Abstract
We present a comprehensive overview of the geochemical characteristics and evolution of the carbonatites from the southern Brazilian Platform (Paraná Basin). The carbonatites from different complexes display large compositional variability in terms of abundances of incompatible and rare earth elements. This is in agreement with an origin from heterogeneous lithospheric sources, as confirmed by isotopic data (see Speziale et al., this issue). The characteristic major and trace element abundances of these carbonatites present compelling evidence for invoking liquid unmixing as the main mechanism of their formation and evolution albeit few exceptions. We propose an evolutionary trend for the Brazilian carbonatites, which can be summarized as following: exsolution of the primary Ca- or Mg-carbonatitic liquids systematically takes place at the phonolite-peralkaline phonolite stage of magma differentiation; this is followed by progressive Fe-enrichment and by final emplacement of fluorocarbonatites associated with hydrothermal fluids.
1 Introduction
The Paraná Basin is a part of the Paraná-Angola-Namibia (Etendeka) Province (PAEP [1]). It is characterized by Early Cretaceous flood basalts (tholeiites) and dyke swarms (130–135 Ma, according to refs. [2,3,4,5] and references therein) associated with alkaline and alkaline–carbonatite complexes of Early Cretaceous to Tertiary age [6,7,8,9,10,11,12,13,14]. The emplacement of these complexes, in and around the PAEP, occurred mainly along tectonic structures active at least since the Early Mesozoic (Figure 1), and up to present day, as indicated also by the distribution of the earthquakes in southern Brazil [15]. Molina and Ussami [16] and Ernesto et al. [3,4] pointed to a clear correlation between geoid anomalies and magmatic/tectonic provinces along southeastern Brazil and Uruguay.
The carbonatitic complexes from southern Brazilian Platform have been the subject of several studies focussing on their geology, petrology, geochemistry, and processes of liquid immiscibility [6,8,9,10,17,18,19,20,21,22,23,24,25,26,27,28,29,30,31,32,33,34,35,36].
The numerous carbonatitic occurrences provide additional information about the geochemical characteristics of the source regions, which are complementary to those from the silicate rocks. Carbonatitic liquids have extremely fast ascent rate and emplacement, and their peculiar chemical and physical characteristics make carbonatitic liquids better suited than silicate ones as indicators of mantle sources [36,37]. Here, we present the overall picture of the geochemical evolution of carbonatite magmatism in the southern Brazilian Platform by using an extended dataset of major and trace elements compositions (see Appendix).
This article and another article dedicated to the isotopic data (Speziale et al., this issue) can be considered a compendium of a series of specific studies from the same group of authors [11,12,13,14,31,32,38,39,40,41,42].
2 Geographic location, tectonic setting, major geolithological characteristics, and classification of the carbonatitic complexes in the Southern Brazilian Platform
The carbonatitic complexes from southern Brazil and Paraguay are found mainly along the following alignments: (1) Araguaia-Alto Paranaíba (APIP; [6])-Cabo Frio; (2) Ponta Grossa Arch (e.g., Jacupiranga, Juquiá, Barra do Itapirapuã); (3) Piquirí lineament (mainly in Eastern Paraguay); (4) Torres syncline; and (5) Rio Grande Arch (Figure 1).
Based on their age relative to the flood basalts and their associated intermediate and acid lava flows [2], these occurrences are pretholeiitic (e.g., Cerro Chiriguelo and Cerro Sarambí; 136–143 Ma), syn-tholeiitic (e.g., Anitápolis, Jacupiranga, Juquiá; 130–133 Ma), and posttholeiitic (e.g., Sapucai, 128 Ma; Ipanema, 124 Ma; Barra do Itapirapuã, 115 Ma) [cf. refs. 1,13,28,43,44]. In addition, tertiary alkaline complexes (mainly 45–65 Ma) are also present and distributed along the Taiúva-Cabo Frio lineament (Serra do Mar igneous province; cf. ref. [44]).
The geochemical characteristics of the carbonatites appear to be strictly linked to the mineral assemblages in the various evolutionary stages in carbonatites (p. 662 in ref. [31]). The mineral associations in the four main evolutionary stages are presented in Table 1.
Major minerals | Rare metal-bearing minerals | |
---|---|---|
I stage | Calcite, diopside, forsterite, melilite, monticellite, nepheline, phlogopite-biotite, apatite I, Ti-magnetite | Nb-perovskite (Nb), calzirtite (Zr, Nb), monazite (Ce, REE) |
II stage | Mg-calcite ± dolomite, diopside, tetraferriphlogopite, apatite II Mg-magnetite | Baddeleyite (Zr), pyrochlore-I (Nb), hatchettoloite (Nb, Ta, U, Th), zirkelite (Zr, Nb) |
III stage | Calcite, dolomite (Fe-dolomite), tetrapherriphlogopite, apatite III, magnetite, titanite | Pyrochlore (Nb, Th, U), burbankite (Sr, Ba, REE) |
IV stage | Dolomite (Fe-dolomite), ankerite, siderite, magnesite, fluorite rhodochrosite, K-feldspar, quartz | Pyrochlore (U, Th, Nb), bastnäesite (REE), parisite (REE), ancylite (Sr, REE), synchysite (REE), strontianite (Sr), celestine (Sr) |
According to refs. [22] and [27], carbonatite occurrences are believed to be produced by processes of liquid immiscibility. The rock association present in the Juquiá complex represents the prototype of all the examined carbonatites, whose evolution, reproduced by mass-balance calculations [22], follows the same sequence of stages: (1) fractionation from a parental basanite melt to a phonotephritic (basanitic) magma by crystallization of olivine clinopyroxenite and minor cumulus of olivine alkali gabbro; (2) separation of the least differentiated mafic nepheline syenite from the essexitic magma through fractionation of syenodioritic assemblages; and (3) exsolution of carbonate liquid from the CO2-enriched nepheline syenite magma, which further fractionates producing ijolite–melteigite–urtite cumulates.
The line of evolution (alkaline gabbro to syenogabbro to nepheline syenite) is linked to the removal of large amounts of cumulitic material, mainly olivine and clinopyroxene, as indicated by the abundance of pyroxenitic and dunitic rocks in the field (cf. Figures 2 and 3 of ref. [31]). Clinopyroxene and olivine fractionation is required for the transition from olivine nephelinite/ankaratrite to phonolite/peralkaline phonolite. The exsolution of carbonatite liquids appears to be associated with the evolution of phonolite to peralkaline phonolite liquids [18].
2.1 Petrographic classification
The rock associations present in the alkaline complexes of Southern Brazil are described in detail in refs. [11,14,39]. On the basis of the petrographic associations [14], the carbonatitic occurrences of the Paraná Basin can be classified as follows:
Magmatic carbonatites
Occurrences associated with rock types of the urtite–ijolite–melteigite series, without the presence of extrusive nephelinites (Brazil: Vale do Ribeira: Anitápolis, Ipanema, Itapirapuã, Jacupiranga, Mato Preto and Juquiá; Goiás: Caiapó and Morro do Engenho; Paraguay: Cerro Sarambí and Sapucai).
Brazilian occurrences associated with only olivinites and pyroxenites as ultramafitites (±syenites) as Salitre I and Serra Negra, and with glimmerites as Araxá, Catalão I, Catalão II and Salitre II.
2.2 Major elements’ chemistry
If we neglect those containing SiO2 > 10 wt%, the investigated carbonatites vary from calciocarbonatites (CaO, 39–45; MgO, 0.4–8.1; FeO, 0.1–10.1 wt%) to magnesiocarbonatites (CaO, 0.9–29; MgO, 12.6–46.8; FeO, 1.1–10.9 wt%) and ferruginous (i.e., iron-rich) calciocarbonatites (CaO, 28–36; MgO, 4.3–13.4; FeO, 10.0–30.3 wt%; cf. ref. [11]). However, all the three rock types are rarely associated in the same complex (e.g., Araxá, Barra do Itapirapuã, Itapirapuã; cf. refs. [30,28]). Notably, the Cerro Manomó carbonatite (Bolivia) represents the only example of a ferrocarbonatite (CaO, 7.7; MgO, 0.34; FeO, 40.5; MnO, 7.1 wt% [33,52]). The molar ratio CaO/(CaO + MgO + FeOt + MnO) used as a differentiation index (DI) of carbonatites from Southern Brazil shows a general negative correlation with (MgO + FeOt + MnO) wt% due to Ca–Mg–Fe–Mn substitutions typical of the main carbonate minerals [11]. The data are well consistent with multistage carbonatite evolution associated with changes of the rock-forming mineral assemblages [45], with DI decreasing from the stage I to the stage 4 of Table 1.
2.2.1 Magmatic carbonatites
2.2.1.1 Carbonatites associated with rock types of the urtite–ijolite–melteigite series, without the occurrence of extrusive nephelinites
Whole-rock chemistry data were plotted in the carbonatite classification [60,61] and appear represented by calciocarbonatites followed by magnesiocarbonatites and by ferruginous carbonatites (Figure 2, IA and IB).
In the region of Vale do Ribeira, alkaline carbonatite complexes are present in Anitápolis, Ipanema, Itapirapuã, Jacupiranga, and Juquiá (Figure 2, IA: Early Cretaceous age, 132–109 Ma; cf. ref. [39] and Table 1A of the Appendix). Early-stage magnesiocarbonatites are usually rich in apatite and phlogopite and are found in the same carbonatitic complex only at Jacupiranga, which is considered to be a primary carbonatite [25]. On the opposite, the Juquiá magnesiocarbonatites (the only rock type present in this complex) are modeled as the result of fractionation from exsolved calciocarbonatite magma [22]. This model [22] may represent a suitable picture for all the examined carbonatitic complexes, where various stages of evolution are identified, together with an additional late Fe-enrichment of carbonate liquids (Figure 2, IA and II). A similar picture applies to the genesis and evolution of the Eastern Paraguay carbonatites [27].
