versión On-line ISSN 2007-2902
versión impresa ISSN 1026-8774
Rev. mex. cienc. geol vol.28 no.1 México abr. 2011
New tectonic discrimination diagrams for basic and ultrabasic volcanic rocks through logtransformed ratios of high field strength elements and implications for petrogenetic processes
Nuevos diagramas de discriminación tectónica para rocas volcánicas básicas y ultrabásicas por medio de relaciones logtransformadas de elementos de alto potencial iónico e implicaciones para procesos tectónicos
Surendra P. Verma1,* and Salil Agrawal2
1 Departamento de Sistemas Energéticos, Centro de Investigación en Energía, Universidad Nacional Autónoma de México, 62580, Temixco, Mor., México.
2 Department of Geology, University of Rajasthan, Jaipur 3002 004, India. *firstname.lastname@example.org
Manuscript received: March 1, 2010
Corrected manuscript received: August 25, 2010
Manuscript accepted: August 26, 2010
The statistically correct handling of compositional data requires logratio transformation whereas the multivariate technique of linear discriminant analysis (LDA) assumes a normal distribution of the transformed variables. In addition to other requirements, both these aspects were considered for proposing five new discriminant function diagrams based on logratios of five highfield strength elements (TiO2)adj, Nb, V, Y, and Zr. A representative world database of 1877 analyses of basic and ultrabasic magmas from four tectonic settings of island arc, continental rift, oceanisland, and midocean ridge, was used. After identifying discordant outliers in logtransformed ratios using single outlier tests, 1793 analyses proved to be normally distributed in terms of the following four variables: ln(Nb/(TiO2)adj), ln(V/(TiO2)adj), ln(Y/(TiO2)adj), and ln(Zr/(TiO2)adj). Use of LDA of the complete dataset of 1877 analyses divided into 1477 analyses for training set and 400 for testing set provided high success rates of 78.592.2% and 81.793.0% for the discrimination of the four tectonic settings based on the training and testing sets, respectively. However, using LDA of the normally distributed 1793 analyses divided into 1393 for training set and 400 for testing set, we obtained new diagrams that showed still higher success rates of 80.293.5% and 84.094.0%, respectively. The advantage of fulfilling the requirement of normal distributions of logratio variables resides in the observation that an overall net gain in success rates of 0.53.3% was achieved when the LDA was correctly applied to discordantoutlierfree logtransformed ratios (1793 analyses) than to the complete data set (1877 analyses). The application of these discrimination diagrams to ophiolites from Taitao Peninsula (southern Chile), Gabal Gerf complex (northeastern Africa), Jormua (northeastern Finland) and Macquarie Island (southwest Pacific) indicated tectonic setting of midocean ridge, transitional between island arc and midocean ridge, midocean ridge and continental rift, respectively. Although only a few rock samples from a study of southcentral Sweden could be identified as mafic, the present diagrams indicated an arc setting for this area. The application to three case studies from Turkey, being a country with highly complex geological history, suggested continental rift setting for Kula Quaternary basic volcanic rocks, inconclusive evidence for Jurassic volcanic rocks from eastern Pontides, arc setting for Tauride belt ophiolite, and continental rift setting for East Anatolian and Dead Sea fault zones, the latter application being based on probability calculations for each sample without any need to plot the samples in the discrimination diagrams. The use of normal discordant outlierfree samples of logtransformed ratios from each area in our new discrimination diagrams reinforced these conclusions for all areas, providing somewhat better discrimination in those cases in which such discordant observations were observed. We suggest that the new diagrams be used for tectonic discrimination of basic and ultrabasic rock samples that are confirmed to have discordant outlierfree normally distributed logtransformed variables. Basic and ultrabasic character of the rock samples could be determined from computer program SINCLAS and the discordant outliers of logtransformed variables from DODESYS, whereas the use of new diagrams proposed during 20042010 would be facilitated from program TecD.
Key words: discordant outliers, normal sample, tectonic setting, logtransformation, adjusted majorelements, ophiolites, Archaean, Turkey, Sweden.
El manejo estadísticamente correcto de datos composicionales requiere transformaciones logarítmicas de relaciones de composiciones, mientras que la técnica multivariable de análisis discriminante lineal (LDA) supone una distribución normal de las variables transformadas. Adicionalmente a otros requerimientos, ambos aspectos fueron tomados en cuenta para proponer cinco nuevos diagramas de funciones discriminantes basados en relacioneslog de cinco elementos de alta fuerza de campo (TiO2)adj, Nb, V, Y y Zr. Una base mundial representativa de datos de 1877 análisis de magmas básicos y ultrabásicos de cuatro ambientes tectónicos de arco de isla, rift continental, isla oceánica y cresta midoceánica, fue empleada. Después de identificar valores discordantes en las relaciones logtransformadas mediante pruebas de discordancia de tipo sencillo, 1793 análisis demostraron ser distribuidos en forma normal en términos de las cuatro variables siguientes: ln(Nb/(TiO2)adj), ln(V/(TiO2)adj), ln(Y/(TiO2)adj) y ln(Zr/(TiO2)adj). El uso de LDA con el conjunto de datos completos de 1877 análisis divididos entre 1477 análisis para el entrenamiento y 400 para la prueba proporcionó altos valores de éxito de 78.592.2% y 81.793.0% para la discriminación de los cuatro ambientes tectónicos basados en los conjuntos de entrenamiento y prueba, respectivamente. Sin embargo, usando LDA de los 1793 análisis distribuidos normalmente divididos entre 1393 análisis para el entrenamiento y 400 para el de prueba, obtuvimos diagramas nuevos que demostraron aún más altos valores de éxito de 80.293.5% y 84.094.0%, respectivamente. La ventaja de cumplir con el requerimiento de distribuciones normales de las variables logtransformadas reside en la observación de que se obtuvo una ganancia neta de 0.53.3% en los valores de éxito cuando el LDA fue aplicada correctamente a relaciones logtransformadas libres de valores discordantes (1793 análisis) en comparación con el conjunto completo de datos (1877 análisis). La aplicación de estos diagramas discriminantes a ofiolitas de la Península de Taitao (sur de Chile), complejo Gabal Gerf (noreste de África), Jormua (noreste de Finlandia) e Isla Macquarie (suroeste del Pacífico), indicó el ambiente tectónico de cresta midoceánica, transicional entre el arco de isla y cresta midoceánica, cresta midoceánica y rift continental, respectivamente. Aunque solamente pocas muestras de rocas de un estudio sobre Suecia surcentral pudieron ser identificadas como máficas, los diagramas propuestos indicaron un ambiente de arco para esta área. La aplicación a tres estudios de Turquía, siendo un país con un historial geológico sumamente complejo, sugirieron el ambiente de rift continental para las rocas volcánicas cuaternarias de Kula, evidencia inconclusa para rocas volcánicas jurásicas de Pontides oriental, ambiente de arco para ofiolitas de cinturón de Tauride y rift continental para zonas de este de Anatolia y las fallas del Mar Muerto, la última aplicación estuvo basada en los cálculos de las probabilidades para cada muestra sin la necesidad de graficar las muestras en los diagramas de discriminación. El uso de las muestras de relaciones logtransformadas libres de valores discordantes de cada área en nuestros nuevos diagramas discriminantes confirman estas conclusiones para todas las áreas, proporcionando una discriminación mejor en todos aquellos casos en donde se observaron estos valores discordantes. Sugerimos que los diagramas nuevos sean usados para la discriminación tectónica de muestras de rocas básicas y ultrabásicas con una distribución normal de las variables logtransformadas, libres de valores discordantes. La naturaleza básica y ultrabásica de las muestras a utilizar deberá ser determinada con el programa computacional SINCLAS y los valores discordantes de las variables logtransformadas con el programa DODESYS, mientras que el uso de los nuevos diagramas propuestos entre 2004 y 2010 podría ser facilitado por el programa TecD.
Palabras clave: valores desviados, muestra normal, ambiente tectónico, transformaciónlog, elementos mayores ajustados, Ofiolitas, Arqueano, Turquía, Suecia.
