5227 ± 0.0003	38.1979 ± 0.0010
	JAC08	CCmg	1.2	< 0.1	17.1148 ± 0.0003	15.3942 ± 0.0002	37.8880 ± 0.0007
	JAC09	DC	0.6	< 0.1	17.0785 ± 0.0003	15.4004 ± 0.0003	37.7101 ± 0.0010
	JAC04	CCap	3.5	4.0	17.4241 ± 0.0002	15.4358 ± 0.0003	37.9761 ± 0.0008
	JAC44	CCap	2.36	0.50	17.1637 ± 0.0003	15.4051 ± 0.0003	37.7545 ± 0.0010

204 

Pb for the analyzed Jacupiranga rocks. Compiled Jacupiranga data are from

  .

	SAMPLE	Lithotype	Lu ppm	Hf ppm	176 Lu/	177 Hf	176 Hf/	177 Hf (±2σ)	176 Hf/	177 Hfi	εHf	ΔεHf	T DM Ga
	JAC45	CPX	0.08	6	0.002	0.282761 ±	0.000005	0.282757	-0.38 4.10	0.71
	JAC45.B	CPX	0.08	6	0.002	0.282768 ±	0.000007	0.282764	-0.13 4.13	0.70
	JAC18	Ne-CPX	0.1	4.1	0.003	0.282708 ±	0.000004	0.282699	-2.27 3.89	0.82
	JAC29.2	IJL	0.08	1.9	0.006	0.282667 ±	0.000003	0.282653	-3.70 3.48	0.93
	JAC243	WEH	0.009 0.072	0.016	0.282566 ±	0.000005	0.282526	-7.28 -0.19	1.65
	JAC248	DUN	0.011 0.090	0.017	0.282814 ±	0.000004	0.282770	1.47 4.71	1.12
	JAC46.1	LAM	0.42	11	0.005	0.282495 ±	0.000004	0.282482	-9.81 -1.64	1.21
	JAC46.2	LAM	0.2	6.6	0.004	0.282432 ±	0.000006	0.282422 -12.01 0.11	1.27
	JAC22	MDIO	0.26	2.5	0.014	0.282306 ±	0.000005	0.282271 -16.48 0.67	2.08
	JAC46.3	AFS	0.21	6.7	0.004	0.282544 ±	0.000007	0.282533	-8.07 -1.16	1.10
	JAC31	MSY	0.36	9.5	0.005	0.282473 ±	0.000005	0.282460 -10.57 -2.27	1.24
	JAC25	MON	0.31	7.8	0.005	0.282320 ±	0.000008	0.282306 -15.98 -1.87	1.49

  comumente considerados para explicar o variável espectro composicional de associações alcalinas. No capítulo 5 este modelo é discutido tanto com base na composição química das rochas do complexo quanto pelo cálculo do líquido em equilíbrio com núcleos

	de minerais. A composição química dos lamprófiros (CaO/Al 2 O 3 : 0,74-1,72) e do líquido
	calculado em equilíbrio com o clinopiroxênio dos clinopiroxenitos (elevadas razões La N /Zr N e
	baixo Ti N /Eu N ) indicam eventos metassomáticos de caráter carbonatítico na fonte mantélica,
	que, por sua vez, levam à formação de veios wehrlíticos no manto peridotítico. Constata-se,
	ainda, diferentes proporções modais cpx/granada na fonte, devido a variações na razão
	Hf/Y. As diferenças composicionais observadas nestes líquidos não podem ser explicadas
	por um modelo simples que considera apenas diferentes taxas de fusão. Ao contrário,
	sugere-se que estas variações derivem da mistura, em diferentes proporções, de líquidos
	gerados a partir da fusão dos veios wehrlíticos (mais enriquecido) e da encaixante
	peridotítica (depletada) e também de variações modais no manto residual. O predomínio do
	componente enriquecido é também indicado pelas baixas razões iniciais de Nd e Hf das
	rochas da unidade, conforme discutido no Capítulo 6.
	Em linhas gerais, os dados isotópicos de Nd-Sr-Pb-Hf indicam uma importante
	contribuição do manto subcontinental litosférico (SCLM) na gênese das rochas do Complexo
	de Jacupiranga, como discutido no Capítulo 6. As amostras analisadas, em sua maioria, se
	sobrepõem ao campo do magmatismo alcalino-carbonatítico do sudeste da Plataforma Sul-
	Americana (Comin-Chiaramonti et al., 2007) e se dispõem próximas ao polo do manto
	enriquecido do tipo 1 (EM1) com alguma contribuição do polo HIMU. Esta assinatura
	pressupõe um manto litosférico subcontinental com características heterogêneas,
	decorrentes dos diferentes graus dos eventos metassomáticos que o afetaram (e.g. Gibson

  Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: WEHwehrlito; CPXmagnetita clinopiroxenito; Nnúcleo do cristal; Bborda do cristal.

	1,000 0,016 0,002 0,949 0,033 1,000 2,4 1,6 0,6 2,0 0,0 JAC45 CPX N 46.54 2,86 5,72 0,01 6,52 0,08 13,10 24,72 0,41 99,96 1,727 0,250 0,022 2,000 0,142 0,080 46.2 Tabela A1 -Amostra Mg M2 Fe 2+ M2 Mn M2 Ca M2 0,980 0,977 0,974 0,975 0,970 0,976 0,968 0,972 Na M2 0,029 0,033 0,041 0,031 0,037 0,030 0,036 0,028 K M2 0,000 M2 subtotal 1,009 1,010 1,015 1,007 1,006 1,006 1,004 1,000 Jd 2,2 2,5 3,1 2,5 2,9 2,3 2,7 2,4 Ae 1,4 1,7 2,0 1,2 1,6 1,5 1,8 0,8 Es 0,7 1,2 1,3 0,3 0,3 0,9 1,0 0,3 CaTiTs 2,0 1,8 1,8 2,1 2,0 3,4 2,0 1,9 CaTs 0,3 0,1 0,0 0,2 0,0 0,1 0,0 0,5 Wo 47,5 47,3 47,1 47,5 47,3 46.6 46.9 47,2 JAC243 JAC45 JAC45 JAC45 JAC45 JAC45 JAC45 JAC45 Litotipo WEH CPX CPX CPX CPX CPX CPX CPX Local N N B N B B N B SiO 2 53,58 46.06 47,82 46.06 47,84 47,35 46.15 48,20 TiO 2 0,65 2,84 2,63 2,95 2,48 2,60 2,90 2,20 Al 2 O 3 1,33 5,79 5,60 5,71 5,16 5,42 5,87 4,91 Cr 2 O 3 0,74 0,02 0,02 0,01 0,03 0,01 0,02 0,02 FeO 3,44 6,59 4,78 6,71 5,60 5,75 6,55 5,24 MnO 0,07 0,09 0,07 0,08 0,07 0,06 0,08 0,05 MgO 15,91 12,82 13,69 13,01 13,79 13,38 12,96 14,05 CaO 24,79 24,61 24,81 24,58 24,89 24,87 24,61 24,99 Na 2 O 0,55 0,42 0,36 0,38 0,35 0,41 0,36 0,40 K 2 O Total 101,07 99,24 99,77 99,47 100,20 99,86 99,49 100,06 Si T 1,939 1,723 1,769 1,720 1,764 1,754 1,722 1,776 Al T 0,057 0,255 0,231 0,251 0,224 0,237 0,258 0,213 Fe 3+ T 0,004 0,022 0,029 0,011 0,009 0,020 0,011 T subtotal 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 Al M1 0,013 Fe 3+ M1 0,042 0,147 0,098 0,142 0,123 0,130 0,141 0,130 Ti M1 0,018 0,080 0,073 0,083 0,069 0,072 0,081 0,061 Cr M1	1,001 0,966 0,033 0,999 2,7 1,3 0,1 2,0 0,0 JAC45 CPX B 47,26 2,72 5,83 0,02 5,57 0,05 13,47 24,76 0,35 100,01 1,748 0,252 2,000 0,002 0,124 0,076	0,982 0,984 0,033 0,000 1,018 2,5 1,7 0,6 2,2 0,0 JAC45 CPX N 46.47 2,90 5,97 0,01 6,56 0,08 12,98 24,71 0,39 100,08 1,723 0,261 0,016 2,000 0,142 0,081	0,983 0,986 0,031 1,017 2,3 1,6 1,1 1,9 0,1 JAC45 CPX B 47,76 2,26 5,13 0,02 5,36 0,05 13,70 25,00 0,38 99,65 1,769 0,224 0,007 2,000 0,131 0,063	0,985 0,984 0,031 1,015 2,4 1,5 0,8 1,9 0,3 JAC45 CPX B 48,17 2,13 4,90 0,01 5,09 0,05 13,82 24,96 0,36 99,50 1,786 0,214 0,000 2,000 0,121 0,059	0,997 0,968 0,035 1,003 2,6 1,7 0,8 1,9 0,0 JAC45 CPX B 47,31 2,58 5,73 0,01 5,23 0,06 13,62 24,84 0,38 99,75 1,751 0,249 2,000 0,001 0,131 0,072	1,000 0,002 0,002 0,965 0,032 1,000 2,4 1,6 0,6 2,0 0,0 JAC45 CPX N 46.72 2,76 5,71 0,01 6,15 0,07 13,13 24,56 0,40 99,52 1,740 0,251 0,010 2,000 0,134 0,077	0,989 0,971 0,039 0,000 1,011 3,0 2,0 1,6 2,2 0,1 JAC45 CPX N 46.43 3,04 6,10 0,01 5,88 0,07 13,30 24,72 0,38 99,93 1,720 0,266 0,013 2,000 0,137 0,085	0,990 0,978 0,032 1,010 2,5 1,4 0,6 1,7 0,0 JAC45 CPX N 47,40 2,66 5,66 0,01 5,82 0,06 13,42 24,80 0,39 100,22 1,750 0,246 0,004 2,000 0,130 0,074

  Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: CPXmagnetita clinopiroxenito; Nnúcleo do cristal; Bborda do cristal.

	Mg M2 Fe 2+ M2 Mn M2 Ca M2 Na M2 K M2 M2 subtotal Litotipo Local SiO 2 TiO 2 Al 2 O 3 Cr 2 O 3 FeO MnO MgO CaO Na 2 O K 2 O Total Si T Al T Fe 3+ T T subtotal Al M1 Fe 3+ M1 Jd Tabela A1 -Amostra JAC45 0,961 0,038 1,000 CPX N 47,63 2,45 5,42 0,01 5,59 0,07 13,60 24,84 0,41 100,02 1,759 0,236 0,005 2,000 0,134 Ti M1	0,983 0,987 0,031 1,017 JAC45 CPX B 46.26 2,96 5,87 0,02 6,47 0,09 12,86 24,86 0,40 99,77 1,722 0,257 0,021 2,000 0,141	0,991 0,983 0,026 1,009 JAC45 CPX B 47,70 2,51 5,49 0,03 5,54 0,07 13,54 24,69 0,39 99,97 1,764 0,236 0,000 2,000 0,003 0,120	0,989 0,983 0,027 1,011 JAC45 CPX B 46.57 3,01 6,14 0,01 6,25 0,07 12,85 24,79 0,43 100,12 1,726 0,268 0,006 2,000 0,136	0,991 0,983 0,025 1,009 JAC45 CPX B 47,42 2,66 5,52 0,02 5,84 0,05 13,46 24,81 0,38 100,17 1,752 0,240 0,007 2,000 0,127	0,983 0,987 0,030 1,017 JAC45 CPX B 47,08 2,81 5,68 0,01 6,26 0,05 13,17 24,66 0,41 100,12 1,743 0,248 0,008 2,000 0,129	0,990 0,984 0,026 1,010 JAC45 CPX B 47,15 2,78 5,56 0,01 6,37 0,09 13,36 24,85 0,40 100,57 1,738 0,242 0,021 2,000 0,136	0,985 0,986 0,028 1,015 JAC45 CPX N 46.90 2,87 5,85 0,02 6,88 0,08 12,99 24,76 0,40 100,75 1,730 0,254 0,016 2,000 0,139	0,987 0,983 0,029 1,013 JAC45 CPX N 46.72 2,88 5,85 0,01 6,81 0,09 12,96 24,67 0,38 100,36 1,730 0,255 0,015 2,000 0,137	0,994 0,981 0,025 1,006 JAC45 CPX N 46.39 2,88 5,69 0,01 6,81 0,09 13,04 24,62 0,39 99,93 1,724 0,249 0,026 2,000 0,142	0,990 0,982 0,028 1,010 JAC45 CPX N 46.88 2,92 5,66 0,01 6,69 0,07 12,92 24,75 0,32 100,21 1,740 0,247 0,013 2,000 0,120	0,981 0,992 0,027 1,019 JAC45 CPX N 46.85 2,91 5,76 0,01 6,03 0,05 13,37 24,87 0,38 100,21 1,732 0,251 0,018 2,000 0,133	0,983 0,991 0,026 1,017 JAC45 CPX N 47,04 2,84 5,99 0,01 5,82 0,06 13,27 24,92 0,38 100,32 1,736 0,260 0,003 2,000 0,133	0,988 0,985 0,027 1,012 JAC45 CPX N 47,16 2,83 5,74 0,02 5,88 0,07 13,51 24,96 0,42 100,58 1,735 0,249 0,016 2,000 0,138	0,991 0,980 0,029 1,009 JAC45 CPX N 47,52 2,60 5,48 0,02 5,38 0,05 13,72 25,09 0,38 100,23 1,751 0,238 0,011 2,000 0,131	0,991 0,981 0,027 1,009 JAC45 CPX N 46.96 2,72 5,41 0,04 5,93 0,06 13,55 24,81 0,36 99,85 1,741 0,236 0,023 2,000 0,133	0,991 0,981 0,028 1,009 JAC45 CPX N 48,38 2,43 4,83 0,06 5,67 0,06 13,75 24,97 0,39 100,54 1,780 0,209 0,011 2,000 0,112

  Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: CPX, magnetita clinopiroxenito; OLCPX, clinopiroxenito com olivina; NECPX, clinopiroxenito com nefelina. Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: NECPX, clinopiroxenito com nefelina; IJO, ijolito; MDIO, meladiorito; N, núcleo do cristal; B, borda do cristal.

