International Journal of Mineralogy

International Journal of Mineralogy / 2014 / Article

Research Article | Open Access

Volume 2014 |Article ID 217916 |

Gloria Vaggelli, Margherita Serra, Roberto Cossio, Alessandro Borghi, "A New Approach for Provenance Studies of Archaeological Finds: Inferences from Trace Elements in Carbonate Minerals of Alpine White Marbles by a Bench-to-Top μ-XRF Spectrometer", International Journal of Mineralogy, vol. 2014, Article ID 217916, 11 pages, 2014.

A New Approach for Provenance Studies of Archaeological Finds: Inferences from Trace Elements in Carbonate Minerals of Alpine White Marbles by a Bench-to-Top μ-XRF Spectrometer

Academic Editor: Basilios Tsikouras
Received04 Oct 2013
Accepted15 Dec 2013
Published06 Feb 2014


The metamorphic rocks outcropping in the Western Alps are characterised by a great variety of white marbles which have been used since the antiquity. This variety mostly includes nine historical Piedmont white marbles (Ornavasso, Candoglia, Crevola, Pont Canavese, Foresto, Chianocco, Prali, Brossasco, and Garessio marbles) coming from well-known quarry sites and belonging to different metamorphic geological units of the Western Alps. The petrographical, minerochemical, and C–O isotopic data of these white marbles have been integrated with CaO and trace element (Fe, Mn, and Sr) concentration determined on single crystals of carbonate minerals (i.e., calcite and/or dolomite) by means of a bench-to-top µ-XRF spectrometer. Principal component analysis and hierarchical cluster analysis were performed on a data set of 178 observations containing CaO, Fe, Mn, and Sr concentration as well as the maximum grain size (MGS), δ18O and δ13C. The use of only five selected variables (CaO, Fe, Mn, Sr, and δ18O) has provided the correct allocation of each individual observation to its relevant class. Therefore, this approach based mostly on a noninvasive µ-XRF determination will be useful to define the provenance of unknown marbles of alpine origin used in antiquity for cultural heritage.

Dedicated to the memory of Margherita Serra, unforgettable Ph.D. Student and friend who early left an indelible sign behind her

1. Introduction

One of the most difficult problems that archaeometry has faced in recent decades is certainly the identification of white marbles used in antiquity. Determining the provenance of marbles used in antiquity for architectural and sculptural artefacts can, indeed, yield important archaeological information on their history. Up to nowadays, different methods have been developed to distinguish white marbles coming from different quarry districts [1]. The optimal first steps in sourcing a lithic artefact should be the macroscopic and thin section study with the petrographic microscope. Unfortunately, it is often the case that it is not allowed to take a sample which is suitable for thin section preparation from precious artefacts. Instead, a common procedure is to analyse powder samples in various ways. The system most widely used today is that of determining C–O isotopic signatures [25]. However, with the rapidly growing of databank, the compositional fields in the isotope discriminative diagrams have been progressively expanded, so many classical marbles show relatively large overlapping ranges.

Other techniques employed for marble characterization are cathodoluminescence [6, 7], trace and rare earth element contents [810], electron paramagnetic/spin resonance [11], and 87Sr/86Sr isotopic ratios [1214].

Chemical analyses were also attempted as a criterion for ascribing a marble to a specific source, and a large number of papers (see e.g., [15]) on this topic have been published following the first work by [16]. Multielement neutron activation analysis of various trace elements was applied to pinpoint the origins of marbles, and this method has been used successfully for characterizing marble quarries in different geographic areas [8, 1719].

However, single provenance determinations using only one method are still insufficient because overlapping results within and between different sample regions occur. Therefore, a number of techniques have been combined to precisely determine the marble provenance [6, 10, 2127].

Aim of this paper is to present a new chemical approach to discriminate white marbles, in addition to the conventionally used methods based on petrography, cathodoluminescence, and stable isotope analysis, in order to ascribe their provenance to a specific quarry site or at least to a defined geological unit. Abandoning the idea of a traditional approach to bulk analysis, this paper aims to evaluate the effectiveness of a new methodological approach based on major and trace element characterization of carbonate mineral phases, calcite and dolomite, being the main rock-forming minerals of white marbles.

