V Renson
email: vrenson@vub.ac.be

A Martínez-Cortizas

Nadine Mattielli

J Coenaerts

C Sauvage

François De Vleeschouwer

C Lorre

F Vanhaecke

Richard Bindler

M Rautman

K Nys

Ph Claeys

Lead isotopic analysis within a multiproxy approach to trace pottery sources. The example of White Slip II sherds from Late Bronze Age sites in Cyprus and Syria

teaching and research institutions in France or abroad, or from public or private research centers.   Lead isotopic analysis within a multiproxy approach to trace pottery sources. The example of White Slip II sherds from Late Bronze Age sites in Cyprus and Syria

Introduction

Pottery fragments constitute artifacts widely found at archaeological sites all around the world and their study documents numerous technological, economic and socio-cultural aspects of ancient civilizations. Among the questions commonly raised, that of their provenance often requires the use of a multiproxy approach. Elemental analyses are indeed widely and successfully applied to trace pottery origins (e.g., Knapp and Cherry, 1994;[START_REF] Gomez | The source provenance of Bronze Age and Roman pottery from Cyprus[END_REF][START_REF] Mommsen | Attic pottery production, imports, and exports during the Mycenaean period by Neutron Activation Analysis[END_REF][START_REF] Kennett | Geochemical characterization of Lapita pottery via Inductively Coupled Plasma-Mass Spectrometry (ICP-MS)[END_REF][START_REF] Asaro | The history of the Lawrence Berkeley National Laboratory instrumental neutron activation analysis programme for archaeological and geological materials[END_REF][START_REF] Ben-Shlomo | Neutron activation and petrographic analysis of selected Late Bronze Age and Iron Age pottery from Tell es-Safi/Gath, Israel[END_REF][START_REF] Tschegg | State of the art multi-analytical geoscientific approach to identify Cypriot Bichrome Wheelmade Ware reproduction in the Eastern Nile delta (Egypt)[END_REF][START_REF] Tschegg | Integrated geological, petrologic and geochemical approach to establish source material and technology of Late Cypriot Bronze Age Plain White ware ceramics[END_REF]. A recent study [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF] established that Pb isotope analysis, so far rarely considered for this purpose, constitutes an efficient tool to identify pottery sources.

The main goal of the present study is to further investigate the effectiveness of isotopic analysis of Pb in pottery provenance studies using a multiproxy approach that not only compares pottery sets but also pottery and its potential raw materials. The latter remains an under-investigated field although successful examples exist (e.g. [START_REF] Claeys | Local pottery provenience studies: a role for clay analysis[END_REF][START_REF] Tschegg | Integrated geological, petrologic and geochemical approach to establish source material and technology of Late Cypriot Bronze Age Plain White ware ceramics[END_REF].

White Slip ware, a hand-made pottery, characterized by a white or light slip applied on a dark clay and which most commonly has a hemispherical bowl shape [START_REF] Popham | White slip ware[END_REF], originates from Cyprus and was largely spread in the Eastern Mediterranean during the 14th and 13th centuries BC [START_REF] Popham | White slip ware[END_REF]. The chemical and mineralogical composition (clay matrix, inclusions and slip) has been documented on fragments from several sites using different methods [START_REF] Courtois | Petrographic and Electron Microprobe studies of Cypriote White Slip Ware (Late Bronze Age). Revue d'Archéométrie[END_REF][START_REF] Artzy | Cypriote pottery at Ras Shamra[END_REF][START_REF] Rautman | Neutron activation analysis of Late Roman ceramics from Kalavasos-Kopetra and the environs of the Vasilikos valley[END_REF][START_REF] Gomez | Clays related to the production of White Slip Ware[END_REF] and several authors have investigated the possible provenances of the different constitutive parts of the pottery (e.g., [START_REF] Gomez | Clays related to the production of White Slip Ware[END_REF][START_REF] Gomez | A preliminary petrographic analysis of Cypriot White Slip II ware[END_REF]. Although the entire foothills of the Troodos Mountains (corresponding to the Troodos Ophiolite located in central Cyprus, Fig. 1a) have been proposed as the source of the basaltic clay used for White Slip II production, Sanidha-Moutti tou Ayiou Serkou (hereafter Sanidha) is the only site, so far, where archaeological evidence attests to the existence of such production [START_REF] Todd | Excavations at Sanidha. A Late Bronze Age ceramic manufacturing centre[END_REF]. Moreover, it was shown that the clay used for White Slip II ware production in Sanidha corresponded to smectite group clays resulting from the weathering of the leucocratic gabbros surrounding the site [START_REF] Rautman | Neutron activation analysis of Late Roman ceramics from Kalavasos-Kopetra and the environs of the Vasilikos valley[END_REF][START_REF] Gomez | Clays related to the production of White Slip Ware[END_REF]. Additionally, in Sanidha, aside White Slip, numerous Monochrome ware sherds were found which were also produced on the site. Monochrome ware represents an ordinary utilitarian pottery without painting or painted in a single color [START_REF] Yon | Dictionnaire illustré multilingue de la céramique du Proche Orient ancient, Collection de la Maison de l'Orient Méditérranéen[END_REF][START_REF] Todd | Excavations at Sanida 1990[END_REF]. In Sanidha, Monochrome ware presents no slip and occurs in a finer or coarser version respectively called Monochrome and Coarse Monochrome [START_REF] Todd | Excavations at Sanida 1990[END_REF].