	0,002 0,988 0,984 0,028 1,012 JAC18 OLCPX OLCPX NECPX NECPX NECPX NECPX NECPX NECPX NECPX NECPX NECPX NECPX 0,992 0,990 0,993 0,994 0,991 0,993 0,988 0,987 0,986 0,982 0,988 0,978 0,981 0,978 0,979 0,980 0,984 0,985 0,985 0,984 0,991 0,985 0,029 0,028 0,029 0,027 0,028 0,023 0,027 0,027 0,030 0,027 0,026 1,008 1,010 1,007 1,006 1,009 1,007 1,012 1,013 1,014 1,018 1,012 JAC13 JAC13 JAC18 JAC18 JAC18 JAC18 JAC18 JAC18 JAC18 JAC18 JAC18 N N B B N B B N B N B B 49,21 50,41 48,68 48,18 49,28 48,44 48,47 48,78 48,41 48,81 48,97 48,84 2,04 1,32 1,80 2,13 1,79 2,03 1,92 2,01 2,04 2,17 1,72 1,72 4,88 3,28 3,97 4,37 3,90 4,39 4,17 4,32 4,41 4,43 3,82 3,78 0,08 0,10 0,02 0,02 0,03 0,02 0,04 0,03 0,01 0,03 0,03 0,02 7,22 6,54 7,23 6,34 5,41 6,66 6,04 5,79 5,95 5,96 7,29 7,08 0,15 0,12 0,14 0,10 0,06 0,12 0,07 0,07 0,08 0,08 0,14 0,13 12,18 13,31 13,23 13,44 14,16 13,17 13,49 13,79 13,52 13,77 13,02 12,87 23,41 23,71 24,39 24,53 24,92 24,32 24,44 24,56 24,69 24,54 24,47 24,25 0,82 0,62 0,51 0,48 0,48 0,60 0,62 0,40 0,55 0,52 0,56 0,63 99,99 99,41 99,98 99,59 100,03 99,75 99,25 99,76 99,67 100,32 100,00 99,31 1,830 1,878 1,807 1,791 1,816 1,800 1,804 1,807 1,795 1,798 1,819 1,825 0,170 0,122 0,174 0,191 0,169 0,192 0,183 0,189 0,193 0,192 0,167 0,166 0,019 0,017 0,015 0,008 0,013 0,004 0,012 0,010 0,014 0,008 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 0,044 0,022 0,068 0,068 0,129 0,124 0,119 0,130 0,131 0,109 0,131 0,118 0,125 0,123 0,057 0,037 0,050 0,060 0,050 0,057 0,054 0,056 0,057 0,060 0,048 0,048 0,675 0,739 0,732 0,745 0,778 0,729 0,749 0,762 0,747 0,756 0,721 0,717 0,153 0,131 0,077 0,056 0,033 0,069 0,044 0,067 0,042 0,056 0,087 0,090 0,004 0,003 0,002 0,004 0,002 0,002 0,003 0,002 0,004 0,004 1,000 1,000 0,993 0,988 0,982 0,989 0,981 0,996 0,979 0,994 0,986 0,983 0,003 0,005 0,005 0,004 0,933 0,946 0,970 0,977 0,984 0,968 0,975 0,975 0,981 0,969 0,974 0,971 0,059 0,045 0,037 0,035 0,034 0,043 0,044 0,029 0,040 0,037 0,040 0,045 1,000 1,000 1,007 1,012 1,018 1,011 1,019 1,004 1,021 1,006 1,014 1,017 5,5 3,9 2,8 2,6 2,6 3,3 3,3 2,2 3,0 2,8 3,0 3,4 JAC18 JAC29,2 JAC29,2 JAC29,2 JAC29,2 JAC29,2 JAC29,2 JAC29,2 JAC29,2 JAC29,2 JAC29,2 JAC29,2 JAC29,2 JAC29,2 JAC22 0,980 0,994 0,985 0,990 0,992 0,978 0,984 0,982 0,029 0,028 0,031 0,027 1,020 1,006 1,015 1,010 JAC45 JAC45 JAC45 JAC45 CPX CPX CPX CPX N N N N 46.96 48,38 47,75 47,44 2,72 2,43 2,57 2,69 5,41 4,83 5,15 5,54 0,04 0,06 0,05 0,07 5,93 5,67 5,66 5,59 0,06 0,06 0,07 0,06 13,55 13,75 13,52 13,50 24,81 24,97 24,85 24,72 0,36 0,39 0,39 0,39 99,85 100,54 100,02 99,99 1,741 1,780 1,766 1,755 0,236 0,209 0,224 0,242 0,023 0,011 0,009 0,003 2,000 2,000 2,000 2,000 0,133 0,112 0,117 0,121 0,076 0,067 0,072 0,075 0,749 0,754 0,746 0,744 0,028 0,052 0,048 0,048 0,002 0,002 0,002 0,002 0,988 0,988 0,987 0,992 0,985 0,984 0,985 0,980 0,026 0,028 0,028 0,028 1,012 1,012 1,013 1,008 2,0 2,1 2,1 2,1 JAC22 NECPX NECPX 0,987 0,983 0,030 1,013 JAC45 CPX N 47,52 2,60 5,48 0,02 5,38 0,05 13,72 25,09 0,38 100,23 1,751 0,238 0,011 2,000 0,131 0,072 0,753 0,024 0,002 0,982 0,991 0,027 1,018 2,0 Tabela A1 -Amostra M1 subtotal Mg M2 Fe 2+ M2 Mn M2 Ca M2 Na M2 K M2 M2 subtotal Litotipo Local SiO 2 TiO 2 Al 2 O 3 Cr 2 O 3 FeO MnO MgO CaO Na 2 O K 2 O Total Si T Al T Fe 3+ T T subtotal Al M1 Fe 3+ M1 Ti M1 Mg M1 Fe 2+ M1 Mn M1 M1 subtotal Mg M2 Fe 2+ M2 Mn M2 Ca M2 Na M2 K M2 M2 subtotal Jd JAC18 Litotipo IJO IJO IJO IJO IJO IJO IJO IJO IJO IJO IJO IJO IJO MDIO MDIO Local N B N B B N N N B N B N B B B N N SiO 2 48,50 49,08 48,88 49,81 49,83 49,72 49,11 48,80 48,41 49,15 48,78 49,52 49,16 49,36 48,83 52,06 52,00 TiO 2 2,07 1,77 2,02 1,56 1,88 1,96 2,02 2,19 2,30 1,99 2,11 1,91 2,09 2,17 2,05 0,46 0,58 Al 2 O 3 4,40 3,68 4,36 3,47 3,05 3,43 3,37 3,59 4,04 3,30 3,87 3,18 3,71 3,93 3,80 1,67 1,95 Cr 2 O 3 0,05 0,03 0,03 0,02 0,00 0,02 0,01 0,00 0,02 0,01 0,01 0,02 0,01 0,01 0,01 0,00 0,00 FeO 5,85 7,24 5,90 7,05 7,04 7,09 7,07 7,19 7,37 7,14 7,21 7,06 7,27 7,28 7,20 8,26 8,34 MnO 0,10 0,15 0,10 0,15 0,11 0,15 0,12 0,11 0,14 0,14 0,12 0,13 0,14 0,12 0,13 0,49 0,52 MgO 13,69 13,00 13,72 13,28 13,37 13,13 13,27 13,00 12,92 13,23 12,96 13,23 13,00 13,07 12,88 13,34 13,20 CaO 24,54 24,40 24,65 24,28 24,45 24,40 24,03 24,42 24,15 24,40 24,48 24,54 24,14 24,47 24,04 23,36 23,33 Na 2 O 0,49 0,58 0,56 0,57 0,57 0,66 0,54 0,54 0,61 0,58 0,51 0,52 0,54 0,60 0,58 0,77 0,76 K 2 O Total 99,67 99,91 100,21 100,18 100,31 100,55 99,53 99,83 99,97 99,93 100,05 100,11 100,06 101,02 99,51 100,42 100,69 Si T 1,798 1,825 1,801 1,845 1,845 1,836 1,832 1,818 1,801 1,827 1,813 1,838 1,827 1,817 1,824 1,926 1,921 Al T 0,192 0,161 0,190 0,152 0,133 0,149 0,148 0,158 0,177 0,145 0,170 0,139 0,163 0,171 0,167 0,073 0,079 Fe 3+ T 0,010 0,014 0,009 0,004 0,022 0,014 0,019 0,024 0,022 0,029 0,017 0,022 0,010 0,013 0,008 0,001 0,000 T subtotal 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 Al M1 0,000 0,000 0,005 Fe 3+ M1 0,121 0,118 0,126 0,108 0,091 0,101 0,093 0,098 0,114 0,103 0,106 0,092 0,094 0,106 0,102 0,103 0,096 Ti M1 0,058 0,049 0,056 0,044 0,052 0,054 0,057 0,061 0,064 0,056 0,059 0,053 0,059 0,060 0,058 0,013 0,016 Jd Tabela A1 -Amostra Cr M1 0,001 0,001 0,002 0,001 0,002 0,002 0,003 0,001 0,001 0,001 0,001 0,001 0,001 0,000 0,001 0,001 0,001 Cr M1
	Ae	1,3	1,3	1,4	1,4	1,4	0,7	1,1	1,8	1,7	1,7	2,2	2,2	1,4	2,0	1,9	2,0	2,3
	Es	5,2	5,3	4,2	4,5	4,7	2,7	2,3	4,6	4,5	4,2	4,3	4,3	4,0	4,5	4,0	4,2	3,9
	CaTiTs	7,2	7,6	6,7	7,2	7,5	5,7	3,7	5,0	6,0	5,0	5,7	5,4	5,6	5,7	6,0	4,8	4,8
	CaTs	3,3	2,9	2,4	2,7	3,2	2,0	1,3	1,8	1,9	1,8	1,8	1,5	2,4	2,0	1,7	1,5	1,2
	Wo	41,7	41,4	42,6	42,1	41,3	41,4	43,7	42,8	42,7	43,7	42,5	43,1	42,8	42,9	42,5	43,4	43,6
	En	37,7	37,4	37,7	37,3	37,2	33,8	37,0	36,6	37,2	38,9	36,5	37,4	38,1	37,4	37,8	36,0	35,9
	Fs	1,2	1,4	2,6	2,4	2,4	7,8	6,8	3,8	2,8	1,7	3,4	2,2	3,3	2,1	2,8	4,4	4,5
	mg#	82,0	80,3	81,2	81,0	81,1	75,1	78,4	76,5	79,1	82,3	77,9	79,9	80,9	80,2	80,5	76,1	76,4

  Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: MDIO, meladiorito; MSY, melassienito; N, núcleo do cristal; B, borda do cristal.