As μ-XRF technique is a prominent system for the nondestructive and/or noninvasive analysis of trace elements in glasses [28] and in minerals occurring in ornamental stones from cultural heritage [29, 30], our attention has been focused on the provenance study of marbles used in antiquity by trace elements determination in the main carbonate mineral phase. Therefore, the multianalytical approach based on petrographic (optical and scanning electron microscope), electron microprobe, and stable isotope analysis on calcite and dolomite from white marbles occurring in Western Alps (Piedmont, Italy) reported by [20] has been integrated with trace elements analysis through μ-XRF. This new analytical protocol was used to characterize and identify different marble varieties and understand the effective discriminative power of trace element patterns in carbonate mineral phases.

2. Geological Setting of Alpine White Marbles

The Western Alps of Northern Italy represent a segment of the Alpine-Himalayan orogenic chain associated with the closure of the Western Tethys ocean [31]. Morphologically they are the expression of the continental collision between the European and the Adriatic (African) plates. Many geological units of the Piedmont Western Alps (Northern Italy) have provided a great variety of white marbles (Figure 1) which can be grouped in two classes: the marbles belonging to the Pre-Triassic (Palaeozoic) crystalline basement of the Western Alps, characterised by polymetamorphic evolution and the Triassic marbles coming from the metasedimentary cover, with monometamorphic evolution. The Palaeozoic marbles include the Ornavasso marble (from Ivrea-Verbano zone in Ossola valley), the Prali and Brossasco marbles (from Dora Maira Massif), and the Pont Canavese marble (from Sesia Lanzo zone). The Triassic ones consist of Foresto and Chianocco marbles (from the metasedimentary cover of Dora Maira Massif), Crevola marble (from the deepest Penninic unit in Ossola valley), and finally the Garessio marble (from Briançonnais zone).

Less known than the more famous Apuan varieties (the well-known Carrara marbles), white marbles from western Alps (Piedmont region) have been widely used in the past for sculptural and architectural purposes [32]. Since Roman times to late Baroque, Piedmont region shows the signs of an intensive quarry activity, which results in renowned examples from the Augustus Arc in Susa to the Savoy architecture in Turin.

Besides the interest for provenance purposes, Piedmont Alpine white marbles provide also the opportunity to investigate variations in trace elements composition according to different pressure-temperature conditions and to combine the microchemical results with C–O isotope data on the same marble. The main varieties, indeed, occur as small lenses intercalated to schists and gneisses belonging to separate geological units which suffered different metamorphic conditions (i.e., different - genetic conditions) during different times.

3. Samples and Experimental Techniques

3.1. Sample Descriptions

This work has been carried out on white marbles collected in 9 different quarries located in Piedmont Western Alps. Approximate geographical locations of the quarries are given in Figure 1.

The studied marbles come from the private collection of DST-UNITO and were previously studied by [20]. A list of the selected samples corresponding to alpine marble types, commercially known, is reported on Table 1 together with their main petrographic features, C–O isotope data, and metamorphic conditions.

Piedmont alpine marblesMain carbonate mineral phaseAcronyms used in text and figuresMetamorphicconditions O (δ%0) C (δ%0)AGS(mm)MGS(mm)

BrossascoCalciteBRO-CHP Eclogite−
GaressioCalciteGAR-CGreen Schists−
Crevola (2 varieties)DolomiteCRE-D1/ CRE-D2Amphibolite−3.0/−5.31.4/2.00.14/0.320.9
Pont CanaveseDolomitePONT-DEclogite−

AGS and MGS terminology according to [4, 39, 40].
C and O data are expressed versus PDB standard [41].
Analytical protocol according to [42]. Standard deviation: 0.1 (δ%0) for O and for C.
*Data from [43]. In acronyms: C: calcite; D: dolomite.

The studied alpine marbles were classified according to the main carbonate component, calcite (CaCO3) or dolomite [CaMg(CO3)2]. The calcitic marbles, are characterized by a maximum 20% dolomite to calcite ratio and correspond to Brossasco, Garessio, Ornavasso, and Candoglia marbles. Marble from Prali, in Dora Maira massif, is mainly calcitic, with a dolomite content up to 50%, and therefore both carbonate phases are almost equally abundant. Finally, over 50% dolomite concentration characterizes Pont Canavese, Foresto, and Chianocco marbles as well as Crevola marble which presents two varieties of commercial interest, showing different mineropetrographic features, though they are exploited in the same quarry site [20].