In the present study, the Pb isotopic variability, previously observed [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF] within a set of 30 White Slip II sherds excavated in Hala Sultan Tekke, is compared to White Slip II sherds from Sanidha and to a larger set of clay sources collected in the surroundings of this site. In parallel, White Slip II sherds found in Minet el-Beida, the harbor of Ugarit (Syria), were also analyzed to explore their possible sources. More specifically, the aims of this study are to: (1) investigate the Pb isotopic composition of pottery sherds from the only attested White Slip II production center, namely Sanidha; (2) examine the compatibility of the isotopic composition of the White Slip II sherds from Hala Sultan Tekke previously analyzed [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF] with that of Sanidha; (3) compare the Pb isotopic composition of White Slip II sherds with that of a set of clays (including clays derived from the weathering of gabbros from Sanidha area) and with the results of [START_REF] Gomez | Clays related to the production of White Slip Ware[END_REF]; (4) test the hypothesis that proposed clays from the Moni formation (silt and bentonite clays embedding fragments from various lithologies from the Triassic to the Upper Cretaceous, Fig. 1c) as a potential raw material for White Slip II production [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF]; and (5) scrutinize the compatibility of the isotopic composition of a set of White Slip II sherds excavated in Minet el-Beida (Syria) with that of an assemblage of White Slip II sherds and clays from Cyprus. Elemental chemistry determined by X-ray fluorescence (XRF) and subsequent Principal Component Analysis (PCA) are combined with the Pb isotope ratio data on selected sherds and clays to explore the significance of the Pb isotope signatures. To complement this study, elemental analyses were carried out on 4 sherds using a scanning electron microscope (SEM) equipped with an energy dispersive X-ray detection (EDX) system and the bulk mineralogy as well as the clay mineralogy of the sediments was identified using X-ray diffraction (XRD).

Archaeological settings of the pottery samples

Hala Sultan Tekke

The Late Bronze Age settlement of Hala Sultan Tekke lies on the west shore of the Larnaca salt lake in southeastern Cyprus (Fig. 1a). The material culture indicates that the town flourished from the second half of the 14th century BC to the first half of the 12th century BC. Undoubtedly, Hala Sultan Tekke is one of the Cypriot urban polities that actively participated in the Eastern Mediterranean exchange network, in particular during this timespan (Åström, 1986). White Slip sherds investigated here are mainly from the settlement and include sherds from a sherd deposit (F6031) studied by Öbrink (1979). Three samples (HST 13,16 and 17) are from Tomb 24, located in the vicinity of the settlement [START_REF] Åström | Hala Sultan Tekke 12. Tomb 24, Stone Anchors, Faunal Remains and Pottery Provenance[END_REF]. The Pb isotopic composition of this set of White Slip II sherds from Hala Sultan Tekke was investigated in a former paper [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF] and archaeological contexts are detailed in Öbrink (1979), [START_REF] Åström | Hala Sultan Tekke 12. Tomb 24, Stone Anchors, Faunal Remains and Pottery Provenance[END_REF] and [START_REF] Renson | Provenance determination of pottery from Hala Sultan Tekke using lead isotopic analysis: preliminary results[END_REF].

Sanidha

The Late Bronze Age site of Sanidha is located in the foothills of the Troodos Mountains (Fig. 1a). The excavations revealed exceptionally important quantities of White Slip II and Monochrome fragments. Archaeological remains showed that Sanidha was a large-scale production center for these pottery wares [START_REF] Todd | Excavations at Sanidha. A Late Bronze Age ceramic manufacturing centre[END_REF][START_REF] Todd | The Field Survey of the Vasilikos Valley 1. Vasilikos Valley Project 9[END_REF]. The site was already occupied in the Middle Bronze Age, but only became a pottery production center in the Late Bronze Age [START_REF] Todd | Sanidha-Moutti tou Ayiou Serkou: a Late Bronze Age Site in the Troodos Foothills[END_REF] and White Slip II material is dated to the Late Cypriote II [START_REF] Todd | Sanidha-Moutti tou Ayiou Serkou: a Late Bronze Age Site in the Troodos Foothills[END_REF]) that ranges from the last quarter of the 15th century BC to the end of the 13th century BC (Knapp and Cherry, 1994;[START_REF] Eriksson | The Creative Independence of Late Bronze Age Cyprus. An Account of the Archaeological Importance of White Slip Ware[END_REF]. The site was not a permanent settlement, but was mainly devoted to the manufacture of pottery [START_REF] Todd | Excavations at Sanida 1990[END_REF] and was probably connected in some way to the important contemporary site of Kalavasos-Ayios Dhimitrios located around 10 km SE [START_REF] Todd | The Field Survey of the Vasilikos Valley 1. Vasilikos Valley Project 9[END_REF]. Petrographic analyses of White Slip II and Monochrome sherds from Sanidha indicated that the fabrics were similar and that the clay used for their production was identical (Xenophontos in [START_REF] Todd | Excavations at Sanida 1990[END_REF]). Moreover, these authors suggested that the clays were probably local because the mineralogical composition of the sherds corresponded to that of raw material available around the site (Xenophontos in [START_REF] Todd | Excavations at Sanida 1990[END_REF]). According to its chemical and mineralogical composition, White Slip II could originate from different locations of the circum-Troodos area, but so far Sanidha remains the only attested production center. A representative set of sherds was selected to define the Pb isotopic composition of Sanidha pottery production: 19 White Slip II sherds, 7 Monochrome sherds and 4 Coarse Monochrome sherds. All sherds came from the surface [START_REF] Todd | The Field Survey of the Vasilikos Valley 1. Vasilikos Valley Project 9[END_REF].