Discrimination diagrams constitute a widely used complementary technique to other petrological methods for interpreting compositional data (Pearce and Cann, 1973 cited ~1750 times according to the Institute for Scientific Information database as confirmed on August 8, 2010, with ~275 cites during the last five years; Pearce and Gale, 1977 with ~150 cites, of which ~30 are recent cites; Pearce et al., 1977, 1984 with ~175 and ~2050 cites, respectively, of which ~20 and ~670 are recent cites; Wood, 1980 with ~540 cites, of which ~200 are recent cites; Shervais, 1982 with ~685 cites, of which ~200 are recent cites; Cabanis and Lecolle, 1989 with ~150 cites, of which ~70 are recent cites; Rollinson, 1993; Verma, 2000, 2010; Agrawal et al., 2004, 2008, with ~15 and ~20 recent cites, respectively; Verma et al., 2006 with ~10 recent cites). Such diagrams have been in use practically since the advent of plate tectonics. More importantly, they are still in wide use even today (see the recent cites mentioned above). J.A. Pearce and J.R. Cann, with their papers (Pearce and Cann, 1971, 1973), were the pioneers in this adventure. A large number of diagrams have been proposed that vary from binary and ternary to complex discriminant function types (Rollinson, 1993; Verma, 2010).
There are several inherent requirements for good discrimination diagrams (Agrawal and Verma, 2007); these are representative databases, objective probability based boundaries replacing those drawn by eye, correct statistical treatment of compositional data, and the immobile nature of chemical elements used. Major advancement has been achieved through extensive, carefully validated databases (Agrawal et al., 2004), objective boundaries (Agrawal, 1999), linear discriminant analysis of natural logarithmratio transformed compositional data (Verma et al., 2006), and use of relatively immobile elements (Agrawal et al., 2008).
Recently, Vermeesch (2007), Sheth (2008), and Verma (2010) have evaluated most existing discrimination diagrams. It appears that the newer discriminant function diagrams (Agrawal et al., 2004, 2008; Verma et al., 2006) obtained from linear discriminant analysis (LDA) work well (Sheth, 2008; Verma, 2010), whereas the older bivariate and ternary diagrams all plagued by erroneous treatment of compositional data (Aitchison, 1986; Agrawal and Verma, 2007; Verma, 2010) and generally show very low success rates. When success rates are higher, these diagrams then discriminate only two tectonic settings under the broad names of "withinplate" and "plate margin".
In spite of these recent advances achieved during 20042008 (see Verma, 2010), newer diagrams based on immobile elements that could be easily determined by conventional analytical techniques such as xray fluorescence spectrometry, are still required. Correct application of LDA is another requirement. LDA implicitly requires that the individual variables (logtransformed ratios used in the present study) be normally distributed. With these additional requirements in mind, we developed a set of five new discriminant function discrimination diagrams that use natural logarithmratios of five highfield strength elements (TiO2)adj, Nb, V, Y, and Zr for magmas from four tectonic settings of island arc, continental rift, oceanisland, and midocean ridge. The subscript adj refers to adjusted data as explained in the following section. The elements Ti, Nb, Y, and Zr are generally classified as highfield strength elements (e.g., Rollinson, 1993). Nevertheless, although V is classified as a transition metal, it can also be considered as a highfield strength element because of its high charge (generally +5) and small ionic radius (e.g., Shannon and Prewitt, 1969).
DATABASE AND LINEAR DISCRIMINANT ANALYSIS (LDA)
The database used for this work was a modified and completed version of those used by Verma et al. (2006), Agrawal et al. (2004, 2008), and Verma (2010). Because full description of the compiled locations and references can be obtained from these papers and to keep the present paper relatively short, we have restrained from giving more details in the present work. Nevertheless, we provide here a list of the complete dataset of basic and ultrabasic rocks as randomly divided into training and testing sets (see the electronic supplement to this paper). These are reproduced in Tables A1 (1477 analyses) and A2 (400 analyses), respectively.
The need to objectively divide the database into training and testing sets arises from the fact that in all statistical analyses leading to new development, it is desirable to have an independent unbiased estimate of their overall success or success rates. The statistical analysis of a part of the samples (called training set) provides such an estimate, but the randomly selected remaining samples (called testing set) give us an independent, unbiased estimate of the results. Of course, the future applications to statistical samples of the entire population will again be independent estimates of the quality of the new diagrams and the parameters used for constructing them.
We assigned a proper rock name and magma type (basic or ultrabasic) to each compiled rock sample following the IUGS volcanic rock classification scheme (Le Bas et al., 1986, Le Bas, 2000), using the computer program SINCLAS (Verma et al., 2002, 2003) under the Middlemost (1989) option for Feoxidation adjustment. This implicitly requires that complete chemical analysis involving all 10 major oxides be available for a rock sample to be qualified for inclusion in our database even if we are not using all majorelements in our diagrams. The majorelement composition after SINCLAS processing is identified by the subscript adj added to each majoroxide name. The use of SINCLAS emphasizes the basic idea of initially complying with the closed space of 100% for all ten majorelement variables (including both Feoxidation varieties as determined by SINCLAS), but without volatiles and traceelements, and thus standardize the use of TiO2 as (TiO2)adj in the new diagrams. This also requires that for any given sample all ten majorelement variables should be available for their use in the new discrimination diagrams irrespective of the fact that only (TiO2)adj is explicitly used.
Basic requirements for constructing the database were that the tectonic setting should be explicitly and unambiguously described by the author(s) and (SiO2)adj ≤ 52% after SINCLAS processing. Basic (and ultrabasic) rock samples were assigned to one of the four classes or tectonic settings of island arc (IAB; group no. 1), continental rift (CRB; group no. 2), oceanisland (OIB; group no. 3), and midocean ridge (MORB; group no. 4). Samples from doubtful and complex settings were excluded from the database.
Only the socalled immobile elements were considered, and several combinations of these elements were evaluated through exploratory discriminant analysis. The combination of five highfield strength elements (TiO2)adj, Nb, V, Y, and Zr demonstrated the overall best performance.
Following the recommendation of Aitchison (1986) for correct statistical treatment of compositional data, the LDA was carried out on four natural logarithmtransformed ratios of these five elements using (TiO2)adj as the common denominator. LDA requires that complete information of these components for the analyses be available in this multivariate technique (e.g., Agrawal and Verma, 2007). Therefore, samples with complete majorelement analysis (all ten oxides from (SiO2)adj to (P2O5)adj, including the two Feoxidation varieties) and the four traceelements (Nb, V, Y, and Zr) were separated from the database for further analysis. Our database constituted a total of 1877 analyses (Tables A1 and A2 in the electronic supplement).
The other basic requirement of LDA is that the parameters used in the statistical analysis of the samples for a given tectonic setting represent a normal distribution (e.g., Morrison, 1990), which was attained by processing the four logtransformed ratios 1n(Nb/(TiO2)adj), 1n(V/(TiO2)adj), 1n(Y/TiO2)adj), and 1n(Zr/(TiO2)adj), for possible discordant outliers (Barnett and Lewis, 1994; Verma, 1997, 2005), using computer program DODESSYS (S.P. Verma and L. DíazGonzález, manuscript in preparation) at 99% confidence level. This program is based on new, precise and accurate critical values for discordancy tests (Verma and QuirozRuiz, 2006a, 2006b, 2008; Verma et al., 2008). A total of 84 analyses (< 4.5%) from the four tectonic settings were identified as discordant (see Table A3 in the electronic supplement); the remaining (1793 analyses) were considered in the final LDA and new discriminant function diagrams. The discordant nature of logratio variables in a few samples (< 4.5% of all complied samples) more likely implies the role of sampling (field sampling as well as representativity of very small sample mass fractions to be analyzed) and analytical (calibration as well as "unknown" sample measurement) errors. Unfortunately, this cannot be fully ascertained because most published papers do not report details on all these errors, at least not individually for each sample. Therefore, given the requirement of LDA regarding normality of logratio transformed variables, it would be best to use discordant outlierfree samples in this statistical analysis. Nevertheless, we stress that for LDA the logtransformed ratio variables, and not the crude compositional variables, must be discordant outlierfree normal samples.