3.2. Instrumentation

Micro-XRF Eagle III-XPL (Röntgenanalytik Messtechnik GmbH, Germany) was used for trace elements analysis of calcite and dolomite in rock samples.

The system includes a Rh X-ray tube working at a maximum voltage of 50 kV and a maximum current of 1 mA. The X-ray fluorescence is detected by means of a liquid nitrogen cooled ultrapure Si detector which has an active area of 30 mm2 and 5 μm beryllium window. The energy resolution results to be lower than 135 eV. Polycapillary lenses collimate X-ray microbeam at the sample surface (30 μm). The sample positioning is controlled by a two CCD video cameras, respectively, with a 10x and 100x magnification and optical focusing. The X-Y-Z stage minimum step is 1.5 μm. The instrument can work both in air or in vacuum and data can be acquired selecting single spot, line-scan, or element mapping scan mode.

Peak to background ratio can be optimized in the energetic range of interest with a set of different primary filters and accordingly adjusting analytical conditions. Available primary filters correspond to Al-25 μm, Al-250 μm, Ti-25 μm, Ni-25 μm, Nb-35 μm, and Rh-50 μm thickness. Filtering the primary radiation is one of the most effective methods to reduce the importance of diffraction peaks in the spectra as well as to drastically reduce the counts of lighter elements and to increase the peak/background ratio for heavier elements. It is, therefore, clear that the selection of proper primary filters must be a compromise between the optimization of peak to background ratio in the energetic range of interest and the minimization of coherent scattering phenomena. The Ti-25 filter was found proper for the quantification of trace elements in the energetic range of transition metals up to Nb to minimize the intensity of diffraction lines and accordingly avoid drastic reduction of total count rates with heavier filters.

In addition to Ti-filtering, the final spectra were obtained combining five spectra acquired on the same spot areas after rotation along a vertical axis located in the centre of the analysed area.

The object of rotating the sample in its analysis plane was to identify and remove artifact lines from the characteristic spectra. A specific facility called Del Diff-Peaks in Spc Preview routine of Vision32 software was used for this purpose and the final X-ray spectra result from 5 rotations after removal of peaks whose position change with the angle between the incoming radiation and the sample crystalline lattice. Sample rotation angles were defined as separated by 72° because 5-fold symmetry (360/5) does not exist in Earth minerals: this means that the 0°, 72°, 140°, 212°, and 288° rotations were chosen. The subtraction of the diffraction contribution, channel by channel, occurs when the component spectra (rotated by 72°) differ by more than 5 times σ: in this case the final spectrum takes the minimum value (i.e., the minimum diffraction contribution) or the average value (i.e., in absence of diffraction).

3.3. Analytical Conditions

Analyses were performed on big samples cut into 4 × 4 × 2 cm flat blocks in order to test the chemical composition homogeneity of calcite. However, the minimum size of the sample, which is connected to the lateral and depth resolution of the method, can be approximately 100 × 100 × 300 μm. In regard to the maximum size, an object of approximately 150 × 150 × 70 mm can be logged entirely inside the sample chamber. Finally, because the lateral resolution of the X-ray beam is 30 μm, the flatness of the surface affects the result very little but the surface (i.e., the spot area to be analysed) has to be clean; indeed, dirt or patinas could contain the same elements as the sample and possibly invalidate the final quantification.

In addition to C and O which form the carbonate ion, undetectable by micro-XRF, Ca is the major element for calcite and Ca and Mg for dolomite, respectively. The analytical method proposed for the measurements of trace elements in carbonate phase does not allow measuring Mg. Indeed the use of a Ti-filter drastically reduces the X-ray counts and in particular light elements with 10 < Z < 16 become more or less undetectable. However, the MgO/CaO ratio is mostly constant in dolomite, and therefore the only quantification of CaO is able to easily distinguish between dolomite and calcite crystals (some 31 and 56 wt.%, resp.). In regard to trace elements, only Fe, Mn, and Sr were the detected elements, which, moreover, correspond to the most abundant and common trace elements occurring in carbonate minerals.

