Agpaitic Alkaline Rocks in Southern Brazilian Platform: A Review

Abstract

General information is presented on ten agpaitic occurrences located in southern Brazil and at the border between Brazil and Paraguay. All the Brazilian agpaitic rocks are Late Cretaceous in age, whereas the Paraguayan ones are older than Early Triassic. The most significant occurrence is Poços de Caldas, the largest alkaline massif in South America. In general, these agpaitic rocks contain mineral assemblages that indicate presence of typical halogen-bearing Na–Ca–HFSE phases, eudialyte-, rinkite- and wöhlerite-group minerals being the most frequent ones. However, these associations are indeed more complex in terms of composition, with accessory phases in some cases consisting of various minerals, including U–Th oxides/silicates, Nb oxides, REE–Sr–Ba bearing carbonates–fluorocarbonates–phosphates–silicates and Zr–Na rich silicates. They usually form late magmatic stage to hydrothermal/deuteric assemblages linked with coarse and fine-grained, mainly silica-undersaturated evolved rocks. Data also indicate significant differences in type, amount and composition of agpaitic minerals in all investigated occurrences.

1. Introduction

Agpaitic rocks are defined by the IUGS Subcommission on the Systematics of Igneous Rocks as peralkaline nepheline syenites (and phonolites) characterized by complex Zr and Ti minerals, such as eudialyte and rinkite, rather than simple minerals such as zircon and ilmenite [1,2]. This term was first proposed by [3] to describe rocks from Ilímaussaq complex with a peralkaline index greater than 1.2 and its definition has undergone considerable change since its first introduction [4,5,6]. Recently, [7] proposed that the term “agpaitic rocks” should be used as descriptive terms to distinguish igneous rocks according to their primary magmatic HFSE mineralogy, irrespective of their whole-rock composition.

Agpaitic and miaskitic types can be identified via mineralogy which changes from one type to another [1,7,8]. On this basis, according to [7], the miaskitic types characteristically contain zircon, baddeleyite and titanite, whereas the agpaitic types contain aenigmatite, astrophyllite, eudialyte, lamprophyllite, F-disilicates, and wadeite. In addition, a detailed distinction between “normal” miaskitic variants and low, medium and highly agpaitic up to hyperagpaitic types, depending on the presence of diagnostic minerals, was previously proposed by [9].

This peculiar mineralogy is related to large presences of specific elements, such as Large Ion Lithophile Elements (LILE, such as Li, Na, K and Rb), halogens (F, and Cl), Rare Earth Elements (REE, the lanthanides) and High Field Strength Elements (HFSE, such as Zr, Ti, Nb and U–Th) [8]. Examined in more mineralogical detail, these mineral assemblages correspond to different types of silicates, mainly eudialyte and F-disilicates (rinkite and wöhlerite groups), but they can also involve a wide variety of other species, such as HFSE oxides, REE–Sr-rich phosphates, carbonates, and REE–F carbonates [8,10,11]. Mineral assemblages may also be characterized by the enrichment of major mafic constituents in alkali and iron and by the presence of accessory minerals with high concentrations of Na and Ca in their composition, as suggested by some F-disilicates (e.g., rosenbuschite, wöhlerite). These mineral associations, which are occasionally distinguished by a high content of volatile components (e.g., CO₂, F, Cl and H₂O), also include sodic and ferric varieties of clinopyroxene and amphibole. Late minerals are not only associated with deuteric stages of crystallization resulting from interactions among water-rich solutions during the cooling of the same magmatic body, but also with mineralizing fluids that percolate through the crystallizing body, leading to the formation of accessory fluorocarbonates and hydrate carbonates.

Agpaitic mineral assemblages are thought to originate from crystallization of residual magmatic liquids rich in very distinctive elements, such as REE, HFSE, LILE, and volatiles (F, Cl). These assemblages may preferentially form in the late-magmatic and hydrothermal/deuteric stages, as indicated by textural evidence (

Table 1. General information on agpaitic occurrences.

	Massif	Age (Ma)	Agpaitic Bodies	Agpaitic Assemblage	Main References
1	Poços de Caldas	79–87 (Ar-Ar, K-Ar)	phonolite stocks	late-magmatic	[12,13,14]
			lujavrite and khibinite lopoliths	main to late-magmatic
2	Itatiaia	67.5–71.3 Ma (U-Pb)	ring-like nepheline syenite and phonolite bodies	late-magmatic	[15,16,17]
3	Passa Quatro	67–77 Ma (K-Ar, Rb-Sr)	ring-like and plug-like nepheline syenite and phonolite bodies	late-magmatic	[18,19,20]
4	Bom Repouso	76.5–78.8 Ma (Ar-Ar)	phonolite plugs	late-magmatic	[21,22]
5	Búzios Island	≈78 Ma (Rb-Sr)	thin phonolite dikes	main to late-magmatic	[23,24]
6	Monte de Trigo Island	86.6 (Ar-Ar)	thin nepheline microsyenite dikes	main to late-magmatic	[25,26]
7	Itapirapuã	102 Ma (Ar-Ar)	thin phonolite dike	main to late-magmatic	[27,28]
8	Lages	76–82 Ma (Rb-Sr, K-Ar)	phonolite sill	late-magmatic	[29,30,31]
9	Cerro Siete Cabezas	244–249 Ma (K-Ar)	nepheline syenite stock	late-magmatic to deuteric	[32,33,34]
10	Cerro Boggiani	241–248 Ma (K-Ar, Ar-Ar)	phonolite lava flow	late-magmatic to deuteric	[32,33,34]

).

Agpaitic assemblages commonly derive from miaskitic peralkaline igneous rocks of foid syenite composition (mainly nepheline syenites and their fine-grained varieties) formed during final magma differentiation stages [7,8]. The petrological evolution of agpaitic rocks, and their associated eudialyte-group minerals, F-disilicates, astrophyllite-group minerals or aenigmatite crystallization, depends upon peralkalinity, silica, chlorine, fluorine, water activities and fO₂ [7,10,35]. The processes by which agpaitic mineral assemblages are formed can be also responsible for unusual and exotic suites of interstitial minerals of different classes, mostly of highly complex chemical composition. Thus, some agpaitic occurrences are marked by an unusually large number of rare minerals, such as Lovozero and Khibina with over 500 identified minerals [9] and Mont Saint-Hilaire with approximately 250 minerals [8].

One of the most remarkable characteristics of the Mesozoic–Cenozoic alkaline magmatism that took place in the southern portion of the Brazilian platform is the abundance of more evolved rock-types [14,15,19,20,36,37,38,39,40,41]. Silicate alkaline rocks, the most abundant petrographic type present, include evolved nepheline syenites and syenites and their corresponding fine-grained varieties, forming large isolated, unique or composite intrusions or even multiple plutons. Main examples of these massifs are Poços de Caldas [14,42] and Itatiaia [15,43]. A small fraction of these evolved lithologies consists of agpaitic types, such as lujavrites (melanocratic—in this case, M > 30 vol.%—agpaitic variety of nepheline syenite rich in eudialyte, arfvedsonite and/or aegirine with a laminated structure), khibinites (a variety of eudialyte–nepheline syenite with aegirine, alkali amphibole and many accessory minerals, particularly those containing Ti and Zr) and eudialyte/aenigmatite phonolites [12,14,20,26]. However, the amount of information available on the exotic accessory assemblage found in these agpaitic rocks is still limited. In this paper, we present a general overview of the main agpaitic alkaline rocks of the southern Brazilian platform and the current knowledge of their exotic accessory mineralogy.

2. Alkaline Magmatism in Southern Brazilian Platform: Background Information

The abundance of alkaline rocks in Brazilian and Paraguayan territories is attested by over two hundred occurrences [44,45]. Subordinately, alkaline types are also present in Bolivia and Uruguay. They are found mainly in and around sedimentary formations of the Paraná and Bauru basins, with their emplacement controlled by regional tectonic factors [46,47] (Figure 1). In Brazil, alkaline centers occur predominantly dispersed over the eastern flanks of the country, but also as several individual bodies along two very distinct NE and NW trends that extend for many kilometers [47,48]. The first trend, which corresponds to the Serra do Mar province, consists of inland and island intrusions parallel to the coasts of São Paulo and Rio de Janeiro (Figure 2). The second trend includes occurrences located in inner portions of the country, forming two distinct groups in the states of Minas Gerais (Alto Paranaíba province) and Goiás (Goiás province), respectively. Some Brazilian carbonatite complexes of the first group, such as Araxá and Tapira, are of economic importance, having been exploited for niobium and phosphate in carbonatites. Poços de Caldas, the largest alkaline massif in South America, is tectonically related to the Cabo Frio Magmatic Lineament, a curved, 1150 km long WNW-ESE-trending feature [47]. Other Brazilian alkaline occurrences are distributed along a prominent NW-trending alignment, the Ponta Grossa arch [49]. Only two alkaline carbonatite complexes occur in southern Brazil, to the west of Florianópolis, being tectonically related to the Anitápolis-Lages lineament in the state of Santa Catarina [50] and the phonolitic volcanism of Piratini, which is associated with the Rio Grande structural feature [51]. In Paraguay, alkaline magmatism is concentrated mainly in the central-eastern part of the country, where a complex NW- to EW-oriented structure, the Asunción rift, controls several such intrusions [52]. This magmatism is also represented by occurrences within domains of the NE-trending Ponta Porã arch in the northeastern part of the country, the Amambay region [53,54], and, less frequently, in the southernmost areas in close relation to the NW-trending Santa Rosa lineament [55]. At the border between Brazil and Paraguay, alkaline bodies follow a narrow NS-trending belt along both margins of the Paraguay River, forming the Alto Paraguay province [32].

The alkaline rocks of the southern portions of the Brazilian platform correspond in age to a wide, approximately 200 Ma interval of magmatic activity pulses recorded from the Mesozoic to the Cenozoic [45]. The oldest events (241 Ma) are related to the intrusions that form the Alto Paraguay province [32], among which are agpaitic rocks of the Cerro Boggiani and Cerro Siete Cabezas stocks (Figure 1; Table 1). Some alkaline occurrences are contemporary to tholeiitic lava flows of the Paraná Large Igneous Province [56,57], with an estimated age of about 130 Ma. However, no typical agpaitic rocks are associated with this age interval. Itapirapuã, located in the Ponta Grossa Arch province, is a small occurrence whose recent radiometric Ar/Ar results confirm its age as falling within a 100–110 Ma interval [28] (Table 1). The magmatic events dated ~70–90 Ma [38,45] are the most abundant and widespread ones, assembling all the remaining Brazilian alkaline centers. They include rock bodies of agpaitic affinity, of which the Poços de Caldas [14,58,59,60,61], Itatiaia [15,40,43], Passa Quatro [19,20], Bom Repouso [21], Monte de Trigo Island [25,62], Lages [63] and Búzios Island [64,65] suites are examples.

In general, alkaline magmatism is characterized by the large number of occurrences in a large variety of igneous forms, yet intrusive forms clearly prevail [38,48]. The more abundant silicate alkaline rocks with agpaitic varieties consist of evolved nepheline syenites and syenites and their fine-grained equivalent types, forming large isolated, unique or composite intrusions, or even multiple plutons. On the other hand, less evolved types are present in minor amounts, mainly as small dikes in several occurrences.

Individual alkaline evolved suites with agpaitic rocks range in area from a few m² to hundreds of km². In addition to Poços de Caldas, which extends over approximately 800 km², other occurrences occupying large areas are the Itatiaia (215 km²) and Passa Quatro (148 km²) massifs. Minor intrusions are the Búzios Island (7.5 km²), Itapirapuã (4 km²), Cerro Siete Cabezas (4 km²), Cerro Boggiani (4 km²), Monte de Trigo Island (1.3 km²) and Bom Repouso (1 km²) suites. In all these intrusions, the occurrences of agpaitic rocks are very subordinated or completely minor relative to other alkaline types.