The Late Cretaceous (70–86 Ma) Goiás carbonatites from Caiapó, Morro do Engenho, and Santo Antônio da Barra are present in Ca and Mg variants, similar to the Early Cretaceous carbonatites of Cerro Sarambí (139 Ma) and Sapucai (121 Ma) in Paraguay (Figure 2, IB and Table 1A of the Appendix).
2.2.1.2 Alkaline–carbonatite complexes with only olivinite and pyroxenites as ultramafic rocks (±syenites) or with glimmerites
All the complexes of this group belong to the Late Cretaceous (81–86 Ma) episode of alkaline carbonatite magmatism. Both Salitre [64,65] and Serra Negra [66] are without glimmerites (cf. Figure 2, III). Conversely, the complexes of Araxá [67], Catalão I [68], and Catalão II [69] contain glimmerites. Serra Negra and Catalão II calciocarbonatites and magnesiocarbonatites are found in Salitre, whereas only magnesiocarbonatites are found in Araxá and Catalão I (Figure 2, III). Notably, the evolution from phonolite to peralkaline phonolite liquids trend is shown in Figure 2, II [18] and Figure 2 of ref. [12].
2.2.1.3 Carbonatites associated with melilitolites and melilitites
The Upper Cretaceous complexes of Tapira (70 Ma; [62,54]) and Lages (82 Ma; [30]) are the only two representatives of this group. Tapira complex contains calciocarbonatites and subordinate magnesiocarbonatites associated with ultramelilitolites, while in Lages, only ferruginous calciocarbonatites are present (Figure 3, IV) associated with olivine melilitites. According to ref. [70], complete or partial separation of carbonatites from the melite-rich silicate fractions (eventually producing intrusive melilitolites or extrusive melilitites) is related to carbonate–silicate immiscibility, probably occurred under pressure less than 14 kbar and temperature higher than 1,300°C. Subsequently, carbonatites might reach the surface as a separate eruption.
2.2.2 Hydrothermal carbonatites
The carbonatitic complex of Barra do Itapirapuã (115 Ma), according to ref. [28], is represented by rare calciocarbonatites and dominant magnesiocarbonatites with subordinate ferruginous calciocarbonatites (Figure 3, V). Notably, all the rock types formed under hydrothermal conditions at temperatures between 375°C and 80°C [28,71].
The complex of Cerro Chiriguelo (Figure 3, V, 128 Ma) [21,41] shows calciocarbonatites in the central part and veins of ferruginous carbonatite cutting the carbonatitic core.
Finally, Cerro Manomó (139 Ma), in Bolivia, contains carbonate blocks, interpreted by ref. [72] as ferrocarbonatites (Figure 3, V and Table 2 of Appendix). According to ref. [33], the latter rock types are made up of sideritic-ankeritic carbonate, altered at hydrothermal conditions and associated mainly with rare earth elements (REE) fluorocarbonates.
2.2.3 Occurrences with unusual geometric relationships
This group consists of extremely small carbonatite occurrences with geometries that are not present in other carbonatitic complexes in Southern Brazil. A 0.3 m thick fine-grained beforsitic (ferruginous calciocarbonatitic) dyke crosses tinguatic rocks in Itanhaém (Brazil [58]). Basanitic dykes are found in Valle-mí (Paraguay) patches (probably exsolved) of calciocarbonatite[37]. In Cerro Canãda and Cerro E Santa Elena (Paraguay), ocelli made of dolomite, phlogopite, clinopyroxene, olivine, magnetite, and amphibole are contained in trachyandesitic dykes [1,11,12] (Figure 4). Representative analyses are presented in Table 3 of the Appendix and plotted in Figure 3, VI.
2.3 Incompatible elements (IEs)
The results discussed in this section is presented in the same order as the previous section, that is, (1) magmatic carbonatites, (2) hydrothermal carbonatites, and (3) occurrences with unusual geometric relationships (cf. Figures 2 and 3).
2.3.1 Magmatic carbonatites
IE concentrations, which are reported in the Appendix, are shown in Figures 5 (group A) and 6 (groups B and C) as spidergrams normalized to primitive mantle concentrations [73].
The normalized values of the Early and Late Cretaceous magmatic carbonatites appear strongly enriched in La, Ce, Nd, Sm, and Eu, whereas K and Ti are systematically the least enriched elements, or they are depleted. P and Zr present very large variations probably linked to the occasional presence of apatite or phlogopite. As a matter of fact, IE in Brazilian carbonatites typically shows very large variations in the normalized values from one carbonatite complex to another for any given incompatible element [26]. The IE scatter between the different carbonatites reflects to some extent the variable distribution and concentration of mineral phases, which have high contents of selected IE such as phosphates (e.g., apatite and monazite for REE), oxides (e.g., pyrochlore for Nb, REE, Th, and U; calzirtite for Ti and Zr; zirconolite for Ti, Zr, and Nb; and loparite for REE, Ti, and Nb), REE carbonates, and REE fluorocarbonates (e.g., ancylite, bastnäsite, burbankite, and parisite).
Experiments on natural and synthetic mixtures show that carbonatite melts might be enriched in K, P, Sr, Ba, Th, and REE, as well as in F and Cl ([77] and references therein). The presence of F in silicate–carbonate systems positively influences the fractionation of Nb (Ta, U, Th, and REE) in the carbonate phase. Partitioning of IE and REE into the carbonate melt is also supported by experimental results on Nb and light rare earth element (LREE) solubility in synthetic carbonate liquids [78].
Moreover, according to ref. [79], calciocarbonatite liquids can dissolve 5–7.5 wt% of Nb2O5 at 950–600°C. Crystallization of these liquids at first promotes the precipitation of a perovskite-type phase followed by pyrochlore together with calcite. Phase relationships in the join calcite-La-hydroxide of the CaCO3–Ca(OH)2–La(OH)3 system [77,80,81] show that, with the temperature variation from 610 to 700°C and increasing CO2/H2O ratio, the solubility of the LREE hydroxides in simplified carbonatite systems changes from 20% to 40% [81]. Bastnäsite may crystallize together with calcite from magmatic carbonate liquids with a temperature falling from liquidus (650–625°C) to eutectic (about 540°C) and under definite relations between carbon dioxide, water, and fluorine contents.
As shown in ref. [82], Brazilian carbonatites cover a wide range in a La versus La/Yb plot (cf. Figure 4 of ref. [37]), with the carbonate fractions of carbonatites displaying La/Yb ratios and La content two to three times higher than those of the parental rocks [11]. The La versus La/Yb trend of Rio Apa dykes was quantitatively modeled in ref. [37] by assuming that basanite was the carbonatites parental magma. The chemical evolution was described in terms of two main steps: (1) differentiation from basanite to trachyphonolite to phonolite by fractional crystallization and concentration of CO2-rich fluids and (2) exsolution of about 20% carbonatitic liquids from the differentiated phonolitic magma (Figure 7).
Phlogopite-picrite rocks associated with carbonatites in Tapira as well as in other alkaline–carbonatitic complexes in the APIP show a strong compositional affinity to kamafugites present in the northern part of the APIP [6,62,65,83]. Notably, ref. [54] show that liquid immiscibility was a common process (from early phlogopite-picrites to late syenites) in the evolution of the Tapira complex, indicating liquid immiscibility of carbonatitic pockets at the very early stages (Figure 2 of ref. [54]). An exhaustive description of the relationships between carbonatites and associated kamafugites was presented in [39].
The overall very large variability of IE contents between primary carbonatites (formed by early-stage liquid immiscibility) from the different complexes supports the hypothesis that the alkaline–carbonatitic magmatism was produced by local heterogeneous subcontinental mantle sources connected to metasomatic events attributed to Neoarchean to Neoproterozoic time based on isotopic systematics ([11,12]; see also the study by Speziale et al., this issue). Some of this complexity, especially in the pattern of REE contents, can be due to the process of carbonatitic magma unmixing that produce characteristic crossing between the patterns of carbonatites and associated silicate rocks [84].
2.3.2 Hydrothermal carbonatites
REE carbonates, REE fluorocarbonates, and oxides, which are the products of hydrothermal environments, represent to some extent the individual fenitizing fluids enriched in IE rather than the primary carbonates [37]. For instance, different generations of carbonatite dykes are present in the Barra do Itapirapuã complex (Figure 3, V) [28, 85, 86]. In Barra do Itapirapuã, carbonatites are present as dykes and veins stockwork in which at least three main carbonatitic phases are recognized (Figure 3, V), that is, prevailing magnesiocarbonatites, ferruginous calciocarbonatites, and subordinate calciocarbonatites (Figure 8). These carbonatites are generally overprinted by pervasive hydrothermal events at temperatures between 375°C and 80°C during which significant amounts of REE fluorocarbonate minerals, relatively Th- and Sr-rich were deposited. Synchysite, parasite, and bastnäsite may occur as single crystals and/or polycrystals. Textural and chemical relationships between the REE fluorocarbonates provide insights into the mobility of REEs during fluid–rock interaction [28,31,85].
At Cerro Chiriguelo (Figure 8), calciocarbonatites are the prevailing rock types and show relatively high contents of Ba, Ta, Th, and Nb. The subordinate ferruginous calciocarbonatites also display high contents of Nb, Ta, and REE. Nb and Th contents of these rocks appear related to the local abundance of uranpyrochlore [21].