The analytical conditions used for determining CaO and trace elements (Mn, Fe, and Sr) in calcite and dolomite include the following instrumental parameters: voltage, 40 kV; beam current, 1000 μA live time, 1000 s. In addition, a titanium primary filter (25 μm in thickness) was inserted between anode and samples. All analyses were carried out in vacuum conditions even if the vacuum is indispensable only for the detection of light elements (Z < 15). The final composition was quantified adopting the intensity method proposed by [33] using an internal working standard of either calcite (M43) or dolomite (Dolo22), as a result of the identical matrices with respect to calcite and dolomite in the studied samples.

The used calcite working standard is from M43 Carrara marble, internationally used as standard for C and O isotope. It was, first, measured by ICP-OES and ICP-MS techniques, according to HCl 5% bulk rock dissolution method (CaO = 56 wt.%, Sr = 157 ppm, Fe = 64 ppm, and Mn = 10 ppm) and finally by multiple μ-XRF tests to check the homogeneity of the calcite grains. M43 calcite was then used to quantify the dolomite working standard (Dolo22 from the standards library of the SPI Supplies and the C. M. Taylor Company) using Fp-with standard method according to [28].

4. Data Treatment

All selected samples (i.e., alpine marble types) are of known provenance; therefore, in this work, we are trying to verify the reliability of the proposed method to discriminate between white marbles using chemical information corroborated by a geomineralogical approach. In the studied marbles, the MGS (and subordinately AGS) as well as the δ18O and δ13C values resulted in the more variable petrographic parameters, and therefore useful for discriminative purposes according to a multivariate analysis approach in addition to the chemical major and trace composition of the main carbonate phase (calcite or dolomite). The recourse to a multivariate statistical treatment of the available data to obtain a classification of samples in groups of common provenance has long been known in the field of archaeometry [8, 3436].

The parameter determined on the analyzed carbonate crystals (CaO, Fe, Mn, and Sr concentration, MGS, δ18O and δ13C) was used to perform an unsupervised pattern recognition and to identify groups of marbles sharing a possible common provenance. This process was carried out running principal component analyses (PCA) and hierarchical agglomerative cluster analysis (HCA) by means of OriginPro 8.6.0 package (2011-OriginLab Corporation: http://www. As the variables are measured on different scales (CaO wt% range, Mn, Fe, Sr ppm range, δ18O, and δ13C δ%o range), the correlation matrix S (covariance matrix weighted by the standard deviation of variable) was used to process the data and to calculate the Eigenvalues and eigenvectors parameters. In this way, scores for each principal component are scaled by the square root of its eigenvalue.

HCA was performed using the squared “Euclidean distance” (geometric distance in multidimensional space) function, where the greater emphasis to objects that are further apart is stressed. The “group average” option was also used, that is, the distance between two clusters calculated as the average distance between all pairs of objects in different clusters.

5. Results and Discussions

5.1. Trace Elements in Calcite and Dolomite

According to the main carbonate phase of each alpine white marble, calcite or dolomite phases were analysed for major and trace element determination. In particular, calcite was analysed in Ornavasso (ORN-C) and Candoglia (CAN-C) as well as in Brossasco (BRO-C) and Garessio (GAR-C) marbles, dolomite in Pont Canavese (PONT-D), Foresto (FOR-D), and Chianocco (CHI-D) marbles and in both Crevola varieties (CRE-D1; CRE-D2) while calcite and dolomite, occurring in almost the same amounts, were analysed in Prali marble (PRA-C and PRA-D, resp.).

Our set of measurements included, on the whole, 178 μ-XRF spectra, diffraction subtracted, measured on nine different alpine white marbles, using the method described above: Ca was expressed as wt% oxide (CaO), Mn, Fe, and Sr as ppm element (part per million by weight). It has to be pointed out that Crevola marble is represented by two classes corresponding to two varieties (CRE-D1 and CRE-D2) as well as Prali marble, which contains similar amounts of calcite and dolomite which were both analyzed (PRA-C and PRA-D); therefore, the nine marble types are represented by eleven classes.