3. Main Alkaline Massifs with Agpaitic Rocks

Except for the Poços de Caldas massif [42], where extensively outcropping agpaitic rocks form shallow subsurface lopolith bodies that are easily distinguished during fieldwork (e.g., lujavrite-khibinite outcrop of Pedra do Balão, khibinite Botelhos area, Morro do Serrote structure) (Figure 2C), and the irregular phonolitic intrusion of Bom Repouso [21] (Figure 2B), all remaining occurrences are present as minor components, especially compared to miaskitic types, being represented mainly by small bodies (stocks, dikes, sills and plugs) of fine-grained silica-undersaturated microsyenites and phonolites (Table 1). A general description of the main alkaline massifs containing agpaitic rocks is presented below.

3.1. Poços de Caldas

One of the largest alkaline igneous bodies in the world [42], Poços de Caldas intrudes Precambrian rocks, forming an isolated circular complex detached from numerous Late Cretaceous alkaline occurrences of the Alto Paranaíba (to the NE) and the Serra do Mar (to the SE) provinces (Figure 2C). The size of this intrusion (>800 km²) is smaller than Khibina massif (Kola Peninsula, ~1350 km²; [66]) but comparable to that of Lovozero (Kola Peninsula, 600 km²; [66]) and Pilanesberg (South Africa, ~625 km²; [67]). The massif includes dominant phonolites and their subvolcanic and plutonic counterparts (tinguaites and nepheline syenites, respectively), with a presence of strongly agpaitic types (lujavrites and khibinites) that are especially abundant in the northern ring area (Pedra Balão).

Along the western border of the Poços de Caldas complex, there is a depressed area, Vale do Quartel, which consists of pyroclastic products (agglomerates, lapilli, tuffs) and lava flow remnants, mostly of mafic–ultramafic composition. Phlogopite lamprophyric dikes occur in these and other sites, such as in the Osamu Utsumi uranium mine and amidst basement mangerites close to the massif’s border (Minas Pedras quarry), associated with a wide variety of basic–ultrabasic types and scarce carbonatite dikes. Considerable inner portions of the complex have been subject to hydrothermal alteration and brecciation to some extent due to subvolcanic magmatic activity, which led to the formation of different types of mineralization, mainly U, Th, Mo and Zr.

The bulk-rock major and trace element geochemistry of nepheline syenites and phonolites, with the marked presence of eudialyte, F-disilicates, aenigmatite and lamprophyllite, indicates the agpaitic affinity of these highly evolved melts. Unlike other agpaitic intrusions, a most peculiar feature in the Poços de Caldas is the absence of pure miaskitic rocks, because the prevailing nepheline syenites and phonolites are characterized by an assemblage showing the contemporaneous presence of minerals typical of miaskitic (e.g., zircon, baddeleyite and titanite) and agpaitic rocks (such as F-disilicates, eudialyte, aenigmatite and astrophyllite), [14] which are defined as a “transitional agpaitic” type, as proposed by [7]. The Poços de Caldas evolved melts are qualitatively derived from mafic–ultramafic melts via clinopyroxene removal in a prolonged fractional crystallization process. It is observable that the highly evolved melts are formed by removal of potassic alkali feldspar and nepheline associated with very small amounts of “incompatible” element-rich accessory phases [14].

3.2. Itatiaia

Itatiaia alkaline massif, the second largest alkaline occurrence in Brazil, intrudes the Precambrian basement, being overlain by Tertiary sedimentary rocks in some areas. The massif has a roughly ellipsoidal shape, its major, NW-trending axis lying parallel to regional tectonic lineaments of the Ribeira belt. The massif is located in the Serra da Mantiqueira ridge domains near the Passa Quatro and Morro Redondo massifs to the southeast of the Poços de Caldas complex, its terrain reaching altitudes as high as 2792 m at the Agulhas Negras peak, the fifth-highest peak in Brazil. The occurrence has been the subject of several studies [15,36,39,40]. A new geological map of Itatiaia published recently [43] suggests for the massif an evolution from a migratory magmatic center that manifested as ring structures and successive moon-shaped intrusions from SE to NW. Three different sectors are recognized in the Itatiaia alkaline massif based on lithological and geomorphological characteristics: a southeastern, a central, and a northern one. The southeastern sector consists of miaskitic to agpaitic nepheline syenites that are cut by aphyric to porphyritic dikes of phonolite and trachyte (some of them with pseudoleucites), and nephelinites. The central sector, which forms a ring-like structure, consists of most of the same lithologies plus silica-oversaturated rock types (pulaskites, nordmarkites and quartz-alkali feldspar syenites) in its inner portions. A small intrusive body of alaskite occurs near the center of the ring. The northern sector includes nepheline syenites and nordmarkites, and locally cumulatic melagabbro and biotite monzonite. The mineralogy, including peralkaline syenites and silica-oversaturated rock types, is characterized by the presence of variable F-disilicates and numerous accessory phases bearing HFSE and REE [40].

3.3. Passa Quatro

Similarly to the Poços de Caldas and Itatiaia occurrences, the Passa Quatro massif, which reaches altitudes as high as 2797 m [68], is conditioned by the WNW-ESE-trending Cabo Frio alignment, a prominent structural feature that affects several alkaline intrusions in southern Brazil [39]. The massif also takes in part of the Serra do Mar province, which assembles the two abovementioned Late Cretaceous occurrences, lying mostly across the central portions of the lineament area. In plan view, it appears as a subcircular unit intruded into the Precambrian basement. Field relationships with host rocks are only observed at a few sites due to the presence of a large detrital talus and polymictic breccia bodies [19]. The massif is mainly composed of strongly undersaturated felsic intrusive (nepheline syenites and alkali syenites) and subvolcanic rocks (phonolites) forming small, dominantly NE-oriented dikes. Basic and intermediate lithologies are completely lacking. A noticeable characteristic of the Passa Quatro nepheline syenites and alkali syenites, with minor phonolitic dikes, is the marked presence of accessory minerals of complex and variable composition [20].

3.4. Bom Repouso

Bom Repouso corresponds to a crescent-moon shaped intrusion that forms an irregular, 2.6 km long EW-trending body and two small satellite plugs consisting primarily of silica-undersaturated agpaitic rocks (Figure 2B). Lying 62 km NNW of the Poços de Caldas complex intruding Precambrian granitoid rocks, Bom Repouso has been geologically investigated [21]. Phonolites and porphyritic phonolites are the dominant lithologies. The alkaline rocks are all of sodic composition and agpaitic affinity, with some exceedingly rare accessory minerals including calciohilairite and niobophyllite.

3.5. Búzios Island

In the state of São Paulo, Brazil, alkaline coastal islands include São Sebastião, the largest island encompassing three isolated syenitic stocks (São Sebastião, Serraria and Mirante), Búzios and Vitória to the northeast, and Monte do Trigo massif to the west. All these islands follow a NE trend that is tectonically related to the Southeastern Brazilian Continental Rifting [47]. Similarly to the previously mentioned alkaline centers, these coastal islands also take in part of the Serra do Mar province. Búzios Island corresponds to an alkaline body of irregular shape lying approximately 30 km from the continent [64,65]. In its NW and SW sectors, the stock is emplaced into Precambrian basement rocks, namely charnockites and, subordinately, gneisses and amphibolites. The stock consists principally of syenitic rocks cut by numerous dikes, most of them NE-trending ones. The dikes consist of two distinct suites. The first, felsic, of variable composition, ranges from silica-undersaturated (nepheline/sodalite microsyenites and sodalite phonolites) to silica-saturated (microsyenites and trachytes), the most widespread rocks across the island, and silica-oversaturated (rhyolites) types. The second suite is mafic–ultramafic in composition, consisting of different alkaline petrographic types (alkali basalts, basanites, tephrites, trachybasalts and lamprophyres). A primary assemblage of mostly silicate minerals bearing Zr, Ti, Nb and REE, and rare, chemically complex post-magmatic phases is identified in association with nepheline (sodalite) microsyenite and phonolite dikes of agpaitic affinity [65].

3.6. Monte de Trigo Island

Monte de Trigo is a small, ellipse-shaped alkaline stock located approximately 10 km from the coastline (Barra do Una beach). The stock intrudes Precambrian gneissic and migmatitic rocks of the Ribeira belt [25], being morphologically conditioned by N40W and N50E lineaments. Upon systematic investigation of the stock [25] it has been proposed that the development of this occurrence involved four distinct episodes of magmatic activity. A cumulate mafic–ultramafic association is thought to correspond to the oldest event, predominantly showing nepheline-bearing olivine melagabbros and melatheralites and their fine-grained varieties together with clinopyroxenites and olivine clinopyroxenites. An intrusive breccia pipe of about 50–60 m in diameter showing fragments derived from the mafic–ultramafic body and from the Precambrian country-rocks corresponds to the second magmatic event. The third magmatic event is represented by a miaskitic nepheline to nepheline-bearing alkali feldspar syenite stock in genetical association with nepheline microsyenite dikes of miaskitic and agpaitic affinity cutting all the previously described rock types. The last magmatic event corresponds to the intrusion of a series of porphyritic dikes of aphanitic groundmass whose composition varies from lamprophyre to phonolite. Agpaitic nepheline microsyenite dikes, the less frequent types, are thought to have crystallized from a more evolved magma fraction than the miaskitic dikes. These types are characterized by the presence of several exotic phases, such as eudialyte- and wöhlerite-group minerals [26].

3.7. Itapirapuã

Itapirapuã is a small alkaline stock of irregular NW-trending shape composed of silica-undersaturated rocks, melanite-bearing and melanite-free nepheline syenites, and subordinate mafic types (biotite melteigites, malignites) [27]. Decimetric, mainly NW-oriented phonolite (tinguaite) dikes cut both the intrusive body and the granitic country-rocks. Centimetric carbonatite veins penetrate the nepheline syenites. Magmatic breccia extending over a small area is also present at the southern part of the intrusion. Iron ore, chiefly consisting of idiomorphic magnetite, had been exploited in the area several years ago. Eudialyte-group minerals are described in association with peralkaline syenitic dikes [27].

3.8. Lages

Extending across 2100 km² and emplaced into sedimentary Gondwanic sequences, the alkaline-carbonatitic district of Lages, which is limited to the west by the Paraná flood basalts, is related to the uplift of a large crustal block, the Lages Dome [29]. The alkaline rocks display hypabyssal forms and the volcanic intrusions follow a ring-shaped distribution dispersed as relatively small outcrops over a vast region. They are assembled into four main groups: carbonatites and associated rocks, pipe breccias and kimberlites, ultrabasic rocks, and leucocratic rocks [30,50]. Carbonatites occupy the northern sector of the dome, with Fazenda Varela, a 20 m wide tabular body, as their main exposure area. Kimberlites are found at a variety of sites. Diatremes and pipe breccias (tuffisitic breccias) are also known to exist. Ultrabasic rocks occur as dikes of variable dimensions and compositions (olivine melilitite, olivine nephelinite, basanite). Minor dikes of phonotephrite and trachyphonolite are also present. Leucocratic terms prevail over other rock types, corresponding to approximately 50 km² of the total outcropping area, represented by peralkaline and porphyritic peralkaline phonolites and nepheline syenites. Agpaitic minerals are associated with peralkaline phonolites at Fazenda Nova do Tributo, an area in the central portion of the alkaline district [30].