	Tabela A1 -Amostra JAC22	JAC22	JAC22	JAC22	JAC22	JAC22	JAC22	JAC22	JAC22	JAC31	JAC31	JAC31	JAC31	JAC31	JAC31	JAC31	JAC31
	Litotipo	MDIO	MDIO	MDIO	MDIO	MDIO	MDIO	MDIO	MDIO	MDIO	MSY	MSY	MSY	MSY	MSY	MSY	MSY	MSY
	Local	N	N	N	N	N	N	N	N	N	N	N	N	N	N	N	N	N
	SiO 2	51,84	51,64	51,41	52,02	51,87	52,27	51,78	51,40	51,05	50,93	50,30	50,87	50,73	50,83	51,03	50,66	51,65
	TiO 2	0,57	0,66	0,71	0,80	0,68	0,63	0,65	0,63	0,71	0,78	1,79	1,15	1,12	1,04	0,87	1,19	1,03
	Al 2 O 3	1,72	1,86	2,63	2,19	1,96	1,71	1,70	1,89	2,47	2,45	2,86	2,74	2,67	2,49	2,30	2,54	2,46
	Cr 2 O 3	0,00	0,01	0,00	0,01	0,00	0,01	0,00	0,01									0,30
	FeO	8,52	8,71	8,84	7,88	8,84	8,74	8,23	8,37	8,86	10,95	7,57	9,13	9,34	10,58	10,15	10,48	7,14
	MnO	0,50	0,55	0,48	0,53	0,54	0,53	0,56	0,51	0,52	0,47	0,31	0,37	0,38	0,41	0,42	0,41	0,31
	MgO	13,59	13,43	13,10	14,23	13,27	13,69	13,78	13,16	12,72	10,74	12,73	11,96	11,72	11,01	11,38	11,03	13,43
	CaO	22,81	22,83	22,94	22,62	22,73	22,88	22,09	22,58	22,70	21,99	23,41	22,63	22,65	22,28	22,38	22,29	21,60
	Na 2 O	0,69	0,62	0,61	0,60	0,67	0,64	0,58	0,58	0,70	1,68	1,07	1,35	1,32	1,57	1,47	1,75	1,51
	K 2 O											0,01	0,01				0,02
	Total	100,23	100,31	100,73	100,88	100,56	101,10	99,37	99,12	99,72	99,98	100,04	100,20	99,94	100,21	99,99	100,37	99,43
	Si T	1,922	1,916	1,902	1,911	1,921	1,924	1,936	1,931	1,909	1,908	1,867	1,891	1,894	1,899	1,907	1,887	1,915
	Al T	0,075	0,081	0,098	0,089	0,079	0,074	0,064	0,069	0,091	0,092	0,125	0,109	0,106	0,101	0,093	0,111	0,085
	Fe	3+ T	0,003	0,002	0,000	0,000	0,000	0,002				0,000	0,008					0,002
	T subtotal	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000
	Al M1																
		2+ M1	0,051	0,093	0,047	0,106	0,105	0,103	0,108	0,101	0,093	0,090	0,101	0,105	0,122	0,105	0,114	0,148	0,156
	Mn M1	0,003	0,005	0,003	0,005	0,004	0,005	0,004	0,004	0,004	0,004	0,004	0,004	0,004	0,004	0,004	
	M1 subtotal	0,990	0,986	0,986	0,996	0,990	0,987	1,000	0,986	0,993	0,987	0,988	0,987	1,000	0,992	0,996	1,000	1,000
	Mg M2																
	Fe	2+ M2																0,003	0,006
	Mn M2																0,015	0,016
	Ca M2	0,975	0,972	0,974	0,963	0,970	0,966	0,961	0,975	0,962	0,972	0,975	0,976	0,961	0,965	0,962	0,926	0,923
	Na M2	0,035	0,042	0,040	0,041	0,041	0,047	0,039	0,039	0,044	0,041	0,037	0,037	0,039	0,043	0,042	0,055	0,054
	K M2																
	M2 subtotal	1,010	1,014	1,014	1,004	1,010	1,013	1,000	1,014	1,007	1,013	1,012	1,013	1,000	1,008	1,004	1,000	1,000
	Jd		2,7	3,1	3,0	3,0	3,0	3,5	2,9	2,9	3,3	3,1	2,8	2,8	2,9	3,2	3,1	4,1	4,2
	Ae	1,8	2,1	2,0	2,0	2,0	2,3	2,0	2,0	2,2	2,1	1,8	1,9	1,9	2,1	2,1	2,8	2,4
	Es	4,3	3,8	4,3	3,4	2,5	2,7	2,7	3,0	3,5	3,1	3,4	2,7	2,8	3,2	3,0	2,4	2,4
	CaTiTs	5,8	4,9	5,6	4,4	5,2	5,4	5,7	6,1	6,4	5,6	5,9	5,3	5,9	6,0	5,8	1,3	1,6
	CaTs	2,1	1,0	1,9	1,2	0,0	0,0	0,0	0,0	0,2	0,0	0,7	0,0	0,3	0,4	0,5	0,0	0,0
	Wo	42,7	43,7	42,8	43,7	44,6	44,2	43,8	44,2	43,0	44,3	43,7	44,8	43,6	43,5	43,5	44,5	44,2
	En	37,8	36,0	37,7	36,7	36,9	36,2	36,9	36,1	35,8	36,7	35,9	36,6	36,0	35,8	35,9	36,8	36,3
	Fs		2,5	4,7	2,3	5,3	5,2	5,2	5,4	5,1	4,7	4,5	5,1	5,3	6,1	5,3	5,7	7,6	8,1
	mg#	80,7	76,2	80,6	77,0	77,2	76,8	77,0	76,3	75,8	76,8	76,2	77,0	76,1	76,2	76,1	74,2	73,8

  Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: MSY, melassienito; AFS, álcali-feldspato sienito; LAMP, lamprófiro; N, núcleo do cristal; B, borda do cristal.

	Tabela A1 -Amostra JAC31	JAC31	JAC31	JAC31	JAC31	JAC31	32	32	32	32	32	32	32	32	32	JAC46.1 JAC46.1
	Litotipo	MSY	MSY	MSY	MSY	MSY	MSY	AFS	AFS	AFS	AFS	AFS	AFS	AFS	AFS	AFS	LAMP	LAMP
	Local	B	N	N	B	B	N	B	B	B	B	B	B	N	N	N	N	N
	SiO 2	50,78	51,37	51,39	50,77	52,21	51,87	52,63	48,73	51,04	51,04	48,43	49,89	51,41	51,44	50,92	52,26	49,95
	TiO 2	1,05	0,64	0,60	1,13	0,55	0,75	0,31	0,56	0,96	0,70	0,67	0,50	1,04	1,10	1,08	0,59	1,50
	Al 2 O 3	2,55	1,96	2,17	2,62	1,45	2,05	1,80	3,11	2,37	2,36	2,96	2,35	2,35	2,73	2,74	2,08	3,41
	Cr 2 O 3	0,03	0,04	0,15	0,03	0,00	0,01	0,00	0,01	0,01	0,00	0,01	0,01				0,02	0,03
	FeO	10,00	10,57	11,57	8,29	7,86	8,31	9,07	16,88	8,89	10,36	18,01	16,83	7,96	7,83	8,83	9,27	8,81
	MnO	0,41	0,46	0,44	0,37	0,53	0,45	0,45	0,69	0,46	0,48	0,75	0,70	0,46	0,40	0,44	0,34	0,30
	MgO	11,10	11,11	10,35	12,17	12,97	12,30	11,89	6,72	11,91	10,93	6,00	6,96	12,52	12,78	11,88	12,11	12,02
	CaO	22,10	21,83	21,16	22,80	23,00	22,69	22,37	20,53	22,66	22,30	19,65	20,66	22,64	23,15	22,87	22,57	22,64
	Na 2 O	1,52	1,72	1,98	1,25	1,15	1,30	1,34	2,21	1,32	1,52	2,53	1,99	1,29	1,05	1,30	1,35	1,38
	K 2 O																	
	Total	99,53	99,70	99,80	99,43	99,73	99,74	99,86	99,46	99,61	99,70	99,01	99,88	99,66	100,49	100,06	100,59	100,05
	Si T	1,908	1,925	1,930	1,898	1,942	1,932	1,963	1,877	1,909	1,916	1,880	1,918	1,914	1,901	1,895	1,934	1,857
	Al T	0,092	0,075	0,070	0,102	0,058	0,068	0,037	0,123	0,091	0,084	0,120	0,082	0,086	0,099	0,105	0,066	0,143
	Fe	3+ T																	
	T subtotal	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000
	Al M1	0,020	0,012	0,026	0,014	0,005	0,022	0,042	0,018	0,013	0,020	0,016	0,024	0,017	0,019	0,016	0,025	0,006
	Fe	3+ M1	0,123	0,150	0,149	0,114	0,106	0,097	0,075	0,237	0,120	0,135	0,255	0,178	0,103	0,094	0,122	0,104	0,152
	Ti M1																	
												1,004	1,009	0,999	1,001	1,005	1,003	1,017	1,000
	Jd		3,7	3,3	3,7	3,4	3,8	3,4	3,4	3,5	4,2	9,5	5,8	7,6	7,5	8,7	8,2	9,5	8,7
	Ae	2,5	2,2	1,4	1,8	2,1	2,3	1,6	1,4	1,6	5,3	3,9	4,3	4,2	5,2	4,9	6,4	4,3
	Es	2,3	2,3	2,9	2,2	2,0	2,1	1,4	1,6	2,6	2,4	1,6	2,2	2,2	2,1	2,2	2,3	0,9
	CaTiTs	1,6	1,8	2,0	2,2	1,9	1,7	1,8	1,8	2,0	2,2	5,0	3,2	3,1	2,9	2,4	3,3	2,9
	CaTs	0,0	0,0	1,6	0,4	0,0	0,0	0,0	0,3	0,9	0,0	0,0	0,0	0,0	0,0	0,0	0,0	0,0
	Wo	43,4	43,3	42,2	42,1	43,1	43,2	42,7	43,6	42,7	41,8	43,2	42,3	42,6	42,1	42,5	41,6	41,0
	En	37,6	37,2	36,1	39,0	36,6	37,5	38,4	36,8	35,4	30,0	35,2	33,1	32,6	30,7	31,7	30,6	37,1
	Fs		8,3	8,9	9,4	8,1	9,6	9,0	9,9	10,1	9,6	9,4	5,8	7,6	8,2	9,2	8,7	7,6	5,8
	mg#	74,0	73,3	72,5	76,3	72,8	73,6	74,9	73,7	71,9	63,6	75,0	70,0	69,1	65,0	66,6	65,2	77,0

  Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: LAMP, lamprófiro; N, núcleo do cristal; B, borda do cristal.

	Tabela A1 -Amostra JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1
	Litotipo	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP
	Local	N	N	N	N	N	N	N	N	N	B	B	N	B	N	B	N	N
	SiO 2	50,91	49,99	51,85	49,59	51,25	50,60	52,09	51,44	51,30	51,20	50,16	51,69	51,14	51,40	48,47	52,00	51,93
	TiO 2	1,21	1,59	1,05	1,79	0,95	1,26	1,32	1,37	1,38	1,19	1,61	1,40	1,42	1,43	2,16	1,31	1,23
	Al 2 O 3	2,67	3,42	2,12	4,05	2,31	2,92	2,23	2,20	2,59	2,71	3,53	2,25	2,38	2,27	4,70	2,07	2,12
	Cr 2 O 3	0,04	0,05	0,01	0,01	0,02	0,02	0,55	0,56	0,53	0,02	0,03	0,56	0,02	0,57	0,02	0,61	0,60
	FeO	8,26	8,32	8,43	8,35	8,75	8,19	5,21	5,88	5,51	7,85	8,39	5,40	6,91	4,57	9,06	4,34	5,26
	MnO	0,35	0,27	0,33	0,34	0,41	0,30	0,22	0,20	0,19	0,31	0,34	0,20	0,26	0,11	0,28	0,11	0,21
	MgO	12,81	12,64	12,80	12,44	12,70	12,67	14,46	14,37	14,22	12,85	12,44	14,55	13,81	15,36	11,51	15,55	14,46
	CaO	22,73	23,12	22,61	22,51	22,80	22,50	23,78	23,75	23,79	22,90	22,82	24,00	22,91	24,15	22,41	24,14	23,65
	Na 2 O	0,95	1,04	1,18	1,13	0,93	1,06	0,77	0,78	0,80	1,03	1,03	0,72	0,89	0,26	1,24	0,36	0,76
	K 2 O																	
	Total	99,93	100,44	100,39	100,19	100,11	99,52	100,62	100,56	100,32	100,07	100,35	100,76	99,75	100,12	99,85	100,49	100,22
	Si T	1,894	1,850	1,919	1,840	1,907	1,889	1,908	1,888	1,885	1,899	1,860	1,892	1,896	1,890	1,811	1,902	1,910
	Al T	0,106	0,149	0,081	0,160	0,093	0,111	0,092	0,095	0,112	0,101	0,140	0,097	0,104	0,098	0,189	0,089	0,090
	Fe	3+ T		0,001						0,017	0,002			0,011		0,012		0,009	
	T subtotal	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000
	Al M1	0,011	0,000	0,011	0,017	0,008	0,017	0,004	0,000		0,018	0,015		0,000		0,018		0,002
	Fe	3+ M1	0,095	0,134	0,096	0,124	0,099	0,099	0,054	0,076	0,080	0,091	0,109	0,066	0,088	0,033	0,139	0,034	0,058
	Ti M1	0,034	0,044	0,029	0,050	0,026	0,035	0,036	0,038	0,038	0,033	0,045	0,039	0,040	0,039	0,061	0,036	0,034
	Cr M1	0,001	0,002	0,000	0,000	0,000	0,000	0,016	0,016	0,015	0,001	0,001	0,016	0,001	0,017	0,000	0,018	0,017
	Mg M1	0,711	0,697	0,706	0,688	0,704	0,705	0,790	0,786	0,779	0,711	0,688	0,794	0,763	0,842	0,641	0,848	0,793
	Fe	2+ M1	0,149	0,122	0,157	0,121	0,162	0,142	0,100	0,083	0,087	0,147	0,143	0,086	0,109	0,069	0,140	0,065	0,097
	Mn M1																	
	M1 subtotal	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000
	Mg M2																	
	Fe	2+ M2	0,014	0,000	0,008	0,014	0,011	0,014	0,006	0,004	0,000	0,006	0,008	0,002	0,018	0,027	0,004	0,025	0,007
	Mn M2	0,011	0,009	0,010	0,011	0,013	0,010	0,007	0,006	0,006	0,010	0,011	0,006	0,008	0,003	0,009	0,004	0,006
	Ca M2	0,906	0,917	0,897	0,895	0,909	0,900	0,933	0,934	0,937	0,910	0,907	0,941	0,910	0,951	0,897	0,946	0,932
	Na M2	0,069	0,075	0,085	0,081	0,067	0,077	0,054	0,056	0,057	0,074	0,074	0,051	0,064	0,019	0,090	0,026	0,054
	K M2																	
	M2 subtotal	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000
	Jd		5,4	5,6	6,7	6,5	5,2	6,2	4,2	4,2	4,3	6,0	5,9	3,8	4,8	1,4	7,2	1,9	4,1
	Ae	2,9	3,7	3,7	3,2	3,0	3,0	2,5	2,8	2,9	2,8	3,0	2,5	3,2	0,9	3,6	1,3	2,6
	Es	1,9	3,0	1,1	3,0	2,0	2,0	0,2	1,0	1,1	1,7	2,5	0,8	1,2	0,7	3,4	0,4	0,2
	CaTiTs	3,4	4,4	2,9	5,0	2,6	3,5	3,6	3,8	3,8	3,3	4,5	3,9	4,0	3,9	6,1	3,6	
	Wo	42,2	42,0	40,9	43,2	44,4	43,6	43,8	39,3	43,1	42,7	37,9	40,5	43,0	43,3	43,0	43,1	41,5
	En	31,1	31,1	29,0	33,9	35,9	34,2	33,1	19,3	33,2	30,6	17,4	19,9	34,8	35,2	33,0	33,4	33,3
	Fs		9,6	9,1	10,7	7,2	6,9	8,1	10,4	15,4	7,9	9,5	16,5	18,2	7,2	7,4	7,6	9,2	6,1
	mg#	66,4	65,2	61,5	72,4	74,6	72,5	70,0	41,5	70,5	65,3	37,3	42,4	73,7	74,4	70,6	70,0	70,8

  Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: LAMP, lamprófiro; N, núcleo do cristal; B, borda do cristal.