Cerro Manomó presents rare blocks of ferrocarbonatite made up of altered sideritic–ankeritic carbonatite with subordinate goethite–limonite, apatite, and REE-F-carbonates [52]. The latter produces a strong REE enrichment clearly shown in Figure 8.
2.3.3 Occurrences with unusual geometric relationships
The Itanhaém carbonatite (129 Ma, according to ref. [58], is represented by fine-grained Fe-dolomite veins in tinguaitic dykes, particularly enriched in Th and LREE, which make this complex a Th source of economic interest [87]).
Basanitic dykes (about 139 Ma) with a microcrystalline groundmass consisting of about 20 vol% of primary calciocarbonates are present near the town of Valle-mí in Paraguay [41]. The carbonates show large enrichment of Th (Nb and Ta), REE, and Sr, and strong depletion of K and Ti with respect to mantle abundances (Figure 9).
The ijolitic host rocks in Cerro Cañada and Cerro E. Santa Elena alkaline complexes (notional age, 126 Ma [88]) are characterized by ocelli containing dolomite (magnesiocarbonatite; Figure 4) highly enriched in Ba, Sr, and REE ([11,37] and references therein) as shown in Figure 9.
Notably, the IE spidergrams (Figures 5–9) display remarkable scattering even within individual complexes. This is particularly evident between samples of Ca, Mg, and ferroginous calciocarbonatite belonging to different stages of crystallization of the same complex (i.e., magmatic to late-magmatic and hydrothermal conditions).
Different types of distinctive behaviors emerge if we plot REE spidergrams. In Figure 10, we grouped the different carbonatites as a function of their age of emplacement. Here, we can identify three main types of distribution [31]:
Patterns with a strong decrease from La to Lu, which can be observed for instance in the rocks from Cerro Chiriguelo, Jacupiranga, and APIP [6,62] magnesiocarbonatites, Mato Preto, and Lages (both early and late carbonatites). It should be noted that the REE enrichment in Mato Preto and Lages appear to be controlled by late, secondary, carbonatite veins.
Patterns with a relative weakly decrease from La to Lu, as shown in Jacupiranga (calciocarbonatites), Juquiá (magnesiocarbonatites and calciocarbonatites), Anitápolis, and Barra do Itapirapuã (calciocarbonatites).
Concave patterns with a steady decrease from LREE to Dy and an HREE plateau, as found in Valle-mí and Barra do Itapirapuã occurrences. The carbonatites from the latter location contain the highest LREE concentrations due to the presence of REE fluorocarbonates [25,31,32,37,50,62]. Fluorite deposits are also present in Barra do Itapirapuã.
In conclusion, the different behaviors of the early-crystallized carbonatites, which are believed to be “primary” carbonatitic liquids (calciocarbonatites and magnesiocarbonatites), would reflect the chemical signatures of their parental melts (cf. primary calciocarbonatites and magnesiocarbonatites of the Jacupiranga and Juquiá complexes, respectively), as also outlined by ref. [89] and confirm the presence of local scale heterogeneous subcontinental mantle sources of possible due to metasomatic events dating back to the Neoarchean to Neoproterozoic based on radiogenic isotopes systematics [11,12]. The presence of late-crystallized ferruginous calciocarbonatites, variably enriched in fluorocarbonates, indicates hydrothermal processes, also supported by the observed low-temperature mineral associations (cf. [38,39]).
3 Concluding remarks
The alkaline–carbonatitic magmatism from the Southern Brazil is distributed along tectonic lineaments in both American and African continents.
The carbonatites mainly occur in the inner parts of circular/oval-shaped alkaline–carbonatitic complexes, being the rock bodies usually associated with evolved silicate rocks where liquid immiscibility processes played an important role in their genesis.
The geochemical data, major and trace elements, show that the genesis of the magmatism from the Southern Brazilian Platform requires heterogeneous mantle sources. As a matter of fact, the large variation of IE and REE appear related to hydrothermal processes, probably connected to metasomatic sensu lato events that occurred between Neoarchean and Neoproterozoic times [11,12].
The areal distribution of magmatism suggests that the alkaline–carbonatitic magmatism originated from large- to small-scale heterogeneous subcontinental mantle. All the results indicate that asthenospheric components derived from mantle plumes (i.e., Tristan da Cunha and Trindade hot spots [91]) did not significantly contribute to the genesis of the alkaline–carbonatitic magmatism, consistent with the conclusions reached by refs. [2,3,4,11,82,92] for the petrogenesis of the Paraná flood tholeiites
Regional thermal anomalies in the deep mantle, mapped by geoid and seismic tomography, support a nonplume-related heat source for the southern Brazil magmatism [4,93,96], where the hotspot tracks of Walvis Ridge and Rio Grande Rise, as well as the Victória–Trindade chain, might reflect the accommodation of stresses in the lithosphere during rifting rather than continuous magmatic activity induced by mantle plumes beneath the moving lithospheric plates (cf. also the study by Speziale et al., this issue), where the main conclusions relative to the Brazilian carbonatites are reported).