Minet el-Beida

Ugarit is situated on the Ras Shamra tell, on the northern Syrian coast (Fig. 1b) near modern Lattaquia. The site, capital of a kingdom of the same name, was occupied continuously from the end of the 8th until the end of the 2nd millennium BC, but is best known for its Late Bronze Age remains. It was ideally located at the junction of two major routes linking the coast and inner Syria and running along the Mediterranean. Because of this strategic position, its well-sheltered main harbor Minet el-Beida, and its natural resources, the site experienced great prosperity and was a major trade center, as demonstrated by imported materials (e.g., Schaeffer, 1949, pp. 136-233;[START_REF] Yon | Céramiques Mycéniennes d'Ougarit[END_REF], and by international diplomatic correspondence and treaties written in Akkadian [START_REF] Moran | The Amarna Letters[END_REF][START_REF] Beckman | Hittite Diplomatic Texts[END_REF][START_REF] Lackenbacher | Textes Akkadiens d'Ugarit[END_REF]. The 5 White Slip II and 6 White Slip II late sherds studied in this article come from the ashlar-built chamber tomb III [1005] located at Minet el-Beida (for the description of the tomb, its architecture, and a brief description of its material, see Schaeffer, 1929, p. 291;Schaeffer, 1949, pp. 144-149;[START_REF] Marchegay | Les tombes d'Ougarit : architecture, localisation et relation avec l'habitat[END_REF]. White Slip II late corresponds to the final version of White Slip II and to a general deterioration of the ware with the use of coarser material, badly formed bowls, unevenly applied slip and more simplified painted decoration [START_REF] Popham | White slip ware[END_REF][START_REF] Eriksson | The Creative Independence of Late Bronze Age Cyprus. An Account of the Archaeological Importance of White Slip Ware[END_REF]. In the chamber, the material found on the pavement included locally made oil lamps, Cypriot vases (White Slip II ware bowls, Monochrome ware bowls, and Base-ring ware bowls and juglets), Mycenaean ceramics, faience stirrup jars, Egyptian alabasters, metals, a cylinder seal, ivories, and the remains of three individuals. This tomb was probably used over a large period of time starting in the 14th c. BC until late in the 13th c. BC.

Clay samples

Sanidha is located in the Southern Troodos Transform Fault Zone, a geologically complex area, intensively faulted and characterized by rocks from the different sequences of the Troodos Ophiolite (Volcanic, Intrusive, Plutonic and Mantle sequences) and from the Transform sequence. In the SW and SE of this area, clays from the Upper Cretaceous Perapedhi, Kannaviou and Moni formations are developed (Fig. 1c). A set of 29 clays/soils was collected in the surroundings of Sanidha (less than 10 km, except samples C7 O 2 and O 12, located at 20 km). More precisely, samples were collected in the clays from the Moni formation (6), in the shales, umbers and clay from the Perapedhi formation (4), in clays derived from the weathering of the rocks from the Volcanic Sequence (3), the Intrusive Sequence (1) and the Plutonic Sequence (7, all weathered gabbros). Finally, samples of four soils were collected in the surroundings of Sanidha. The sampling in this area was carried out based on the geological maps published by the Geological Survey of Cyprus [START_REF] Gass | The Geology of the Southern Troodos Transform Fault Zone[END_REF][START_REF] Gsd | Geological Survey Department of Cyprus[END_REF]. Sediments were collected after the outcrop had been carefully cleaned and the coordinates of every sample were obtained using a GPS (Fig. 1c and Table 5). The set of clays analyzed here also includes samples previously measured for elemental composition by [START_REF] Rautman | Neutron activation analysis of Late Roman ceramics from Kalavasos-Kopetra and the environs of the Vasilikos valley[END_REF] and correspond to sediments from the Upper Cretaceous Kannaviou and Perapedhi formations and to a weathered gabbro sample. These latter samples are labeled as KKP.

Methods

Lead isotopic analysis

The samples were dried at 40 °C and milled in an agate mortar under an extracting hood. To remove any slip, painting or trace of weathering, the sherd surfaces were first entirely cleaned using a micro-drill equipped with diamond-bits, prior to crushing. The resulting powders were heated at 550 °C during 4 h. The acid digestions of the sample powders and subsequent Pb separation by ion exchange chromatography were carried out following the procedure described in [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF]. Lead isotope ratios were measured using two multi-collector -inductively coupled plasma -mass spectrometers (MC-ICP-MS): a Nu Plasma (Nu Instruments) in operation at the Earth and Environmental Science Department of the ''Université Libre de Bruxelles'', Belgium, and a Thermo Scientific Neptune (Thermo Scientific) in operation at the Department of Analytical Chemistry of Ghent University, Belgium (the reproducibility of the measurements is discussed in [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF]. The analytical conditions were identical to those described in [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF] and are only briefly summarized below. Thallium was added to each sample and to the standard to monitor and correct for instrumental mass discrimination. Sample solutions were prepared to obtain a beam intensity in the axial collector ( 204 Pb) of a minimum of 100 mV and a Pb/Tl ratio of $ 5, matching the Pb and Tl concentration ratio of the NIST SRM 981 ''Common lead'' isotopic standard (150 ng/g in Pb, with 50 ng/g in Tl). The NIST SRM 981 standard was measured several times before each analytical session and between each set of two samples on both devices (sample-standard bracketing). The standard values obtained agree with the long-term laboratory values and the MC-ICP-MS values of [START_REF] Weis | High-precision isotopic characterization of USGS reference materials by TIMS and MC-ICP-MS[END_REF]. These values are also in agreement with thermal ionization mass spectrometry (TIMS) triplespike values previously published by [START_REF] Galer | Practical applications of lead triple spiking correction of instrumental mass discrimination[END_REF].