3.9. Cerro Siete Cabezas

Cerro Siete Cabezas represents the southernmost alkaline occurrence of the Alto Paraguay province. The complex is circular in shape, with a central depression evidencing cauldron subsidence, being related to two minor satellite bodies [32]. Cerro Siete Cabezas rises up to 158 m above the alluvial plain of the Paraguay River, consisting mainly of medium to coarse-grained silica-undersaturated syenitic rocks. The satellites are characterized by a more variable composition, with prevalence of quartz-bearing varieties in stock I and the presence of both silica-undersaturated and silica-oversaturated syenitic types in stock II. The authors of [32] report eudialyte as a common accessory mineral in nepheline syenites within the main body of the complex.

3.10. Cerro Boggiani

The northernmost alkaline center along the Paraguay River, the rounded-shape intrusion of Cerro Boggiani is part of a series of major complexes and some minor stocks, lava flows and dikes that constitute the Early Triassic Alto Paraguay province, the oldest magmatic activity around the Paraná basin [32]. The intrusion consists of monadnocks that crop out above alluvial sediments of the Paraguay River, the largest intrusion forming a small, 0.5 km diameter hill lower than 150 m [34]. The complex mainly consists of sodalite syenites and nepheline syenites, with modal nepheline and sodalite contents of 16–28% and 8–17%, respectively. The extrusive rocks (lava flows and dikes) are phonolitic in composition. The Cerro Boggiani rocks show a late-stage magmatic to hydrothermal/deuteric mineralogy with several unusual accessory phases [34,69,70,71,72].

4. Main Features of Agpaitic Rocks

4.1. Rock-Forming Minerals

Data on rock-forming minerals were compiled from previous works [14,20,21,33,40,62,65]. The dominant mineral assemblage of the agpaitic rock types includes alkali feldspar and nepheline for the silica-undersaturated varieties and alkali feldspar and quartz for the silica-oversaturated varieties. These rocks are mostly leucocratic, with clinopyroxene and amphibole as the main mafic phases. Alkali feldspar with perthitic to mesoperthitic exsolution lamellae is the most abundant mineral. Plagioclase is very scarce, usually with a low anorthite content. Feldspathoids consist mainly of nepheline and, subordinately, sodalite, reaching high modal amounts in some occurrences (e.g., 42% in Cerro Boggiani). Clinopyroxene varies in composition, mainly from aegirine–augite to aegirine (predominant). Zoning is a common feature of the clinopyroxenes, as indicated by chemical and optical evidence. The normal zoning points to enrichment in Fe and Na content towards the crystal rims, frequently accompanied by corresponding variations in pleochroism, from light green to dark green. Amphiboles mainly present sodic compositions, including riebeckite, arfvedsonite and Mg-arfvedsonite, sometimes occurring as late-stage poikilitic crystals, partially or totally associated with clinopyroxenes.

Clinopyroxene, present not just in agpaitic varieties but also in the main rocks of the studied alkaline massifs, is considered an important monitor of the degree of magmatic evolution [14,20,27,39]. The main trends, considering the differentiation of the entire massifs, indicate compositions varying from diopside to hedenbergite to aegirine–augite and finally to aegirine (Figure 3), characterizing progressive enrichments in Fe³⁺ and Na for the formation of agpaitic rocks. The main trends for Poços de Caldas, Itatitaia, Passa Quatro, Cierro Siete Cabezas, Cerro Boggiani, Itapirapuã, amphibole-free rocks from Búzios, and part of the peralkaline phonolites from Lages are very similar. The clinopyroxene of Monte de Trigo and part of Búzios Island matches present compositional variations partially controlled by amphibole crystallization, with initial extensive evolution in the diopside–hedenbergite series; on the other hand, some peralkaline dikes from Lages do not present significant Fe²⁺ enrichment prior to Na⁺ increase. Poços de Caldas, Bom Repouso and Passa Quatro aegirines present high amounts of Zr (up to 3 wt% and 1.73 of ZrO₂ in Passa Quatro and Bom Repouso, respectively), especially for agpaitic varieties [20,21,73], whereas in Itatiaia clinopyroxenes Zr is very low [40]. The incorporation of Zr contents in clinopyroxene could have an important influence in the assemblage of rare accessory minerals [11].

4.2. Geochemical Characteristics

The peralkaline varieties of the main massifs of this study share important geochemical fingerprints, summarized in

Table 2. Whole rock geochemical characteristics of peralkaline varieties from the studied massifs. Souces: 1. [14], 2. [15,40]; 3. [19]; 4. [21]; 5. [65]; 6. [26]; 7. [27,74]. * just one sample for La and Ce values; 8. [75]; 9. and 10. [32].

	1. Poços de Caldas	2. Itatiaia	3. Passa Quatro	4.Bom Repouso	5. Búzios Island	6. Monte de Trigo Island	7. Itapirapuã	8. Lages	9. Cerro Siete Cabezas	10. Cerro Boggiani
	n = 95	n = 17	n = 29	n = 32	n = 4	n = 3	n = 11	n = 6	n = 22	n = 19
Peralk. Index	1.01–1.37	1.0–1.15	1.01–1.13	1.03–1.2	1.11–1.24	1.04–1.08	1.0–1.15	1.01–1.22	1.0–1.2	1.07–1.51
TiO2 (wt.%)	0.18–1.24	0.29–0.92	0.12–0.66	0.22–0.37	0.09–0.38	0.12–0.28	0.37–1.5	0.1–0.38	0.39–1.28	0.17–0.63
Na2O (wt.%)	6.73–11.06	6.4–10.11	6.23–10.48	7.88–11.51	8.44–11.04	7.8–10.98	5.38–11.3	9.2–11.9	7.08–10.37	9.65–13.17
Zr (ppm)	332.1–4521.70	319–1680	274–3953	1359–2366	1089–5045	969–2672	150–870	310–1840	348–1194	717–7847
Nb (ppm)	86–626	95–422	71–600	325–594	221–1211	182–383	25–630	46–626	95–199	71–653
Y (ppm)	11–178	26–65	26–69	33.4–101.3	44–229	36.4–73.7	11–280	7.3–45.3	28–65	9–85
La (ppm)	8.3–516	107–335	93.5–325.5	102–463	33–627	42.6–157	62 *	21.3–175	45–156	28–216
Ce (ppm)	15.3718	211–594	122.3–530.7	228–817	64–881	130–276	96 *	42–287	111–233	38–309

, mainly presenting a typical sodic affinity and high levels of Zr (up to 7847 ppm in Cerro Boggiani), Nb (up to 1211 ppm in Búzios Island), and variable REE contents, with the light ones displaying higher concentrations (La and Ce, predominantly). They also present very low MgO, Cr, Ni and V values. Poços de Caldas is the best-known agpaitic occurrence in the Brazilian platform, with higher values in the peralkaline index (PI up to 1.37; [14,42]). No significant Eu anomaly (Eu/Eu* = Eu_N/(Sm_NxGd_N)^0.5 = 1.0–1.1) is recorded in Poços de Caldas nepheline syenites and phonolites [14]. The peralkaline Itatiaia rocks correspond predominantly to varieties of strongly undersaturated nepheline syenites (ne-normative > 20%; [15,40]. The Passa Quatro peralkaline suite includes silica-undersaturated lithotypes, represented mainly by nepheline syenites and alkali syenites, with minor phonolitic dikes with a high degree of incompatible element enrichment, especially Zr and Nb [20]. The Bom Repouso occurrence is represented by felsic silica-undersaturated rocks of phonolitic composition forming the main body and the two small satellites, with high ne-normative contents (7.5–28.8%) being the highest values related to the satellites [21]. In the Búzios island suite, peralkaline phonolitic dikes are the exception in a dominant potassic association of miaskitic affinity [65]. The peralkaline rocks of Monte de Trigo occur as agpaitic nepheline microsyenite dikes of highly variable mineralogy, found only at a few sites within the massif, mainly intrusives in melatheralites, and present high ne- and ac-normative contents [26]. For Itapirapuã massif [27,74], agpaitic compositions are found for some nepheline syenites and a phonolite dike with higher peralkaline index values. Itatiaia, Passa Quatro, Bom Repouso and Monte de Trigo peralkaline rocks present strong light to heavy REE fractionation and significant negative spikes for Eu. The normative composition of Lages peralkaline phonolites are characterized by the abundance of nepheline and a great amount of acmite; almost all samples of this occurrence lack a negative Eu anomaly [75]. The peralkaline varieties from the Cerro Siete Cabezas (associated with the main intrusion and formed by silica-undersaturated syenitic rocks) and from the Cerro Boggiani (formed by fine- and coarse-grained silica-undersaturated varieties) are between trachytic and phonolitic minima in the petrogenetic residual diagram; the Eu negative anomaly is considered a peculiar feature in all complexes of the Alto Paraguay Province, including Cerro Siete Cabezas and Cerro Boggiani [32].

4.3. Mineral Resources

Poços de Caldas is the most important agpaitic occurrence in the Brazilian platform in terms of mineral deposits associated with fine-grained nepheline syenitic rocks (tinguaites and phonolites). These intensely fractured rocks were modified by hydrothermal and weathering processes, especially in the central-eastern area of the massif. U–Mo–Zr (Usamu Utsumi or Cercado mine, decommissioned in 1995), Mo–U–Zr (Agostinho deposit) and Th–REE–Nb (Morro do Ferro deposit) deposits have been intensively exploited from Poços de Caldas rocks [76]. Most of the active exploration sites associated with hydrothermal altered rocks were decommissioned in the 1980s, including the Zr mine and “garimpo” [42]. Bauxite (laterite with 80–90 wt% Al₂O₃, in anhydrous basis) mines and deposits, mainly related to the tinguaite ring-dike, have been explored in many localities in inner parts of the plateau, particularly around the city of Poços de Caldas [76]. Bauxite mines and deposits are also present in Bom Repouso [21]. Small local economically unimportant deposits of bauxite are also known to be present in inner parts of the Passa Quatro massif [77].

5. Rare Accessory Minerals of Agpaitic Rocks

Several rare and exotic mineral phases occur in agpaitic rocks as a result of their crystallization from highly evolved magmas that are enriched in HFSEs and other incompatible elements and halogens. In agpaitic rocks, defining the mineral assemblages is not too easy: they can be subdivided into the early magmatic (±liquidus), late-stage, and hydrothermal/deuteric assemblages. Generally, in the compared intrusions, the early magmatic assemblages are made up of alkali feldspar, nepheline and pyroxene followed by opaque oxides ± fluorite ± sodalite. The late-stages are mainly related to the crystallization of F-disilicates (rinkite- and wöhlerite-groups) ± eudialyte ± aenigmatite ± lamprophyllite; the replacement (hydrothermal/deuteric) assemblages are pectolite, catapleiite, and so on until reaching alteration assemblages (Table 1 and

Table 3. HFSE accessory mineralogy of agpaitic rocks.