Acknowledgements
S.S. acknowledges support from the Deutsche Forschungsgemeinschaft DFG (FOR 2125). We thank the editor Dr. J. Barabach and an anonymous reviewer. F. Stoppa is thanked for his very detailed comments and suggestions which helped us to improve our manuscript. We also thank O. Gerel, V.A.V. Girardi and L. Kogarko for their comments.
Appendix
Magmatic carbonatites
Anitápolis age: 131 (1) Ma | Ipanema age: 124.9 (9.5) Ma | ||||||
---|---|---|---|---|---|---|---|
Sample | SAN 1.0 | 14–49 | 12–78 | 11–101 | 16A–50.5 | 49–82 | 119.2 |
wt% | |||||||
SiO2 | 0.31 | 0.20 | 2.45 | 1.20 | 0.47 | 3.00 | 3.97 |
TiO2 | 0.01 | 0.01 | 0.06 | 0.05 | 0.07 | 0.08 | 0.13 |
Al2O3 | 0.21 | 0.02 | 0.01 | 0.09 | 0.10 | 0.52 | 0.19 |
FeO | 0.08 | 2.59 | 2.03 | 2.95 | 4.49 | 5.96 | 7.61 |
MnO | 0.07 | 0.08 | 0.23 | 0.22 | 0.23 | 1.80 | 0.25 |
MgO | 1.55 | 2.30 | 4.13 | 1.83 | 1.70 | 12.80 | 1.08 |
CaO | 53.59 | 51.25 | 49.36 | 52.15 | 51.80 | 31.43 | 47.60 |
Na2O | 0.05 | 0.16 | 0.34 | 0.01 | 0.07 | 1.51 | 0.37 |
K2O | 0.49 | 0.78 | 0.07 | 0.02 | 0.06 | 1.01 | 0.30 |
P2O5 | 0.48 | 1.31 | 2.37 | 2.89 | 1.80 | 2.12 | 1.73 |
L.O.I. | 42.06 | 40.13 | 38.72 | 38.25 | 38.37 | 38.64 | 35.68 |
Sum | 98.90 | 98.83 | 99.77 | 99.66 | 100.06 | 99.03 | 98.91 |
IE (ppm) | |||||||
Rb | 3.2 | 6.1 | 6.5 | 6.9 | 5.5 | 3.22 | 8 |
Ba | 1052 | 951 | 1579 | 1121 | 894 | 1106 | 500 |
Th | 5.6 | 3.5 | 0.31 | 0.09 | 0.27 | 5.50 | 0.8 |
Nb | 5.2 | 8.9 | 7.8 | 10.4 | 8.3 | 6.32 | 4.0 |
Ta | 1.4 | 0.5 | 1.5 | 1.8 | 1.4 | 1.02 | 0.3 |
K | 4,068 | 6,475 | 581 | 166 | 498 | 83 | 2,491 |
Sr | 2,462 | 2,983 | 6,849 | 4,462 | 2,779 | 2,462 | 5,950 |
P | 20,950 | 5,717 | 10,343 | 12,612 | 7,855 | 524 | 2,550 |
Hf | 0.4 | 0.4 | 1.8 | 0.8 | 0.38 | 0.67 | 1.4 |
Zr | 15.8 | 7.7 | 46.2 | 15.5 | 16.4 | 18.74 | 54 |
Ti | 60 | 60 | 360 | 300 | 420 | 480 | 779 |
Y | 43.7 | 18.8 | 45.9 | 42.9 | 41.5 | 29.81 | 20 |
REE | |||||||
La | 67.1 | 41.2 | 123.4 | 48.6 | 158 | 979 | 76.1 |
Ce | 142.3 | 90.3 | 287 | 106.5 | 372 | 2,657 | 170 |
Pr | 16.8 | 12.2 | 29.2 | 14.5 | 37.8 | 291 | 23.9 |
Nd | 69.6 | 47.5 | 115.7 | 53.5 | 170.4 | 1,154 | 196 |
Sm | 13.8 | 9.4 | 21.33 | 9.44 | 29.22 | 326 | 22 |
Eu | 4.0 | 2.53 | 6.51 | 3.91 | 8.55 | 129.4 | 6.24 |
Gd | 12.6 | 7.91 | 19.83 | 8.90 | 20.61 | 475 | 15.9 |
Tb | 1.87 | 1.35 | 2.17 | 1.59 | 3.48 | 61.3 | 1.6 |
Dy | 9.62 | 7.67 | 11.63 | 9.04 | 12.17 | 728 | 5.9 |
Ho | 1.74 | 1.39 | 2.44 | 1.64 | 2.11 | 131.2 | 0.8 |
Er | 4.81 | 3.17 | 5.90 | 3.74 | 4.43 | 155.7 | 1.9 |
Tm | 0.63 | 0.56 | 0.81 | 0.67 | 0.71 | 23.76 | 0.25 |
Yb | 3.74 | 3.09 | 4.83 | 3.48 | 3.07 | 25.00 | 1.5 |
Lu | 0.59 | 0.44 | 0.65 | 0.51 | 0.36 | 3.21 | 0.19 |
Mol% | |||||||
CaO | 96.0 | 90.6 | 95.9 | 91.0 | 89.5 | 56.8 | 86.2 |
FeO + MnO | 0.2 | 3.7 | 3.5 | 4.3 | 6.4 | 11.0 | 11.1 |
MgO | 3.8 | 5.7 | 0.6 | 4.7 | 4.1 | 32.2 | 2.7 |
MatoPreto age: 70 (1) Ma | Juquiá age: 132 (3) Ma | ||||||||||
---|---|---|---|---|---|---|---|---|---|---|---|
Sample | I—119.3 | I—84.0 | II—77.0 | III—70.0 | III—62.2 | III—622 | S16C | S25 | S26A | S26B | SJT |
Wt% | |||||||||||
SiO2 | 0.30 | 0.23 | 0.52 | 1.91 | 2.28 | 3.22 | 0.24 | 0.30 | 0.27 | 0.36 | 0.29 |
TiO2 | 0.01 | 0.01 | 0.11 | 0.02 | 0.11 | 0.06 | 0.02 | 0.01 | 0.03 | 0.02 | 0.02 |
Al2O3 | 0.23 | 0.14 | 0.21 | 0.21 | 0.59 | 0.81 | 0.07 | 0.10 | 0.09 | 0.11 | 0.10 |
FeO | 1.81 | 0.92 | 2.23 | 1.73 | 10.01 | 4.56 | 1.54 | 1.72 | 1.58 | 1.69 | 1.63 |
MnO | 0.19 | 0.19 | 0.22 | 0.21 | 0.73 | 0.39 | 0.38 | 0.52 | 0.43 | 0.47 | 0.45 |
MgO | 0.99 | 0.33 | 1.32 | 0.51 | 6.12 | 1.49 | 12.59 | 17.11 | 17.52 | 17.55 | 16.49 |
CaO | 54.35 | 54.83 | 53.13 | 55.01 | 39.21 | 49.74 | 37.83 | 30.90 | 31.05 | 30.39 | 32.54 |
Na2O | 0.03 | 0.01 | 0.02 | 0.01 | 0.10 | 0.06 | 0.89 | 0.45 | 0.45 | 0.46 | 0.56 |
K2O | 0.10 | 0.07 | 0.09 | 0.31 | 0.58 | 1.09 | 0.02 | 0.02 | 0.02 | 0.02 | 0.04 |
P2O5 | 0.52 | 0.17 | 0.51 | 0.16 | 0.28 | 1.67 | 13.25 | 5.47 | 5.57 | 5.28 | 6.14 |
L.O.I. | 41.27 | 43.15 | 41.38 | 40.16 | 38.89 | 36.40 | 33.14 | 43.88 | 42.97 | 43.61 | 40.90 |
Sum | 99.83 | 100.05 | 99.74 | 100.24 | 98.90 | 99.49 | 99.97 | 99.98 | 99.98 | 99.96 | 99.16 |
IE | |||||||||||
ppm | |||||||||||
Rb | 2.9 | 4.3 | 6.8 | 10.2 | 1.6 | 189 | 4 | 5 | 6 | 3 | 4.5 |
Ba | 175 | 3,798 | 1,134 | 449 | 8,378 | 2,226 | 1,700 | 3,780 | 12,500 | 4,490 | 5,618 |
Th | 44.8 | 19.9 | 82 | 147 | 811 | 117.8 | 2.73 | 5.00 | 4.51 | 4.68 | 4.23 |
Nb | 251 | 384 | 23 | 95 | 315 | 25.1 | 16 | 8 | 20 | 16 | 16 |
Ta | 9.4 | 18.7 | 0.8 | 6.3 | 11.8 | 1.4 | 0.74 | 2.13 | 0.74 | 1.70 | 1.33 |
K | 830 | 581 | 747 | 2,574 | 4,815 | 9,049 | 166 | 166 | 166 | 166 | 332 |
Sr | 8,735 | 2,134 | 8,758 | 1,053 | 3,693 | 4,652 | 8,450 | 5,540 | 5,720 | 5,190 | 5,985 |
P | 2,269 | 742 | 2,226 | 698 | 1,222 | 7,288 | 57,783 | 23,871 | 24,291 | 23,042 | 26,795 |
Hf | 2.9 | 7.7 | 0.2 | 3.7 | 2.4 | 4.9 | 1.25 | 2.62 | 1.55 | 3.24 | 2.18 |
Zr | 45.9 | 123 | 23 | 183 | 123 | 178 | 16 | 7 | 20 | 16 | 15 |
Ti | 60 | 60 | 659 | 120 | 659 | 179 | 120 | 60 | 180 | 120 | 120 |
Y | 74.3 | 121 | 192 | 225 | 96 | 673 | 339 | 402 | 119 | 202 | 266 |
REE | |||||||||||
La | 198 | 165 | 241 | 3,686 | 852 | 1,112 | 99.3 | 99.1 | 68.6 | 85.2 | 88.1 |
Ce | 377 | 461 | 717 | 6,510 | 1,577 | 1,808 | 262 | 257 | 177 | 221 | 232 |
Pr | 44.3 | 69.5 | 101 | 581 | 155 | 233 | 34.5 | 30.7 | 24.2 | 31.4 | 30.5 |