	Tabela A1 -Amostra JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC39	JAC39	JAC39	JAC39	JAC39
	Litotipo	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP
	Local	N	N	B	N	N	N	N	B	N	N	N	B	N	N	N	N	N
	SiO 2	52,03	51,50	49,51	50,87	50,44	51,38	52,32	49,56	50,34	50,07	49,39	49,61	49,20	51,63	52,73	54,40	50,58
	TiO 2	1,18	0,97	1,86	1,13	1,26	1,09	1,06	1,69	1,48	1,65	1,89	1,73	0,76	0,19	0,16	0,14	1,86
	Al 2 O 3	2,10	2,40	4,06	2,78	2,87	2,35	1,77	3,82	3,02	3,55	2,97	3,76	4,22	1,45	1,16	0,36	2,57
	Cr 2 O 3	0,67	0,03	0,02	0,02			0,73	0,03					0,02	0,02	0,08	0,10	0,36
	FeO	4,96	8,57	8,29	8,69	8,54	8,60	4,18	8,47	7,82	8,01	8,77	8,38	10,21	10,50	9,64	6,53	4,89
	MnO	0,18	0,41	0,27	0,37	0,31	0,34	0,08	0,30	0,29	0,26	0,28	0,27	0,30	0,34	0,28	0,24	0,06
	MgO	14,71	12,70	12,29	12,49	12,60	12,81	16,08	12,22	13,14	12,71	12,82	12,34	10,94	11,65	12,03	14,66	14,93
	CaO	24,07	22,51	22,59	22,65	22,82	22,43	23,80	22,63	22,11	22,78	22,56	22,60	23,42	22,95	22,89	22,72	24,71
	Na 2 O	0,66	1,15	1,10	1,02	1,03	1,13	0,34	1,01	1,10	0,86	1,00	1,01	0,77	1,10	1,22	1,06	0,19
	K 2 O									0,02								
	Total	100,57	100,24	99,99	100,03	99,86	100,13	100,36	99,72	99,33	99,90	99,67	99,71	99,84	99,82	100,19	100,21	100,16
	Si T	1,905	1,910	1,842	1,894	1,879	1,907	1,912	1,851	1,878	1,864	1,845	1,852	1,849	1,936	1,964	1,998	1,864
	Al T	0,091	0,090	0,158	0,106	0,121	0,093	0,076	0,149	0,122	0,136	0,131	0,148	0,151	0,064	0,036	0,002	0,112
	Fe	3+ T	0,004						0,012				0,025						0,024
	T subtotal	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000	2,000
	Al M1		0,014	0,020	0,015	0,005	0,010	0,000	0,019	0,011	0,020		0,017	0,036	0,000	0,014	0,013	
	Fe	3+ M1	0,057	0,104	0,113	0,101	0,120	0,104	0,033	0,108	0,110	0,085	0,122	0,107	0,127	0,132	0,099	0,054	0,036
	Ti M1	0,033	0,027	0,052	0,032	0,035	0,030	0,029	0,048	0,041	0,046	0,053	0,049	0,022	0,005	0,004	0,004	0,051
	Cr M1	0,020	0,001	0,001	0,001			0,021	0,001					0,000	0,001	0,002	0,003	0,011
	Mg M1	0,803	0,702	0,682	0,693	0,700	0,709	0,876	0,680	0,731	0,705	0,714	0,687	0,613	0,652	0,668	0,803	0,820
	Fe	2+ M1	0,088	0,151	0,133	0,158	0,140	0,147	0,042	0,145	0,108	0,143	0,111	0,140	0,193	0,197	0,201	0,123	0,082
	Mn M1													0,009	0,011	0,009		
	M1 subtotal	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,001	0,998	0,998	1,000	1,000
	Mg M2																	
	Fe	2+ M2	0,003	0,010	0,012	0,011	0,005	0,016	0,042	0,012	0,027	0,021	0,016	0,014				0,023	0,009
	Mn M2	0,006	0,013	0,008	0,012	0,010	0,011	0,002	0,009	0,009	0,008	0,009	0,009				0,007	0,002
	Ca M2	0,945	0,894	0,900	0,903	0,911	0,892	0,932	0,905	0,884	0,909	0,903	0,904	0,943	0,922	0,913	0,894	0,976
	Na M2	0,047	0,083	0,079	0,074	0,074	0,081	0,024	0,073	0,080	0,062	0,073	0,073	0,056	0,080	0,088	0,076	0,013
	K M2						0,000			0,001	0,000							
	M2 subtotal	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	1,000	0,999	1,002	1,002	1,000	1,000
	Jd		3,5	6,6	6,4	5,9	5,7	6,4	1,8	6,0	6,3	5,2	5,5	5,9	5,1	6,0	7,0	6,0	1,0
	Ae	2,3	3,4	3,0	2,9	3,5	3,6	1,2	2,7	3,5	2,1	3,6	2,8	1,0	4,0	3,7	3,3	0,7
	Es	0,5	1,8	2,7	2,1	2,5	1,6	0,4	2,7	2,0	2,2	2,5	2,6	5,4	2,6	1,3	0,0	1,1
	CaTiTs	3,3	2,7	5,2	3,2	3,5	3,0	2,9	4,8	4,1	4,6	5,3	4,9					
	Wo	42,7	42,1	42,8	40,7	43,1	42,2	44,8	44,3	44,4	43,0	41,9	44,7	42,9	45,2	40,1	45,3	44,8
	En	35,5	34,9	35,3	34,4	35,2	35,3	39,5	39,3	39,0	35,5	34,4	39,7	38,2	42,1	32,1	42,4	39,6
	Fs		8,1	6,1	8,3	6,7	8,6	7,8	5,3	4,4	4,4	7,7	7,6	4,4	6,3	4,8	7,2	4,5	5,2
	mg#	73,4	73,0	73,0	72,6	72,1	73,4	83,2	81,3	82,1	74,5	72,6	82,8	78,1	85,7	69,4	86,5	83,1

  Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: LAMP, lamprófiro; N, núcleo do cristal; B, borda do cristal. Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: LAMP, lamprófiro; N, núcleo do cristal; B, borda do cristal. Composição química (porcentagem peso) de cristais de clinopiroxênio das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 6 oxigênios e 4 cátions. Abreviações: LAMP, lamprófiro; N, núcleo do cristal; B, borda do cristal.