In Table 2 mean and standard deviation values are reported for each μ-XRF measured element; these quantities are calculated, for any class, from the number of observations reported in “# points” column: this number ranges from a minimum of 10 in dolomite of Prali (PRA-D) to a maximum of 25 in calcite of Foresto marble (FOR-D) and corresponds to the number of analyzed carbonate crystals. The CaO values, since the standard deviation is low, are very close to theoretical values for calcite (some 56.00 wt %) and dolomite (some 31.00 wt %), respectively.

CaO (wt%)Fe (ppm)Sr (ppm)Mn (ppm)# points
Mean Mean Mean Mean



Total # points = 178. C: calcite; D: dolomite.

Figure 2 shows two scatter plots using Fe (ppm) as common abscissa versus Sr (Figure 2(a)) and Mn (Figure 2(b)), respectively. Sr concentration is below 200 ppm, except for PRA-C and PONT-D where it increases up to a mean value of and  ppm values, respectively. Mn concentration is generally very low (below 70 ppm), except for CAN-C and ORN-C samples where it reaches a mean value of and  ppm, respectively. In regard to Fe, it seems the most variable trace element ranging from about 50 ppm in PONT-D and CHI-D marbles to almost 500 ppm in BRO-C marble, respectively.

All the marbles analyzed show compositional zoning rather limited compared to the three trace elements measured. This means that the dispersion of trace elements within the crystal lattice of carbonate minerals is homogeneous and that the method proposed in this work can be worthwhile for discriminating between marbles of different origin.

In Prali marble, the analysis of coexisting and cogenetic calcite and dolomite shows that higher contents of Sr and Fe occur in CaCO3 mineral phase, suggesting the higher distribution coefficient of Sr and Fe in calcite than in dolomite as also supported by previous authors studying the temperature dependence of the distribution coefficient of strontium in calcite and dolomite [37, 38].

However, from the observation of diagrams in Figure 2, the random scattering of the points representative of calcite (empty symbols) and dolomite (black symbols) leads to the conclusion that the concentration of trace elements, in each variety of marble, does not depend primarily on the type of carbonate mineral phase.

Despite some experimental field values of marble varieties plot in well distinguishable fields (e.g. PONT-D, PRA-C, CRE-D2, CAN-C, and BRO-C), in other cases the data points span similar regions in the variable space, without being clearly grouped. Therefore, the discrimination based on scatter-plot diagrams appears to be problematic.

For this reason, in order to obtain more quantitative information, discriminant analyses of the data, using the complete sets of variables, were performed. In this way percentages of correct reassignment may be obtained and the discriminating capability of the proposed technique may be assessed.

5.2. Multivariate Analysis

The whole set of our experimental results can be summarized by a data matrix, which contains the values of 8 variables (MGS, AGS, δ18O, δ13C, CaO, Fe, Mn, and Sr) for the 178 data points, categorized into 11 clusters (ORN-C, CAN-C, BRO-C, GAR-C, PONT-D, FOR-D, CHI-D, CRE-D1, CRE-D2, PRA-C and PRA-D).

As the first step, all observations and all eight continuous variables of Tables 1 and 2 were used in the PCA. We obtained a correlation matrix (Table 3) where MGS and AGS are greatly related to each other (0.99), both strongly inversely correlated with δ18O (−0.86 and −0.89, resp.) and directly correlated with Mn (0.80 and 0.74, resp.). δ13C is also moderately correlated with δ18O (0.58).


O 0.575−0.862−0.8901.000−0.292−0.122−0.235−0.665

Therefore, a lower number of variables might be enough discriminative for our purpose. So an input matrix with a number of variables ranging from 3 to 5 (Fe, Mn, Sr, δ18O, CaO, and/or δ13C) was used: all the PCA diagrams obtained are reported in Figure 3. Tables 4 and 5 are reported all statistical data processing connected to PCA calculation (corresponding to Figures 3(b) and 3(d), resp.), where the correlation matrix with its eigenvalues (in descending order) and extracted eigenvectors (PC1 and PC2 coefficients referring to the first 2 eigenvalues) is reported.