Nd | 156 | 341 | 461 | 884 | 350 | 948 | 164 | 149 | 97.9 | 120 | 148 |
Sm | 25.8 | 73.4 | 91 | 174 | 52 | 79 | 31.5 | 29.5 | 18.9 | 23.2 | 26.8 |
Eu | 8.2 | 22.6 | 22.2 | 56.8 | 17.0 | 25.0 | 17.6 | 21.3 | 7.54 | 11.5 | 12.4 |
Gd | 24.1 | 76.2 | 71 | 161 | 48 | 88 | 66.7 | 72.6 | 21.5 | 32.1 | 49.9 |
Tb | 3.74 | 12.0 | 8.3 | 23.1 | 6.9 | 14.4 | 12.3 | 12.2 | 4.1 | 7.6 | 9.2 |
Dy | 17.3 | 67.3 | 39.9 | 86 | 30.2 | 90 | 59.7 | 70.3 | 21.6 | 36.8 | 53.0 |
Ho | 2.81 | 12.3 | 6.7 | 9.7 | 5.1 | 18.2 | 11.3 | 12.9 | 4.1 | 6.0 | 9.7 |
Er | 7.3 | 24.0 | 16.0 | 26.5 | 10.4 | 47 | 27.6 | 32.2 | 10.5 | 17.0 | 25.8 |
Tm | 1.07 | 2.83 | 2.6 | 3.8 | 1.7 | 6.9 | 3.8 | 4.3 | 1.0 | 1.7 | 3.7 |
Yb | 4.78 | 10.2 | 8.5 | 22.6 | 11.3 | 34.1 | 17.3 | 21.7 | 5.93 | 9.69 | 16.8 |
Lu | 0.42 | 1.53 | 2.20 | 3.34 | 1.8 | 5.7 | 1.65 | 2.07 | 0.52 | 0.64 | 1.60 |
Mol% | |||||||||||
CaO | 94.9 | 97.6 | 93.4 | 96.1 | 69.9 | 89.3 | 66.6 | 54.7 | 54.5 | 53.8 | 57.0 |
FeO + MnO | 2.7 | 1.6 | 3.4 | 2.6 | 15.0 | 7.0 | 2.6 | 3.1 | 2.8 | 3.0 | 2.8 |
MgO | 2.4 | 0.8 | 3.2 | 1.3 | 15.1 | 3.7 | 30.8 | 42.2 | 42.7 | 43.2 | 40.2 |
Goiás | Caiapó age: 86 (6) Ma | Morro do Engenho age: 86 (6) Ma | Santo Antônio da Barra age: 86 (6) Ma | Paraguay Cerro Sarambí age: 138.9 (0.9) Ma | Paraguay Sapucai age: 128.6 (2) Ma | ||
---|---|---|---|---|---|---|---|
CR-09 | ME-C | SAB-12 | GL-SA | GL-SA | SA-958 Trachyphonolite | PS72 Phonotephrite | |
Glimmerite-Carbonatite (whole rock) | Carbonate Fraction (dolomite) | Carbonate Fraction (dolomite) | Carbonate Fraction (calcite 7%) | Carbonate Fraction (24.3 wt%) | |||
Wt% | |||||||
SiO2 | 2.26 | 0.62 | 0.88 | 28.82 | — | — | —- |
TiO2 | 0.27 | 0.15 | 0.07 | 3.22 | 0.06 | 0.05 | — |
Al2O3 | 0.10 | 0.05 | 0.05 | 7.37 | — | — | — |
FeO | 4.71 | 3.14 | 3.53 | 8.71 | 1.49 | 4.25 | 2.51 |
MnO | 0.26 | 0.23 | 0.28 | 0.11 | — | — | 0.26 |
MgO | 3.78 | 4.71 | 14.85 | 19.27 | 20.83 | 3.95 | 20.17 |
CaO | 45.94 | 46.30 | 32.85 | 9.23 | 30.21 | 48.12 | 30.04 |
Na2O | 0.28 | 0.19 | 0.05 | 0.29 | — | — | 0.25 |
K2O | 0.10 | 0.12 | 0.04 | 3.35 | 0.08 | 0.07 | — |
P2O5 | 7.70 | 1.01 | 2.29 | 0.31 | 0.39 | 0.33 | — |
L.O.I. | 33.02 | 41.04 | 42.39 | 16.21 | 47.19 | 43.37 | 46.77 |
Sum | 98.42 | 97.56 | 97.28 | 97.99 | 100.00 | 100 | 100.00 |
IE | |||||||
ppm | |||||||
Rb | 2.0 | 4.0 | 2.3 | 138.1 | 6.7 | 16.9 | 0.21 |
Ba | 4,454 | 4,872 | 16,469 | 2,082 | 101 | 36 | 262 |
Th | 301 | 103 | 104 | 12.5 | 26 | 37 | 0.32 |
Nb | 53.1 | 113 | 50.1 | 94 | 93 | 112 | 0.90 |
Ta | 12.9 | 4.4 | 4.5 | 7.7 | 6.8 | 9.2 | 0.76 |
K | 830 | 996 | 332 | 27,812 | 664 | 581 | — |
Sr | 11,669 | 10,542 | 10,851 | 1,387 | 2,860 | 4,066 | 268 |
P | 33,603 | 4,408 | 5,014 | 1,353 | 1,702 | 1,444 | — |
Hf | 8.9 | 2.23 | 2.23 | 7.1 | 6.6 | 5.4 | — |
Zr | 324 | 125 | 171 | 289 | 370 | 292 | — |
Ti | 1,619 | 899 | 420 | 19,304 | 360 | 300 | — |
Y | 377 | 107 | 129 | 23 | 8.6 | 23 | 23.75 |
REE | |||||||
La | 455 | 1,011 | 909 | 167 | 513 | 343 | 239 |
Ce | 1,093 | 1,647 | 1,725 | 319 | 980 | 654 | 420 |
Pr | 147 | 162 | 103 | 35.6 | 45.3 | 41 | 46.8 |
Nd | 637 | 513 | 682 | 123 | 139 | 138 | 159.9 |
Sm | 119 | 92.8 | 133 | 14.7 | 20.1 | 18.3 | 19.1 |
Eu | 59.5 | 25.0 | 33.7 | 3.9 | 6.1 | 5.25 | 3.90 |
Gd | 140 | 64.7 | 82.9 | 10.1 | 19.3 | 10.4 | 14.90 |
Tb | 19.8 | 6.54 | 7.96 | 1.03 | 2.14 | 1.65 | 2.12 |
Dy | 89.4 | 26.5 | 32.4 | 7.6 | 12.9 | 8.7 | 10.57 |
Ho | 14.9 | 4.89 | 4.99 | 1.1 | 2.51 | 1.9 | 2.05 |
Er | 22.7 | 6.04 | 7.22 | 2.9 | 6.27 | 4.8 | 5.40 |
Tm | 2.88 | 0.45 | 0.54 | 0.40 | 0.68 | 0.53 | 3.16 |
Yb | 10.0 | 2.07 | 2.55 | 1.70 | 3.28 | 2.53 | 24.7 |
Lu | 1.11 | 0.92 | 0.35 | 0.23 | 0.43 | 0.34 | 0.32 |
Mol% | |||||||
CaO | 83.4 | 83.5 | 59.0 | 21.5 | 50.1 | 84.5 | 49.9 |
FeO + MnO | 7.1 | 4.7 | 5.4 | 16.0 | 1.9 | 5.8 | 3.6 |
MgO | 9.5 | 11.8 | 35.6 | 62.5 | 48.0 | 9.7 | 46.5 |
Sample | Salitre I Age: 86.3 (4.2) Ma | ||||||
---|---|---|---|---|---|---|---|
C1 | C4 | ASL013 | ASL031 | ASL034 | ASL036 | 09A-60A | |
Wt% | |||||||
SiO2 | 0.06 | 1.34 | 0.22 | 0.33 | 0.42 | 0.24 | 0.26 |
TiO2 | 0.01 | 0.38 | 0.17 | 0.06 | 0.01 | 0.01 | 0.01 |
Al2O3 | 0.01 | 0.09 | 0.17 | 0.32 | 0.19 | 0.23 | 0.01 |
FeO | 1.46 | 2.35 | 2.88 | 3.09 | 0.66 | 1.67 | 0.18 |
MnO | 0.12 | 0.56 | 0.39 | 0.19 | 0.15 | 0.22 | 0.08 |
MgO | 0.79 | 14.65 | 18.48 | 14.88 | 5.17 | 19.35 | 1.57 |
CaO | 53.84 | 28.75 | 25.13 | 35.40 | 46.11 | 29.72 | 53.94 |
Na2O | 0.17 | 0.17 | 0.10 | 0.19 | 0.46 | 0.50 | 0.13 |
K2O | 0.11 | 0.22 | 0.03 | 0.05 | 0.01 | 0.16 | 0.11 |
P2O5 | 0.01 | 6.69 | 0.43 | 10.16 | 0.01 | 0.66 | 0.99 |
L.O.I. | 40.70 | 32.20 | 46.14 | 34.77 | 44.70 | 46.04 | 41.20 |
Sum | 97.25 | 99.04 | 94.14 | 99.47 | 97.89 | 98.77 | 98.49 |
IE | |||||||
ppm | |||||||
Rb | 1.6 | 4.4 | 15.3 | 3.3 | 6.5 | 10.7 | 5.7 |
Ba | 3,178 | 5,007 | 28,394 | 32 | 32.6 | 266 | 326.5 |
Th | 10.5 | 57.8 | 164 | 1.5 | 80.2 | 20.5 | 155 |
Nb | 14.2 | 88.9 | 77.3 | 629 | 695 | 161 | 524 |
Ta | 0.10 | 0.5 | 1.13 | n.a. | n.a. | 2.9 | 23.9 |
K | 913 | 1,826 | 249 | 415 | 83 | 1,328 | 913 |
Sr | 17,56o | 26,480 | 10,147 | 6,683 | 6,661 | 7,100 | 3,180 |
P | 44 | 29,195 | 1,877 | 44,338 | 83 | 2,880 | 4,320 |
Hf | 0.11 | 3.0 | 0.24 | n.a. | n.a. | 0.37 | 25.1 |
Zr | 3.50 | 97.3 | 4.2 | 44.1 | 14.9 | 6.7 | 1,071 |
Ti | 60 | 2,278 | 1,019 | 360 | 60 | 60 | 60 |
Y | 53.9 | 95 | 66.5 | 54 | 20.5 | 15.6 | 79.1 |