Silicates	Mineral Name	Chemical Formulae *	Occurrence
Nesosilicates	Coffinite	U(SiO4)·nH2O	PC
	Thorite	(Th,U)(SiO4)	CB, IT
Disilicates	Fersmanite	Ca4(Na,Ca)4(Ti,Nb)4(Si2O7)2O8F3	PC
	Götzenite	Ca4NaCa2Ti(Si2O7)2(OF)F2	PC
	Hainite	(Ca3Y)Na(NaCa)Ti(Si2O7)2(OF)F2	IT, PC
	Hiortdahlite	Na2Ca4(Ca0.5Zr0.5)Zr(Si2O7)2OF3	BI, IT, MTI, PQ
	Kochite	Ca2MnZrNa3Ti(Si2O7)2(OF)F2	BI
	Lamprophyllite	(SrNa)Ti2Na3Ti(Si2O7)2O2(OH)2	BI, L, PC
	Låvenite	(NaCa)4(Mn2+,Fe2+)2(Zr,Ti,Nb)2(Si2O7)2(O,F)4	BI, CB, IT, L, MTI, PQ
	Mosandrite-(Ce)	(Ca3REE)[H2O)2Ca0.5□0.5]Ti(Si2O7)2	BI, CB, PC
	Normandite	Na2Ca2(Mn,Fe)(Ti,Nb,Zr)2(Si2O7)2O2F2	CB, PC, PQ
	Rinkite-(Ce)	(Ca3REE)Na(NaCa)Ti(Si2O7)2(OF)F2	IT, PC, PQ
	Rosenbuschite	Ca6Zr2Na6ZrTi(Si2O7)4(OF)2F4	BI, CB, IT, PQ
	Wöhlerite	Na2Ca4Zr(Nb,Ti)(Si2O7)2(OF)4	BI, CB, IT, MTI, PQ
Cyclosilicates	Catapleiite	Na2Zr(Si3O9)·2H2O	BR, CB, IT, L, MTI, PC, PQ
	Eudialyte	Na15Ca6Fe3Zr3Si(Si25O73)(O,OH,H2O)3(Cl,OH)2	BI, BR, CB, CSC, L, MTI, PC, PQ
	Ferrokentbrooksite	Na15Ca6Fe3Zr3Nb(Si25O73)(O,OH,H2O)3(F,Cl)2	PC
	Gaidonnayite	Na2Zr(Si3O9)·2H2O	PC
	Georgechaoite	NaKZr(Si3O9)·2H2O	PC
	Hilairite	Na2Zr(SiO3)3·3H2O	PC
	Manganoeudialyte	Na14Ca6Mn3Zr3[Si26O72(OH)2](H2O,Cl,O,OH)6	PC
	Kentbrooksite	(Na,REE)15(Ca,REE)6Mn3Zr3Nb(Si25O73)(O,OH,H2O)3(F,Cl)2	MTI, PC, PQ
	Wadeite	K2ZrSi3O9	PC
Inosilicates	Aenigmatite	Na4(Fe2+10Ti2)O4(Si12O36)	BI, BR, CB, IT, PC
	Astrophyllite	K2NaFe2+7Ti2(Si4O12)2O2(OH)4F	BI, BR, CB, L, PC, PQ
	Calciohilairite	CaZrSi3O9·3H2O	BR, PC
	Kupletskite	K2NaMn2+7Ti2(Si4O12)2O2(OH)4F	IT, PQ, PC
	Lorenzenite	Na2Ti2O3(Si2O6)	PC
	Narsarsukite	Na4(Ti,Fe)2(Si8O20)(O,OH,F)2	PC
	Niobophyllite	K2NaFe2+7(Nb,Ti)2(Si4O12)2O2(OH)4(O,F)	BR
	Pectolite	NaCa2Si3O8(OH)	BR, ITp, L, PC, PQ
	Serandite	NaMn2+2Si3O8(OH)	BR, L, PC
	Elpidite	Na2ZrSi6O15·3H2O	PC
Phyllosilicates	Neptunite	KNa2LiFe2+2Ti2Si8O24	BR, L, PC
	Tuperssuatsiaite	Na2(Fe3+, Mn2+)3Si8O20(OH)2·4H2O	PC

Abbreviations: BI, Búzios Island; BR, Bom Repouso; CB, Cerro Boggiani; CSC, Cerro Siete Cabezas; IT, Itatiaia; ITp, Itapirapuã; L, Lages; MTI, Monte de Trigo Island; PC, Poços de Caldas; PQ, Passa Quatro. Chemical analyses for most minerals are reported from the following sources: BI [24,65]; BR [21]; CB [32,34,69,70,71,72]; CSC [32]; IT [40]; L [30,50]; MTI [26,62]; PC [14,42,78,79,80,81,82,83,84,85,86,87]; PQ [20]. Notes: □, means vacancy in the site; *, according to IMA.

). Among these mineral species, aenigmatite and eudialyte-, rinkite- and wöhlerite-groups are the most abundant and characteristic ones, with

Table 4. Disilicate compositions.