	Wo SiO 2 TiO 2 Al 2 O 3 Cr 2 O 3 FeO MnO MgO CaO Na 2 O K 2 O Total Si T Al T Fe 3+ T T subtotal Al M1 Fe 3+ M1 Ti M1 Cr M1 Mg M1 Fe 2+ M1 Mn M1 M1 subtotal Mg M2 Fe 2+ M2 Mn M2 Ca M2 Na M2 K M2 M2 subtotal Jd Ae Es CaTiTs CaTs Wo Tabela A1 -Amostra JAC39 45,3 52,07 1,29 1,48 0,44 4,40 0,07 15,46 24,53 0,17 99,91 1,919 0,064 0,017 2,000 0,009 0,036 0,013 0,850 0,093 1,000 0,017 0,002 0,969 0,012 1,000 0,9 0,7 0,0 3,6 0,0 46.6 Litotipo LAMP Local N SiO 2 50,38 TiO 2 0,50 Al 2 O 3 3,24 Cr 2 O 3 0,06 FeO 9,60 MnO 0,30 MgO 11,51 CaO 23,21 Na 2 O 0,78 K 2 O Total 99,57 Si T 1,893 Al T 0,107 Fe 3+ T T subtotal 2,000 Al M1 0,037 Fe 3+ M1 0,097 Ti M1 0,014 Cr M1 0,002 Mg M1 0,645 Fe 2+ M1 0,205 Mn M1 0,010 M1 subtotal 1,008 Mg M2 Fe 2+ M2 Mn M2 Ca M2 0,935 Na M2 0,057 K M2 M2 subtotal 0,992 Jd 5,2 Ae 1,0 Es 3,8 CaTiTs 1,4 CaTs 2,9 Wo 42,7 Tabela A1 -Amostra JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 42,5 41,1 42,5 42,5 42,3 44,9 41,6 41,1 42,0 41,3 41,5 41,2 44,5 44,8 44,5 45,7 B N N N 49,74 51,39 51,89 51,98 51,97 52,36 51,55 43,00 51,82 50,77 50,65 50,70 50,55 54,75 54,83 55,08 1,74 1,67 0,19 1,35 0,23 0,14 0,42 2,85 1,22 1,93 1,82 1,76 1,78 0,31 0,27 0,17 3,24 1,98 1,52 1,57 1,30 1,17 2,15 10,18 1,57 1,78 1,81 2,07 1,80 0,09 0,02 0,05 0,00 0,20 0,30 0,45 0,02 0,00 0,15 0,05 0,06 0,06 0,07 0,53 0,06 0,03 0,02 0,02 7,97 5,05 9,88 4,69 10,54 9,93 8,59 13,66 5,07 5,32 5,46 4,88 5,25 3,24 3,19 2,50 0,21 0,10 0,28 0,11 0,33 0,32 0,30 0,27 0,09 0,10 0,09 0,06 0,08 0,12 0,10 0,10 12,62 15,21 11,91 15,00 11,60 11,88 12,32 13,17 14,79 14,85 15,06 14,58 14,40 16,29 16,46 16,91 23,99 24,73 23,01 24,74 23,02 22,66 23,74 13,25 24,51 24,17 24,42 24,48 24,24 24,99 25,04 25,53 0,55 0,23 1,17 0,29 1,15 1,33 0,79 0,66 0,27 0,22 0,23 0,28 0,28 0,54 0,43 0,29 100,07 100,55 100,15 100,17 100,16 99,80 100,01 97,08 99,39 99,20 99,60 99,33 98,45 100,36 100,34 100,66 1,854 1,885 1,935 1,914 1,943 1,958 1,922 1,655 1,923 1,892 1,877 1,886 1,898 1,990 1,994 1,992 0,142 0,085 0,065 0,068 0,057 0,042 0,078 0,345 0,069 0,078 0,079 0,091 0,080 0,004 0,001 0,002 0,004 0,030 0,018 0,008 0,030 0,044 0,023 0,022 0,006 0,006 0,006 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 0,002 0,000 0,009 0,016 0,117 0,088 0,033 0,127 0,018 0,126 0,121 0,091 0,111 0,026 0,014 0,036 0,020 0,019 0,030 0,021 0,019 0,049 0,046 0,005 0,037 0,007 0,004 0,012 0,082 0,034 0,054 0,051 0,049 0,050 0,008 0,007 0,005 0,000 0,006 0,009 0,013 0,000 0,000 0,004 0,001 0,002 0,002 0,002 0,015 0,002 0,001 0,000 0,000 0,701 0,832 0,662 0,823 0,647 0,662 0,685 0,688 0,818 0,825 0,832 0,809 0,806 0,883 0,892 0,912 0,157 0,083 0,181 0,108 0,204 0,189 0,177 0,120 0,105 0,079 0,107 0,122 0,062 0,070 0,051 0,007 0,009 0,011 0,010 0,010 0,004 0,003 0,003 1,002 1,000 0,996 1,000 0,994 0,996 0,995 1,000 1,000 1,000 1,000 1,000 1,000 0,988 0,994 0,990 0,000 0,067 0,000 0,009 0,000 0,328 0,003 0,016 0,011 0,002 0,002 0,000 0,003 0,003 0,009 0,003 0,003 0,003 0,002 0,003 0,958 0,972 0,920 0,976 0,922 0,908 0,948 0,546 0,975 0,965 0,970 0,976 0,975 0,973 0,975 0,989 0,040 0,016 0,085 0,020 0,083 0,096 0,057 0,049 0,019 0,016 0,017 0,020 0,020 0,038 0,030 0,021 0,998 1,000 1,004 1,000 1,006 1,004 1,005 1,000 1,000 1,000 1,000 1,000 1,000 1,012 1,006 1,010 3,0 1,2 6,4 1,5 6,2 7,4 4,7 4,9 1,4 1,2 1,3 1,5 1,5 2,9 2,3 1,5 2,0 0,8 4,1 1,1 4,1 4,3 2,0 0,0 1,0 0,8 0,8 1,0 1,0 2,1 1,7 1,1 2,4 0,9 2,3 0,0 2,2 1,7 2,5 5,6 0,3 0,0 1,0 0,0 0,0 0,0 0,0 0,0 4,9 4,6 0,5 3,7 0,7 0,4 1,2 8,2 3,4 5,4 5,1 4,9 5,0 0,8 0,7 0,5 0,2 0,0 0,0 0,0 0,0 0,0 0,7 12,4 0,0 0,0 0,0 0,0 0,0 0,0 0,0 0,0 44,2 45,9 44,6 46.9 44,7 44,3 45,2 14,2 46.9 45,5 45,5 46.3 46.2 48,2 48,4 49,2 JAC39 JAC39 JAC39 JAC39 JAC39 JAC39 JAC39 JAC39 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP N N N N N N B B N B B N N B N N 51,47 51,89 52,01 50,83 50,86 49,92 50,21 49,79 46.90 52,05 51,76 51,48 48,06 48,42 48,60 50,71 0,24 0,21 0,25 0,41 1,70 2,08 1,93 2,11 2,43 0,95 1,05 0,98 2,09 1,98 1,98 1,47 2,04 1,29 1,56 3,12 1,88 3,12 2,61 2,73 7,33 2,85 3,28 3,13 6,25 6,32 6,10 3,11 0,02 0,02 0,03 0,00 0,15 0,23 0,19 0,31 0,01 0,49 0,19 0,18 0,36 0,11 0,39 0,13 9,89 10,84 9,47 9,76 5,10 5,42 5,35 6,30 8,22 6,67 7,87 8,03 7,70 8,17 7,81 6,79 0,32 0,32 0,28 0,30 0,09 0,11 0,09 0,15 0,16 0,13 0,19 0,21 0,17 0,17 0,14 0,13 11,74 11,14 12,10 11,69 15,19 14,12 14,68 14,07 11,69 16,23 15,69 16,19 13,36 13,30 13,50 14,67 23,09 21,92 22,47 23,27 24,37 24,74 24,66 24,00 21,67 20,63 20,21 19,51 21,01 21,33 21,13 22,98 0,97 1,54 1,27 0,87 0,24 0,30 0,24 0,38 1,43 0,37 0,46 0,46 0,71 0,72 0,66 0,29 99,79 99,17 99,45 100,25 99,58 100,04 99,95 99,85 99,85 100,37 100,71 100,16 99,72 100,50 100,32 100,27 1,929 1,958 1,948 1,895 1,883 1,847 1,856 1,849 1,740 1,906 1,895 1,891 1,785 1,785 1,795 1,871 0,071 0,042 0,052 0,105 0,082 0,136 0,114 0,120 0,260 0,094 0,105 0,109 0,215 0,215 0,205 0,129 0,035 0,016 0,030 0,031 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 0,019 0,016 0,017 0,032 0,060 0,030 0,037 0,027 0,059 0,060 0,061 0,006 0,109 0,126 0,113 0,113 0,034 0,052 0,049 0,051 0,167 0,023 0,037 0,056 0,079 0,093 0,069 0,058 0,007 0,006 0,007 0,011 0,047 0,058 0,054 0,059 0,068 0,026 0,029 0,027 0,059 0,055 0,055 0,041 0,001 0,000 0,001 0,000 0,004 0,007 0,005 0,009 0,000 0,014 0,005 0,005 0,011 0,003 0,011 0,004 0,656 0,627 0,675 0,650 0,838 0,779 0,809 0,779 0,647 0,886 0,857 0,885 0,740 0,731 0,744 0,807 0,201 0,216 0,184 0,192 0,076 0,100 0,084 0,102 0,058 0,020 0,035 0,053 0,058 0,060 0,084 0,010 0,010 0,009 0,009 0,003 1,002 1,001 1,006 1,007 1,000 0,998 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 0,001 0,013 0,000 0,003 0,012 0,031 0,161 0,169 0,191 0,107 0,101 0,112 0,067 0,003 0,000 0,003 0,005 0,005 0,004 0,006 0,007 0,005 0,005 0,004 0,004 0,927 0,886 0,902 0,930 0,967 0,981 0,977 0,955 0,861 0,810 0,793 0,768 0,836 0,843 0,836 0,909 0,071 0,113 0,093 0,063 0,017 0,021 0,017 0,028 0,103 0,026 0,033 0,033 0,051 0,051 0,047 0,021 0,998 0,999 0,994 0,993 1,000 1,002 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 5,8 8,8 7,4 5,5 1,3 1,6 1,3 2,1 9,3 2,6 3,3 3,2 5,1 5,1 4,7 1,7 2,6 4,8 3,8 1,6 0,8 1,1 0,9 1,4 2,1 0,0 0,0 0,3 0,0 0,0 0,0 0,7 2,8 1,5 1,9 4,1 0,9 1,5 1,6 1,2 6,2 1,2 1,8 2,5 4,0 4,6 3,5 2,2 0,7 0,6 0,7 1,1 4,7 5,8 5,4 5,9 6,8 2,6 2,9 2,7 5,9 5,5 5,5 4,1 0,3 0,0 0,0 2,5 0,0 0,0 0,0 0,0 4,1 2,2 2,5 2,4 5,3 5,7 5,4 1,7 44,4 43,3 43,8 42,6 45,5 45,4 45,4 44,2 34,5 37,5 36,0 34,6 34,3 34,2 34,6 41,5 Litotipo LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP Local N N B B N B N N B B N N B N N B N SiO 2 45,22 51,07 46.41 49,36 51,63 55,13 47,03 50,71 51,31 50,64 48,95 49,12 46.19 46.61 48,99 47,40 47,17 TiO 2 3,70 1,29 2,83 1,46 1,01 0,04 2,55 1,49 1,22 1,55 1,79 1,74 3,07 2,59 1,68 2,43 2,64 Al 2 O 3 7,41 3,43 7,01 5,51 3,79 0,33 7,34 3,66 2,96 3,40 6,28 5,51 6,71 7,35 5,60 6,11 6,87 Cr 2 O 3 0,02 0,10 0,01 0,46 0,24 0,03 0,26 0,10 0,14 0,05 0,55 0,50 0,06 0,32 0,33 0,01 0,23 FeO 9,27 7,26 8,78 7,17 6,81 5,34 8,62 7,35 6,87 7,25 7,38 6,94 8,24 8,60 7,80 8,64 8,62 MnO 0,15 0,16 0,15 0,15 0,17 0,25 0,15 0,19 0,17 0,14 0,15 0,15 0,15 0,15 0,16 0,12 0,13 MgO 11,41 14,54 11,95 14,30 15,62 15,61 12,94 14,55 15,03 14,46 14,55 14,21 12,13 12,88 13,92 12,60 12,82 CaO 22,62 21,75 22,45 21,11 20,92 23,35 21,01 22,04 22,42 22,35 20,79 21,42 22,75 21,00 21,20 22,55 21,04 Na 2 O 0,57 0,78 0,66 0,60 0,67 0,97 0,61 0,61 0,33 0,32 0,64 0,62 0,61 0,60 0,64 0,42 0,61 K 2 O Total 100,37 100,39 100,23 100,13 100,86 101,06 100,51 100,70 100,45 100,17 101,07 100,20 99,91 100,09 100,32 100,27 100,12 Si T 1,691 1,876 1,728 1,819 1,879 1,997 1,740 1,861 1,886 1,873 1,786 1,809 1,725 1,732 1,806 1,763 1,754 Al T 0,309 0,124 0,272 0,181 0,121 0,003 0,260 0,139 0,114 0,127 0,214 0,191 0,275 0,268 0,194 0,237 0,246 Fe 3+ T T subtotal 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 Al M1 0,017 0,025 0,036 0,058 0,042 0,011 0,060 0,019 0,015 0,021 0,056 0,049 0,020 0,054 0,049 0,031 0,055 Fe 3+ M1 0,125 0,081 0,124 0,072 0,063 0,057 0,094 0,079 0,051 0,042 0,089 0,075 0,124 0,103 0,087 0,099 0,081 Ti M1 0,104 0,036 0,079 0,040 0,028 0,001 0,071 0,041 0,034 0,043 0,049 0,048 0,086 0,072 0,047 0,068 0,074 Cr M1 0,001 0,003 0,000 0,014 0,007 0,001 0,007 0,003 0,004 0,001 0,016 0,014 0,002 0,009 0,010 0,000 0,007 Mg M1 0,636 0,796 0,663 0,785 0,848 0,843 0,714 0,796 0,824 0,797 0,790 0,781 0,675 0,713 0,765 0,699 0,711 Fe 2+ M1 0,117 0,059 0,097 0,031 0,012 0,087 0,054 0,062 0,073 0,095 0,033 0,092 0,048 0,041 0,102 0,073 Mn M1 M1 subtotal 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 Mg M2 0,001 Fe 2+ M2 0,048 0,083 0,052 0,119 0,132 0,018 0,119 0,084 0,088 0,087 0,136 0,106 0,041 0,116 0,111 0,067 0,114 Mn M2 0,005 0,005 0,005 0,005 0,005 0,008 0,005 0,006 0,005 0,004 0,005 0,005 0,005 0,005 0,005 0,004 0,004 Ca M2 0,906 0,856 0,896 0,833 0,816 0,906 0,833 0,866 0,883 0,886 0,813 0,845 0,910 0,836 0,837 0,899 0,838 Na M2 0,041 0,056 0,047 0,043 0,047 0,068 0,043 0,043 0,024 0,023 0,045 0,044 0,044 0,043 0,046 0,030 0,044 K M2 M2 subtotal 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 1,000 Jd 3,5 4,8 4,5 4,3 4,6 5,4 4,3 3,7 2,2 2,3 4,5 4,4 3,8 4,3 4,6 3,0 4,4 Ae 1,2 1,6 0,6 0,0 0,3 2,9 0,0 1,2 0,4 0,1 0,0 0,0 1,2 0,0 0,0 0,0 0,0 Es 5,0 2,5 5,6 3,6 2,9 0,0 4,7 2,7 2,1 2,0 4,4 3,8 5,0 5,2 4,4 5,0 4,1 CaTiTs 10,4 3,6 7,9 4,0 2,8 0,1 7,1 4,1 3,4 4,3 4,9 4,8 8,6 7,2 4,7 6,8 7,4 CaTs 3,9 1,1 5,1 5,8 3,0 0,0 6,7 1,6 1,8 1,9 6,3 4,9 3,9 6,7 5,2 5,1 5,5 Wo 35,7 39,3 35,5 35,0 36,5 45,2 32,4 39,1 40,5 40,2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 JAC46.2 Litotipo LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP MDIO Local B B B N B N N N N N N N N N N SiO 2 48,42 48,38 46.43 48,78 46.60 49,71 46.50 47,97 48,17 45,22 50,24 49,67 47,36 50,44 50,14 TiO 2 2,18 1,92 2,67 1,86 2,87 1,77 3,12 2,19 2,24 3,47 1,56 1,90 2,71 1,67 1,68 Al 2 O 3 6,14 5,27 6,62 5,86 6,75 3,72 6,54 5,26 4,62 7,63 3,68 4,37 6,16 4,19 4,13 Cr 2 O 3 0,47 0,56 0,01 0,36 0,43 0,03 0,15 0,30 0,00 0,17 0,04 0,02 0,09 0,02 0,02 FeO 7,64 7,43 8,76 7,17 7,54 7,70 8,38 7,82 8,74 8,51 8,28 7,66 7,54 7,38 7,09 MnO 0,14 0,14 0,16 0,16 0,18 0,17 0,13 0,12 0,15 0,13 0,18 0,24 0,16 0,20 0,22 MgO 13,50 13,62 12,07 12,56 11,92 14,09 12,43 13,24 12,93 11,65 14,51 12,78 12,34 13,79 13,59 CaO 21,48 22,27 22,57 22,11 22,48 22,71 22,65 22,83 22,54 22,49 21,25 22,04 22,98 21,97 22,03 Na 2 O 0,62 0,47 0,64 1,35 1,33 0,36 0,42 0,43 0,37 0,81 0,41 1,50 0,96 1,07 1,25 K 2 O Total 100,59 100,05 99,91 100,21 100,11 100,27 100,31 100,15 99,78 100,06 100,16 100,18 100,31 100,73 100,15 Si T 1,785 1,794 1,734 1,798 1,727 1,840 1,732 1,781 1,802 1,687 1,860 1,832 1,753 1,848 1,845 Al T 0,215 0,206 0,266 0,202 0,273 0,160 0,268 0,219 0,198 0,313 0,140 0,168 0,247 0,152 0,155 Fe 3+ T T subtotal 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 2,000 32,8 Tabela A1 -Amostra Al M1
	En En En	40,2 42,5 32,2	35,1 35,1 32,8	34,1 41,6 31,3	34,6 33,1 33,8	35,0 41,2 32,5	35,4 32,3 41,9	43,8 33,1 38,9	34,0 34,2 40,4	36,5 34,4 39,0	35,3 40,9 32,3	35,7 41,2 44,3	34,3 41,6 42,8	30,6 40,4 44,3	32,6 40,3 37,0	33,4 44,1 36,5	40,1 44,6 37,2	41,0 45,6 40,3
	Fs Fs Fs	4,5 5,3 10,2	8,1 7,8 10,1	7,3 4,6 10,8	8,5 9,0 9,2	7,3 5,3 9,6	8,2 10,2 4,4	4,2 9,5 5,0	7,9 8,8 4,3	6,7 16,4 5,7	8,2 6,2 4,4	6,4 6,0 9,0	7,7 4,5 10,2	9,7 5,4 9,6	9,9 6,2 8,0	10,1 2,7 7,9	6,9 3,1 8,6	4,5 2,5 7,6
	mg# mg# mg#	84,1 86,2 68,1	72,5 73,8 67,9	72,6 84,3 64,7	71,9 68,2 69,5	72,5 85,1 68,1	72,7 66,2 84,1	87,3 68,1 82,3	72,0 71,9 83,0	75,0 63,2 79,9	73,9 83,9 71,7	72,3 83,3 81,3	72,4 83,1 78,1	65,6 84,2 78,2	66,4 83,0 75,6	69,0 90,0 74,4	80,0 90,2 75,5	84,5 92,3 79,4