The available discordant outlierfree data, comprising these 1793 analyses, were randomly divided into training and testing sets (Table 1). A synthesis of these data pertinent to LDA is included in Table 2. All logtransformed ratios are negative because we have chosen the majorelement (TiO2)adj as the denominator. Both negative and positive values could have been obtained had we chosen a trace element as the denominator. A qualitative comparison of logtransformed mean ratios reveals that CRB and OIB show rather similar mean values, but generally different from both IAB and MORB, the latter are characterized by some differences between their chemical compositions. Table 3 gives the results of the tests of equality for these elements and their ratios. Both tests (Wilks' lambda < < 1 and Fratio > > 1) show that there are statistically significant differences among the four tectonic groups at an extremely low significance level (see the very small "Significance" values practically approaching zero for all variables in Table 3).
RESULTS OF THE DISCRIMINANT ANALYSIS
Success rates or correct discrimination of training and testing sets
The results of LDA performed on the training and testing sets (Table 2) are presented in Table 4 for both complete dataset (1877 analyses divided into 1477 training and 400 testing samples) as well as discordant outlierfree data (1793 analyses divided into 1393 training and 400 testing samples). The discriminant analysis was carried out five times, once for all four groups with CRB and OIB combined together and four times for all possible combinations of three groups at a time. Because we purposely wanted to better train the LDA than the testing operation, we maintained much greater number of samples in the training than the testing set (Table 4). In spite of this, for the complete dataset (1877 analyses) the overall success rates of 78.592.2% for the training set are comparable to (even slightly smaller than) 81.793.0% obtained for the testing set (see Overall % for B process in Table 4). Similarly, LDA of the normally distributed outlierfree dataset (1793 analyses) the overall success rates of 80.293.5% and 84.094.0% were obtained for the training and testing sets, respectively (see Overall % for C process in Table 4).
An alternative to the approach of subdividing the dataset into training and testing sets might be a method called "Leave one out", which consists of using all but one sample for the training set and checking the sole sample left out for its correct or incorrect discrimination. In this method, all samples one at a time are left out, and the success rates are estimated from all of them in this objective way. The final LDA results can then be reported for all samples from a database, without excluding any of them.
The advantage of logratio transformation (correct statistical treatment) in comparison with the use of crude compositional data (incorrect statistical treatment; Aitchison, 1986; Agrawal and Verma, 2007) has already been well documented by Verma et al. (2006) and Agrawal et al. (2008). The latter authors also commented on the advantage of combining CRB and OIB settings as a single group in the first discriminant analysis as compared to dealing them separately as done earlier by Agrawal et al. (2004) and Verma et al. (2006).
Here we document the advantage of fulfilling the basic requirement of normal distributions of logtransformed variables. In Table 4, the rows marked B are for original complete dataset whereas those marked C are for discordantoutlierfree dataset. There is an overall net gain in success rates of 0.53.3% when the LDA is correctly applied to discordantoutlierfree logtransformed ratios (see the last column in Table 4).
Good understanding of correct as well as incorrect discrimination by LDA can be achieved from Table 5, in which actual number and percentages are reported for all 1793 samples in our database. The testing set samples (400 analyses) are plotted in the five discriminant function discrimination diagrams (Figure 1a1e); the training set samples (being too numerous, 1393 analyses) are not shown in Figures, but their results are summarized in Table 5. Four of the five diagrams apply for a given tectonic setting. The success rates for IAB vary from 85.298.6% for training set and 8899% for testing set, with the incorrect discrimination mainly as MORB (13.514.0% and 11%, respectively, for training and testing sets). The highest rates of about 99% (correct discrimination) for both training and testing sets of IAB are obtained for Figure 1b, in which MORB setting is absent (see Table 5). When CRB and OIB settings are combined together (Figure 1a), these samples show very high success rates of 9499.5%, with slightly greater misdiscrimination of CRB as MORB in comparison with CRB as IAB (Table 5). Such high correct discrimination (95.399.2%) was also obtained when these settings were not present together in a diagram (viz., Figure 1c, 1d; Table 5). However, when both settings were present as in Figure 1b, 1e, the correct discrimination was less (7386%). Finally, MORB samples were very efficiently discriminated (9396.3%), with the misdiscrimination mainly as CRB or IAB.
The equations for computing the DF1 and DF2 functions (x and yaxes) of Figure 1a1e are given in Table 6; note in these equations (TiO2)adj from SINCLAS should be used instead of actually measured, crude, unadjusted TiO2. In all diagrams (Figure 1a1e), including Figure 1a, we are dealing with three groups at a time. Therefore, the two functions (DF1 and DF2) together account for 100% of betweengroups variance in all the above threegroups at a time analyses. Finally, we note that these diagrams (Figure 1a1e) are easy to reproduce, because the boundaries are clearly specified by their coordinates in each of them (see explanation of Figure 1).
Probability based boundaries and petrogenetic models
As ascertained by Agrawal (1999), the boundaries in diagrams created by LDA are based on probability calculations. These boundaries represent about 50% (0.50) probability (see boundaries shown by solid lines in Figures 1 and 2) when they separate two fields or tectonic settings, but as one approaches the triple point (intersection of three boundaries), the probability reaches to about 33.3% for any given field. We have calculated the probability for other areas of the diagrams and have drawn probability based boundaries for 70% and 90% (see green dashed and blue longdashed boundaries in Figure 2a2e). It is interesting to note that the probability to belong to a certain group increases very rapidly as we move away from the discrimination boundaries (solid blank lines) into a given field.
For illustration purposes, groupcentroids for the four tectonic groups from our database as well as average compositions of highMgO (MgO > 7%, an arbitrarily chosen value for this subdivision; the use of any other MgO for this subdivision will not change any of the conclusions) and lowMgO samples (up to 7%) were plotted in Figure 2a2e. These compositions plot close to the discrimination boundaries. We also computed the effects of fractional crystallization (FC) of common minerals (olivine, orthopyroxene, clinopyroxene, plagioclases, garnet and amphiboles), along with the partition coefficient values from TorresAlvarado et al. (2003). In all cases, the FC vectors remain within the designated tectonic field for degrees of fractional crystallization (f) of up to 0.15 a reasonable maximum value of f to maintain the rock type to basic variety. With greater degrees of f, the rock types may change to intermediate magmas, for which these diagrams should be used with caution although our earlier discriminant function diagrams (Verma et al., 2006) have been successfully used for charnockitesmagmas with intermediate SiO2 values (Rajesh 2007). On the other hand, the diagrams proposed by Verma et al. (2006) and Agrawal et al. (2004, 2008) were unsuccessful for intermediate magmas from central Mexico (RodriguezRíos and TorresAguilera, 2009; S.P. Verma, unpublished results).
For modeling partial melting processes, we added in Figure 2a2e average compositions of depleted MORB mantle (DM of Xu et al., 2005; see also, Salters and Stracke, 2004) and bulk silicate earth (BSE of McDonough and Sun, 1995). Both sources lie in the IAB field (Figure 2a2e). This observation has important bearing on the use of these discrimination diagramsthey should, in principle, not be used for source rocks; they are meant for the discrimination of magmas resulting from partial melting of source rocks. After all, the discrimination boundaries result from LDA of magmatic rock samples compiled from all over the world, and not from cumulates or source rocks. It is possible that the diagrams work consistently for cumulates or source rocks, but the conclusions drawn from magmas should be given more weight when the two results do not fully agree.
Batch partial melting models were calculated for DM source corresponding to 015% of olivine, orthopyroxene, or clinopyroxene individually and for 05% of plagioclases, garnet and amphiboles, which is not a realistic process. For a realistic process of partial melting of DM and BSE sources with combined 030% melting of olivine, orthopyroxene and clinopyroxene (in the proportion of 50:25:25, respectively), the thick solid pink curves show that the partial melts of CRB, OIB and MORB tectonic types can be generated depending on the degree of melting. Low degrees of melting favor melts of CRB and OIB types, whereas higher degree melts are of MORB types.