Some samples having lower Pb concentrations were analyzed using a DSN (Desolvating Nebuliser System) for sample introduction into the MC-ICP-MS unit. Thallium was also added to each sample and sample solutions were prepared to obtain a beam intensity in the axial collector ( 204 Pb) of a minimum of 100 mV and a Pb/Tl ratio of $ 4-5 corresponding to the Pb and Tl concentration ratio of the NIST SRM 981 ''Common lead'' isotopic standard (here 25 ng/g in Pb, with 6 ng/g in Tl). Values were corrected for instrumental mass discrimination using the NIST SRM 981 standard solution and the sample-standard bracketing method [START_REF] White | High-precision isotopic characterization of USGS reference materials by TIMS and MC-ICP. High-precision analysis of Pb isotope ratios by multi-collector ICP-MS[END_REF] and 5 replicates (i.e. second analysis of the same sample) and 5 duplicates (i.e. the entire procedure was reproduced on the same sample) were measured to test the reproducibility (Tables 4 and5).

X-ray fluorescence

The concentrations of selected major and trace elements were measured on 300 mg of dried and homogenized powder using a Bruker S8 Tiger wavelength-dispersive X-ray Fluorescence (WD-XRF) analyzer in the Department of Ecology and Environmental Science at the University of Umeå, Sweden. Powders were transferred in 10 mm diameter plastic cups, with a 2.5 lm mylar film at the base. Each powder was slightly compressed manually to reduce porosity effects. A specific calibration was developed in order to optimize the WD-XRF approach for the matrices of the samples. The methodological details can be found in De [START_REF] De | Quantitative WD-XRF calibration for small ceramic samples and their source material[END_REF]. Briefly, it involved the development of a calibration procedure using certified reference materials that display the same matrices as the ceramic samples. Concentrations of the following elements were measured: Si, Ti, Al, Fe, Mn, Mg, Ca, Na, K, P, S, V, Ni, Cu, Zn, Rb, Sr and Pb.

4.3. Mineralogy of clay samples (XRD) and elemental analysis of selected sherds (SEM-EDX)

X-ray diffraction was used to describe the bulk mineralogy of the sediments (method description in [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF]. Classification for quantitative estimations follows that proposed by [START_REF] Cook | Methods of sample preparation and X-ray diffraction data analysis, X-ray Mineralogy Laboratory[END_REF]: trace, <5%; present, 5-25%; abundant, 25-65% and major, >65%. No correction factor is available for serpentine. However, because traces of this mineral were detected on a few spectra, it has been reported in Table 1a. The XRD methodology was also used to detail the clay mineralogy of selected sediment samples after elimination of the carbonates. Around 3 cm 3 of sample were gently dispersed in deionized water and sieved using a 63 lm mesh filter. Any carbonate was removed from the <63 lm fraction by adding dilute (0.1 M) HCl. The solution was then rinsed with deionized water to remove any trace of acid. The clay fraction (<2 lm) was separated by settling according to Stoke's law. Oriented mounts were prepared according to the procedure described in [START_REF] Moore | X-Ray Diffraction and the Identification and Analysis of Clay Minerals[END_REF] and analyzed using a Brucker D8 Advance diffractometer. Each slide was analyzed three times: (1) after natural dry air conditions, (2) after ethylene-glycol solvation for 24 h, (3) after heating at 500 °C for 4 h. Clay species were identified using the resulting three diffraction spectra. The proportion of illite sheets in the interstratified smectite-illite was defined according to [START_REF] Moore | X-Ray Diffraction and the Identification and Analysis of Clay Minerals[END_REF]. Bulk mineralogy of samples KKP201, KKP202 and KKP204 was not determined.

Major elements of the sherd matrix were measured using a JEOL-JSM-6400 scanning electron microscope (SEM) equipped with an energy-dispersive X-ray detection (EDX) facility (Thermo Noran Pioneer with Si-Li detector) at 15 kV and a working distance of 39 mm. Carbon coating of the thin sections was carried out using an EMITECH-Carbon evaporation K450. Elemental mapping was conducted at several locations at various dimensions (460 lm  580 lm or 1000 lm  1500 lm) for each sherd. Several (8-14) measurements were then performed at various places on the matrix of each sherd. Minerals present as inclusions were also analyzed. The measurements were made on a single point representing the size of the beam (1 lm 2 ). No external standard was used.

Statistical analysis

A principal components analysis (PCA) was performed using the concentrations of Si, Ti, Al, Fe, Mn, Mg, Ca, Na, K, V, Ni, Cu, Zn, Rb, Sr, Pb and the 208 Pb/ 204 Pb, 207 Pb/ 204 Pb and 206 Pb/ 204 Pb ratios. Phosphorus was not included in the analysis because it can be linked to post-depositional processes in a burial context [START_REF] Freestone | Retention of phosphate in buried ceramics: an electron microbeam approach[END_REF]. As indicated by [START_REF] Baxter | Detecting multivariate outliers in artifact compositional data[END_REF], statistical analysis of compositional data is usually undertaken on transformed data. PCA was performed on two types of transformed data: (1) standardized concentrations (Z scores, Z = (Xi À X avg )/SD; where Xi is the value of an element in a given sample, X avg is the average of all samples for that element and SD is the standard deviation), and (2) log (to base 10) transformation of concentrations. Transformations are applied to avoid the close data and scaling effects, and provide average centering.

Eight samples having largely different Pb isotopic or elemental composition were considered as gross outliers (in the sense applied by [START_REF] Baxter | Detecting multivariate outliers in artifact compositional data[END_REF]) and not included in the PCA because they strongly affected the results and limited the identification of the covariation structure. These were three clay samples (C7 63, C8 8a and C8 70) and five sherds (HST 4d,WS 33,WS 35,WS 36 and WS 70). After PCA analysis two clay samples (C9 42 and C9 44) were also found to be moderate outliers each one in a different principal component, but their elimination did not affect the extraction of the components or the distribution of the other samples (clays and sherds) on the projection of components (i.e. the ordination plots). Consequently, they were kept in the analysis.