	Hainite				Hiortdahlite						Lamprophyllite				Låvenite
	PC				BI	IT		MTI	PQ		PC				BI	CB	IT	MTI	PQ
Sample	PC 1 *	PC 2 **	PC 1a	PC 1b	167A2	IT60	IT111	mtr04c	PQ12C	PQ41	PC1	PC2 (P7 391)	PC 1c	PC 1d		RP4	IT54	Mtr01h	PQ42	PQ1
wt%
SiO2	31.44	31.7	31.85	31.54	29.37	30.53	31.35	29.25	29.6	30.3	30.87	28.55	30.88	30.34	28.36	30.95	30.88	29.31	31.1	29.2
TiO2	9.83	9.39	9.17	8.80	0.4	0.95	6.98	0.56	0.96	1.02	29.06	27.82	26.74	27.56	2.94	4.37	6.1	3.74	8.43	6.16
ZrO2	2.33	2.84	7.09	5.21	17.51	17.76	16.78	17.62	16	17.1					27.23	27.76	20.82	26.89	16.5	19.6
HfO2			0.00	0.01	0.34			0.31							0.29			0.26
Al2O3	0.04	0.05	0.11	0.12	0.003			<0.01	0.08		0.23	0.15	0.26	0.24	<0.02		0.26	<0.01	0.09	0.11
Nb2O5	0.82	1.06	1.25	1.45	3.03	3.06	0.44	3	1.66	2.15	0.48	0.89	0.77	0.82	5.22	2.1	2.93	2.95	2.88	4.11
Ta2O5					0.17			0.23										0.05
MnO	0.92	0.68	1.79	1.91	2.45	2.07	1.5	1.4	3.74	2.83	5.23	6.97	4.66	4.31	5.66	6.09	6.16	4.23	9.66	8.37
MgO	0.03	0.04	0.02	0.02	<0.02	0.08		0.15	0.19		0.3	0.04	0.51	0.35	0.05	0.11	0.43	0.61	0.17	0.02
FeO	0.75	0.81	0.54	0.64	1.11	0.82	0.5	1.18	1.32	1.22	1.59	1.09	2.83	2.78	4.55	2.82	4.75	3.87	4.08	4.15
CaO	36.03	34.77	30.97	31.91	27.48	31.24	27.87	29.39	30.5	31.5	0.52	0.06	1.08	0.95	8.09	12.7	14.89	13.24	13.3	11.4
SrO	0.79	0.6	1.43	1.51	<0.04	0.35			0.71	0.11	16.96	13.06	15.79	16.41	<0.04				0.88	0.41
La2O3	1.17	1.2	0.76	1.04	0.22	0.37	0.31	0.12	0.33	0.47	0.04		0.44	0.80	<0.05			<0.01
Ce2O3	1.96	2.86	0.94	1.65	0.64	0.46		0.46	0.87	0.46	0.03		0.22	0.38	<0.09			<0.02	0.06
Pr2O3	0.18	0.27
Nd2O3	0.39	0.81	0.30	0.41	0.25	0.3	0.59	0.33	0.14				0.30	0.45				<0.01
Sm2O3			0.11	0.10			0.31		0.41				0.35	0.41
Y2O3	0.11	0.49	0.11	0.18	1.09			0.97					0.70		0.33			0.39
ThO2	0.11	0.08	0.10	0.12		0.23	0.02		0.03				0.18	0.22			0.34
UO2			0.12	0.14									0.22	0.18
Na2O	6.17	6.74	8.40	7.81	7.54	7.11	9.41	7.84	6.8	7.1	10.99	11.51	11.01	11.03	10.93	8.53	10.35	11.96	10.2	9.99
K2O					<0.02			0.01			0.77	0.82	0.75	0.54	0.03			0.02
BaO													1.30	1.26
H2O	2.43	2.46
F	5.13	5.19	7.02	7.06	6.33	6.33	7.43	8.36	6.94	7.32	0.98	0.61	2.05	1.48	2.97	5.76	5.43	4.97	5.36	5.49
Cl	<0.02	<0.02			<0.03			<0.01							<0.03			<0.01
O=F	2.16	2.18	2.95	2.97	2.66	2.67	3.13	3.52	2.92	3.08	0.22		0.86	0.62	1.25	2.43	2.29	2.09	2.26	2.31
Total	98.47	99.86	99.16	98.73	95.28	99.3	100.4	97.66	97.3	98.8	97.97	94.35	98.49	97.72	95.4	98.77	101.3	100.4	100.4	97.5
apfu
Si	8	8	8	8	8	8	8	8	8	8	8	8	8	8	8	8	8	8	8	8
Ti	1.881	1.782	1.724	1.671	0.082	0.187	1.340	0.115	0.195	0.203	5.664	5.863	5.211	5.475	0.624	0.850	1.189	0.768	1.631	1.269
Zr	0.289	0.349	0.872	0.642	2.326	2.269	2.088	2.350	2.108	2.201					3.745	3.499	2.630	3.579	2.069	2.618
Hf				0.002	0.026			0.024							0.023			0.020
Al	0.012	0.015	0.045	0.050	0.001				0.025		0.070	0.050	0.079	0.076			0.079		0.027	0.036
Nb	0.094	0.121	0.141	0.167	0.373	0.362	0.051	0.371	0.203	0.257	0.056	0.113	0.089	0.097	0.666	0.245	0.343	0.364	0.335	0.509
Ta					0.013			0.017
Mn	0.198	0.145	0.381	0.409	0.565	0.459	0.324	0.324	0.856	0.633	1.148	1.654	1.020	0.965	1.352	1.333	1.352	0.978	2.104	1.942
Mg	0.011	0.015	0.038	0.032		0.031		0.061	0.077		0.116	0.017	0.200	0.139	0.021	0.042	0.166	0.248	0.065	0.008
Fe2+	0.160	0.171	0.131	0.143	0.253	0.180	0.107	0.270	0.298	0.269	0.345	0.255	0.615	0.609	1.073	0.610	1.029	0.883	0.878	0.951
Ca	9.822	9.401	8.295	8.629	8.019	8.770	7.619	8.612	8.831	8.910	0.144	0.018	0.298	0.270	2.445	3.517	4.133	3.872	3.665	3.346
Sr	0.117	0.088	0.209	0.228		0.053			0.111	0.017	2.548	2.122	2.379	2.515					0.131	0.065
La	0.110	0.112	0.083	0.101	0.022	0.036	0.029	0.012	0.033	0.046	0.004
Ce	0.183	0.264	0.086	0.158	0.064	0.044		0.046	0.086	0.044	0.003		0.042	0.076					0.006
Pr	0.017	0.025											0.020	0.048
Nd	0.035	0.073	0.034	0.047	0.024	0.028	0.054	0.032	0.014				0.028	0.041
Sm			0.023	0.025			0.027		0.038				0.031	0.036
Y	0.015	0.066	0.073	0.054	0.158			0.141					0.096		0.050			0.057
Th	0.006	0.005	0.013	0.012		0.014	0.001		0.002				0.010	0.013			0.020
U			0.012	0.016									0.013	0.021
Na	3.044	3.298	4.079	3.825	3.982	3.612	4.655	4.157	3.563	3.634	5.522	6.253	5.522	5.620	5.977	4.275	5.198	6.329	5.087	5.306
K								0.003			0.255	0.293	0.248	0.182	0.011			0.007
Ba													0.131	0.129
OH	4.124	4.141
F	4.128	4.142	5.543	5.639	5.452	5.245	5.995	7.230	5.931	6.111	0.803	0.540	1.677	1.233	2.649	4.708	4.448	4.290	4.360	4.756
	Mosandrite					Normandite						Rinkite			Rosenbuschite
	BI		PC			PQ		PC				PQ	PC		BI		CB	PQ
Sample			PC 1a		PC 1b	PQ42	PQ39	PC1	PC 1c		PC 1d	PQ68	PC 1e	PC 1f				PQ39	PQ42
wt%
SiO2	29.57		27.99		31.55	30.30	31.70	32.90	32.26		31.57	31.30	30.32	30.15	31.08		31.22	31.50	31.60
TiO2	6.10		9.07		9.22	10.40	19.00	19.00	16.83		18.04	8.46	8.79	8.48	6.79		7.63	8.56	8.08
ZrO2	2.44		0.13		1.62	13.30	1.65	1.42	3.70		2.36		1.04	2.15	13.27		14.36	12.10	14.80
HfO2															<0.11
Al2O3	0.07		0.33		1.09	0.09	0.13	0.04	0.07		0.11	0.32	0.10	0.13	<0.02			0.08	0.05
Nb2O5	3.41		2.18		3.55	3.37	1.80	1.83	2.52		1.53		1.31	1.36	2.84		1.25	0.97	0.58
Ta2O5
MnO	0.09		0.26		0.48	11.60	11.10	6.78	8.34		7.02		0.49	0.66	2.12		2.71	4.56	3.75
MgO	<0.02		0.03		0.04	0.13	0.22	0.27	0.19		0.27		0.05	0.01	0.05		0.12
FeO	<0.06		0.15		0.47	4.02	6.13	7.46	7.08		8.69	0.47	0.36	0.31	0.83		0.95	1.22	0.62
CaO	22.16		23.16		26.50	13.60	15.30	17.00	15.61		16.58	27.50	31.98	31.80	25.91		24.09	24.10	24.10
SrO	<0.04		1.40		3.99	0.50	0.41	0.10	0.59		1.06		1.59	2.58	<0.04			0.44	0.45
La2O3	4.86		5.60		6.12	0.13		0.01	0.39		0.08	5.42	3.29	2.55	0.10			0.42	0.36
Ce2O3	10.44		8.88		8.29		0.23	0.02	0.22		0.06	9.49	5.15	4.07	0.38			0.26	0.38
Pr2O3								0.01
Nd2O3	2.55		1.42		1.57	0.26		0.01	0.10		0.25	3.21	1.01	1.11	0.23				0.42
Sm2O3			0.13		0.65				0.25		0.14	0.35	0.13	0.09
Y2O3	1.25		0.11		0.64								0.08	0.15	0.67
ThO2			0.68		1.41				0.07		0.07	0.11	0.29	0.32
UO2			0.34		0.00				0.10		0.10		0.13	0.11
Na2O	8.57		4.27		7.35	9.48	9.56	8.80	9.91		8.73	8.36	7.03	7.01	9.34		9.39	10.60	10.90
K2O	0.05							0.02							0.04
H2O
F	7.02		3.93		5.40	4.46	5.96	3.03	5.46		4.66	5.00	6.48	6.59	5.04		8.16	8.12	7.22
Cl	<0.03														<0.03
O=F, Cl	2.96		1.65		2.28	1.88	2.51	0.68	2.30		1.96	2.10	2.73	2.78	2.12		3.43	3.42	3.04
Total	95.61		88.41		97.96	99.80	100.90	98.01	101.36		99.37	98.50	96.89	96.84	96.56		96.44	99.50	100.30
apfu
Si	8		8		8	8	8	8	8		8	8	8	8	8		8	8	8
Ti	1.241		1.930		1.862	2.065	3.606	3.475	3.130		3.422	1.626	1.741	1.685	1.315		1.471	1.635	1.539
Zr	0.322		0.042		0.221	1.712	0.203	0.168	0.447		0.292		0.181	0.275	1.665		1.794	1.498	1.827
Hf
Al	0.022		0.115		0.314	0.028	0.039	0.011	0.034		0.033	0.096	0.044	0.067				0.024	0.015
Nb	0.417		0.285		0.391	0.402	0.205	0.201	0.282		0.176		0.157	0.162	0.330		0.145	0.111	0.066
Ta
Mn	0.021		0.097		0.109	2.594	2.372	1.396	1.747		1.501		0.129	0.145	0.462		0.588	0.981	0.804
Mg			0.030		0.016	0.051	0.083	0.098	0.071		0.101		0.045	0.018	0.019		0.046
Fe2+			0.062		0.096	0.888	1.294	1.517	1.466		1.834	0.100	0.111	0.079	0.179		0.204	0.259	0.131
Ca	6.423		6.955		7.707	3.847	4.137	4.429	4.136		4.482	7.530	9.005	8.993	7.145		6.613	6.557	6.536
Sr			0.239		0.622	0.077	0.060	0.014	0.085		0.155		0.274	0.398				0.065	0.066
La	0.485		0.590		0.631	0.013		0.001	0.050		0.021	0.511	0.322	0.250	0.009			0.039	0.034
Ce	1.034		0.930		0.832		0.021	0.002	0.035		0.006	0.888	0.500	0.396	0.036			0.024	0.035
Pr								0.001
Nd	0.246		0.148		0.141	0.025		0.001	0.021		0.030	0.293	0.101	0.114	0.021				0.038
Sm			0.051						0.030		0.020	0.031	0.035	0.029
Y	0.180		0.136		0.092								0.101	0.100	0.092
Th			0.046		0.086				0.007		0.007	0.006	0.023	0.025
U			0.030						0.012		0.015		0.016	0.010
Na	4.495		2.319		3.693	4.852	4.677	4.148	4.756		4.275	4.142	3.575	3.582	4.661		4.665	5.219	5.350
K	0.017							0.006							0.013
OH
F	6.006		3.467		4.163	3.724	4.756	2.330	4.266		3.722	4.041	5.475	5.482	4.102		6.612	6.521	5.780
	Wöhlerite
	BI					IT						MTI			PQ
Sample						IT60			IT111			Mtr01h			PQ12C			PQ41
wt%
SiO2	29.19					30.38			30.43			30.93			29			29.9
TiO2	1.25					1.3			1.97			1.7			1.81			0.8
ZrO2	14.56					14.08			14.67			15.91			14			14.1
HfO2	0.21											0.36
Al2O3	<0.02					0.22			0.17			0.05						0.51
Nb2O5	13.43					10.94			10.42			9.63			9.25			12.8
Ta2O5												0.36
MnO	1.39					2.08			2.42			2.19			4.47			4.85
MgO	0.07														0.64			0.15
FeO	0.95											0.46			1.1			0.54
CaO	25.91					28.98			26.22			26.57			26.2			25.7
SrO	<0.04					0.39			0.43						0.95			0.69
La2O3	<0.05								0.56			0.03
Ce2O3	0.25					0.06			0.56			0.04						0.05
Pr2O3
Nd2O3						0.1			0.39			<0.01			0.34
Sm2O3
Y2O3	0.42								0.12			0.47
ThO2						0.1			0.19						0.11			0.05
Na2O	7.4					7.43			8.01			8.23			7.44			7.48
K2O	<0.02											0.49
H2O
F	3.29					3.62			3.8			4.56			4.67			4.43
Cl	<0.03											<0.01
O=F, Cl	1.39					1.53			1.6			1.92			1.97			1.87
Total	96.92					99			99.2			100.36			98.2			100.8
apfu
Si	8					8			8			8			8			8
Ti	0.258					0.257			0.39			0.331			0.376			0.161
Zr	1.946					1.808			1.88			2.006			1.883			1.839
Hf	0.016											0.027
Al						0.068			0.053			0.015						0.161
Nb	1.664					1.302			1.238			1.126			1.154			1.548
Ta												0.025
Mn	0.323					0.464			0.539			0.48			1.044			1.099
Mg	0.029														0.263			0.06
Fe2+	0.218											0.099			0.254			0.121
Ca	7.608					8.176			7.385			7.362			7.743			7.367
Sr						0.06			0.066						0.152			0.107
La									0.054			0.003
Ce	0.025					0.006			0.054			0.004						0.005
Pr
Nd						0.009			0.037						0.034
Sm
Y	0.061								0.017			0.065
Th						0.006			0.011						0.007			0.003
Na	3.932					3.793			4.083			4.127			3.979			3.88
K												0.162
OH
F	2.851					3.014			3.159			3.73			4.074			3.748

Numbers of cations on the basis of 8Si. Notes: PC 1 *, Bortolan quarry, avg. (average) of 3 analyses; PC 2 **, Prefeitura quarry, avg. of 6 analyses [80]; PC 1a in nepheline syenites, avg. of 25 analyses and PC 1b in phonolites, avg. of 34 analyses [14]; PC¹, [82], avg. of 10 analyses; PC², [78]; PC 1c in nepheline syenites, avg. of 13 analyses and PC 1d in phonolite, avg. of 11 analyses [14]. For other data sources, see Table 3. PC 1a in nepheline syenites, avg. of 36 analyses; PC 1b in phonolites, avg. of 4 analyses; PC 1c in nepheline syenites, avg. of 7 analyses; PC 1d in phonolites, avg. of 8 analyses; PC 1e in nepheline syenites, avg. of 55 analyses; and PC 1f in phonolites, avg. of 14 analyses [14]; PC¹, avg. of 10 analyses [82]. For other data sources, see Table 3.

,

Table 5. Cyclosilicate compositions.

	Catapleiite		Eudialyte							Mn-Eudialyte		Kent
	CB	PC2	BI	CB	CSC	MTI	PQ	PC1	PCa	PCb	PC2	PQ
Sample	RP33	P7164		RP33	RP74	mtr01b	PQ42		PC39b	PC16	P7398	PQ39
wt%
SiO2	44.69	45.36	47.60	48.81	51.80	47.62	48.20	49.95	50.34	42.76	44.01	43.80
TiO2		0.07	0.09	0.46	0.26	0.33	0.41	0.52	0.13	0.25	0.06	0.13
ZrO2	31.00	35.13	12.21	12.88	13.35	11.94	12.30	12.01	11.11	10.32	10.99	10.80
HfO2		0.41	0.28			0.23		0.21			0.17
Al2O3			0.30	0.16		<0.01	0.20	0.12	0.10			0.08
Nb2O5			2.38	1.32	0.56	2.05	0.52	1.02	1.88	3.97	3.29	2.10
MnO			4.97	3.36	3.17	4.00	5.38	2.56	1.77	9.56	6.04	6.29
MgO			<0.02	0.07	0.04	0.02		0.04	0.00			0.05
FeO			5.09	4.90	4.90	3.33	4.27	4.11	5.55	0.55	0.52	2.58
CaO	13.82	0.67	8.17	10.54	8.46	12.51	9.58	10.30	11.58	6.09	9.73	8.34
SrO		0.32	<0.04				0.23	2.59	2.47	4.68	6.54	2.92
La2O3			1.20			0.90	1.66	0.13		2.62	1.52	3.49
Ce2O3			1.71	0.40	2.02	1.17	2.11	0.16		3.35	1.49	3.87
Nd2O3			0.34			0.23	0.15	0.01	0.10	0.29	0.18
Sm2O3									0.87
Y2O3			0.51			0.86
ThO2									0.20		0.14
PbO									0.59	0.21
Na2O	0.32	9.09	8.11	10.46	12.55	10.73	12.70	13.05	10.48	10.23	8.31	11.20
K2O	0.01	0.06	0.29	0.26	0.10	0.24	0.35	0.59	2.72	0.41	1.13	0.33
H2O	9.15
F			0.46	0.69	0.05	0.20	0.98			0.73	0.06	2.05
Cl			1.35	0.94	0.82	1.75		1.22	0.71	0.37	0.27
O=F, Cl			0.49	0.49		0.48		0.27
Total	98.99	91.11	94.53	94.76	97.72	97.87	99	98.07	100.6	96.4	94.54	99.3
apfu
Si	3	3	25.039	25.177	25.566	25.230	25.425	25.476	25.694	24.914	25.050	25.299
Ti		0.003	0.036	0.178	0.097	0.131	0.163	0.199	0.048	0.110	0.026	0.056
Zr	1.015	1.133	3.132	3.239	3.213	3.084	3.164	2.987	2.764	2.931	3.050	3.042
Hf			0.042			0.035		0.031			0.028
Al			0.186	0.097			0.124	0.072	0.060			0.054
Nb			0.566	0.308	0.125	0.491	0.124	0.235	0.434	1.045	0.847	0.548
Ta						0.029
Mn			2.214	1.468	1.325	1.795	2.403	1.106	0.764	4.716	2.912	3.077
Mg				0.054	0.029	0.016		0.030	0.000	0.000		0.043
Fe2+			2.239	2.113	2.022	1.475	1.883	1.753	2.367	0.269	0.247	1.246
Ca	0.994	0.047	4.604	5.825	4.473	7.101	5.414	5.628	6.332	3.799	5.933	5.161
Sr		0.012					0.070	0.766	0.732	1.581	2.158	0.978
La			0.233			0.176	0.323	0.024		0.564	0.319	0.743
Ce			0.329	0.076	0.365	0.227	0.407	0.030		0.714	0.310	0.818
Nd			0.064			0.044	0.028	0.002	0.018	0.061	0.037
Sm									0.153
Y			0.143			0.242
Th									0.023		0.018
Pb									0.082	0.032
Na	0.042	1.166	8.271	10.460	12.008	11.021	12.988	12.904	10.375	11.551	9.170	12.542
K	0.001	0.005	0.195	0.171	0.063	0.162	0.236	0.384	1.772	0.303	0.820	0.243
OH	4.097
F			0.765	1.125	0.078	0.335	1.635		0.000	0.671	0.108	3.744
Cl			1.204	0.822	0.686	1.571		1.055	0.637	0.370	0.260