Probability calculations for individual samples
We briefly present the procedure to estimate probability for each given sample from the initial training and testing sets or the application databases, to belong to any of the tectonic settings in a given DF1DF2 discriminant function diagram. Let us assume that a sample is characterized by df1s, df2s coordinates or scores in this diagram. First, the centroid or mean values for each discriminant function and for each group are calculated from the training set; let us denominate them as mdf1g1 and mdf2g1 for group 1, mdf1g2 and mdf2g2 for group 2, and mdf1g3 and mdf2g3 for group 3. Note that in the discrimination scheme (e.g., Figure 1a1e), only three groups are discriminated at a time, including Figure 1a where CRB and OIB are treated as a single group. It is mandatory that the training set be used for this purpose, because the discrimination diagrams and the field boundaries are based on these data. These values are reported in Table A4 for all five diagrams.
These mean values are then used to estimate the squared distances of the sample under evaluation from the centroid of each group as follows:
New functions sg1, sg2, and sg3 based on these squared distances for that particular sample, are then computed as follows:
Finally, the probabilities for belonging to each of three groups, P1s, P2s and P3s, are then calculated from the above parameters as follows:
Although the probabilities are generally referred to as fractional numbers, we may also express them in percentage to establish analogy with the success rates (referring to individual samples) as follows:
These calculations must be repeated five times to obtain probabilities for all five discrimination diagrams. The probability estimates thus obtained can be directly used to assign any given sample to a tectonic setting without any need to plot the data in discrimination diagrams. Simply the sample is assigned to the tectonic setting showing the highest probability. Thus, a set of samples from any given area under study can be easily counted for their highest probabilities and the success rates can be calculated.
Before final counting of correctly discriminated samples and calculating success rates, we may also ascertain that all samples under study show normally distributed logtransformed ratios. Any discordant sample(s) can thus be excluded from the counting or success rate calculations.
APPLICATIONS TO DIFFERENT AREAS AND ROCKS AROUND THE WORLD
Although the IUGS classification is not ideal for older, probably altered rocks, the widely used alternative schemes (Floyd and Winchester, 1975, 1978; Winchester and Floyd, 1976, 1977) too do not provide a satisfactory classification scheme (Verma et al., 2010). Therefore, we used the IUGS classification scheme also for ascertaining the basic and ultrabasic nature of all samples used in our application examples. Furthermore, adjusted TiO2 values (Verma et al., 2002) were always used in all discrimination diagrams.
We clarify that for assigning rock names and ascertaining magma types to our application samples, we had to use the TAS classification (Le Bas et al., 1986; Le Bas, 2000; Verma et al., 2002, 2003), because no efficient diagrams exist in the literature to correctly classify altered volcanic rocks (Verma et al., 2010). Use of computer program SINCLAS (available on request to the first author SPV) is also recommended to ascertain the basic or ultrabasic nature of the samples and to estimate (TiO2)adj values that have to be involved in this work instead of crude estimates (measured TiO2 values).
Recently, Pearce (2008) used Nb/YbTh/Yb and Nb/YbTiO2/Yb diagrams to classify ophiolites into four types: Contaminated MORB (CMORB), Normal MORB (NMORB), Enriched MORB (EMORB), and Plume MORB (PMORB). We compiled their CMORB ophiolite example from Taitao Peninsula (Le Moigne et al., 1996), NMORB from Gabal Gerf complex (Zimmer et al., 1995), and EMORB from Jormua (Peltonen et al., 1996) and Macquarie Island (Kamenetsky et al., 2000). Then, we used our new discriminant function diagrams (Figure 3a 3e) and summarized the results of discrimination in Table 7.
Taitao Peninsula of southern Chile is considered an example of a subducted ridge (35 Ma) on land (Le Moigne et al., 1996; Guivel et al., 2003; Lagabrielle et al., 2009). We will describe in more detail how to use our new discrimination diagrams for a given locality or region. The analyses presented by Le Moigne et al. (1996) will be used as an example. However, the use of normally distributed discordant outlierfree samples (facilitated by DODESSYS computer program) should be preferred; see below the section of "Correct statistical treatment of compositional data for application examples".
First, using SINCLAS computer program (Verma et al., 2002), we classified the samples into basic and ultrabasic magmas (10 samples) and intermediate magmas (16 samples). Because our diagrams should be used preferably for basic and ultrabasic rocks, the identity of magma types must be maintained. The basic and ultrabasic rocks were plotted in Figure 3a, which has three fields (IAB, CRB+OIB, and MORB), and shows that most samples plot in MORB field (9 out of 10; Table 7). Thus, this diagram clearly indicates a MORB setting for the Taitao samples. Now, these samples are evaluated in three of the other four diagrams. In this case, the diagram of IABCRBOIB (Figure 3b), in which the indicated setting of MORB is not present, should be excluded from further consideration. In all the remaining three diagrams (Figure 3c3e), a large proportion of these basic and ultrabasic rocks (from a total of 10 samples) plot in the MORB field (9, 9, and 10 samples, respectively in Figure 3c, Figure 3d, and Figure 3e; Table 7). Thus, after excluding the "unused" or "inapplicable" diagram (Figure 3b), all the four applicable diagrams suggest MORB setting for these samples. Incidentally, the same conclusion is reached from the intermediate magmas (16 samples) from Taitao Peninsula, because most (14 to 16) of these samples plot in the MORB field (Table 7). If this were not the case, the conclusion reached from basic and ultrabasic magmas should be considered as valid.
The present discrimination diagrams were used for pillow and sheeted dykes from Harga Zarga and Heiani of 600700 Ma old Gabal Gerf ophiolite complex, northeastern Africa (Zimmer et al., 1995). Pearce (2008) classified these (a total of 23) samples as NMORB. However, three of these samples proved to be of intermediate rocks and were excluded from our diagrams (Figure 3a3e), which are based on 20 samples of basic rocks (Table 7). Nevertheless, our diagrams do not discriminate them as MORB setting; the samples are divided into MORB and arc settings, with somewhat greater number of samples plotting as IAB.
Our next example of ophiolites is for Jormua, northeastern Finland (Peltronen et al., 1996). These authors considered Jormua ophiolite as a unique fragment of Red Seatype oceanic crust formed in a setting of continental breakup 1950 Ma ago. Thirtysix samples from early dikes and main basalt suite from this complex (Peltronen et al., 1996), being EMORB of Pearce (2008), classified as basic and ultrabasic magmas (30 samples) and intermediate magmas (6 samples), plotted mainly (28 samples) or completely (6 samples), respectively, in the MORB field (Figure 3a,3c3e; Figure 3b being the "inapplicable" diagram; Table 7), clearly establishing thus MORB setting for Jormua ophiolites. Continental rift setting envisioned by Peltronen et al. (1996) was not observed.
Finally, Kamenetsky et al. (2000) reported two groups of Miocene glassy rocks, which they called Group I (primitive) and Group II (differentiated), from "uplifted" crest of the Macquarie ridge on the Macquarie Island, southwestern Pacific. These rocks with unusual compositions were termed as EMORB by Pearce (2008). Eighteen basic rock samples belonging to Group I and thirtyseven of Group II (also basic rocks with the exception of one sample of intermediate magma) had complete chemical analyses for our discrimination diagrams (Figure 3a3e; Table 7). These rocks indicated a continental rift setting (Figure 3a3c,3e, with Figure 3d being the "inapplicable" diagram), because most of them plotted in the CRB+OIB field (Figure 3a) or CRB field (Figure 3b,3c,3e; Table 7). Thus, these unusual compositions of basaltic glasses from the Macquarie Islands are more consistent with continental rift setting rather than MORB or OIB setting. Their designation as EMORB by Pearce (2008) does not seem to be justified from our diagrams (see Verma, 2010 who showed that EMORB magmas generally plot in the MORB field). Nevertheless, more work is required to clarify these discrepancies.