The PCA was performed using a varimax rotation to maximize the variance of the elements in the principal components [START_REF] Eriksson | Introduction to Multiand Mega-Variate Data Analysis using Projection Methods[END_REF]. A preliminary comparison produced almost identical results using the standardized and logged data, in agreement with what was found by [START_REF] Baxter | Standardization and transformation in principal component analysis, with applications to archaeometry[END_REF], which may be due to the elimination of the gross outliers [START_REF] Baxter | Statistical modelling of artifact compositional data[END_REF]. Here, only the results obtained in the standardized data matrix are presented.

Results

Bulk and clay mineralogy of the sediments

The semi-quantitative results of the bulk mineralogy are reported in Table 1a. In the samples from the Moni formation, the main components are clay minerals; quartz is present in every sample. Plagioclase, calcite and cristobalite are also present but irregularly distributed across the Moni clay samples. Umbers (Fe, Mn-rich clays) and shales from the Perapedhi formation have a variable mineralogy: sample C8 63a contains amorphous material and the clay minerals, quartz, calcite and goethite are present; sample C8 63b is dominantly amorphous and the only mineral identified is goethite; clay minerals (mainly palygorskite) are abundant in samples C8 76b along with the presence of quartz, calcite and goethite and in C8 76a where quartz is also present. Samples from the Upper Cretaceous Volcanic sequence are mainly composed of clay minerals and quartz occurs (in traces or present). In some samples of this group, plagioclase, K-feldspar, dolomite, pyroxene, muscovite and serpentine can be identified in various proportions. The sample derived from the weathering of the Upper Cretaceous Intrusive sequence mainly consists of chlorite, with the presence of quartz. Samples from the weathered gabbros (Upper Cretaceous Plutonic sequence) are mainly composed of clay minerals. Sample C7 72a is a pure chlorite. The other samples from this group are also made of plagioclase. Amphibole is observed in most cases and less frequently, quartz, pyroxene, talc and serpentine. In the soil samples, clay minerals are also the main component. The assemblage of minerals observed in the soils is quite variable and details are reported in Table 1a.

The clay mineralogy of seven samples is presented in Table 1b.

SEM-EDX

In the four White Slip II sherds from Sanidha, the elemental composition of the clay matrix shows relatively high contents in SiO 2 and Al 2 O 3 that vary from 41 to 66.3 wt.% and 4.1 to 36.5 wt.%, respectively (Table 2). This alumino-silicate matrix displays large variations in FeO, MgO and CaO, which range from 0 to 29.7 wt.%, from 0 to 17.4 wt.% and from 0.5 to 15.8 wt.%, respectively (Table 2). The TiO 2 , Na 2 O and K 2 O contents vary from 0 to 5.4 wt.%, from 0 to 3.6 wt.% and from 0 to 2.6 wt.%, respectively (Table 2). The minerals observed in the thin sections of these pot-tery fragments are pyroxene, plagioclase, magnetite, ilmenite, quartz, olivine, sphene and epidote. Similar data were obtained for six White Slip II sherds from Hala Sultan Tekke in [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF] and additional measurements were made on these sherds. Moreover, to present the chemical composition typical for the clay matrix, part of the data previously obtained and obviously corresponding to the composition of fresh minerals commonly present in the sherds was discarded. The values for SiO 2 , Al 2 O 3 , FeO, MgO and CaO range from 41.5 to 69.7 wt.%, from 16.9 to 33.4 wt.%, from 0 to 11 wt.%, from 0.4 to 20.3 wt.% and from 0.6 to 18.3 wt.%, respectively. The TiO 2 , Na 2 O and K 2 O contents vary from 0 to 2.1 wt.%, from 0 to 7.6 wt.% and from 0 to 6.8 wt.%, respectively. Minerals observed in thin sections, using SEM-EDX analysis, are pyroxene, plagioclases, magnetite, rutile, pseudorutile, ulvospinel, quartz, sphene, epidote, amphibole and chlorite.

XRF

The XRF results, as well as detection limits, accuracies and reproducibility are reported in Table 3. The concentrations of Si, Ti, Al, Fe, Mn, Mg, Ca, Na, K, P, S, V, Ni, Cu, Zn, Rb, Sr and Pb are displayed, as well as the average and standard deviation for each element in the different pottery and clay groups.

Lead isotope ratios

With the exception of the San 28 sample (with values of 15.704 and 18.977 for 207 Pb/ 204 Pb and 206 Pb/ 204 Pb ratios, respectively), all White Slip II sherds from Sanidha display a narrow range of values between 15.674 and 15.685 and between 18.853 and 18.976 for 207 Pb/ 204 Pb and 206 Pb/ 204 Pb ratios, respectively (Table 4 and Fig. 2a). The composition of the Coarse Monochrome varies from 15.677 to 15.686 and from 18.940 to 18.957 and that of the Monochrome from 15.671 to 15.684 and from 18.861 to 18.957 (Table 4 and Fig. 2a). The isotopic composition of the three wares from Sanidha is thus identical (Table 4 and Fig. 2a). The isotopic field of the White Slip II from Hala Sultan Tekke has a larger variability (Fig. 2b andc, see also [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF] for the values of the Pb isotope ratios). Except for two samples (WS 33 and WS 35) that show lower values in both ratios, the isotopic composition ranges from Pb/ 204 Pb ratios, respectively. The majority of White Slip II samples from Hala Sultan Tekke (24 out of 31) plot in the range of the Sanidha production (Fig. 2b andc). White Slip II sherds from Minet el-Beida have values ranging from 15.681 to 15.697 and from 18.872 to 18.991 for 207 Pb/ 204 Pb and 206 Pb/ 204 Pb ratios (Table 4 and Fig. 2b). The White Slip sherds from Minet el-Beida can be divided into two groups according to their Pb isotopic composition. Three White Slip II sherds have a signature compatible with that of White Slip II from Sanidha, while the others (2 White Slip II and 6 White Slip II late) are spread along a trend that does not overlap with the main cluster (Fig. 2b).