Numbers of cations on the basis of 3Si for catapleiite and 29(Si+Al+Ti+Nb+Zr+Hf) for eudialyte-group minerals. Abbreviations: Kent, kentbrooksite. Notes: PC¹, [82], avg. of 20 analyses; PC², [78]; PC^a and PC^b are both single analyses [14]. For other data sources, see Table 3.

,

Table 6. Inosilicate compositions.

	Aenigmatite			Astrophyllite			Kuple	Loren	Pectolite			Serandite
	BI	CB	PC	PC2	PQ	BI	PQ	PC2	PC1	PC2	L	PC2 *	L
Sample	167A2	RP42	PC 1b	P7A09	PQ10		PQ12	P7297		P729	LM106	P7100	LM88
wt%
SiO2	40.71	41.50	39.79	33.91	34.20	33.65	33.80	34.31	52.10	54.27	53.82	51.84	51.69
TiO2	9.05	8.99	9.39	10.90	8.87	9.68	8.71	43.46	0.02				0.19
ZrO2	<0.05			0.64	3.75	0.90	5.00
Al2O3	0.53	0.35	1.13	1.57	1.61	1.36	1.54	0.04	0.01		1.37		0.09
Nb2O5	<0.05	1.66		0.61	1.40	1.62	0.11		0.00
MnO	6.46	1.94	4.99	11.82	13.30	8.28	25.80		14.08	1.47	5.87	21.70	19.63
MgO	0.17	0.01	0.75	2.36	1.04	0.24	0.41		0.05				0.01
FeO	35.01	39.80	36.29	20.66	22.00	26.79	10.30	0.60	0.75	0.47	0.17	0.56	0.66
CaO	0.06	0.19	0.29	2.10	1.57	1.56	1.59	0.04	20.41	30.63	26.48	13.12	15.71
SrO				0.45	0.54	<0.04	1.53		0.03	0.06		1.05
La2O3									0.04
Ce2O3						<0.08			0.11	0.02		0.43
Na2O	7.43	7.10	7.40	1.57	2.81	2.21	2.55	17.40	8.92	9.51	9.77	7.89	9.40
K2O	<0.02	0.01		7.03	6.08	6.34	6.05	0.03			0.74		0.10
H2O					2.73		1.90
F				0.79		0.84
Cl						<0.03
O=F, Cl						0.35
Total	99.4	99.9	100.0	94.4	99.9	93.1	99.2	96.8	96.6	96.4	98.2	96.6	97.5
apfu
Si	5.890	5.885	5.652	7.647	7.519	7.780	7.501	2.052	3.034	3.062	3.012	3.069	3.020
Ti	0.985	0.959	1.003	1.849	1.467	1.683	1.454	1.955	0.001				0.008
Zr				0.070	0.402	0.101	0.541
Al	0.090	0.058	0.189	0.417	0.417	0.371	0.403	0.003	0.001		0.090		0.006
Nb		0.106		0.062	0.139	0.169	0.011
Mn	0.792	0.233	0.601	2.258	2.476	1.621	4.849		0.695	0.070	0.278	1.088	0.971
Mg	0.037	0.002	0.159	0.793	0.341	0.083	0.136		0.004				0.001
Fe2+	4.235	4.719	4.313	3.896	4.044	5.179	1.911	0.030	0.037	0.022	0.008	0.028	0.032
Ca	0.009	0.029	0.044	0.507	0.370	0.386	0.378	0.003	1.274	1.851	1.588	0.832	0.983
Sr				0.059	0.069		0.197		0.001	0.002		0.036
La									0.001
Ce									0.002			0.009
Na	2.084	1.952	2.038	0.686	1.198	0.991	1.097	2.018	1.007	1.040	1.060	0.906	1.065
K		0.002		2.022	1.705	1.870	1.713	0.002			0.053		0.007
OH					4.003		2.812
F				0.563		0.614
Cl								0.124

Numbers of cations on the basis of 20 O for aenigmatite, 28.5 O for astrophyllite-group minerals, 9 O for lorenzenite, and 8.5 O for pectolite–serandite. Abbreviations: Kuple, kupletskite; Loren, lorenzenite. Notes: PC 1b in phonolites, avg. of 23 analyses [14]; *, EDS analysis; PC¹, [82], avg. of 16 analyses; PC², [78]; for other data sources, see Table 3.

and

Table 7. Phyllosilicate compositions.

	Nept	Tuper
	PC2 *	PC3
Sample	P7178
wt%
SiO2	52.48	55.13
TiO2	17.39
Al2O3	0	0.33
Fe2O3		25.45
MnO	0.56	0.43
MgO		0.15
FeO	14.66	0.5
CaO		0.12
Na2O		4.26
K2O	6.67	0.77
H2O	5.38	12.63 **
Total	97.14	100
apfu
Si	8	8
Ti	1.994
Al		0.056
Fe3+		2.779
Mn	0.072	0.053
Mg		0.032
Fe2+	1.869	0.061
Ca		0.019
Na		1.198
K	1.297	0.143
OH	5.47	12.224

Numbers of cations on the basis of 8Si. Abbreviations: Neptu, neptunite; Tuper, tuperssuatsiaite. Notes: *, EDS analysis: **, calculated; PC², [78]; PC³, [79].

showing the results of some representative analyses.

The rinkite mineral group includes several Ti-rich disilicates, such as rinkite-(Ce), and end-members, such as hainite, mosandrite-(Ce) and rosenbuschite [88], which are commonly found in several occurrences. Chemical analyses of hainite from two localities within the Poços de Caldas massif (Bortolan and Prefeitura quarries, in nepheline syenites and phonolites) reveal a calcium silicate mineral of quite homogeneous composition bearing high amounts of TiO₂ (8.80–9.83 wt%), Na₂O (6.17–8.40 wt%) and F (5.13–7.06 wt%) and some LREE (Table 4). Mosandrite-(Ce), a rare Ca-Ti silicate, has only been identified in the Poços de Caldas massif, Búzios Island and Cerro Boggiani rocks. Data from the Poços de Caldas massif and Búzios Island rocks indicate that the mineral contains significant amounts of Na₂O (4.27–7.35 and 8.57 wt%, respectively) and F (3.93–5.40 and 7.02 wt%, respectively), having been strongly enriched in LREE, with Ce₂O₃ concentrations reaching up to 8.88 and 10.44 wt%, respectively. Compositions of rosenbuschite exhibit small variations in major components TiO₂ (6.79–8.56 wt%), ZrO₂ (12.1–14.8 wt%), CaO (24.09–25.91 wt%), Na₂O (9.34–10.9 wt%) and F (5.04–8.16 wt%) and allow the Passa Quatro specimen to be distinguished as having the lowest Nb₂O₅ (0.58–0.97 wt%) and highest MnO (3.75–4.56 wt%) contents. Rinkite-(Ce)_ss is present in the Passa Quatro, Itatiaia and Poços de Caldas assemblages. When compared to other minerals of the same group, especially rosenbuschite, data indicate, for the first specimen, a low concentration of ZrO₂ and considerable amounts of LREE, with Ce₂O₃ clearly prevailing over La₂O₃ (Table 4). An important Ti host mineral is lamprophyllite, described in the Poços de Caldas massif [14,78,82] (Table 4). The Poços de Caldas lamprophyllites have high average concentrations of TiO₂ (26.74–29.06 wt%), MnO (4.31–6.97 wt%), Na₂O (10.99–11.51 wt%) and SrO (13.06–16.96 wt%) along with some REE content (REE up to 2.03 wt%) and F (0–2.05 wt%). Representative mineral analysis of the Morro do Serrote rocks [78] does not differ greatly from the previously available mean composition, with high contents of TiO₂ (27.82 wt%), MnO (6.97 wt%), Na₂O (11.51 wt%) and SrO (13.06 wt%; a second analysis showing 16 wt%).

Wöhlerite, hiortdahlite, låvenite and normandite, Na-, Ca- and Zr-rich disilicates of the cuspidine–wöhlerite group [89], are known to be present in most of the compiled occurrences (Table 3). Hiortdahlite, a rich calcium-silicate phase (27.48–31.24 wt%), had its composition determined at four occurrences, where it was characterized by high proportions of Zr₂O (16.0–17.76 wt%), Na₂O (6.80–9.41 wt%) and F (6.33–8.36 wt%). A sample collected from the Itatiaia massif is noteworthy for its unusual concentration of TiO₂ (6.98 wt%). Låvenite is a common constituent of the group, analyses having been performed for five occurrences indicating heterogeneous composition and large differences regarding TiO₂ (2.94–8.43 wt%), ZrO₂ (16.5–27.76 wt%), MnO (4.23–9.66 wt%), CaO (8.09–14.89 wt%) and F (2.97–5.76 wt%). SiO₂ and Na₂O variations lie within a narrow interval (Table 4). Analyses for normandite derive from Poços de Caldas and Passa Quatro syenitic rocks, showing significant differences in the average values. Compared to those of Passa Quatro, Poços de Caldas samples are higher in TiO₂ and poor in ZrO₂ and tend to be slightly enriched in FeO and CaO. Na₂O and F remain constant, whereas MnO is higher in Passa Quatro than in Poços de Caldas analyses (Table 4). Wöhlerite is a Ca–Zr–Nb silicate whose composition remains, to a great extent, constant regarding major elements of different occurrences: ZrO₂ (14.0–15.91 wt%), Nb₂O₅ (9.25–13.43 wt%), CaO (25.7–28.98 wt%), Na₂O (7.40–8.23 wt%) and F (3.29–4.67 wt%). MnO concentrations are higher in Passa Quatro mineral specimens (Table 4).