Mafic rock discrimination
Rutanen and Andersson (2009) reported geochemistry of mafic intrusive rocks from the TransScandinavian igneous belt and Hedesunda igneous complex in the Fennoscandian shield of southcentral Sweden. From several lines of evidence they inferred a continental arc setting for their samples. We used our present discrimination diagrams to evaluate their samples in Figure 4a4e. Although these authors designated their rocks as mafic, chemically they represent magma of ultrabasic (one sample), basic (three samples), and intermediate (13 samples) types. Because our diagrams should be used for basic and ultrabasic magmas, the results are individually presented for basic+ultrabasic and intermediate rocks (Table 8). The basic and ultrabasic magmas (four samples) show consistently an arc setting, and thus support the conclusion of the original authors (Rutanen and Andersson, 2009). More samples of basic and ultrabasic rocks are required for confirmation of the tectonic setting of this area. On the other hand, although the intermediate magmas (13 samples) are almost equally divided between IAB and MORB settings, these results cannot be considered decisive, because our diagrams are not recommended to be used for differentiated magmas. Obviously, appropriate diagrams will have to be proposed for such magmas.
Discrimination of volcanic and ophiolitic rocks from Turkey
Turkey has had a very complicated geological and tectonic evolution, which makes this country fascinating for tectonomagmatic studies. Recently, Verma (2010) considered three case histories from Turkey: (i) Quaternary Kula volcanic rocks from western Anatolia (Tokcaer et al., 2005; Borsi et al., 1972; Ercan et al., 1985, 1997; Güleç, 1991; RichardsonBunbury, 1996; Alici et al., 2002; Agostini, 2004; Innocenti et al., 2005; also F. Innocenti, unpublished datacompiled by S. Agostini); (ii) Jurassic volcanism in the eastern Pontides (Sen, 2007); and (iii) dikes from Tauride belt ophiolite (Lycian ophiolite) in southwestern Turkey (Celik and Chiaradia, 2008). Using majorelement and traceelement (La, Sm, Yb, Nb, and Th) based discriminant function diagrams of Verma et al. (2006) and Agrawal et al. (2008), respectively, Verma (2010) obtained clearly continental rift setting for Kula, probably arc setting for Pontides, and undecisive results for Tauride belt ophiolites probably due to majorelement mobility. For the latter, Agrawal et al. (2008) diagrams could not be used due to the absence of complete traceelement data required. It is therefore interesting to use these newer discriminant function diagrams for these cases.
The application to Kula basic and ultrabasic rocks fully confirmed continental rift setting (Figure 5a5c, 5e; Figure 5d being the "inapplicable" diagram; Table 9). For eastern Pontides, the decision is not conclusive although from basic rocks it seems to be more in favor of MORB setting (Table 9). Finally, for basic rocks from Tauride belt ophiolite of southwestern Turkey, the new diagrams suggest an arc setting (Figure 5a5d; Figure 5e being the "inapplicable" diagram; Table 9). The results for intermediate rocks, although not recommended to be used in this work, are consistent with an arc setting for this ophiolite suite.
For another case study, we compiled the data on 20 Quaternary basalt samples from the East Anatolian and Dead Sea fault zones of southern Turkey (CeyhanOsmaniye plain basalts and Hassa graben basalts; Polat et al., 1997). Instead of using the discrimination diagrams, we will illustrate the use of probability calculations (see equations 112 and Table A4) to discriminate the tectonic setting of these samples. The results are given in Table A5, which will be referred to in the following discussion.
The probabilities for the first set of discriminant functions corresponding to the IABCRB+OIBMORB (groups 12+34) diagram (not shown) reported in the first part of Table A5 show that all 20 samples have the highest probability expressed in percent (90.98699.999%) for the CRB+OIB field and extremely small or negligible for the other two fields (0.0000.140% for IAB and 0.0018.956% for MORB). Therefore, either CRB or OIB setting is likely.
The probabilities for the second set of discriminant functions (IABCRBOIB; groups 123) for CRB are also highest (55.64188.101%) for all 20 samples although the probabilities for OIB (11.8990.44.359%) are not negligible; in fact, they are higher than the bychance probability of 33.333% (35.82744.359%) for 10 out of 20 samples. Nevertheless, CRB setting is more likely.
The probabilities for the third set of discriminant functions (IABCRBMORB; groups 124) for CRB are also highest (85.933100.000%) for all 20 samples. Because the competing OIB setting is missing from this diagram, the probabilities for CRB are very high and for the other two settings are extremely low (0.0000.122% for IAB and 0.00013.944% for MORB). Therefore, again from this third diagram CRB setting is more likely.
Thus, the fourth set of discriminant functions (IABOIBMORB; groups 134) should be considered as inapplicable because the expected CRB setting is missing from this set. Nevertheless, the probabilities for OIB are high (58.419100.000%) for all 20 samples and low for the other two settings. Only for one sample, the probability for MORB (41.277%) exceeds the bychance probability of 33.333%.
Finally, the fifth set of discriminant functions (the CRBOIBMORB diagram; groups 234), provides high probabilities for both CRB (33.66474.039%) and OIB (22.72466.336%). For CRB these probabilities exceed the bychance value of 33.333% for all 20 samples whereas for OIB this is so for only 16 out of 20 samples. For MORB all samples show very low probabilities (0.0003.825%). On the other hand, in terms of the number of samples with the highest probabilities, nine samples indicate CRB setting whereas 11 are consistent with OIB setting. In this context, it is interesting to note that the average probability of all samples for CRB (51.13%) is slightly higher than that for OIB (48.49%). Discordant outlier analysis of complete dataset of 20 samples using DODESSYS did not resolve this complexity of the fifth diagram.
From the above discussion, we conclude that for East Anatolian and Dead Sea fault zones of southern Turkey, CRB setting is more likely. The tectonics of this region is very complex, because this fault zone connects two thrust faults (Polat et al., 1997). Nevertheless, given the complications indicated by the fifth diagram, we should probably have treated the CeyhanOsmaniye plain (10 samples) and Hassa graben (10 samples) as separate areas for applications of discrimination diagrams and applied DODESSYS to individual datasets and not the combined one.
Correct statistical treatment of compositional data for application examples
One way to improve and, in fact, correctly use the new discrimination diagrams would be to ensure that the logratio transformed compositional data for application are normally distributed. This can de achieved in a similar manner as for the initial world database by processing the data for each application separately for discordant outliers (Barnett and Lewis, 1994; Verma, 1997; Verma and QuirozRuiz, 2006a, 2006b, 2008; Verma et al., 2008). We processed each data set (Tables 7, 8, 9) of the four logtransformed ratios, ln(Nb/TiO2)adj), ln(V/TiO2)adj), ln(Y/TiO2)adj), and 1n(Zr/(TiO2)adj) using DODESSYS from only singleoutlier tests (Verma et al., 2009) at 99% confidence level. To avoid possible swamping effects, multipleoutlier tests (GonzálezRamírez et al., 2009) were not used. None or only a few (one to three) discordant outliers were observed in these statistical samples or different datasets.
For ophiolites (Table 7) from Taitao (basic and intermediate rocks), Jormua intermediate rocks, and Macquarie Island group I samples, one discordant observation was indicated by DODESSYS. For Jormua basic rocks two observations and for Macquarie Island group II rocks three observations were identified as discordant, whereas for Gabal Gerf no observation was discordant. The discordant observations were identified in Figure 3a, and the results of application of our new discrimination diagrams to the remaining data are summarized in Table 10. The conclusions remain the same as in the original Table 7 although with somewhat improved discrimination of samples. In other words, the discordant observations were generally the misclassified samples in these cases (compare Tables 7 and 10) [8,9].
Finally, for each the three case studies from Turkey, one observation was inferred as discordant for Kula Quaternary basic volcanic rocks, Eastern Pontides intermediate rocks, and Tauride belt intermediate ophiolites. Two observations were discordant for Tauride belt basic ophiolites, and no observation was discordant for Eastern Pontides basic rocks. The results are summarized in Figure 5 and Table 11. Once again, the conclusions of Table 9 are reinforced from Table 11. The success rates (although not reported in Tables 711 [8, 9, 10] to keep the Tables simpler and because we are generally dealing with relatively small number of samples) can be easily calculated. They remain consistently high for most application examples, for which tectonic settings have been inferred in the present work.