REE | |||||||
La | 373 | 6,354 | 1,846 | 264 | 107 | 85.1 | 431 |
Ce | 701 | 8,541 | 3,486 | 684 | 283 | 181 | 1,203 |
Pr | 68.8 | 700 | 400 | n.a. | n.a. | 7.8 | 149 |
Nd | 242 | 2,204 | 1,452 | 319 | 128 | 79 | 566 |
Sm | 38.8 | 201 | 202 | 44 | 17.7 | 11.0 | 72.3 |
Eu | 7.28 | 44.8 | 55.4 | n.a. | n.a. | 2.7 | 19.2 |
Gd | 21.16 | 82.0 | 125 | n.a. | n.a. | 6.4 | 41.6 |
Tb | 2.27 | 8.74 | 10.34 | n.a. | n.a. | 0.70 | 5.66 |
Dy | 10.04 | 30.4 | 26.04 | n.a. | n.a. | 2.70 | 18.14 |
Ho | 1.66 | 2.98 | 2.73 | n.a. | n.a. | 0.32 | 2.51 |
Er | 4.02 | 6.66 | 4.91 | n.a. | n.a. | 0.61 | 4.82 |
Tm | 0.60 | 0.76 | 0.70 | n.a. | n.a. | 0.09 | 0.61 |
Yb | 3.48 | 4.27 | 4.84 | n.a. | n.a. | 0.42 | 3.27 |
Lu | 0.53 | 0.45 | 0.68 | n.a. | n.a. | 0.09 | 0.41 |
Mol% | |||||||
CaO | 95.8 | 55.9 | 47.1 | 60.3 | 85.5 | 51.2 | 95.8 |
FeO + MnO | 2.2 | 4.4 | 4.8 | 4.4 | 1.2 | 2.5 | 0.4 |
MgO | 2.0 | 39.7 | 48.1 | 35.3 | 13.3 | 46.3 | 3.8 |
Sample | Serra Negra age: 83(5) Ma | ||||||
---|---|---|---|---|---|---|---|
LG-03-70 | LG-14-28 | LG-06-32 | LG-13-125 | LG20-91.5 | LG32-63.80 | LG38-46-142 | |
wt% | |||||||
SiO2 | 0.54 | 0.88 | 0.65 | 0.74 | 0.20 | 0.92 | 0.14 |
TiO2 | 0.02 | 0.20 | 0.04 | 0.05 | 0.01 | 0.11 | 0.01 |
Al2O3 | 0.01 | 0.09 | 0.04 | 0.03 | 0.02 | 0.34 | 0.01 |
FeO | 1.98 | 5.29 | 1.80 | 4.19 | 1.11 | 2.96 | 1.69 |
MnO | 0.13 | 0.14 | 0.11 | 0.14 | 0.25 | 0.60 | 0.40 |
MgO | 3.60 | 3.15 | 2.97 | 4.51 | 19.44 | 18.98 | 19.50 |
CaO | 48.82 | 45.94 | 48.61 | 45.87 | 29.36 | 27.71 | 29.23 |
Na2O | 0.03 | 0.06 | 0.10 | 0.07 | 0.06 | 0.09 | 0.13 |
K2O | 0.09 | 0.12 | 0.16 | 0.15 | 0.03 | 0.05 | 0.05 |
P2O5 | 0.48 | 3.32 | 3.62 | 2.59 | 0.35 | 0.26 | 0.09 |
L.O.I. | 43.11 | 39.52 | 40.21 | 39.69 | 46.70 | 45.90 | 47.82 |
Sum | 98.81 | 98.70 | 98.31 | 98.03 | 97.53 | 97.93 | 99.07 |
IE | |||||||
ppm | |||||||
Rb | 2.10 | 5.00 | 5.30 | 7.50 | 1.30 | 2.70 | 0.80 |
Ba | 2,768 | 2,314 | 2,391 | 3,515 | 930 | 1,502 | 2,187 |
Th | 2.30 | 38.8 | 44.4 | 7.30 | 31 | 41.2 | 11.6 |
Nb | 97.3 | 373 | 292 | 129 | 280 | 299.4 | 5.30 |
Ta | 22.0 | 28.0 | 23.3 | 8.60 | 16.7 | 3.30 | 0.05 |
K | 747 | 996 | 1,329 | 1,245 | 249 | 415 | 415 |
Sr | 13,268 | 18,833 | 16,122 | 11,354 | 12,051 | 5,517 | 10,003 |
P | 2,095 | 14,488 | 15,798 | 11,303 | 1,527 | 1,134 | 393 |
Hf | 6.40 | 1.60 | 1.20 | 2.10 | 0.40 | 0.10 | 0.05 |
Zr | 326.2 | 73.2 | 46.2 | 89.2 | 13 | 9.20 | 1.80 |
Ti | 120 | 1,199 | 240 | 300 | 60 | 659 | 60 |
Y | 35.3 | 54.8 | 73.9 | 40.9 | 4.90 | 72.4 | 9.10 |
REE | |||||||
La | 290 | 414 | 498 | 374 | 82.4 | 818 | 135 |
Ce | 517 | 783 | 959 | 699 | 152.9 | 1,511 | 201 |
Pr | 60.04 | 93.82 | 122.66 | 85.61 | 17.41 | 215 | 21.14 |
Nd | 202.6 | 321.6 | 427.9 | 291.2 | 59.30 | 805 | 66.90 |
Sm | 24.39 | 41.25 | 54.93 | 36.54 | 6.23 | 103.32 | 7.80 |
Eu | 6.52 | 10.89 | 15.25 | 9.58 | 1.56 | 27.30 | 2.36 |
Gd | 16.31 | 28.04 | 38.42 | 24.09 | 3.67 | 68.44 | 6.93 |
Tb | 1.80 | 3.03 | 4.24 | 2.53 | 0.37 | 7.02 | 0.93 |
Dy | 8.28 | 12.79 | 17.99 | 10.54 | 1.44 | 25.30 | 3.56 |
Ho | 1.26 | 1.93 | 2.60 | 1.45 | 0.18 | 2.77 | 0.38 |
Er | 2.74 | 4.21 | 5.76 | 3.00 | 0.35 | 4.10 | 0.53 |
Tm | 0.35 | 9.56 | 0.76 | 0.41 | 0.04 | 0.45 | 0.07 |
Yb | 2.03 | 3.27 | 4.12 | 2.23 | 0.27 | 2.19 | 0.32 |
Lu | 0.27 | 0.41 | 0.50 | 0.27 | 0.03 | 0.20 | 0.04 |
Mol% | |||||||
CaO | 88.0 | 84.2 | 89.6 | 82.6 | 51.1 | 48.7 | 50.4 |
FeO + MnO | 3.0 | 7.8 | 2.8 | 6.1 | 1.8 | 4.9 | 2.8 |
MgO | 9.0 | 8.0 | 7.6 | 11.3 | 47.1 | 46.4 | 46.8 |
Sample | Araxá age: 88 (10) Ma | Catalão I age: 87 (4) Ma | Catalão II age: 85 (6) Ma | ||||||||||
---|---|---|---|---|---|---|---|---|---|---|---|---|---|
AE 891 Phlo-rich | AR 892 Phlo- rich | AR 893 | C1- L1250 | C1CB02 | C1C4 | C1C12B | C1C14 | C2-AA 165907 | C2A2 | C2B19 | C2B18 | C2B17 | |
wt% | |||||||||||||
SiO2 | 9.74 | 9.93 | 2.15 | 1.75 | 0.25 | 0.64 | 4.67 | 0.22 | 8.95 | 4.02 | 3.46 | 14.89 | 0.21 |
TiO2 | 2.86 | 2.90 | 1.92 | 0.08 | 0.01 | 0.02 | 0.25 | 0.01 | 0.44 | 0.05 | 0.88 | 0.12 | 0.01 |
Al2O3 | 2.76 | 2.81 | 2.79 | 0.08 | 0.11 | 0.05 | 0.13 | 0.02 | 0.20 | 0.06 | 0.03 | 0.28 | 0.01 |
FeO | 11.13 | 9.75 | 10.34 | 8.89 | 5.40 | 1.80 | 10.89 | 1.23 | 9.45 | 2.29 | 4.65 | 7.58 | 0.21 |
MnO | 0.19 | 0.16 | 0.18 | 0.28 | 0.22 | 0.37 | 0.85 | 0.61 | 0.25 | 0.10 | 0.11 | 0.09 | 0.07 |
MgO | 18.10 | 16.54 | 18.31 | 14.60 | 17.36 | 19.26 | 31.30 | 46.81 | 2.56 | 2.82 | 2.51 | 8.12 | 0.56 |
CaO | 13.70 | 14.61 | 16.16 | 23.23 | 33.59 | 25.41 | 10.35 | 0.92 | 39.90 | 46.49 | 46.02 | 32.99 | 53.56 |
Na2O | 0.21 | 0.11 | 0.14 | 0.05 | 0.06 | 0.07 | 0.01 | 0.01 | 0.82 | 0.10 | 0.06 | 0.14 | 0.11 |
K2O | 5.21 | 4.45 | 2.29 | 0.31 | 0.14 | 0.01 | 0.01 | 0.03 | 0.63 | 1.10 | 0.84 | 3.42 | 0.14 |
P2O5 | 0.22 | 0.19 | 0.18 | 4.34 | 0.10 | 1.04 | 2.59 | 0.09 | 1.49 | 1.08 | 2.71 | 14.79 | 0.25 |
L.O.I. | 35.07 | 38.85 | 44.64 | 31.20 | 41.20 | 41.95 | 34.35 | 50.89 | 31.70 | 38.52 | 35.11 | 13.91 | 42.78 |
Sum | 99.19 | 100.30 | 99.18 | 99.24 | 99.06 | 90.60 | 95.39 | 100.07 | 96.41 | 96.65 | 96.39 | 96.36 | 97.89 |
IE | |||||||||||||
ppm | |||||||||||||
Rb | 149 | 138 | 1.1 | 19.5 | 1.7 | 3 | 6 | 2 | 24.6 | 51 | 56 | 233 | 4 |
Ba | 1,299 | 1,203 | 1,648 | 7,622 | 1,573 | 52,300 | 3,936 | 233 | 4,174 | 5,305 | 3,036 | 1,430 | 4,531 |
Th | 18.21 | 16–97 | 23.1 | 18.3 | 12.1 | 26 | 44.8 | 3.2 | 158 | 7.5 | 4.6 | 29.5 | 1.4 |