Eudialyte-group minerals are one of the major Zr-hosts in agpaitic rocks and include several Na- and Ca-rich cyclosilicates with variable amounts of Fe, Mn, Nb, and REE, among other cations [7,90,91]. Minerals of this group occur in various localities (Table 3) and eudialyte_ss have been analyzed in most of the investigated occurrences. They are compositionally variable in SiO₂ (47.60–51.80 wt%), CaO (8.17–12.51 wt%), MnO (4.97–5.38 wt%), and Na₂O (8.11–13.05 wt%). ZrO₂ and FeO concentrations are practically constant (11.94–13.35 wt% and 3.33–5.09 wt%, respectively). A Mn-rich variety, the manganoeudialyte, is found at the locality of Pedra Balão in the Poços de Caldas massif, and also as single crystal in the Poços de Caldas nepheline syenites. The manganoeudialytes show lower SiO₂ and ZrO₂ (42.76–44.01 wt% and 10.32–10.99 wt%, respectively) and higher MnO (6.04–9.56 wt%) and SrO (4.68–6.54 wt%) contents. Nb₂O₅ reaches up to 3.97 wt% (Table 5). Kentbrooksite is restricted to the Passa Quatro massif with the mineral presenting high proportions of ZrO₂ (10.8 wt%) and MnO (6.29 wt%) and significant amounts of LREE. Other analyzed minerals include catapleiite and Ca-catapleiite, Zr-rich silicates represented by two chemically distinct varieties. The first is from Poços de Caldas and is rich in Na₂O (9.09 wt%); the second is from Cerro Boggiani and contains high CaO (13.82 wt%) (Table 5).

Compositions for aenigmatite, a Ca–Ti–Na mineral bearing high amounts of FeO (35.01–39.80 wt%), are available from Búzios Island, Cerro Boggiani and Poços de Caldas rocks, whereas analysis for lorenzenite, a silicate with abundant TiO₂ (43.46 wt%) and Na₂O (17.4 wt%), is available for Poços de Caldas samples (Table 6). Pectolite and serandite are described in Lages and Poços de Caldas occurrences, with chemical analyses given in the last table. Pectolite is richer in CaO (20.41–30.63 wt%) while serandite is higher in MnO (19.63–21.70 wt%). Analysis of pectolite from Poços de Caldas samples [82] also shows high MnO content (14.08 wt%). Na₂O remains practically constant in both minerals (pectolite: 8.92–9.77 wt%; serandite: 7.89–8.40 wt%). Chemical compositions of astrophyllite are determined from three occurrences, indicating a FeO-rich (20.66–26.79 wt%) silicate mineral with some variation in TiO₂ (8.87–10.90 wt%) and MnO (8.28–13.3 wt%). A specimen from Passa Quatro is enriched in ZrO₂ (3.75 wt%). Kupletskite, a mineral present in Passa Quatro rocks, is abundant in MnO (25.8 wt%) and contains significant amounts of TiO₂ (8.71 wt%), ZrO₂ (5.00 wt%), FeO (10.3 wt%) and K₂O (6.05 wt%).

The hydrate mineral neptunite (5.38 wt% H₂O) is characterized by high TiO₂ (17.39 wt%), FeO (14.66 wt%) and K₂O (6.67 wt%) concentrations. It is described in the Bortolan quarry within the Poços de Caldas massif [78]. Another hydrate mineral (12.63 wt% H₂O), tuperssuatsite, is a rare accessory identified at the same quarry [79], being characterized by rich Fe₂O₃ (25.45 wt%) content and the significant presence of Na₂O (4.26 wt%) (Table 7).

In addition to the above constituents, Itatiaia, Passa Quatro and Cerro Boggiani rocks carry a very extensive list of highly diversified minerals formed under varied conditions, mostly late-stage magmatic and hydrothermal/deuteric. Some even derived from metasomatic fluids. The Poços de Caldas massif is especially marked by the outstanding amount of poorly known accessory phases, mostly found in outcrops of the decommissioned Bortolan quarry. In total, 28 different species are preliminarily discussed upon investigating major and accessory minerals of local lithotypes [78]. Some minerals, such as belovite-(Ce) NaCeSr₃(PO₄)₃F, chlobartonite K₆Fe₂₄S₂₆(Cl), götzenite Ca₄NaCa₂Ti(Si₂O₇)₂(OF)F₂, polezhaevaite-(Ce), polezhaevaite-(La) NaSr(Ce,La)F₆, stronadelphite Sr₅(PO₄)₃F, strontiofluorite SrF₂, and vishnevite Na₈(Al₆Si₆)O₂₄(SO₄)·2H₂O, mostly analyzed through EDS, have been described and reported for the first time in Brazilian rocks [78]. Recently, the presence of fluorcaphite SrCaCa₃(PO₄)₃F, strontium apatite (Ca,Sr)₅(PO₄)₃F, and georgechaoite NaKZr(Si₃O₉)·2H₂O, together with stronadelphite Sr₅(PO₄)₃F and strontiofluorite SrF₂, both already identified, were also reported for the first time in this massif [14].

A great number of rare accessory minerals occur in association with agpaitic and miaskitic rocks (

Table 8. Rare accessory minerals in agpaitic and miaskitic rocks.

Mineral Class	Mineral Name	Chemical Formulae *	Occurrence
Oxides	Baddeleyite	ZrO2	IT, MTI, PQ
	Cerianite-(Ce)	CeO2	PC
	Perovskite	CaTiO3	L, MTI
	Pyrochlore	(Na,Ca)2(Nb2O6)(OH,F)	BI, CB, MTI, PQ, PC
	Thorianite	ThO2	CB, PC
	Uraninite	UO2	CB, PC
	Zirconolite	CaZrTi2O7	IT, MTI
Phosphates	Belovite-(Ce)	NaCeSr3(PO4)3F	PC
	Britholite-(Ce)	(Ce,Ca)5(SiO4,PO4)3(OH,F)	BI, CB, IT, MTI, PC
	Cheralite	CaTh(PO4)2	PC
	Florencite-(Ce)	CeAl3(PO4)2(OH)6	PC
	Fluorcaphite	SrCaCa3(PO4)3F	PC
	Monazite-(Ce)	(Ce,La,Nd,Th)(PO4)	BR, CB, IT, PC
	Monazite-(La)	(La,Ce,Nd,Th)(PO4)	PC
	Stronadelphite	Sr5(PO4)3F	PC
	Xenotime-(Y)	Y(PO4)	PC
REE-silicates	Chevkinite-(Ce)	Ce4(Ti,Fe2+,Fe3+)5O8(Si2O7)2	IT
	Perrierite-(Ce)	Ce4MgFe3+2Ti2O8(Si2O7)2	IT
Halides	Polezhaevaite-(Ce)	NaSr(Ce,La)F6	PC
	Polezhaevaite-(La)	NaSr(La,Ce)F6	PC
	Strontiofluorite	SrF2	PC
	Villiaumite	NaF	PC
Carbonates	Ancylite-(Ce)	CeSr(CO3)2(OH)·H2O	CB, PC
	Ancylite-(La)	LaSr(CO3)2(OH)·H2O	CB, PC
	Bastnäsite-(Ce)	Ce(CO3)F	BI, CB, IT, PC
	Burbankite	(Na,Ca)3(Sr,Ba,Ce)3(CO3)5	CB, PC
	Cordylite-(Ce)	(Na,Ca,□)BaCe2(CO3)4(F,O)	CB
	Galgenbergite-(La)	Ca(Ce,La)2(CO3)4·H2O	CB
	Parisite-(Ce)	CaCe2(CO3)3F2	CB
	Rémondite-(Ce)	Na3(Ce,Ca,Na)3(CO3)5	CB
	Strontianite	SrCO3	PC
	Synchysite-(Ce)	CaCe(CO3)2F	BI, CB

For sources, see Table 3. Notes: □ means vacancy in the site; *, according to IMA.

). Pyrochlore is the most significant Nb-bearing oxide, being represented by three different species: plumbopyrochlore, uranopyrochlore and yttropyrochlore. Uraninite and thorianite correspond to the main U and Th oxides, respectively, whereas thorite, a rare Th-rich silicate, is also present. Other oxide phases include baddeleyite, perovskite and zirconolite. REE-rich minerals are represented by numerous crystalline phases consisting of phosphates, silicates and fluorocarbonates. Monazite-(Ce) and -(La) is one of the most common phosphate minerals. In some occurrences britholite-(Ce), a basic phosphate/silicate phase containing high amounts of SiO₂, La₂O₃, Ce₂O₃ and CaO and low amounts of P₂O₅, is found coexisting or inter-grown with apatite. Rare LREE–HFSE-bearing silicates have chevkinite-(Ce) and perrierite-(Ce) as their principal members, showing a significant compositional range that indicates inverse correlation of FeO and CaO, as observed in Itatiaia rocks [40]. Carbonates and fluorocarbonates, mostly REE-bearing phases, are frequent and include various constituents that are largely present in e.g., Cerro Boggiani peralkaline nepheline syenites and phonolites [34,69]. In such occurrences, the minerals present are burbankite and remondite-(Ce), rare Sr and Ce carbonates; fluorocarbonates of the bastnäsite–parisite–synchysite series forming fine-scale complex intergrowths fibroradial to plumose aggregates; cordylite-(Ce), a Ba- fluorocarbonate; and hydrate carbonates containing ancylite-(Ce) and galgenbergite-(La) as main phases.

6. Petrological Considerations

A few studies addressing petrogenetic aspects of the agpaitic occurrences discussed are available in the literature, the most recent and complete ones being the contributions on Itatiaia [40] and Passa Quatro [20] massifs and, most recently, a paper on the mineralogy and geochemistry of Poços de Caldas agpaitic rocks [14]. In general, however, these and other alkaline occurrences in southern Brazil and eastern Paraguay have been interpreted by various authors [20,32,42,62,65] as formed by extensive long-term fractional crystallization processes operating at shallow surface levels (approximately <5 km) from alkaline mafic to ultramafic parental magmas. The occurrences are also believed to have originated from low-degree partial melting of geochemically enriched mantle lithologies. Thus, an episode of mantellic metasomatic pre-enrichment is commonly suggested in order to explain particularities such as the enrichment in halogens, HFSEs, REEs, and incompatible elements [7,8]. A basanitic (plagioclase-bearing) and/or nephelinitic (feldspar-free) composition is preferentially proposed as the primary magma. Small dikes of basanite rocks are commonly known in many places, either directly associated with evolved (miaskitic and agpaitic) peralkaline rocks in the field (e.g., the Búzios and Monte de Trigo coastal islands [25,65]) or emplaced close to alkaline intrusions over distinct areas along the Serra da Mantiqueira [36,41,59].

Numerous studies suggest that both compositions are likely to represent the most important types of parental melts for agpaitic rocks [7]. The distinction of the parental melts of each locality can also be suggested based on the distribution of Sr and REE in eudialyte-group minerals [26,91]. Agpaitic rocks derived from alkali basaltic or basanite magmas are normally low in Sr and have pronounced negative Eu anomalies, due to the extensive plagioclase fractionation that occurred during magmatic evolution. The composition of the eudialyte-group minerals reflects this geochemical signature. Figure 4 exhibits the low Sr content of eudialyte from the Monte de Trigo, Passa Quatro and Búzios massifs, supporting the interpretation of a basanite/alkali basalt parental magma for the whole suite of rocks [20,26,65]. Moreover, no Sr-bearing mineral occurs in these localities. In contrast, when derived from more SiO₂-undersaturated magmas, the Sr content is high, and no marked spikes are noticed for Eu. The parental mafic magma of the agpaitic rocks of the Poços de Caldas massif is interpreted as a more SiO₂-undersaturated parental magma that evolved without plagioclase fractionation [14,42], and where the eudialyte-group minerals have very high Sr content (Figure 4), together with the occurrence of lamprophyllite, a Sr-rich disilicate, among several other Sr-rich minerals (Table 3 and Table 8).