The computer program DODESSYS for objectively identifying outliers as discordant is available on request to the first author (SPV).
Other applications of discriminant function diagrams
The new discriminant function diagrams have been widely used to decipher tectonic settings of several areas around the world. Thus, one or both sets of majorelement based diagrams (Agrawal et al., 2004; Verma et al., 2006) were used in the following studies: South Andaman ophiolite suite (Srivastava et al., 2004); basaltic lavas from the central part of New Mexico, U.S.A. (Maldonado et al., 2006); intermediate and silicic charnockites from southern India (Rajesh, 2007); metabasic volcanic rocks from the Salumber area, Aravalli Supergroup, northwestern India (Shekhawat et al., 2007); Early Cretaceous alkalinemaficultramafic igneous complex from Jasra, Shillong Plateau, northeastern India (Srivastava and Sinha, 2007); magmatic activity in southwestern margin of the East European Craton in Poland (Wiszniewska et al., 2007); Precambrian mafic magmatism in the Western Dharwar Craton, southern India (Ramakrishnan, 2009); ophiolites from Turkey (Verma, 2010); Carboniferous volcanic rocks from Junggar basin, China (Wang et al., 2010); and Miocene to Recent rocks from the central part of the Mexican Volcanic Belt (Verma, 2009; TorresAlvarado et al., 2010). These latter authors also used Agrawal et al. (2008) traceelement based diagrams. Both major and traceelement based sets of diagrams were used by Verma (2006) for deciphering the tectonic setting of volcanic rocks from the Los Tuxtlas volcanic field and by Verma (2010) for Turkey. Similarly, all sets of discrimination diagrams including the present ones, were further tested by Verma et al. (2011) from independent data sets from the four tectonic settings and then used to decipher the tectonic settings of the Mexican Volcanic Belt, Los Tuxtlas volcanic field, and Central American Volcanic Arc. The Agrawal et al. (2008) immobile traceelement based diagrams have been used for constraining geodynamic setting for the Mesoarchean (ca. 3075 Ma) pillow basalts, Archean, (ca. 2970 Ma Ali Polat, personal communication, June 2010) anorthosite and associated metavolcanic rocks, southwestern Greenland (Polat et al. 2009a, 2009b). For all these cases, the present set of new diagrams should prove useful in tectonomagmatic studies.
A computer program TecD by S.P. Verma and M.A. RiveraGómez is available on request to SPV that would facilitate the application of these diagrams to potential users.
A set of five new discriminant function based tectonomagmatic discrimination diagrams based on immobile elements has been successfully proposed. These diagrams have been used for several case studies, and in most cases, consistent results are obtained for the tectonic settings. These new diagrams should prove an excellent addition to the already existing (20042008) discriminant function diagrams based on major as well as traceelements. Our new diagrams are strictly meant to be used for basic and ultrabasic rocks. Their use for intermediate rocks requires caution and consistency of results with basic and ultrabasic rocks. Finally, normally distributed logratio transformed compositional data are to be preferred for use of our diagrams for tectonomagmatic discrimination of four tectonic settings (island arc, continental rift, oceanisland, and midocean ridge). All programs SINCLAS, DODESSYS, and TecD are available on request to SPV; they are not only essential for the use of these new diagrams but also they should facilitate this endeavor.
Samuele Agostini and Dima Kamenetsky are thanked for providing the first author their unpublished compilations on Turkey and Macquarie Island, respectively. We are also grateful to Alfredo QuirozRuiz for frequent help with computer maintenance. Although this work was initiated in 2008, it was concluded during 20092010 when the first author (SPV) was on sabbatical leave at the División de Ciencias Básicas e Ingeniería, Universidad Autónoma MetropolitanaIztapalapa, occupying the Chair (Cátedra) "Ronald Tunstall Ackroyd". We are grateful to Ali Polat and an anonymous reviewer for constructive comments on an earlier version of this paper and the editorinchief Susana AlanisÁlvarez for handling this manuscript and communicating to us her unbiased editorial decision.
Agostini, S., 2004, Il magmatismo postcollisionale dell'Anatolia occidentale: caratteri geochimici e petrologici, distribuzione spaziotemporale, quadro geodinamico (Postcollisional Western Anatolia magmatism: geochemical and petrologic characters, spacetime distribution, geodynamic framework): Pisa, Italy, University of Pisa, Ph.D. thesis. [ Links ]
Agrawal, S., 1999, Geochemical discrimination diagrams: a simple way of replacing eyefitted boundaries with probability based classifier surfaces: Journal of the Geological Society of India, 54, 335346. [ Links ]
Agrawal, S., Verma, S.P., 2007, Comment on "Tectonic classification of basalts with classification trees" by Pieter Vermeesch (2006): Geochimica et Cosmochimica Acta, 71(13), 33883390. [ Links ]
Agrawal, S., Guevara, M., Verma, S.P., 2004, Discriminant analysis applied to establish majorelement field boundaries for tectonic varieties of basic rocks: International Geology Review, 46, 575594. [ Links ]
Agrawal, S., Guevara, M., Verma, S.P., 2008, Tectonic discrimination of basic and ultrabasic volcanic rocks through logtransformed ratios of immobile trace elements: International Geology Review, 50, 10571079. [ Links ]
Aitchison, J., 1986, The Statistical Analysis of Compositional Data: Chapman and Hall, London, 416 p. [ Links ]
Alici, P., Temel, A., Gourgaud, A., 2002, PbNdSr isotope and trace element geochemistry of Quaternary extensionrelated alkaline volcanism: a case study of Kula region (Western Anatolia, Turkey): Journal of Volcanology and Geothermal Research, 115, 487510. [ Links ]
Barnett, V., Lewis, T., 1994, Outliers in Statistical Data: Third edition, John Wiley & Sons, Chichester, UK, 584 p. [ Links ]
Bevington, P.R., Robinson, D.K., 2003, Data Reduction and Error Analysis for the Physical Sciences: McGrawHill, Boston, MA, USA, 320 p. [ Links ]
Borsi, S., Ferrara, G., Innocenti, F., Mazzuoli, R., 1972, Geochronology and petrology of recent volcanics in the eastern Aegean Sea (Western Anatolia and Lesbos Island): Bulletin Volcanologique, 36, 473496. [ Links ]
Cabanis, B., Lecolle, M., 1989, Le diagramme La/10Y/15Nb/8: un outil pour la discrimination des séries volcaniques et la mise en évidence des processus de mélange et/ou de contamination crustale: Comptes Rendus Academie de Sciences Paris Serie II, 309, 20232029. [ Links ]
Celik, O.F., Chiaradia, M., 2008, Geochemical and petrological aspects of dike intrusions in the Lycian ophiolites (SW Turkey): a case study for the dike emplacement along the Tauride Belt Ophiolites. International Journal of Earth Sciences, 97, 11511164. [ Links ]
Ercan, T., Satir, M., Türkecan, A., Akyürek, B., Çevikbas, A., Günay, E., Ates, M., Can, B., 1985, Batý Anadolu Senozoyik volkanitlerine ait yeni kimyasal, izotopik ve radyometrik verilerin yorumu: Türkiye Jeoloji Kurumu Bülteni (Bulletin of the Geological Society of Turkey) 28, 121136. [ Links ]