Nb | 2,750 | 2,514 | 32.1 | 306 | 203 | 231 | 434 | 9 | 310 | 109 | 127 | 238 | 14 |
Ta | 16.5 | 14.9 | 1.22 | 73.5 | 48.7. | 0.1 | 6.9 | 0.1 | 31.6 | 0.70 | 3.4 | 7.5 | 0.20 |
K | 43,253 | 36,944 | 19,812 | 2,784 | 1,162 | 83 | 83 | 249 | 5,230 | 9,132 | 6,974 | 28,393 | 1,162 |
Sr | 1,150 | 1,230 | 5,937 | 18,975 | 10,723 | >10,000 | 6,176 | 2,120 | 13,981 | >10,000 | >10,000 | 8,377 | >10,000 |
P | 960 | 829 | 786 | 18,940 | 436 | 4,539 | 11,303 | 393 | 6,502 | 4,713 | 11,826 | 10,8913 | 1,091 |
Hf | 4.14 | 2.44 | 0.19 | 4.5 | 1.00 | 0.2 | 10.3 | 0.2 | 4.0 | 0.50 | 1.01 | 0.60 | 0.20 |
Zr | 170 | 100 | 7.8 | 171 | 30.4 | 21 | 393 | 6 | 313 | 17 | 28 | 15 | 6 |
Ti | 17,146 | 17,386 | 11,510 | 480 | 60 | 120 | 1,499 | 60 | 2,638 | 300 | 5,276 | 719 | 60 |
Y | 54 | 44 | 90 | 24.1 | 10.7 | 31 | 271 | 19 | 93.5 | 34 | 27 | 56 | 28 |
REE | |||||||||||||
La | 506 | 351 | 413 | 398 | 154 | 729 | 2,000 | 326 | 643 | 388 | 398 | 485 | 398 |
Ce | 1,083 | 657 | 751 | 860 | 375 | 1,660 | 3,000 | 727 | 1,200 | 750 | 784 | 1,060 | 742 |
Pr | 131 | 79 | 91 | 95.7 | 46.0 | 189 | 1,000 | 85.4 | 121 | 81.1 | 85.7 | 123 | 76.2 |
Nd | 320 | 225 | 324 | 362.7 | 181.6 | 569 | 2,000 | 273 | 422.5 | 269 | 224 | 329 | 189 |
Sm | 50.6 | 35.1 | 50.1 | 64.9 | 25.75 | 86.3 | 537 | 46.8 | 50.76 | 32.9 | 32.5 | 48 | 27.3 |
Eu | 12.5 | 7.74 | 15.50 | 11.48 | 6.31 | 23.1 | 121 | 11.5 | 12.1 | 8.74 | 8.22 | 11.7 | 7.13 |
Gd | 35.16 | 24.39 | 34.81 | 34.05 | 11.36 | 53.8 | 277 | 26.2 | 35.88 | 21.8 | 21.3 | 32.8 | 18.7 |
Tb | 4.60 | 2.81 | 4.53 | 2.60 | 1.08 | 4.6 | 24.3 | 2.3 | 4.66 | 2.3 | 2.0 | 3.2 | 1.8 |
Dy | 22.00 | 13.44 | 21.67 | 8.26 | 3.34 | 14.4 | 76.7 | 7.0 | 21.87 | 8.9 | 7.3 | 13.5 | 7.2 |
Ho | 3.39 | 2.07 | 3.34 | 0.92 | 0.31 | 1.6 | 9.8 | 0.8 | 3.35 | 1.4 | 1.0 | 2.2 | 1.0 |
Er | 6.68 | 4.40 | 8.55 | 1.26 | 0.58 | 2.6 | 22.7 | 1.5 | 7.49 | 3.4 | 2.4 | 5.5 | 2.5 |
Tm | 0.79 | 0.52 | 1.01 | 0.15 | 0.08 | <0.05 | <0.05 | <0.06 | 0.93 | 0.41 | 0.26 | 0.68 | 0.29 |
Yb | 3.72 | 2.46 | 4.78 | 0.89 | 0.45 | 0.7 | 5.2 | 0.5 | 5.29 | 2.0 | 1.2 | 3.5 | 1.4 |
Lu | 0–47 | 0.26 | 0.74 | 0.10 | 0.06 | 0.04 | 0.05 | 0.04 | 0.72 | 0.25 | 0.12 | 0.43 | 0.16 |
Mol% | |||||||||||||
CaO | 28.7 | 32.2 | 32.4 | 45.7 | 54.1 | 47.1 | 16.4 | 1.4 | 78.2 | 88.9 | 86.8 | 65.6 | 98.2 |
FeO + MnO | 18.5 | 17.1 | 16.5 | 14.3 | 7.1 | 3.2 | 14.7 | 2.1 | 14.8 | 2.6. | 7.0 | 11.9 | 0.4 |
MgO | 52.8 | 50.7 | 51.1 | 40.0 | 38.8 | 49.7 | 68.9 | 96.5 | 7.0 | 7.5 | 6.5 | 22.5 | 1.4 |
na = not available.
Sample | Tapira age: 70 (9) Ma | Lages age: 82 (6) Ma | |||
---|---|---|---|---|---|
T 1 | T 2 | TPTAPS | SB05A | SB02 | |
Wt% | |||||
SiO2 | 0.70 | 0.02 | 1.16 | 2.53 | 1.46 |
TiO2 | 0.33 | 0.05 | 0.10 | 0.05 | 0.04 |
Al2O3 | 0.20 | 0.07 | 0.06 | 0.87 | 0.83 |
FeO | 10.13 | 0.12 | 3.96 | 10.28 | 17.74 |
MnO | 0.17 | 0.06 | 0.11 | 1.06 | 2.39 |
MgO | 6.35 | 3.85 | 2.44 | 14.16 | 12.72 |
CaO | 38.48 | 51.00 | 50.78 | 34.27 | 29.41 |
Na2O | 0.04 | 0.02 | 0.09 | 0.02 | 0.02 |
K2O | 0.12 | 0.13 | 0.11 | 0.26 | 0.20 |
P2O5 | 0.05 | 0.10 | 4.25 | 0.03 | 0.04 |
L.O.I. | 45.14 | 44.56 | 37.00 | 35.33 | 33.16 |
Sum | 101.71 | 99.99 | 100.06 | 98.86 | 98.01 |
IE | |||||
ppm | |||||
Rb | 7.4 | 0.1 | 2.3 | 6.1 | 3.5 |
Ba | 2,360 | 11,600 | 1,971 | 951 | 13,528 |
Th | 5.73 | 0.68 | 437 | 3.5 | 5.0 |
Nb | 6.14 | 2.02 | 997 | 8.9 | 8.4 |
Ta | 1.40 | 0.53 | 105 | 1.5 | 2.0 |
K | 996 | 1,079 | 913 | 2,159 | 1,660 |
Sr | 12,200 | 9,570 | 13,364 | 2,983 | 8,057 |
P | 248 | 486 | 21,097 | 131 | 175 |
Hf | 2.7 | 0.50 | 3.6 | 0.3 | 0.1 |
Zr | 110 | 18.4 | 112 | 7.7 | 14.3 |
Ti | 1,978 | 399 | 600 | 300 | 240 |
Y | 17.0 | 11.0 | 74 | 18.8 | 45.5 |
REE | |||||
La | 90.2 | 62.2 | 472 | 41.2 | 2,569 |
Ce | 112 | 90 | 1,104 | 90.3 | 5,236 |
Pr | 12.33 | 8.32 | 122 | 12.24 | 551 |
Nd | 47.0 | 31.7 | 477 | 47.54 | 2,184 |
Sm | 7.11 | 4.68 | 62.5 | 9.43 | 376 |
Eu | 1.56 | 1.25 | 15.9 | 2.53 | 80.1 |
Gd | 2.74 | 1.71 | 45.5 | 7.91 | 225 |
Tb | 0.55 | 0.33 | 4.28 | 1.35 | 16.92 |
Dy | 2.72 | 1.63 | 18.0 | 7.67 | 56.91 |
Ho | 0.54 | 0.33 | 2.62 | 1.39 | 18.92 |
Er | 1.85 | 1.08 | 5.41 | 3.17 | 22.45 |
Tm | 0.17 | 0.06 | 0.67 | 0.56 | 8.29 |
Yb | 1.37 | 0.53 | 3.73 | 3.09 | 8.72 |
Lu | 0.13 | 0.06 | 0.49 | 0.44 | 0.86 |
Mol% | |||||
CaO | 69.5 | 90.2 | 88.5 | 54.5 | 50.4 |
FeO + MnO | 14.5 | 0.3 | 5.5 | 14.1 | 19.3 |
MgO | 16.0 | 9.5 | 6.0 | 31.4 | 30.3 |
Sample | Barra do Itapirapuã age: 115 (10) Ma | |||||
---|---|---|---|---|---|---|
I.A; I.B; II.A | IV.A 3 | IV.B 5 | IV B 3 | II A 2 | IV A 5 | |
wt% | ||||||
SiO2 | 0.54 (0.37) | 1.46 | 12.76 | 5.21 | 2.27 | 6.67 |
TiO2 | 0.01 (0.00) | 0.51 | 0.49 | 0.15 | 0.01 | 0.01 |
Al2O3 | 0.02 (0.01) | 0.22 | 1.20 | 1.69 | 0.23 | 1.83 |
FeO | 7.76 (1.32) | 7.64 | 5.80 | 1.36 | 14.48 | 12.28 |
MnO | 1.08 (0.16) | 0.94 | 0.30 | 0.08 | 1.91 | 1.19 |
68MgO | 15.23 (1.15) | 15.06 | 14.82 | 2.64 | 10.55 | 10.51 |
CaO | 30.54 (1.18) | 28.99 | 27.64 | 51.56 | 31.49 | 27.23 |
Na2O | 0.08 (0.01) | 0.09 | 0.03 | 0.42 | 0.08 | 0.06 |
K2O | 0.02 (0.01) | 0.01 | 0.01 | 1.03 | 0.03 | 1.48 |
P2O5 | 1.27 (0.14) | 0.59 | 2.11 | 0.15 | 0.22 | 0.10 |
L.O.I. | 42.30 (2.20) | 43.33 | 34.19 | 35.56 | 37.11 | 37.26 |
Sum | 98.85 | 98.84 | 99.35 | 99.85 | 98.38 | 98.62 |
ppm | ||||||
Rb | 1.9 (0.6) | 3.0 | 2.96 | 83.5 | 5.1 | 47.2 |
Ba | 1,252 (29) | 1,730 | 1,828 | 145.7 | 1,927 | 456 |