In the model proposed for the evolution of the Passa Quatro massif [20], differentiation starts from mafic to ultramafic parental magmas, with generation of phonolites in the first stages being followed by generation of peralkaline phonolites in subsequent stages and, finally, late and post-magmatic phases. Removal of diopside-alkali feldspar–plagioclase would promote generation of alkali syenites, whereas removal of nepheline–aegirine–titanite would lead to generation of nepheline syenites. Removal of many different accessories, e.g., zircon, fluorite, F-disilicates, eudialyte, etc., would originate eudialyte-bearing nepheline syenites and phonolites.

Suppression of such phases is responsible for the enrichment of the residual magmatic liquids with incompatible elements, which onsets the crystallization of HFSE- and REE-F-rich minerals. At the end of this crystallization path, phases containing CO₂ and H₂O in their composition form as REE-carbonates and REE-fluorocarbonates. Therefore, according to the abovementioned authors, the magma that originated the Passa Quatro agpaitic rocks is characterized by geochemical traits such as enrichment in incompatible elements (HFSEs, REEs), high F, and minor CO₂ and H₂O under low oxygen fugacity and water activity conditions.

Based on textural relationships and overall accessory mineral chemistry, the Cerro Boggiani nepheline syenites and phonolites are characterized as a sequence of different minerals that usually crystallize under magmatic, late-stage magmatic and hydrothermal conditions [32,34,69,70,71]. Among the hydrothermal fluids affecting those rocks, it is suggested that a distinction be made between deuteric (H₂O-rich) and metasomatic of carbonatitic origin (CO₂-rich) stage ones. Included in the magmatic stages are U–Th minerals (uraninite–thorianite and thorite), thorianite being more frequently generated under hydrothermal/deuteric conditions. Nb-bearing minerals with pyrochlore as their main phase (oxide) originate in the magmatic field, advancing progressively into the hydrothermal field. Zr-rich silicate phases (eudialyte and lorite), ks, ions, and minor compatible elements, however data for the first mineral is more consistent. Rosenbuschite is restricted to the hydrothermal stage. It is inferred that carbonatitic fluids rich in F, Na and REE percolated through the subvolcanic system and metasomatically interacted with the peralkaline and agpaitic silicate melts during and after their late-stage magmatic crystallization and hydrothermal/deuteric alteration. As a result, a highly diverse mineral assemblage consisting of silicates (Ca-catapleiite), phosphates (monazite), phosphates/silicates (britholite) and especially of different types of carbonates (hydrate carbonates: ancylite, galgenbergite; REE-carbonates: burbankite; REE-fluorocarbonates: cordylite, bastnäsite–parisite–synchisite) was generated from REE–Ca–Sr–Ba-rich carbonatitic fluids of dominantly metasomatic origin under hydrothermal conditions, at relatively low temperatures.

The agpaitic occurrence of Monte de Trigo Island is associated with small nepheline microsyenite dikes that are genetically related to a miaskitic nepheline syenite stock, which occupies mainly the central parts of the intrusion. Compositionally, these dikes consist of alkali feldspar, nepheline, mafic minerals (clinopyroxene, amphibole, biotite) and varied accessories including magnetite, titanite, apatite, zircon, perovskite, pyrochlore, baddeleyite, and zirconolite, which impart a miaskitic character to the rocks. The evolution of the nepheline-bearing alkali feldspar syenite from fractional crystallization led to the formation, as final differentiates, of agpaitic synplutonic nepheline microsyenite dikes, with a high concentration of volatiles and pronounced enrichment in incompatible elements [62]. The rock may be classified as transitional agpaitic [7,8]. The major characteristic of the assemblage is the abundance of late-crystallized calcic minerals. Britholite-(Ce) and Zr–Nb-silicates of the cuspidine–wöhlerite series showing high Ca and Na contents are relatively common. The eudialyte-group minerals are marked by a significant enrichment in Ca, a moderate enrichment in Nb and REE, and a somewhat low Na content when compared to their counterparts in other Brazilian alkaline occurrences [26]. REE and Y concentrate preferentially in britholite-(Ce) (30.9–58.5 wt%) and perovskite (33 wt%), but they are also found in significant amounts in zirconolite (7.7–14.2 wt%), pyrochlore (3.2–13.3 wt%), eudialyte (2.4–4.1 wt%), and in minerals of the cuspidine–wöhlerite group (<3 wt%) [62]. Instead of contributing to the origin of Zr–Nb-bearing silicates, Ti tends to form titanite. At the borders of the dike, accessory minerals are represented exclusively by låvenite and eudialyte-group forms.

Itatiaia rocks are defined as forming a continuous spectrum from nepheline to quartz syenite and granite fields across the SiO₂-saturation boundary [15,40]. In the petrogenetic residual diagram, the nepheline syenites clearly trend towards the phonolitic minimum, while the silica-oversaturated syenites trend towards the rhyolitic minimum without reaching it. The dikes that cut the intrusions are mainly phonolitic in composition. The accessory minerals vary widely in composition, being identified, in addition to the widespread phases (e.g., titanite, Fe–Ti oxides, apatite, zircon), as other, less common ones of complex composition (e.g., REE-HFSE silicates, Zr and Nb oxides, phosphates). Secondary phases comprise Fe-carbonates, fluorocarbonates and hydrate phases (catapleiite). Additionally, variations in major- and trace-element compositions of Itatiaia rocks are directly related to the amount of accessory phases present, as suggested by the enriched chondrite-normalized REE distribution patterns of least- and most-evolved nepheline syenites [40]. The presence of chevknite/perrierite (±allanite) and the abundance of pseudobrookite in quartz syenites and the presence of Ca–F-disilicates, britholite, and pyrophanite-rich compositions in nepheline syenites are among the most striking differences in the accessory phase assemblages. Fluorapatite, an early crystallizing phosphate phase, is typical of silica-oversaturated rocks in contrast to britholite, which frequently joins the apatite in the nepheline syenite. The britholite present is characterized by a remarkable concentration of REE that reaches up to 62 wt%, with La₂O₃ prevailing over Ce₂O₃. The latest crystallized phases in Itatiaia rocks are found as interstitial material, consisting of pectolite, hydrate catapleiite and REE-F carbonates. Two main mineral reactions, both recognized on thin sections, are considered very characteristic of the Itatiaia rocks [40]: (1) the corrosion of early formed titanite crystals and (2) the instability of zircon + fluorite, which react to form F-disilicates due to the remaining concentration of fluorine and other elements in interstitial liquids after the predominant crystallization of felsic phases.

Despite being the occurrence that carries the highest diversity of accessory and exotic phases in the entire agpaitic suite, the mineralogy of Poços de Caldas has not been yet investigated systematically in detail. The only such study available [78] identified, using various analytical techniques, 28 different mineral species, all collected at the Bortolan quarry. These minerals were described and classified mainly based on chemical (WDS and EDS analyses) and crystallographic data; no petrological information on them is presented in the study mentioned, nor is there any other descriptive contribution focusing specifically on tuperssuatsiaite [79], hainite [80], eudialyte [81] and lamprophyllite–normandite [82]. New major oxide, trace element and Sr–Nd isotope analyses coupled with detailed petrographic and mineralogical descriptions, supported by microprobe analyses and LA–ICP–MS mineral chemical study, of the main accessory phases for the Poços de Caldas were carried out by [14]. The eudialyte-group minerals are associated with main to late-stage crystallization assemblages and have colorless to slightly pinkish large anhedral/poikilitic or anhedral aspects. They are especially abundant in lujavrites and khibinites, totaling between 5% and 15% of the modal composition. Lamprophyllite is a phase of late stage of crystallization, commonly forming aggregates, sometimes radiated, and intergrowths with aegirine crystals. Normandite and rinkite occur mainly as single crystals, sometimes as aggregates.

The agpaitic massifs of the Brazilian platform also present distinctive Ti- and Zr-bearing complex silicate assemblages (Table 3 and references therein). Zr- and F-rich disilicates, such as hiortdahlite, wöhlerite and låvenite, prevail in agpaitic rocks from Monte de Trigo Island, in addition to eudialyte. There are no complex Ti-rich silicates, as this element preferentially appears in titanite. The agpaitic rocks from Búzios Island, Passa Quatro, Cerro Boggiani and Itatiaia massifs have somewhat similar paragenesis, with the presence of complex Ti- and Zr-rich silicates. They contain the same Zr- and F-rich disilicates that occur in the Monte de Trigo Island, in addition to rosenbuschite and Ti- and F-rich disilicates, such as hainite, normadite, rinkite-(Ce), and mosandrite-(Ce). In these localities, Ti also occurs in aenigmatite and astrophyllite-group minerals. Eudialyte occurs in all of them except Itatiaia. Thus, the increasing fluorine trend identified by [10] in agpaitic rocks from the Oslo Rift is the main trend of magmatic evolution that led to the formation of the agpaitic rocks from Monte de Trigo Island, Búzios Island, Passa Quatro, Cerro Boggiani and Itatiaia, although locally some samples also show trends of increasing alkali and water.

On the other hand, the Poços de Caldas agpaitic rocks have practically no Zr- and F-rich disilicates, but have several complex Ti-rich silicates, such as hainite, normandite, rinkite-(Ce), lamprophyllite, aenigmatite, and astrophyllite-group minerals. The eudialyte-group minerals, which are quite abundant in this massif, are the major carrier of Zr, along with hydrated zirconosilicates and some Zr that is incorporated in aegirine. It seems that in this case the increasing alkali trend [10] is the main trend that led to the formation of the agpaitic rocks from Poços de Caldas. Moreover, Poços de Caldas has villiaumite, an almost pure NaF mineral that occurs in rocks with extreme alkali enrichment, often associated with hyperagpaitic rocks [7,8].

7. Final Remarks

▪

Agpaitic rocks occur as minor components, being usually subordinate and younger compared to associated miaskitic units in Mesozoic to Cenozoic occurrences in the Brazilian platform.

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The Poços de Caldas massif displays the largest exposure of agpaitic rocks, including lujavrite and khibinite bodies, carrying mineral assemblages that are exclusive to and typical of agpaitic conditions. The massif contains the most significant number of exotic minerals among the occurrences.

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Eudialyte-group, rinkite-group and cuspidine–wöhlerite-group minerals are the main typical constituents of the studied agpaitic rocks, but other exotic phases, such as aenigmatite, astrophyllite, lamprophyllite, etc., are also described in agpaitic rocks.

▪

The studied agpaitic rocks were generated from extensive long-term fractional crystallization processes operating at shallow surface levels (<about 5 km), from highly alkaline mafic to ultramafic parental magmas and deriving from a metasomatized mantle source.

▪

After the early stages of differentiation, fractional crystallization continues after the generation of miaskitic phonolites, reaching peralkaline phonolite compositions in subsequent stages; late and post-magmatic processes also play important roles in the formation of the exotic mineralogy.

▪

After formation of exotic mineralogylites, the enrichment of residual magmatic liquids in incompatible elements may occur. Subsequently, mineral phases such as REE-carbonates and REE-fluorocarbonates form, containing CO₂ and H₂O in their composition.

▪

Geochemical evidence suggests enrichment in REE and incompatible elements and slight to strong LREE/HREE fractionation. Normalized diagrams for incompatible elements are marked by strong negative anomalies in Ba, Sr, P and Ti, whereas the distribution of chondrite-normalized REE normally exhibits a concave upward pattern.

▪

Some occurrences (e.g., Poços de Caldas massif and Monte de Trigo Island) would be more appropriately described as transitional agpaitic, as they contain HFSE minerals such as titanite and eudialyte, which are characteristic of both miaskitic and agpaitic suites.

▪

Villiaumite, a mineral marking the transition from agpaitic to strongly agpaitic stages and characterized by extreme alkali enrichment, is described in fine-grained nepheline syenitic rocks of the Poços de Caldas massif.