The different clay samples analyzed show a large isotopic variability and few display a Pb isotopic composition that falls within the field of White Slip II sherds (Table 5 and Fig. 2c). Among them, the clays from the Moni formation have isotopic values that range between 15.666 and 15.689 Only four clay samples have a composition that corresponds with the field of the Sanidha production (Table 5 and Fig. 2c): two clays from the Moni formation (C7 63 and C9 34) and two clays derived from the weathering of the gabbros (C8 8b and KKP201). Seven other clays have a Pb isotopic composition similar to that of the Sanidha production and these range between 15.662 and 15.689 and 18.812 and 18.859 for the 207 Pb/ 204 Pb and 206 Pb/ 204 Pb ratios, respectively. These clay samples are: four clays from the Moni formation (C8 34, C8 35a, C8 35b and C9 36), one from the Kannaviou formation (KKP204), one from the Perapedhi formation (KKP202) and one soil developed in Sanidha (C9 44).

Discussion

The Sanidha White Slip II sherds analyzed show an alumino-silicate matrix, the composition of which is compatible with that of a smectite. The composition of the ''matrix'' shows large variability in SiO 2 , Al 2 O 3 , FeO, MgO and CaO that can be explained by the elemental replacements normally occurring in smectite clay. The composition of the matrix of the White Slip II sherds from Hala Sultan Tekke resembles that of White Slip II sherds from Sanidha, though Al 2 O 3 and FeO contents show a greater range of variability. The assemblage of minerals present as inclusions is also similar in White Slip sherds from both Sanidha and Hala Sultan Tekke. The matrix composition and the mineral assemblage, as indicated by the SEM-EDX analyses, match the composition of the material resulting from the weathering of basaltic rocks (local gabbros). More specifically, the presence of a few minerals, such as quartz, chlorite and epidote, indicates that the gabbro is characterized by a greenschist facies and low-grade metamorphism. [START_REF] Courtois | Petrographic studies of pottery (preliminary results)[END_REF] [START_REF] Todd | Excavations at Sanida 1990[END_REF]. To summarize the petrographic, XRF and XRD studies, the pottery fragments do have the typical mineralogical composition of White Slip II sherds previously analyzed and whose fabric was shown to be unique and most likely derived from the basic or ultrabasic material of the Troodos Ophiolite [START_REF] Artzy | Cypriote pottery at Ras Shamra[END_REF].

The Pb isotopic composition of the 30 sherds representing three pottery wares from Sanidha (Monochrome, Coarse Monochrome and White Slip II) plots within a narrow field (Fig. 2a). This homogeneity supports the assumption that a single and fairly uniform clay source was used as base material for the production of White Slip II and Monochrome (including Coarse Monochrome) in Sanidha, in agreement with the petrographic data (Xenophontos in [START_REF] Todd | Excavations at Sanida 1990[END_REF]. Most of the White Slip II sherds from Hala Sultan Tekke have a Pb isotopic composition similar to that of White Slip II from Sanidha (Fig. 2b andc). However, it is obvious that a few of them differ from the Pb isotope ratios typical for Sanidha sherds (Fig. 2c). Seven White Slip II sherds from Hala Sultan Tekke indeed extend along a trend between the main Sanidha cluster and lower 207 Pb/ 204 Pb values (Fig. 2b andc), while three others are isolated and display lower values in 207 Pb/ 204 Pb or in both 207 Pb/ 204 Pb and 206 Pb/ 204 Pb ratios (Fig. 2c). It is important to note that SEM-EDX analysis carried out on the clay matrix and on the mineral assemblage present as inclusions did not reveal any mineralogical differences between sherds that plot inside and outside the cluster. The presence of accessory minerals bearing exotic Pb isotopic ratios compared to those of the clay-matrix minerals can most likely be ruled out to explain this isotopic variability. In magmatic rocks, common Pb is in the plagioclases and K-feldspars while radiogenic Pb is found in the accessory minerals. In most cases, because of mass balance, the Pb isotopic composition of the whole rock is consequently more similar to that of the feldspars and plagioclases than to that of the accessory minerals [START_REF] Harlavan | Systematic changes in lead isotopic composition with soil age in glacial granitic terrains[END_REF]. The isotopic composition of the White Slip II is thus most likely dominated by that of the clays derived from the weathering of the dominant minerals constituting the gabbros.

The 207 Pb/ 204 Pb vs 206 Pb/ 204 Pb three-isotope plot (Fig. 2c) shows that the isotopic composition of the White Slip II cluster is similar to that of different types of clay: the ones derived from the weathering of the gabbros, some clays from the Moni formation, and a soil collected in Sanidha. An interstratified smectite-illite rich in smectite sheets dominates the clay mineralogy of these samples. The different clays derived from the weathering of the gabbros were all collected in the vicinity of Sanidha (<5 km), but display highly variable Pb isotopic composition. Some of them have a signature compatible with that of fresh gabbros from the Troodos Ophiolite (Fig. 2c). One sample has very high values of both 207 Pb/ 204 Pb and 206 Pb/ 204 Pb ratios (15.690 and 19.629, respectively). The Pb isotopic composition of two samples (C8 8b and KKP201) is compatible with that of the White Slip II (Fig. 2c). The latter two weathered gabbro samples have values higher than those of the fresh rocks either for the 206 Pb/ 204 Pb ratio or for both the 207 Pb/ 204 Pb and the 206 Pb/ 204 Pb ratios. [START_REF] Nobre-Silva | Leaching systematics and matrix elimination for the determination of ocean island basalts[END_REF] observed a similar shift in the isotopic composition of Pb in basalts, linked to the weathering process. These authors indeed showed that the weathered basalts had higher values of both 207 Pb/ 204 Pb and 206 Pb/ 204 Pb ratios and a higher dispersion than the fresh basalt samples. This isotopic shift most likely accounts for the difference previously observed between the signature of White Slip II sherds and that of the fresh gabbros [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF].