Correlation Matrix









Correlation Matrix






Coef. OCaOFeSrMn


About correlation, matrix it is interesting to note the highest inverse correlation (−0.665) between δ18O and Mn in Table 5 and medium correlation of Sr versus Fe (−0.418), CaO versus Mn (0.384), and CaO versus Fe (0.335) in Tables 4 and 5. It is also notable that, by using only the first two principal components (PC1 and PC2), in both cases of Tables 4 and 5, we extract a cumulative percentage of about 70%. Element vectors of Figure 3 refer to PC1 and PC2 coefficient of Tables 4 and 5 (right and top scale) while single scatter points refer to PC1 and PC2 score (bottom and left scale) corresponding to the linear combination of original variable and principal component coefficients.

In Figure 3(a), the scoreplots obtained using trace elements (Mn, Fe, and Sr) show that only the marble type which is also discriminated in the scatter plots of Figure 2 (ORN-C, CAN-C, CRE-D2, BRO-C, and PONT-D) can be easily distinguished, while partial overlaps remain for the other marble varieties. In Figure 3(b), obtained using trace elements and CaO concentration, a good separation between most marble types, especially between calcite and dolomite marbles, occurs. Only PRA-D and CHI-D marbles are still overlapping. Figure 3(c), where δ18O, δ13C, Mn, Fe, and Sr variables are used, shows that CAN-C and ORN-C partially overlap while a severe overlap occurs between CRE-D2 and FOR-D and between CHI-D and PRA-D, respectively. Finally, in Figure 3(d), where δ18O, CaO, Mn, Fe, Sr variables are used, the dolomite marbles are well separated from the calcite types. Moreover, the different varieties are well distinguished except GAR-C marble which partially overlaps FOR-D field. In Figures 3(b) and 3(d) there is a better separation, but not fully reached, between the 11 classes of the studied marble. For this reason HCA analysis was performed, using the variable selections of Figures 3(b) and 3(d).

Using the HCA method, the dendrograms of Figures 4 and 5 are obtained: the abscissa corresponds to the progressive observation number (from 1 to 178) and the ordinate reports the normalized square Euclidean distance between observations where the horizontal lines indicate the mergence of two clusters. Figure 4 was performed using 4 variables (CaO, Mn, Fe, and Sr) and Figure 5 using 5 variables (δ18O, CaO, Mn, Fe, and Sr). In both figures, the main discriminative parameter resulted in the CaO contents, which allowed separating the marble variety according to their main forming mineral (dolomite at the left branch and calcite at the right branch). In Figure 4, ten cluster are clearly separate, while in, Figure 5, all eleven marble classes are discriminated.

Looking in more details of the calcitic branch (right side of Figure 4), CAN-C and ORN-C are the first to merge (distance of 0.088) being marbles coming from the same geological unit but outcropping in a different quarry district. PRA-C and GAR-C merge at a larger distance (0.137). Finally, Brossasco marble, which has high AGS and MGS, comparable to Ornavasso/Candoglia marble, results, however, chemically more similar to Prali and Garessio (distance = 0.546). All calcitic marbles become a single cluster at distance of 0.713.

In regard to the dolomitic branch (left side of Figure 4), PRA-D and CHI-D constitute a single cluster as they merge at the minimum distance (0.013). CRE-D1 and FOR-D combine at 0.055, and CRE-D2 merges with the previous cited marbles only at 0.222. Therefore, the two varieties of Crevola marble are significantly far and dissimilar. Finally, PONT-D marble differs from all the others and merge, forming a single dolomitic marble cluster, at 0.806. This behavior of Pont Canavese marble is mostly due to the significantly higher Sr concentration as well shown also in scatter plot of Figure 2(a) and PCA plots of Figure 3.

If δ18O variable is added (Figure 5), PRA-D and CHI-D merge at a larger distance (0.062) with respect to Figure 4 (), resulting easier to discriminate. Therefore, HCA with 5 variables allowed separating all 11 clusters. Moreover, in both dolomitic and calcitic branch, a generally significant increase in the distance due to the wide difference in δ18O values is shown (Table 1). However, no changes in clusters occur and the order of hierarchy remains the same. In Table 6, the final centres for each cluster after HCA analysis using four (A) and five (B) variables are reported. Proper grouping observations are obtained for 10 and 11 clusters, respectively (Figures 4 and 5). All variable columns are normalized in the range 0-1. The distance between the cluster centers always improves passing from 4 to 5 variables: the greatest increase (difference = 0.735) is between CAN-C and CRE-D2.