  Tabela A2 -Composição química (porcentagem peso) de cristais de biotita/flogopita das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 22 oxigênios. Abreviações: OLCPX, clinopiroxenito com olivina; NECPX, clinopiroxenito com nefelina; MDIO, meladiorito; MON, monzonito. Composição química (porcentagem peso) de cristais de biotita/flogopita das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 22 oxigênios. Abreviações: AFS, álcali-feldspato sienito; LAMP, lamprófiro, CPX, clinopiroxenito. Composição química (porcentagem peso) de cristais de biotita/flogopita das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 22 oxigênios. Abreviações: LAMP, lamprófiro; CCap, calcita carbonatito com apatita.

	Amostra Tabela A2 -Amostra JAC13 JAC32 Tabela A2 -Amostra JAC46.1 JAC46.1 JAC46.2 JAC46.2 JAC46.2 JAC42 JAC18 JAC18 JAC18 JAC18 JAC18 JAC39 JAC39 JAC39 JAC39 JAC39	JAC18 JAC39 JAC42	JAC18 JAC39 JAC42	JAC18 JAC39 JAC42	JAC22 JAC39 JAC42	JAC22 JAC39 JAC42	JAC22 JAC39 JAC42	JAC22 JAC39 JAC42	JAC22 JAC45 JAC42	JAC22 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC25 JAC25 JAC25 JAC42 JAC42 JAC42 JAC42
	Litotipo Litotipo Litotipo	OLCPX NECPX NECPX NECPX NECPX NECPX NECPX NECPX NECPX MDIO AFS LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP LAMP CCap CCap CCap CCap CCap	MDIO LAMP CCap	MDIO LAMP CCap	MDIO LAMP CCap	MDIO CPX CCap	MDIO LAMP CCap	MON LAMP CCap	MON LAMP CCap	MON LAMP CCap
	SiO 2 SiO 2 SiO 2	37.46 36.87 36.48	35.90 37.72 36.87	35.70 35.77 34.82	37.22 35.49 35.61	36.46 35.78 39.25	36.24 35.78 41.21	36.47 35.77 41.33	36.51 34.98 41.07	37.03 36.40 41.87	36.14 35.86 41.46	36.39 36.04 38.82	36.27 35.76 39.62	36.92 36.55 39.24		36.52 38.52 39.68		36.49 35.71 39.94	34.91 36.13 39.47	36.78 36.81 39.83	37.50 36.45 40.22
	TiO 2 TiO 2 TiO 2	6.89 4.03 6.23	4.13 2.96 5.65	3.00 3.27 7.37	2.56 2.81 6.34	2.87 2.78 2.32	2.51 3.11 0.50	2.38 2.90 0.48	2.47 2.89 0.47	2.27 2.81 0.38	6.28 2.72 0.58	5.88 2.26 0.72	5.95 2.07 0.60	6.07 3.16 0.73		6.06 2.35 0.69		6.19 6.70 0.70	5.26 6.34 0.76	3.63 6.77 0.61	3.14 6.50 0.64
	Al 2 O 3 Al 2 O 3 Al 2 O 3	15.05 13.40 14.03	15.01 14.61 14.21	15.42 14.43 14.68	15.62 14.34 15.20	15.47 14.43 14.37	15.17 14.06 13.71	15.85 13.87 13.40	15.48 13.88 13.59	15.72 14.07 13.30	13.49 13.49 13.15	13.86 13.72 14.17	13.91 13.73 14.40	14.10 13.38 14.38		13.87 16.93 14.43		14.32 14.00 14.50	12.28 14.05 14.59	12.74 13.57 14.24	12.23 14.07 14.36
	FeO FeO FeO	13.17 17.05 14.79	12.40 15.77 13.56	12.05 15.21 18.38	12.04 15.70 16.09	11.87 15.56 12.36	11.42 15.09 3.87	11.39 15.45 3.41	11.46 15.42 3.21	10.78 15.65 3.19	17.50 15.15 2.95	17.53 15.29 3.67	17.48 15.57 3.63	17.19 14.79 3.62		16.76 4.61 3.59		15.34 15.39 3.58	22.40 15.38 3.55	21.60 15.01 3.50	21.49 14.93 3.50
	MnO MnO MnO	0.05 0.48 0.28	0.14 0.31 0.27	0.13 0.29 0.18	0.14 0.29 0.19	0.15 0.26 0.16	0.13 0.27 0.02	0.11 0.32 0.04	0.15 0.35 0.04	0.13 0.28 0.02	0.23 0.27 0.03	0.21 0.28 0.05	0.18 0.30 0.06	0.17 0.29 0.04		0.18 0.01 0.04		0.18 0.26 0.03	0.45 0.27 0.04	0.40 0.26 0.05	0.44 0.27 0.05
	MgO MgO MgO	14.12 13.88 14.49	17.16 14.84 15.44	17.61 14.47 11.72	17.97 15.11 12.59	18.26 15.06 16.59	18.52 14.85 25.77	18.65 15.24 26.06	18.77 15.22 26.08	19.04 15.81 26.34	12.19 15.80 26.12	12.70 16.06 24.36	12.82 16.85 25.02	12.81 16.29 25.06		12.83 23.14 24.94		13.06 13.21 25.15	9.94 14.05 25.02	10.97 14.01 25.01	11.30 13.98 25.27
	CaO CaO CaO	0.00 0.00 0.00	0.00 0.29 0.02	0.00 0.23 0.02	0.00 0.25 0.01	0.00 0.27 0.08	0.00 0.24 0.04	0.00 0.14 0.00	0.00 0.17 0.01	0.00 0.27 0.01	0.10 0.56 0.00	0.00 0.60 0.00	0.00 0.18 0.00	0.01 0.20 0.00		0.10 0.01 0.02		0.06 0.00 0.01	0.00 0.02 0.00	0.00 0.04 0.00	0.00 0.00 0.00
	BaO BaO BaO	0.00 0.11 0.58	1.84 0.12 1.01	1.86 0.81 1.48	1.48 0.29 1.91	1.46 0.12 0.00	1.94 0.68 0.71	1.94 0.10 0.65	1.58 0.27 0.50	1.39 0.10 0.46	0.21 0.04 0.39	0.57 0.01 1.36	0.76 0.14 1.00	0.66 0.05 1.15		0.58 0.68 1.22		0.57 1.62 0.88	1.49 0.74 1.27	0.37 0.25 0.97	0.00 0.47 0.98
	Na 2 O Na 2 O Na 2 O	0.10 0.36 0.40	0.11 0.18 0.33	0.10 0.21 0.27	0.15 0.11 0.44	0.18 0.14 0.44	0.10 0.14 1.12	0.19 0.19 1.14	0.09 0.20 0.79	0.17 0.29 0.93	0.89 0.19 0.91	0.31 0.18 0.25	0.34 0.11 0.20	0.40 0.21 0.24		0.21 1.15 0.25		0.76 0.42 0.22	0.19 0.45 0.23	0.10 0.36 0.18	0.10 0.40 0.17
	K 2 O K 2 O K 2 O	10.54 9.75 10.00	9.91 7.97 10.12	9.74 7.45 9.49	10.21 7.45 9.57	10.10 7.06 10.23	9.57 6.84 9.37	9.97 7.64 9.49	9.84 8.05 9.98	10.18 5.85 9.75	8.97 5.45 9.91	9.93 5.56 9.70	9.91 6.94 10.77	10.16 7.40 10.33		10.12 9.25 10.36		9.03 9.41 10.68	9.06 10.00 10.18	10.11 10.18 10.78	10.14 10.07 10.74
	Total Total Total	97.39 95.93 97.28	96.60 94.76 97.47	95.62 92.13 98.41	97.40 91.84 97.96	96.84 91.47 95.80	95.60 91.07 96.33	96.97 91.62 96.01	96.35 91.42 95.74	96.71 91.52 96.25	96.00 89.54 95.49	97.39 90.01 93.10	97.62 91.64 95.29	98.49 92.34 94.78		97.23 96.65 95.21		96.00 96.72 95.69	95.99 97.42 95.11	96.71 97.26 95.18	96.34 97.14 95.92
	Si T Si T Si T	5.464 5.577 5.410	5.345 5.650 5.440	5.356 5.541 5.225	5.454 5.511 5.319	5.382 5.547 5.771	5.413 5.579 5.794	5.374 5.558 5.820	5.399 5.484 5.799	5.432 5.595 5.864	5.471 5.619 5.854	5.454 5.621 5.688	5.431 5.537 5.681	5.464 5.601 5.654		5.467 5.427 5.688		5.467 5.378 5.689	5.489 5.378 5.661	5.659 5.456 5.710	5.765 5.414 5.716
	Al T Al T TI M Fe 2+ M Mn M Mg M Ca I Ba I Al T	2.536 2.388 0.458 2.157 0.061 3.095 0.000 0.007 2.453	2.634 2.350 0.333 1.975 0.039 3.312 0.047 0.007 2.470	2.644 2.459 0.381 1.971 0.039 3.341 0.037 0.049 2.596	2.546 2.489 0.329 2.039 0.037 3.497 0.041 0.018 2.675	2.618 2.453 0.324 2.017 0.034 3.481 0.046 0.007 2.229 2.290 0.000 2.587 2.626 2.601 2.568 2.406 2.449 2.455 2.459 2.447 0.034 0.092 0.023 0.146 0.010 0.001 0.000 2.421 2.442 2.516 2.405 2.381 2.379 2.463 2.399 2.573 2.485 0.000 0.000 0.364 0.338 0.340 0.325 0.321 0.265 0.241 0.365 0.249 0.759 0.709 0.755 1.968 2.007 2.021 2.011 1.985 1.994 2.016 1.895 0.544 1.939 1.914 1.861 0.035 0.042 0.047 0.037 0.036 0.037 0.039 0.038 0.001 0.033 0.034 0.032 3.452 3.530 3.557 3.623 3.691 3.733 3.889 3.721 4.860 2.830 2.962 2.922 0.041 0.024 0.028 0.044 0.094 0.101 0.030 0.033 0.002 0.000 0.004 0.007 0.041 0.006 0.016 0.006 0.003 0.001 0.008 0.003 0.037 0.096 0.043 0.015 2.206 2.180 2.201 2.136 2.146 2.312 2.319 2.346 2.312 2.311 2.339 0.039 0.036 0.028 0.025 0.021 0.078 0.056 0.065 0.069 0.049 0.071 0.054	0.000 0.012 0.000 0.726 1.855 0.034 2.974 0.000 0.027 0.055
	Na I Na I Na I Na I	0.029 0.037 0.106 0.115	0.032 0.048 0.053 0.094	0.030 0.029 0.063 0.079	0.042 0.048 0.034 0.129	0.051 0.029 0.042 0.126	0.029 0.036 0.043 0.305	0.054 0.030 0.058 0.312	0.025 0.022 0.060 0.217	0.049 0.025 0.085 0.251	0.262 0.007 0.058 0.249	0.091 0.012 0.054 0.071	0.097 0.010 0.033 0.054	0.114 0.010 0.064 0.066		0.061 0.034 0.315 0.068		0.220 0.111 0.123 0.062	0.057 0.088 0.130 0.065	0.029 0.087 0.103 0.051	0.031 0.117 0.115 0.046
	K I K I K I K I	1.962 1.985 1.881 1.891	1.882 1.976 1.522 1.904	1.863 1.934 1.472 1.817	1.909 1.978 1.474 1.823	1.902 1.951 1.397 1.919	1.822 2.010 1.361 1.681	1.874 1.997 1.515 1.705	1.856 1.913 1.609 1.797	1.905 1.764 1.146 1.743	1.732 1.910 1.089 1.784	1.898 1.877 1.106 1.814	1.893 1.893 1.371 1.970	1.918 1.883 1.447 1.899		1.933 1.830 1.663 1.894		1.726 1.905 1.807 1.940	1.817 1.973 1.899 1.863	1.983 1.879 1.926 1.972	1.989 1.947 1.909 1.946
	Total Total Total Total	15.482 15.765 15.765 15.672	15.833 15.742 15.516 15.698	15.890 15.654 15.528 15.592	15.890 15.763 15.603 15.608	15.931 15.778 15.530 15.751	15.896 15.811 15.468 16.010	15.949 15.786 15.620 16.025	15.918 15.730 15.728 16.026	15.936 15.651 15.421 15.995	15.609 15.725 15.388 16.007	15.652 15.722 15.433 15.952	15.666 15.661 15.671 16.050	15.647 15.684 15.582 16.028		15.624 15.729 15.908 16.000		15.544 15.692 15.586 16.020	15.688 15.779 15.694 15.988	15.772 15.711 15.619 16.032	15.773 15.796 15.640 16.010
																1,000	1,000
	Jd	4,4	3,1	4,1	8,5	7,7	2,0	2,8	2,6	2,2	4,9	2,7	8,6	5,7		6,4		7,3	
	Ae	0,0	0,5	1,1	2,2	3,7	1,2	0,6	1,0	1,0	1,8	0,5	4,3	2,3		2,3		3,2	
	Es	3,6	4,2	5,8	4,4	5,0	3,0	4,5	4,4	3,6	5,7	2,6	3,1	4,6		2,9		3,1	
	CaTiTs	6,1	5,3	7,5	5,2	8,0	4,9	8,7	6,1	6,3	9,7	4,4	5,3	7,6		4,6		4,6	
	CaTs	5,1	4,5	4,7	2,7	1,9	1,9	4,1	3,9	2,5	4,1	2,2	0,0	2,4		0,7		0,0	
	Wo	35,0	37,2	36,1	37,5	37,1	40,1	36,5	38,2	39,0	35,2	37,6	39,4	38,2	39,0	39,6
	En	37,1	37,7	33,6	34,5	32,9	38,9	34,5	36,7	36,1	32,4	40,0	35,1	34,1	37,7	37,3
	Fs	8,1	6,9	6,8	4,4	2,9	7,7	8,0	6,8	9,1	5,8	9,8	4,4	4,7		6,1		4,6	
	mg#	75,9	76,6	71,1	75,7	73,8	76,5	72,6	75,1	72,5	70,9	75,8	74,8	74,5	76,9	77,4