Principal component analysis

To discriminate between the different possible clay sources and to further explain the different isotopic composition in the White Slip II fragments investigated here, a PCA was performed on the Pb isotope ratios and the elemental concentrations for selected clay samples and White Slip II sherds. As indicated in the methods section, eight samples were considered as gross outliers and not included in the PCA (clay samples C7 63,C8 8a and C8 70 and sherds HST4d,WS 33,WS 35,WS 36 and WS 70).

Five principal components account for 80.4% of the variance of the chemical and isotopic composition (Fig. 3a). The first component, C1 (23% of total variance), is associated with large positive loadings of V, Fe, Al, Na and 206 Pb/ 204 Pb ratios (0.72-0.90) and a moderate positive loading of the 208 Pb/ 204 Pb ratio (0.62) and Ti (0.53) (Fig. 3a andb). The C1 scores mainly separate the clays (negative scores) from the pottery fragments (positive scores), excepted for sample KKP201, which has a positive score as for the sherds (Fig. 4a). Moreover, on the basis of the scores for C1 in the different pottery groups, it seems that White Slip sherds (White Slip II and White Slip II late) from Minet el-Beida differ from those of Sanidha and Hala Sultan Tekke, while the White Slip II sherds from Sanidha and Hala Sultan Tekke are clearly similar. Vanadium, Fe, Al and Ti are elements that tend to concentrate in the clay fraction of soils and weathering products. The positive scores in C1 observed in the pottery fragments thus indicate an enrichment in fine size grains in comparison with the clays of the area, which could be the result of an intentional man-made grain size selection. Such a selection can be confirmed by comparing the results of samples C8 8b to KKP201. Indeed, these two samples, collected close to each other (< 1 km), both correspond to weathering products of the gabbros from Sanidha and have a similar Pb isotopic composition, compatible with that of Sanidha White Slip II. However, different grain-size selection processes were applied to these samples. Indeed, on one hand no grain size selection was performed on sample C8 8b prior to analyses but on the other hand sample KKP201 was sieved to < 63 lm and only the fine grain size fraction was studied. The large similarity in C1 scores in KKP201 and White Slip II is evidence for a grain-size selection process applied to the raw material prior to pottery production (Fig. 4b).

The second component, C2 (20% of variance), is associated with large positive loadings of Mg, Ca and Ni (0.82-0.95) and a moderate negative loading of Ti (À0.60) (Fig. 3a andb). This component mainly accounts for differences in the clays (Fig. 4a andb) and separates the Moni samples (high negative scores) from the weathered gabbros and the soils (high positive scores). It does not distinguish either the pottery fragments, or sample KKP201, which show quite similar factor scores with values close to zero. The elements of C2 indicate a mafic mineralogy. The fact that sample KKP201 does not have a large score suggests that this variation in composition captured by C2 relates to minerals present in the coarser fraction of the clays. The third component, C3 (14% of variance), is associated almost exclusively with large negative loadings of 207 Pb/ 204 Pb (À0.96) (Fig. 3a andb). This component also accounts for part of the variance of Sr and Mn (Fig. 3b), but a detailed inspection shows that almost all the effect is related to clay sample C9 42 being a moderate outlier in this component. It is intriguing that the 207 Pb/ 204 Pb ratio is not correlated to the other isotopic ratios (at least that of the other uranogenic isotope, the 206 Pb/ 204 Pb ratio). However, from Fig. 4a it is clear that there is a difference between the ceramics: sherds from Hala Sultan Tekke have positive scores, sherds from Sanidha have close to zero scores, while sherds from Minet el-Beida have negative scores. In fact an ANOVA test indicates that sherds from Sanidha and Minet el-Beida have significantly higher 207 Pb/ 204 Pb ratios than samples from Hala Sultan Tekke. The only conclusion we can be advanced, at the moment, is that whatever the mineral phase (or phases) controlling the variations in 207 Pb/ 204 Pb ratios, it is not modeled by the chemical elements that have have analyzed.

The fourth component, C4 (13% of variance), is associated with large positive loadings of Rb, Pb and Si (0.76-0.80) and to a moderate positive loading of K (0.54) (Fig. 3a andb). This component accounts for most of the variation in Pb. Moni clays have high positive C4 scores while the weathered gabbros have high negative scores (Fig. 4a). Within the pottery fragments, scores vary greatly. The elements of C4 indicate a felsic composition. Sediment samples with large positive scores in C2 contain amphibole, which is consistent with higher Ca, Mg and Ni concentrations; while illite/ smectite-illite is more abundant in clays with higher C4 scores (samples of the Moni Formation). Thus, C2 suggests a more basic/ultrabasic and C4 a more acidic mineral component. Moni clays are enriched in elements associated with C4 but depleted in elements associated with C2. Clays from other soils and weathered gabbros are enriched in elements associated with C2. The evidence provided by C1, C2 and C4 chemical signatures, suggests that Moni clays were not used for the production of the White Slip II investigated here. This conclusion is consistent with the bulk mineralogy results.