Final Cluster Centers
4 variables5 variables
CLMarble#CaFeSrMnCLMarble#CaFeSrMn O

1PONT-D19 0.0390.0001.0000.0301PONT-D19 0.0390.0061.0000.0300.463
2CRE-D125 0.0430.2740.0000.2432CRE-D125 0.0430.2790.0000.2430.648
3FOR-D25 0.0000.3640.0540.0313FOR-D25 0.0000.3680.0540.0310.741
4PRA-D/CHI-D25 0.0280.0270.0540.0614PRA-D10 0.0440.0820.0430.0190.481
5CHI-D15 0.0170.0000.0610.0890.704
5CRE-D211 0.0160.6850.0070.2506CRE-D211 0.0160.6870.0070.2500.861
6PRA-C15 0.9340.2710.4440.0007PRA-C15 0.9340.2760.4440.0000.454
7GAR-C23 1.0000.2030.0600.1118GAR-C23 1.0000.2080.0600.1111.000
8BRO-C11 0.9611.0000.0210.0789BRO-C11 0.9611.0000.0210.0780.463
9CAN-C12 0.9990.4610.1130.70910CAN-C12 0.9990.4650.1130.7090.009
10ORN-C12 0.9550.3630.0891.00011ORN-C12 0.9550.3670.0891.0000.000

All variable columns are normalized in the range 0-1. # = number of investigated carbonate grains.

HCA method realizes, in the case of 4 variables, 86% of correct clustering observations since cluster number 4 of Table 6(A) (PRA-D/CHI-D), containing 25 observations (corresponding to 14% of the total), can be considered not properly assigned (Figure 4 and Table 6(A)). In the case of 5 variables, all observations can be considered correctly assigned (Figure 5 and Table 6(B)).

Even if the distance between PRA-D and CHI-D cluster centers remains low (0.062 in Table 6(B)), it, however, allows distinguishing PRA-D and CHI-D and the separation between the different marble types appears complete.

6. Conclusions

In this paper, the petrographical, minerochemical, and C–O isotopic data of white marbles from Western Alps, previously described by means of classical techniques as optical and electron microscope, electron microprobe, and stable isotope analysis [20], have been integrated with trace elements analysis on the carbonate mineral phases (calcite and dolomite) performed by means of a μ-XRF instrument. The results presented above for the multimethod discrimination of the white marbles from Western Alps are certainly encouraging.

The method here proposed seems capable of allowing discrimination among the Western Alps white marbles with acceptable confidence. In particular, the PCA method, using two principal components, based on a maximum of 5 variables, extracts about 70% of the available variance. HCA method properly assigns 86% of observations to ten clusters using CaO, Mn, Fe, and Sr variables and the total observations to proper eleven clusters using δ18O, CaO, Mn, Fe, and Sr variables.

The possibility of making μ-XRF trace element analyses on white marbles provided the opportunity of improving previous archaeometric approaches and will allow performing quantitative analysis either on archaeological finds smaller than 150 × 150 × 70 mm or on small fragments (at least 100 × 100 × 300 μm) by nondestructive analytical procedures. Obviously, the data presented are still few and should be implemented with other measures to make the proposed procedure more significant. Therefore, the proposed discriminative approach, mostly based on trace elements in the carbonate phase and on the δ18O isotopic signature, will be applied to white marbles from the Mediterranean area in order to obtain a complete characterisation of such important natural stones, used from antiquity up to now for cultural heritage.

Conflict of Interests

The authors declare that there is no conflict of interests regarding the publication of this paper.


The μ-XRF measures have been obtained with the equipment acquired by the Interdepartmental Center “G. Scansetti” for Studies on Asbestos and Other Toxic Particulates with a grant from Compagnia di San Paolo, Torino, Italy. Special thanks are due to B. Fubini and R. Compagnoni (Center “G. Scansetti” UNITO) for encouragement and for providing μ-XRF. Financial support by the Italian Ministry of Instruction, University and Research and by the National Council of Research.


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