  ,856 84,086 83,928 84,257 84,198 84,059 83,798 83,900 84,094 84,314 83,951 84,274 84,065 83,868 84,050 84,032 84,055 190 Tabela A3 -Composição química (porcentagem peso) de cristais de olivina das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 4 oxigênios e 3 cátions. Abreviações: WEH, wehrlito; DUN, dunito.

	Cátions Fa Fo mg# Litotipo SiO 2 TiO 2 Al 2 O 3 FeO Cr 2 O 3 MnO NiO MgO CaO Na 2 O K 2 O Total 84,037 83Amostra JAC248 JAC248 JAC248 JAC248 JAC248 JAC248 JAC248 JAC248 JAC248 JAC248 JAC248 JAC248 2,991 2,993 2,990 2,986 2,991 2,991 2,995 2,990 2,993 2,993 3,001 2,995 0,159 0,160 0,161 0,159 0,161 0,157 0,158 0,159 0,162 0,161 0,159 0,157 0,841 0,840 0,839 0,841 0,839 0,843 0,842 0,841 0,838 0,839 0,841 0,843 84,133 DUN DUN DUN DUN DUN DUN DUN DUN DUN DUN DUN DUN 40,17 40,29 40,38 40,48 40,20 40,13 40,37 40,27 40,42 40,32 40,20 40,69 0,02 0,00 0,01 0,00 0,01 0,00 0,01 0,01 0,03 0,01 0,01 0,01 0,01 0,00 0,00 0,00 0,00 0,01 0,01 0,00 0,01 0,00 0,01 0,00 14,92 14,99 15,04 14,90 15,12 15,16 15,17 15,30 15,13 15,10 15,06 15,01 0,01 0,01 0,00 0,01 0,00 0,01 0,01 0,01 0,27 0,28 0,26 0,24 0,30 0,28 0,27 0,27 0,27 0,29 0,27 0,28 0,23 0,23 0,24 0,24 0,19 0,20 0,21 0,20 0,21 0,21 0,21 0,21 44,37 44,35 44,41 44,54 44,52 44,73 44,50 44,83 44,06 44,37 44,31 44,56 0,32 0,48 0,47 0,40 0,48 0,42 0,44 0,50 0,54 0,44 0,47 0,50 0,01 0,00 0,00 0,01 0,00 0,01 0,01 0,00 0,00 0,00 0,00 0,00 0,01 0,00 0,01 0,00 0,00 0,00 0,01 0,00 100,31 100,64 100,82 100,82 100,83 100,94 101,01 101,39 1,35 1,34 1,34 1,35 Si 1,006 1,006 1,007 1,008 1,003 1,000 1,005 1,000 1,009 1,006 1,005	2,998 0,160 0,840	2,992 0,157 0,843	2,993 0,159 0,841	2,993 0,161 0,839	2,993 0,160 0,840	2,993 0,160 0,840	2,991 0,159 0,841

  Composição química (porcentagem peso) de cristais de anfibólio das rochas do Complexo de Jacupiranga.

	Cátions Fa Fo mg# Litotipo Tabela A4 -Amostra 2,994 0,159 0,841 84,132 84,059 84,038 84,194 83,993 84,023 83,950 83,928 83,845 83,968 83,987 84,107 2,994 2,993 2,992 2,997 3,000 2,995 3,000 2,990 2,994 2,995 2,991 0,159 0,160 0,158 0,160 0,160 0,161 0,161 0,162 0,160 0,160 0,159 0,841 0,840 0,842 0,840 0,840 0,839 0,839 0,838 0,840 0,840 0,841 JAC32 JAC32 JAC32 JAC32 JAC32 JAC32 Monzonito Monzonito Monzonito Monzonito Monzonito Monzonito Monzonito Monzonito Monzonito Monzonito Monzonito Monzonito Monzonito AFS SiO 2 45,23 51,74 45,65 47,51 47,62 45,57 46.18 53,13 49,04 47,05 47,63 47,17 47,49 Ponto 15 1 2 3 4 5 40,94 TiO 2 1,38 0,57 1,25 0,93 1 1,11 1,38 0,34 0,64 0,91 0,9 0,99 0,96 Litotipo AFS AFS AFS AFS AFS AFS MDIO MDIO MDIO MDIO MDIO MON MON MON MON MON MON MON MON MON MON MON MON 2,87 Al 2 O 3 6,88 1,52 6,55 5,48 5,58 6,53 6,65 1,23 4,44 5,56 5,22 5,73 5,49 SiO 2 40,26 40,5 39,95 40,55 40,87 40,64 SiO 2 60,91 54,35 56,59 55,28 59,47 58,22 51,24 59,68 64,78 64,56 60,75 64,85 46.51 57,77 50,71 52,88 59,50 11,15 MnO 0,71 0,58 0,69 0,65 0,73 0,79 0,62 0,49 0,79 0,71 0,73 0,71 0,74 TiO 2 3,07 2,92 2,65 11,12 2,87 2,92 Al 2 O 3 25,47 29,44 27,65 28,37 25,95 26,19 32,57 25,74 22,23 18,79 24,92 19,07 37,46 27,82 32,38 31,81 23,61 0,55 FeO 18,8 9,1 19,06 18,11 18,94 20,13 18,16 10,13 18,41 18,24 18,24 19,14 18,25 MgO 10,17 13,53 9,96 11,15 10,63 9,53 10,89 13,66 11,19 11,03 11,12 10,47 11,03 CaO 11,09 20,51 10,95 11,14 11,23 11,19 11,29 19,51 11,38 11,31 11,14 11,1 11,19 Na 2 O 1,98 0,71 1,8 1,87 1,84 1,78 1,87 0,57 1,32 1,81 1,77 1,89 1,81 K 2 O 1,07 0,005 0,99 0,77 0,8 1,01 1,02 0,05 0,644 0,79 0,75 0,83 0,79 Total 0 0 0 0 1 0 0 0 0 0 0 0 0 Si 6,886 7,534 6,968 7,139 7,13 6,946 6,937 7,652 7,316 7,102 7,166 7,098 7,133 Al 1,114 0,261 1,032 0,861 0,87 1,054 1,063 0,209 0,684 0,898 0,834 0,902 0,867 Ti 0,062 T subtotal 8 7,857 8 8 8 8 8 7,898 8 8 8 8 8 Ti 0,158 0,144 0,105 0,113 0,127 0,156 0,072 0,103 0,102 0,112 0,108 Al 0,12 0,146 0,109 0,115 0,119 0,115 0,097 0,091 0,092 0,114 0,105 Fe 3+ 0,125 0,137 0,123 0,112 0,141 0,122 0,191 0,122 0,134 0,128 0,123 Mn 2+ 0,02 0,072 0,011 0,013 0,029 0,022 0,009 0,06 0,045 0,021 0,017 0,017 0,024 Fe 2+ 2,268 1,108 2,296 2,153 2,259 2,425 2,159 1,22 2,106 2,181 2,162 2,28 2,169 Mg 2,308 2,937 2,266 2,498 2,373 2,166 2,439 2,933 2,489 2,482 2,494 2,349 2,47 C subtotal 4,999 4,117 5 5,001 5,001 5 5 4,213 5 5 5,001 5 4,999 Mn 2+ 0,071 0,078 0,07 0,064 0,08 0,07 0,055 0,069 0,076 0,073 Fe Ca 1,809 2 1,791 1,793 1,802 1,828 1,817 2 1,819 1,829 1,796 1,79 1,801 Na 0,12 0,131 0,137 0,134 0,092 0,113 0,126 0,101 0,128 0,137 0,129 B subtotal 2 2 2 2 2 2 2 2 2 1,999 2 2 2 Ca 1,2 Na 0,465 0,2 0,401 0,408 0,4 0,434 0,432 0,159 0,255 0,428 0,388 0,414 0,398 K 0,208 0,001 0,193 0,148 0,153 0,196 0,195 0,009 0,123 0,152 0,144 0,159 0,151 A subtota l 0,673 1,401 0,594 0,556 0,553 0,63 0,627 1,179 0,378 0,58 0,532 0,573 0,549 Total de Cátions 15,672 15,375 15,594 15,557 15,554 15,63 15,627 15,29 15,378 15,579 15,533 15,573 15,548 Classificação magnesio hastingsite edenite ferro-pargasite edenite edenite hastingsite magnesio-hastingsite edenite actinolite edenite edenite edenite edenite magnesio-magnesio-magnesio-edenite magnesio-magnesio-Rica em Ti Cátions hastingsita Total de 16,004 16,001 16 15,782 15,989 16,007 magnesio-A subtota l 1,006 1,004 1,044 1,087 0,989 1,012 16,013 K 0,342 0,339 0,337 0,344 0,336 0,346 1,022 Na 0,664 0,665 0,707 0,743 0,653 0,666 0,344 Ca 0,678 B subtotal 2 2 2 2 2 2 1,011 Na 0,193 0,249 0,202 0,192 0,275 0,252 2 Ca 1,807 1,751 1,798 1,808 1,717 1,748 0,217 Mg 1,783 Fe 2+ Mg Mn 0,008 2+ 2+ C subtotal 4,998 4,997 4,956 4,695 5 4,995 0,07 Mg 2,337 2,286 2,258 2,351 2,38 2,36 4,991 Fe 2+ 1,882 1,868 1,782 2,14 1,793 1,799 2,438 Mn 2+ 0,071 0,072 0,075 0,074 0,06 0,068 1,769 Fe 3+ 0,242 0,272 0,425 0,297 0,297 0,07 Al 0,114 0,166 0,112 0,143 0,139 0,23 Ti 0,352 0,333 0,304 0,13 0,327 0,332 0,158 T subtotal 8 8 8 8 8 8 0,326 Fe 3+ 8 Ti 1,167 Fe 3+ Al 1,867 1,856 1,9 0,545 1,81 1,85 0,037 Si 6,133 6,144 6,1 6,288 6,19 6,15 1,824 Fórmula estrutural calculada na base de 23 oxigênios 6,176 Total 0 0 0 0 0 0 Fórmula estrutural calculada na base de 23 oxigênios K 2 O 1,76 1,75 1,73 1,74 1,74 1,79 0 Na 2 O 2,9 3,11 3,07 3,11 3,16 3,13 1,79 CaO 11,07 10,77 10,99 10,88 10,58 10,78 3,06 MgO 10,29 10,11 9,92 10,17 10,54 10,46 11,03 FeO 16,67 16,87 17,28 16,5 16,5 16,56 10,84 MnO 0,55 0,56 0,58 0,56 0,53 0,53 15,84 Al 2 O 3 11,03 11,31 11,18 2,98 10,94 11,15 TiO 2
	Classificação	hastingsita	hastingsita	hastingsita	hastingsita	hastingsita
		Rica em Ti Rica em Ti Rica em Ti	Rica em Ti Rica em Ti
						192

  Composição química (porcentagem peso) de cristais de feldspato das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 32 oxigênios. Abreviações: MON, monzonito; AFS, álcali-feldspato sienito; LAMP, lamprófiro.