Ercan, T., Satir, M., Sevin, D., Türkecan, A., 1997, Bati Anadolu'daki tersiyer ve Kuvaterner Yasli Volkanik Kayaçlarda yeni yapilan radyometrik yas ölçumlerinin yorumu (Some new radiometric ages from Tertiary to Quaternary volcanic rocks from W. Anatolia (Turkey)): Maden Tetkik Arama Dergisi 119, 60 pp. [ Links ]
Floyd, P.A., Winchester, J.A., 1975, Magma type and tectonic setting discrimination using immobile elements: Earth and Planetary Science Letters, 27(2), 211218. [ Links ]
Floyd, P.A., Winchester, J.A., 1978, Identification and discrimination of altered and metamorphosed volcanic rocks using immobile elements: Chemical Geology, 21, 291306. [ Links ]
GonzálezRamírez, R., DíazGonzález, L., Verma, S.P., 2009, Eficiencia relativa de 15 pruebas de discordancia con 33 variantes aplicadas al procesamiento de datos geoquímicos: Revista Mexicana de Ciencias Geológicas, 26(2), 501515. [ Links ]
Guivel, C., Lagabrielle, Y., Bourgois, J., Martin, H., Arnaud, N., Fourcade, S., Cotton, J., Maury, R.C., 2003, Very shallow melting of oceanic crust during spreading ridge subduction: origin of neartrench Quaternary volcanism at the Chile triple junction: Journal of Geophysical Research, 108, doi:10.1029/2002JB002119. [ Links ]
Güleç, N., 1991, Crustmantle interaction in western Turkey: implications from Sr and Nd isotope geochemistry of Tertiary and Quaternary volcanics. Geological Magazine, 128, 417435. [ Links ]
Innocenti, F., Agostini, S., Di Vincenzo, G., Doglioni, C., Manetti, P., Savascin, M.Y., Tonarini, S., 2005, Neogene and Quaternary volcanism in Western Anatolia: Magma sources and geodynamic evolution. Marine Geology, 221, 397421. [ Links ]
Kamenetsky, V.S., Everard, J.L., Crawford, A.J., Varne, R., Eggins, S.M., and Lanyon, R., 2000, Enriched endmember of primitive MORB melts: petrology and geochemistry of glasses from Macquarie island (SW Pacific): Journal of Petrology, 41, 411430. [ Links ]
Lagabrielle, Y., Le Moigne, J., Maury, R.C., Cotton, J., Bourgois, J., 2009, Volcanic record of the subduction of an active spreading ridge, Taitao Peninsula (southern Chile): Geology, 22(11), 515518. [ Links ]
Le Bas, M.J., 2000, IUGS reclassification of the highMg and picritic volcanic rocks: Journal of Petrology, 41, 14671470. [ Links ]
Le Bas, M.J., Le Maitre, R.W., Streckeisen, A., Zanettin, B., 1986, A chemical classification of volcanic rocks based on the total alkalisilica diagram: Journal of Petrology, 27, 745750. [ Links ]
Le Moigne, J., Lagabrielle, Y., Whitechurch, H., Girardeau, J., Bourgois, J., Maury C., R., 1996, Petrology and geochemistry of the Ophiolitic and Volcanic Suites of the Taitao Peninsula Chile Triple Junction Area: Journal of South American Earth Sciences, 9, 4358. [ Links ]
Maldonado, F., Budahn, J.R., Peters, L., Unruh, D.M., 2006, Geology, geochronology, and geochemistry of basaltic flows of the Cat Hills, Cat Mesa, Wind Mesa, Cerro Verde, and Mesita Negra, central New Mexico: Canadian Journal of Earth Sciences, 43(9), 12511268. [ Links ]
McDonough, W.F., Sun, S.s., 1995, The composition of the Earth: Chemical Geology, 120, 223253. [ Links ]
Middlemost, E.A.K., 1989, Iron oxidation ratios, norms and the classification of volcanic rocks: Chemical Geology, 77, 1926. [ Links ]
Morrison, D.F., 1990, Multivariate statistical methods: McGrawHill, New York, 495 p. [ Links ]
Pearce, J.A., 2008, Geochemical fingerprinting of oceanic basalts with applications to ophiolite classification and the search for Archean oceanic crust: Lithos, 100, 1448. [ Links ]
Pearce, J.A., Cann, J.R., 1971, Ophiolite origin investigated by discriminant analysis using Ti, Zr and Y: Earth and Planetary Science Letters, 12, 339349. [ Links ]
Pearce, J.A., Cann, J.R., 1973, Tectonic setting of basic volcanic rocks determined using trace element analyses: Earth and Planetary Science Letters, 19, 290300. [ Links ]
Pearce, J.A., Gale, G.H., 1977, Identification of oredeposition environment from traceelement geochemistry of associated igneous host rocks: Geological Society, London, Special Publication, 7, 1424. [ Links ]
Pearce, T.H., Gorman, B.E., Birkett, T.C., 1977, The relationship between major element chemistry and tectonic environment of basic and intermediate volcanic rocks. Earth and Planetary Science Letters, 36, 121132. [ Links ]
Pearce, J.A., Harris, N.B.W., Tindle, A.G., 1984, Trace element discrimination diagrams for the tectonic interpretation of granitic rocks. Journal of Petrology, 25, 956983. [ Links ]
Peltonen, P., Kontinen, A., Huhma, H., 1996, Petrology and geochemistry of metabasalts from the 1.95 Ga Jormua ophiolite, northeastern Finland: Journal of Petrology, 37, 13591383. [ Links ]
Polat, A., Kerrich, R., Casey, J.F., 1997, Geochemistry of Quaternary basalts erupted along the east Anatolian and Dead Sea fault zone of southern Turkey: implications for mantle sources: Lithos, 40(12), 5568. [ Links ]
Polat, A., Appel, P.W.U., Fryer, B., Windley, B., Frei, R., 2009a, Trace element systematics of the Neoarchean Fiskenæsset anorthosite complex and associated metavolcanic rocks, SW Greenland: Evidence for a magmatic arc origin: Precambrian Research, 175, 87115. [ Links ]
Polat, A., Frei, R, Fryer, B., Appel, P.W.U., 2009b, The origin of geochemical trends and Eoarchean (ca. 3700 Ma) zircons in Mesoarchean (ca. 3075 Ma) ocellihosting pillow basalts, Ivisaartoq greenstone belt, SW Greenland: Evidence for crustal contamination versus crustal recycling: Chemical Geology, 268, 248271. [ Links ]
Rajesh, H.M., 2007, The petrogenetic characterization of intermediate and silicic charnockites in highgrade terrains: a case study from southern India: Contributions to Mineralogy and Petrology, 154, 591606. [ Links ]
Ramakrishnan, M., 2009, Precambrian mafic magmatism in the Western Dharwar Craton, southern India: Journal of Geological Society of India, 73(1), 101116. [ Links ]
RichardsonBunbury, J.M., 1996, The Kula volcanic field, western Turkey: the development of a Holocene alkali basalt province and the adjacent normalfaulting graben: Geological Magazine, 133, 275283. [ Links ]
RodriguezRíos, R., TorresAguilera, J.M., 2009, Evolución petrológica y geoquímica de un vulcanismo bimodal oligocénico en el Campo Volcánico de San Luis Potosí (México): Revista Mexicana de Ciencias Geológicas, 26(3), 658673. [ Links ]
Rollinson, H.R., 1993, Using geochemical data: evaluation, presentation, interpretation: Longman Scientific Technical, Essex, 344 p. [ Links ]
Rutanen, H., Andersson, U.B., 2009, Mafic plutonic rocks in a continentalarc setting: geochemistry of 1.871.78 Ga rocks from southcentral Sweden and models of their palaeotectonic setting: Geological Journal, 44, DOI: 10.1002/gj.1133. [ Links ]
Salters, V.J.M., Stracke, A., 2004, Composition of depleted mantle. Geochemistry Geophysics Geosystems, 5, Q05004, doi:10.1029/2003GC000597. [ Links ]
Sen, C., 2007, Jurassic volcanism in the eastern Pontides: Is it rift related or subduction related? Turkish Journal of Earth Sciences 16, 523539. [ Links ]
Shannon, R.D., Prewitt, C.T., 1969, Effective ionic radii in oxides and fluorides: Acta Crystallographica, B25, 928929. [ Links ]
Shekhawat, L.S., Pandit, M.K. Joshi, D.W., 2007, Geology and geochemistry of palaeoproterozoic lowgrade metabasic volcanic rocks from Salumber area, Aravalli Supergroup, NW India. Journal of Earth System Science, 116 (6): 511524. [ Links ]