Th | 122.5 (25.0) | 64.5 | 185 | 7.9 | 246 | 114 |
Nb | 165 (48) | — | 38.1 | 4.3 | 48 | 721 |
Ta | 1.5 (0.4) | — | 1.9 | 0.7 | 0.8 | 41.5 |
Sr | 1,743 (382) | 1,150 | 3,016 | 782 | 2,955 | 2,052 |
Hf | 0.51 (0.02) | 0.5 | 3.1 | 0.9 | 1.0 | 0.3 |
Zr | 145 (32) | 88.4 | 27.5 | 10.4 | 19.2 | 7.0 |
Y | 20.1 (1.4) | 43.5 | 291.8 | 45.6 | 76 | 4.3 |
La | 150 (45) | 734 | 633 | 35.44 | 1,070 | 294 |
Ce | 347 (65) | 923 | 935 | 47.71 | 1,397 | 457 |
Pr | 46 (14) | 78.4 | 110 | 6.57 | 184 | 51 |
Nd | 123 (12) | 208 | 383 | 29.74 | 826 | 167 |
Sm | 25.4 (14.0) | 24.20 | 58.74 | 6.36 | 117 | 16.67 |
Eu | 8.25 (2.92) | 6.79 | 22.46 | 1.81 | 30.2 | 4.02 |
Gd | 27.00 (10.2) | 18.0 | 77.37 | 7.88 | 91.3 | 8.47 |
Tb | 4.15 (2.05) | 2.10 | 14.10 | 1.39 | 11.7 | 0.87 |
Dy | 25.2 (11.7) | 10.90 | 84.03 | 6.80 | 37.4 | 4.06 |
Ho | 3.46 (2.68) | 1.92 | 17.23 | 1.40 | 3.72 | 0.86 |
Er | 4.22 (2.23) | 4.71 | 44.20 | 4.04 | 12.5 | 3.15 |
Tm | 0.78 (0.25) | 0.64 | 6.50 | 0.67 | 1.75 | 0.42 |
Yb | 6.74 (4.16) | 3.04 | 38.85 | 4.46 | 10.1 | 2.98 |
Lu | 0.97 (0.53) | 0.53 | 5.63 | 0.70 | 1.38 | 0.48 |
Mol% | ||||||
CaO | 52.1 | 51.2 | 62.5 | 91.5 | 53.4 | 52.0 |
FeO + MnO | 11.8 | 11.8 | 10.8 | 2.0 | 21.7 | 20.1 |
MgO | 36.1 | 37.0 | 26.7 | 6.5 | 24.9 | 27.9 |
Sample | Cerro Chiriguelo age: 128 (5) Ma | Cerro Manomó age: 139 (3) Ma | |||||
---|---|---|---|---|---|---|---|
3,411 | 3,414 | 3,422 | 3,434 | 3,440 | 3,443 | PV-69C | |
wt% | |||||||
SiO2 | 2.26 | 5.44 | 5.05 | 7.18 | 10.55 | 6.25 | 3.02 |
TiO2 | 0.05 | 0.05 | 0.01 | 0.10 | 3.41 | 0.30 | 0.02 |
Al2O3 | 0.22 | 0.25 | 0.30 | 0.56 | 1.44 | 0.53 | 0.11 |
FeO | 3.25 | 2.84 | 3.19 | 2.99 | 15.20 | 0.40 | 40.49 |
MnO | 0.60 | 0.45 | 0.28 | 0.15 | 0.64 | 0.40 | 7.13 |
MgO | 0.10 | 0.15 | 0.41 | 0.50 | 2.80 | 1.00 | 1.34 |
CaO | 48.45 | 47.15 | 47.00 | 46.98 | 30.89 | 44.62 | 7.68 |
Na2O | 0.08 | 0.08 | 0.03 | 0.04 | 0.03 | 0.10 | 0.08 |
K2O | 0.07 | 0.15 | 0.28 | 0.50 | 1.61 | 0.42 | 0.02 |
P2O5 | 0.80 | 0.95 | 0.69 | 0.48 | 0.54 | 1.20 | 0.10 |
L.O.I. | 40.99 | 40.07 | 38.29 | 38.05 | 31.94 | 39.08 | 35.28 |
Sum | 96.87 | 97.59 | 95.53 | 97.53 | 99.05 | 97.15 | 95.27 |
ppm | |||||||
Rb | 24 | 32 | 39 | 36 | 151 | 59 | 0.1 |
Ba | 25,885 | 23,989 | 22,123 | 10,390 | 5,464 | 19,532 | 1,560 |
Th | 40 | 29.7 | 11 | 28 | 8 | 12 | 481 |
Nb | 109 | 81 | 178 | 100 | 260 | 495 | 25 |
Ta | — | — | 13.5 | 7.6 | 20 | 37.6 | 0.29 |
K | 581 | 1,245 | 2,325 | 4,151 | 13,366 | 3,487 | 166 |
Sr | 2,875 | 2,031 | 5,243 | 7,441 | 1,776 | 7,103 | 2,342 |
P | 3,971 | 4,716 | 3,425 | 2,383 | 2,681 | 5,957 | 496 |
Hf | — | — | 5.1 | 10.0 | 11.6 | — | 0.19 |
Zr | 133 | 87 | 219 | 430 | 506 | 39 | 15 |
Ti | 300 | 300 | 60 | 600 | 20,442 | 1,799 | 120 |
Y | 4 | 3.9 | 3.7 | 10 | 29 | 5.0 | 49 |
REE | |||||||
La | 1,336 | 1,257 | 1,169 | 590 | 312 | 889 | 2,570 |
Ce | 1,305 | 1,240 | 1,102 | 633 | 227 | 1,022 | 5,328 |
Pr | 120 | 128 | 101 | 63.1 | 22.6 | 79 | 787 |
Nd | 151 | 181 | 178 | 120 | 110 | 151 | 2,142 |
Sm | 94 | 31.5 | 30.0 | 20.1 | 12 | 29.2 | 369 |
Eu | 32 | 10.8 | 10.2 | 6.9 | 4.1 | 9.8 | 79 |
Gd | 101 | 34.1 | 32.4 | 21.8 | 13.0 | 29.9 | 221 |
Tb | 16.3 | 5.5 | 5.20 | 3.6 | 2.1 | 4.8 | 13 |
Dy | 96 | 32.8 | 31.0 | 21.2 | — | 28.9 | 60 |
Ho | 18.3 | 6.09 | 5.87 | 4.06 | — | 5.66 | 10 |
Er | 44 | 14.7 | 14.2 | 9.9 | — | 14.5 | 24 |
Tm | 5.3 | 1.77 | 1.71 | 1.23 | 0.84 | 1.80 | 3 |
Yb | 17.1 | 8.68 | 8.04 | 6.03 | 4.42 | 9.02 | 9 |
Lu | 3.3 | 1.13 | 0.77 | 0.68 | 0.45 | 1.02 | 1 |
Mol% | |||||||
CaO | 93.5 | 94.4 | 93.5 | 93.7 | 65.5 | 90.4 | 16.4 |
FeO + MnO | 6.2 | 5.2 | 5.4 | 4.9 | 26.2 | 6.8 | 79.6 |
MgO | 0.3 | 0.4 | 1.1 | 1.4 | 8.3 | 2.8 | 4.0 |
Sample | Itanhaém Age:129 (5) Ma | Valle-mí Age: 138.7 (0.2) Ma | Cerro Cañada Age: 124.6 (0.7) Ma | Cerro E Santa Elena Age: 127 (8) |
---|---|---|---|---|
IA-2 | VM1 Carbonate Fraction (15.56 wt%) | Dolomite Fraction (15.5 wt%) In ijolite | ||
wt% | ||||
SiO2 | 5.58 | — | — | 0.29 |
TiO2 | 0.92 | 0.05 | 0.01 | 0.02 |
Al2O3 | 1.84 | 0.01 | — | 0.89 |
FeO | 11.79 | 0.29 | 2.25 | 1.63 |
MnO | 0.62 | 0.01 | 0.20 | 0.45 |
MgO | 6.23 | 0.20 | 18.20 | 16.23 |
CaO | 36.06 | 6.67 | 31.30 | 32.54 |
Na2O | 0.37 | 0.01 | 0.25 | 0.40 |
K2O | 0.18 | 0.01 | 0.01 | 0.02 |
P2O5 | 4.64 | 0.08 | 0.01 | 0.44 |
L.O.I. | 30.70 | 8.13 | 47.79 | 46.92 |
Sum | 98.91 | 15.56 | 100.02 | 100.00 |
ppm | ||||
Rb | 0.8 | 0.90 | 2.36 | 4.5 |
Ba | 1,546 | 435 | 2,950 | 5,618 |
Th | 233 | 20 | 2.82 | 4.23 |
Nb | 448 | 64 | 10.3 | 15.0 |
Ta | 24.4 | 4.8 | 1.11 | 1.32 |
K | 1,494 | 83 | 81 | 166 |
Sr | 3,248 | 128 | 3,246 | 6,225 |
P | 20,249 | 349 | 41 | 1,920 |
Hf | 0.8 | 10 | 1.05 | 1.71 |
Zr | 17.0 | 39 | 12 | 18.8 |
Ti | 5,515 | 300 | 59 | 118 |
Y | 57 | 16.0 | 24.2 | 25.5 |
REE | ||||
La | 2,773 | 155 | 164 | 188 |
Ce | 4,902 | 340 | 325 | 409 |
Pr | 337 | 43.5 | 36.5 | 30.2 |
Nd | 1,181 | 168 | 146.3 | 184 |
Sm | 132 | 27.7 | 22.45 | 25.8 |
Eu | 29.7 | 10.66 | 8.2 | 14.4 |
Gd | 79 | 33.12 | 31.4 | 48.2 |
Tb | 6.4 | 5.24 | 3.3 | 5.1 |
Dy | 37 | 30.0 | 30.5 | 47.1 |
Ho | 7.2 | 5.95 | 5.7 | 8.9 |
Er | 14.8 | 12.27 | 13.6 | 21.8 |
Tm | 1.61 | 1.34 | 2.1 | 2.7 |
Yb | 11.7 | 5.95 | 21.7 | 31.1 |
Lu | 0.90 | 0.67 | 0.77 | 1.22 |
Mol% | ||||
CaO | 66.2 | 92.8 | 53.5 | 49.9 |
FeO + MnO | 17.8 | 3.3 | 3.3 | 3.6 |
MgO | 16.0 | 3.9 | 43.2 | 46.5 |
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