	Tabela A5 -Amostra JAC25	JAC25	JAC32	JAC32	JAC32	JAC32	JAC32	JAC39	JAC39	JAC39	JAC39	JAC39	JAC39	JAC39 JAC46.1 JAC46.1 JAC46.1
	Litotipo	MON	MON	AFS	AFS	AFS	AFS	AFS	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP
	SiO 2	55,16	61,47	64,80	65,13	65,91	64,63	64,30	51,37	63,45	63,39	63,12	66,44	63,30	63,84	68,55	65,29	65,55
	Al 2 O 3	29,43	24,71	20,12	19,84	20,32	19,55	19,95	1,65	19,73	19,29	19,67	20,42	19,53	19,37	19,26	19,59	19,65
	TiO 2																	
	Total	19,804	20,021	20,018	20,052	19,947	20,193	20,426	19,978	19,899	19,972	19,970	20,148	20,447	20,332	20,416	20,385	20,456
	An	31,5	54,7	42,6	48,0	34,2	0,7	40,1	33,5	15,4	0,8	28,3	0,5	51,9	22,8	45,0	35,0	0,3
	Ab	66,7	44,3	55,6	51,0	63,8	12,3	58,9	65,2	82,3	18,5	70,1	12,6	47,0	76,1	53,7	63,7	18,8
	Or	1,8	1,0	1,8	1,0	2,0	87,0	1,0	1,4	2,4	80,7	1,6	86,9	1,1	1,2	1,3	1,2	80,8

  Composição química (porcentagem peso) de cristais de feldspato das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 32 oxigênios. Abreviações: LAMP, lamprófiro.

	Tabela A5 -Amostra JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.1 JAC46.2 JAC46.2						
	Litotipo	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP	LAMP						
	SiO 2	68,55	64,87	65,07	61,57	61,13	60,80	61,79	62,15	63,51	64,61	55,09						
	Al 2 O 3	20,14	21,29	21,29	22,87	22,28	24,04	22,98	22,70	22,56	22,71	26,43						
	TiO 2																	
																		0,001
	Ca	1,218	0,333	0,054	0,076	0,094	0,004	0,072	4,766	0,025	0,018	0,033	0,165	0,016	0,013	0,218	0,065	0,085
	Na	2,890	3,713	2,074	1,980	2,206	0,240	1,374	0,656	0,991	1,022	1,005	3,633	1,001	1,097	3,557	1,819	2,226
	K	0,061	0,220	1,850	1,978	1,674	3,663	2,592	0,000	2,888	2,986	2,916	0,067	2,901	2,866	0,239	2,143	1,749
	Sr	0,014	0,000	0,057	0,032	0,032	0,000	0,040	0,000	0,067	0,053	0,078	0,027	0,067	0,053	0,004	0,036	0,044
	Ba	0,001	0,000	0,004	0,003	0,003	0,006	0,004	0,000	0,011	0,009	0,011	0,000	0,011	0,010	0,000	0,003	0,003
	Total	20,395	20,422	20,063	20,079	20,035	19,957	20,090	21,580	19,990	20,062	20,027	19,947	19,995	20,032	19,953	20,061	20,084
	An	29,2	7,8	1,4	1,9	2,4	0,1	1,8	87,9	0,6	0,4	0,8	4,3	0,4	0,3	5,4	1,6	2,1
	Ab	69,3	87,0	52,1	49,1	55,5	6,1	34,0	12,1	25,4	25,4	25,4	94,0	25,6	27,6	88,6	45,2	54,8
	Or	1,5	5,2	46.5	49,0	42,1	93,8	64,2	0,0	74,0	74,2	73,7	1,7	74,1	72,1	6,0	53,2	43,1
																		195

47,2 47,8 47,7 47,7 47,0 47,0 46.6 47,8 En 42,6 42,9 42,7 42,2 42,1 41,5 42,8 42,4 43,3 42,5 42,4 42,6 42,5 43,1 42,8 42,1 42,4 Fs 2,7 1,8 1,1 3,4 3,3 3,2 2,1 3,8 3,2 3,6 2,3 1,7 2,4 2,2 3,1 1,5 3,0 mg# 89,8 89,6 89,0 89,5 89,1 87,9 89,0 89,6 88,5 89,5 89,8 89,5 90,1 89,8 89,2 88,2 89,3

2,9 2,3 2,2 2,1 1,9 2,2 2,0 2,1 2,2 1,9 2,1 2,0 1,9 2,1 2,2 2,0 2,1 Ae 1,9 1,5 0,6 1,4 1,3 1,5 1,3 1,4 1,5 1,2 1,4 1,3 1,3 1,3 1,4 1,4 1,4 Es 0,2 5,8 4,2 5,7 4,9 5,0 5,7 5,1 5,6 5,0 5,7 5,2 4,8 5,3 5,3 5,5 5,1 CaTiTs 1,8 8,0 7,3 8,3 6,9 7,2 8,1 6,1 8,0 7,6 8,1 6,3 5,9 7,2 7,7 8,5 7,4 CaTs 0,0 3,2 3,6 2,9 3,1 3,1 3,5 3,1 3,1 3,9 3,5 3,5 3,5 4,0 3,3 3,5 3,5 Wo 47,1 40,8 41,6 40,7 41,8 41,7 40,5 42,2 40,8 40,8 40,4 42,1 42,5 41,0 40,8 40,4 41,1 En 42,9 35,8 37,7 36,2 37,9 37,0 36,1 38,6 36,2 37,1 35,9 37,8 38,2 37,6 36,4 36,7 36,9 Fs 2,9 1,9 2,5 1,9 1,9 2,0 2,2 1,0 1,9 2,4 2,3 1,4 1,8 1,5 2,4 1,6 2,3 mg# 89,2 77,6 83,6 77,6 81,4 80,6 77,9 82,7 78,2 81,2 77,9 82,0 82,9 82,3 79,2 80,1 80,4

2,2 2,2 2,2 2,3 2,1 2,2 2,1 2,2 2,0 2,1 1,7 2,0 2,0 2,2 2,0 2,0 2,1 Ae 1,5 1,4 1,2 1,5 1,4 1,5 1,4 1,4 1,3 1,4 1,1 1,3 1,4 1,5 1,3 1,3 1,4 Es 5,2 5,6 4,8 5,3 5,0 5,0 5,4 5,5 5,5 5,7 4,9 5,3 5,3 5,4 5,2 5,3 4,2 CaTiTs 6,8 8,3 7,0 8,4 7,4 7,8 7,7 8,0 8,0 8,0 8,1 8,1 7,9 7,8 7,2 7,6 6,7 CaTs 3,5 3,2 3,6 3,5 3,2 3,1 3,0 3,3 3,4 3,0 3,1 3,1 3,8 3,1 3,3 2,9 2,4 Wo 41,4 41,1 41,2 40,7 41,3 41,0 41,0 40,5 40,5 40,6 41,1 41,0 40,8 41,0 41,7 41,4 42,6 En 37,4 35,7 37,3 35,5 37,1 36,3 36,7 35,7 35,8 36,1 35,7 36,8 36,5 37,0 37,7 37,4 37,7 Fs 1,7 2,0 2,6 2,6 2,3 2,8 2,0 2,8 3,0 2,1 3,7 1,8 2,2 1,3 1,2 1,4 2,6 mg# 81,3 78,0 81,3 78,5 80,4 78,9 78,9 77,1 77,2 77,3 77,5 79,8 80,3 80,4 82,0 80,3 81,2

35,5 36,7 32,3 34,8 36,5 33,4 En 31,8 39,8 33,2 39,3 42,4 42,2 35,7 39,8 41,2 39,9 39,5 39,0 33,8 35,7 38,3 34,9 35,5 Fs 8,2 7,1 7,5 7,5 7,2 5,2 8,6 7,3 8,0 9,1 6,8 6,9 6,6 8,2 7,6 8,5 9,3 mg# 68,7 78,1 70,8 78,0 80,3 83,9 72,8 77,9 79,6 78,1 77,9 78,5 72,4 72,8 76,1 72,2 72,6

Acknowledgements

L. Chmyz is grateful to the Coordenação de Aperfeiçoamento Pessoal de Nível Superior (CAPES, Brazil) -Process 99999.003713/2014-08 for the PhD scholarship. The authors are grateful to FAPESP (Procs. 2010/20425-8, RGA; 2012/06082-6, ER) for financial support.

We thank VALE Fertilizantes for providing access to the carbonatite mine. We are indebted to H. Fossen for the revision of the English text. Constructive comments from anonymous reviewers helped us to considerably improve the discussion and the overall presentation of the manuscript.

NEW CONSTRAINTS ON THE PETROGENESIS OF THE JACUPIRANGA ULTRAMAFIC-ALKALINE CARBONATITE COMPLEX (BR) FROM Pb AND Hf

ISOTOPE DATA

Manuscrito em preparação.

 , 1997). Delta ε Hf (Δε Hf ) is defined as the difference between the measured (or initial) Hf isotope ratio and that predicted from the oceanic basalt Nd-Hf isotope correlation line of [START_REF] Vervoort | Relationships between Lu-Hf and Sm-Nd isotopic systems in the global sedimentary system[END_REF]. The correlation line is defined as ε Hf (OIB) = 1.33ε Nd + 3.19 (where OIB is ocean island basalt). Hf T DM was calculated et al., 2013). Our data (Chmyz et al., 2016, submitted et al., 1995). Recent studies support the view that metasomatic pyroxenitic clinopyroxene is more likely to represent the main source of negative εHf than peridotitic clinopyroxene or garnet [START_REF] Pearson | Re-Os and Lu-Hf isotope constraints on the origin and age of pyroxenites from the Beni Bousera peridotite massif: implications for mixed peridotite-pyroxenite mantle sources[END_REF][START_REF] Choukroun | Hf isotopes of MARID (mica-amphibole-rutile-ilmenite-diopside) rutile trace metasomatic processes in the lithospheric mantle[END_REF], which is coherent with the information provided by the in-situ trace element analyses on the clinopyroxene in the Jacupiranga clinopyroxenites (Chmyz et al., submitted manuscript).

The majority of the rocks from the Heterogeneous Zone plot close to or just below the mantle array in the εHf vs. εNd diagram, whereas clinopyroxenites, ijolite, and dunite plot above that line, with ΔεHf values more positive than 3. Negative ΔεHf values are thought to be a characteristic of SCML [START_REF] Davies | Trace element and Sr-Pb-Nd-Hf isotope evidence for ancient, fluid-dominated enrichment of the source of Aldan Shield lamproites[END_REF], since this reservoir has been largely

affected by metasomatic trace element enrichment and remained isolated for billions of years [START_REF] Pearson | The age of continental roots[END_REF]. Melts in equilibrium with a garnet-bearing residua show greater Lu/Hf fractionation than Sm/Nd. Therefore, over long periods of time (> 1 Ga), their crystallization product will evolve to isotopic compositions below the mantle array (i.e. negative ΔεHf values). To date, highly metasomatized mantle xenoliths (i.e. MARID suite) yield f Sm/Nd and f Lu/Hf values able to produce negative ΔεHf values over time (e.g. [START_REF] Nowell | Hf isotope systematics of kimberlites and their megacrysts: new constraints on their source regions[END_REF].

Therefore, the combined Nd-Hf isotope data on most of the Jacupiranga samples are coherent with a SCLM source metasomatized by melts derived from the garnet stability field.

On the other hand, even when considering that the data used to define the mantle array have significant scatter values, the positive ΔεHf values of the Jacupiranga rocks are out of the range of modern oceanic basalts (e.g. [START_REF] Vervoort | Relationships between Lu-Hf and Sm-Nd isotopic systems in the global sedimentary system[END_REF]. Those ΔεHf positive values may be suggestive of a slightly higher contribution of a garnet peridotite source for those rocks, as peridotitic clinopyroxene and garnet are both characterized by more radiogenic 176 Hf/ 177 Hf [START_REF] Carlson R | Timing of Precambrian melt depletion and Phanerozoic refertilization events in the lithospheric mantle of the Wyoming Craton and adjacent Central Plains Orogen[END_REF][START_REF] Ionov | Hf isotope compositions and HREE variations in off-craton garnet and spinel peridotite xenoliths from central Asia[END_REF][START_REF] Simon | The origin and evolution of the Kaapvaal cratonic lithospheric mantle[END_REF].

Supplementary material -Table A1 Tabela A4 -Composição química (porcentagem peso) de cristais de anfibólio das rochas do Complexo de Jacupiranga. Tabela A5 -Composição química (porcentagem peso) de cristais de feldspato das rochas do Complexo de Jacupiranga. Fórmula estrutural calculada na base de 32 oxigênios. Abreviações: MDIO, meladiorito; MON, monzonito.