Shervais, J.W., 1982, TiV plots and the petrogenesis of modern and ophiolitic lavas. Earth and Planetary Science Letters, 59, 101118. [ Links ]
Sheth, H.C., 2008, Do major oxide tectonic discrimination diagrams work? Evaluating new logratio and discriminantanalysisbased diagrams with Indian Ocean mafic volcanics and Asian ophiolites: Terra Nova, 20, 229236. [ Links ]
Srivastava, R.K., Sinha, A.K., 2007, Nd and Sr isotope systematics and geochemistry of plume related early Cretaceous alkalinemaficultramafic igneous complex from Jasra, Shillong Plateau, Northeastern India. In: G.R. Foulger and D.M. Jurdy (Editors) The origins of melting anomalies: Plates, Plumes, and Planetary Processes: Geological Society of America Special Paper, 430, 815830. [ Links ]
Srivastava, R.K., Chandra, R., Shastry, A., 2004, HighTi type NMORB parentage of basalts from the south Andaman ophiolite suite, India: Proceedings of Indian Academy of Sciences (Earth and Planetray Sciences), 113(4), 605618. [ Links ]
Tokcaer, M., Agostini, S., Savascin, M.Y., 2005, Geotectonic setting and origin of the youngest Kula volcanics (western Anatolia), with a new emplacement model. Turkish Journal of Earth Sciences, 14, 145166. [ Links ]
TorresAlvarado, I.S., Verma, S.P., PalaciosBerruete, H., Guevara, M., GonzálezCastillo, O.Y., 2003, DC_Base: a database system to manage Nernst distribution coefficients and its application to partial melting modeling: Computers & Geosciences, 29, 11911198. [ Links ]
TorresAlvarado, I.S., Smith, A.D., CastilloRomán, J., 2011, Sr, Nd, and Pb isotopic and geochemical constraints for the origin of magmas in Popocatépetl volcano (Central Mexico) and their relationship with adjacent volcanic fields: International Geology Review, 53 (1), 84115. [ Links ]
Verma, S.P., 1997, Sixteen statistical tests for outlier detection and rejection in evaluation of International Geochemical Reference Materials: example of microgabbro PMS: Geostandards Newsletter. The Journal of Geostandards and Geoanalysis, 21(1), 5975. [ Links ]
Verma, S.P., 2000, Geochemistry of the subducting Cocos plate and the origin of subductionunrelated mafic magmas at the volcanic front of the central part of the Mexican Volcanic Belt. In: DelgadoGranados, H., AguirreDíaz, G., Stock, J.M., eds., Cenozoic Tectonics and Volcanism of Mexico: Boulder, Colorado. Geological Society of America Special Paper 334, Chapter 13, 195222. [ Links ]
Verma, S.P., 2005, Estadística Básica para el Manejo de Datos Experimentales: Aplicación en la Geoquímica (Geoquimiometría): Universidad Nacional Autónoma de México, Mexico City, Mexico, 186 p. [ Links ]
Verma, S.P., 2006, Extension related origin of magmas from a garnetbearing source in the Los Tuxtlas volcanic field, Mexico: International Journal of Earth Sciences, 95, 871901. [ Links ]
Verma, S.P., 2009, Continental rift setting for the central part of the Mexican Volcanic Belt: A statistical approach: Open Geology Journal, 3, 829. [ Links ]
Verma, S.P., 2010, Statistical evaluation of bivariate, ternary and discriminant function tectonomagmatic discrimination diagrams: Turkish Journal of Earth Sciences, 19(2), 185238. [ Links ]
Verma, S.P., QuirozRuiz, A., 2006a, Critical values for six Dixon tests for outliers in normal samples up to sizes 100, and applications in science and engineering: Revista Mexicana de Ciencias Geológicas, 23(2), 133161. [ Links ]
Verma, S.P., QuirozRuiz, A., 2006b, Critical values for 22 discordancy test variants for outliers in normal samples up to sizes 100, and applications in science and engineering: Revista Mexicana de Ciencias Geológicas, 23(3), 302319. [ Links ]
Verma, S.P., QuirozRuiz, A., 2008, Critical values for 33 discordancy test variants for outliers in normal samples of very large sizes from 1,000 to 30,000 and evaluation of different regression models for the interpolation and extrapolation of critical values: Revista Mexicana de Ciencias Geológicas, 25(3), 369381. [ Links ]
Verma, S.P., TorresAlvarado, I.S., SoteloRodríguez, Z.T., 2002, SINCLAS: standard igneous norm and volcanic rock classification system: Computers & Geosciences, 28, 711715. [ Links ]
Verma, S.P., TorresAlvarado, I.S., VelascoTapia, F., 2003, A revised CIPW norm: Schweizerische Mineralogische und Petrographische Mitteilungen, 83, 197216. [ Links ]
Verma, S.P., Guevara, M., Agrawal, S., 2006, Discriminating four tectonic settings: five new geochemical diagrams for basic and ultrabasic volcanic rocks based on logratio transformation of majorelement data: Journal of Earth System Science, 115(5), 485528. [ Links ]
Verma, S.P., QuirozRuiz, A., DíazGonzález, L., 2008, Critical values for 33 discordancy test variants for outliers in normal samples up to sizes 1000, and applications in quality control in Earth Sciences: Revista Mexicana de Ciencias Geológicas, 25(1), 8296. [ Links ]
Verma, S.P., DíazGonzález, L., GonzálezRamírez, R., 2009, Relative efficiency of singleoutlier discordancy tests for processing geochemical data on reference materials: Geostandards and Geoanalytical Research, 33(1), 2949. [ Links ]
Verma, S.P., RodríguezRíos, R., GonzálezRamírez, R., 2010, Statistical evaluation of classification diagrams for altered igneous Rocks: Turkish Journal of Earth Sciences, 19(2), 239265. [ Links ]
Verma, S.P., Verma, S.K., Pandarinath, K., RiveraGómez, M.A., 2011, Evaluation of recent tectonomagmatic discrimination diagrams and their application to the origin of basic magmas in Southern Mexico and Central America: Pure and Applied Geophysics (in press). [ Links ]
Vermeesch, P., 2007, Tectonic discrimination diagrams revisited: Geochemistry Geophysics Geosystems, 7, doi:10.1029/2005GC001092. [ Links ]
Wang, L., Li, J.H., Shi, Y.M., Zhang, L.W., 2010, The identification and prediction of Carboniferous volcanic rocks in Dixi area, Junggar basin: Acta Petrologica Sinica, 26 (1), 242254. [ Links ]
Winchester, J.A., Floyd, P.A., 1976, Geochemical magma type discrimination: application to altered and metamorphosed basic igneous rocks: Earth and Planetary Science Letters, 28, 459469. [ Links ]
Winchester, J.A., Floyd, P.A., 1977, Geochemical discrimination of different magma series and their differentiation products using immobile elements: Chemical Geology, 20, 325343. [ Links ]
Wiszniewska, J., Krzeminska, E., Dörr, W., 2007, Evidence of arcrelated Svecofennian magmatic activity in the southwestern margin of the East European Craton in Poland: Gondwana Research, 12, 268278. [ Links ]
Wood, D.A., 1980, The application of a ThHfTa diagram to problems of tectonomagmatic classification and to establishing the nature of crustal contamination of basaltic lavas of the British Tertiary volcanic province: Earth and Planetary Science Letters, 50, 1130. [ Links ]
Xu, G., Frey, F.A., Clague, D.A., Weis, D., Beeson, M.H., 2005, East Molokai and other Keatrend volcanoes: magmatic processes and sources as they migrate away from the Hawaiian hot spot. Geochemistry Geophysics Geosystems, 6, Q05008, doi: 10.1029/2004GC000830. [ Links ]
Zimmer, M., Kroner, A., Jochum, K.P., Reischmann, T., Todt, W., 1995, The Gabal Gerf complex: A Precambrian NMORB ophiolite in the Nubian Shield, NE Africa: Chemical Geology, 123, 2951. [ Links ]