Finally, C5 (11% of variance) is associated with large positive loadings of Cu and Zn (0.73-0.91) (Fig. 3a andb). Most of the sherds from Minet el-Beida and a few from Hala Sultan Tekke have high positive scores in C5, which indicates higher Cu and Zn contents in these samples (Fig. 4a). In the geological context of the Troodos Ophiolite foothills of Sanidha area, these Cu and Zn contents can be related to sulfide deposits. It is worth noting that Pb occurs in these sulfide ores [START_REF] Gale | Bronze Age copper sources in the Mediterranean: a new approach[END_REF].

PCA results also seem to indicate that the 206 Pb/ 204 Pb and 208 Pb/ 204 Pb ratios vary with C1 (Fig. 5). The higher the fine fraction content, the higher these two isotope ratios. This means that the grain-size selection performed on the clays prior to pottery production influenced the isotopic composition, but in a limited range that does not affect the possibility of linking the pottery to its original raw material (Fig. 2c). This process does not affect the 207 Pb/ 204 Pb ratio (Fig. 5). The fifth component, C5 (related to Cu and Zn content), controls part of the Pb content variability (Pb res in Fig. 6a). As the Cu and Zn contents increase, the Pb res content also increases but not in the same proportion in all the pottery groups. Sanidha sherds and Hala Sultan Tekke sherds share a similar trend. The Minet el-Beida samples are divided in two groups according to this component. Two of the three samples (White Slip II) having an isotopic composition similar to that of Sanidha White Slip II show a link between Pb res and Cu-Zn contents that is similar to White Slip II from Sanidha. Six samples from Minet el-Beida (2 White Slip II and 3 White Slip II late which do not share the isotopic composition of Sanidha White Slip II and one White Slip II that does share it), show a stronger influence on Pb res ; because the Pb res content is more affected by the Cu-Zn content than in the other pottery groups (the slope of the regression is twice for these samples than for the other group, Fig. 6a). The fifth component, related to the presence of Cu-Zn-(Pb) bearing sulfides, also controls part of the isotopic variability (Fig. 6b). Sulfides seem to increase total Pb concentration at the same time they produce a decrease in the isotopic ratios (Fig. 6a andb).

The White Slip II from Sanidha, most White Slip II from Hala Sultan Tekke, and three White Slip II from Minet el-Beida, share a common origin that corresponds to the local weathered gabbros outcropping in the proximity of Sanidha. This conclusion is in agreement with that of [START_REF] Gomez | Clays related to the production of White Slip Ware[END_REF]. Clearly, these samples were processed by removing part of the coarse fraction prior to pottery making.

The lower values of isotopic ratios of some White Slip II sherds from Hala Sultan Tekke could be related to a higher content of sulfides in the clay matrix. Indeed, [START_REF] Booij | Pb-isotope systematics of a fossil hydrothermal system from the Troodos ophiolite, Cyprus: evidence for a polyphased alteration history[END_REF] showed that sulfides have lower Pb isotope ratios than their source rocks, in this case greenschist samples from the Troodos Ophiolite. The lower isotopic values of some of the pottery samples analyzed in the present study can be interpreted as the result of the presence of sulfides in the clay derived from the greenschist facies gabbros that were used for White Slip II production. In this context, in terms of sources, the variability in isotopic composition of some White Slip II sherds from Hala Sultan Tekke could be explained by a variability of the sulfide content of the clays used for their production. Nevertheless, these White Slip II sherds from Hala Sultan Tekke and Sanidha most likely originated from the same source and were produced using very similar raw materials.

The last three samples from Hala Sultan Tekke, which have an isolated isotopic composition (WS 33, WS 35 and WS 36), were not included in the PCA. Their very different signature could be explained by seawater contamination of the clay used for their production. Such a contamination is likely because they show an Eu anomaly (Hatcher, personal communication) compatible with seawater contamination. On-going studies using Sr isotopes could confirm or refute this hypothesis.

In her investigation of ceramics from Sanidha, Herscher (in [START_REF] Todd | Excavations at Sanida 1990[END_REF]) indicated that the dominant style of White Slip II was similar to that of ceramics excavated in Kalavasos-Ayios Dhimitrios and to that from the sherd deposit from Hala Sultan Tekke investigated by Öbrink (1979). Most of the White Slip II from Hala Sultan Tekke analyzed here are part of this assemblage studied by Öbrink. The results also favor the use of a common clay source for the pottery made at Sanidha and for the White Slip II sherds assemblage from Hala Sultan Tekke studied here. However, because no clear source can be proposed for samples WS 33, WS 35 and WS 36, this conclusion is not valid for these three sherds, so far.

The sherds from Minet el-Beida (2 White Slip II and 3 White Slip II late), which do not share the isotopic composition of Sanidha, show a different relationship between Pb and Cu-Zn contents. Moreover, the clay used for their production was processed in a significantly different way. It is less enriched in fine grain size fraction than the Sanidha pottery (close to zero or negative C1 scores; Fig. 6b). This clearly suggests that this White Slip II group originates from another source with a different mode of preparation of the clay. The White Slip sherds excavated in Tomb III in Minet el-Beida originate from two different sources, one of them being consistent with a Sanidha origin and another with a, so far, unknown clay that could come from a different location in the foothills of the Troodos Ophiolite or perhaps from Syria.

Conclusions

The Pb isotopic composition of the pottery production in Sanidha is homogeneous and confirms the effectiveness of the method to identify pottery assemblages. Lead isotopic analysis also constitutes an efficient tool to further refine the links between the pottery sherds to the local clays derived from the weathering of the surrounding lithologies (in this case the gabbros). Here, the good concordance of the Pb isotope results with the study of [START_REF] Gomez | Clays related to the production of White Slip Ware[END_REF] reinforces the identification of the weathered gabbro as the source for pottery production in Sanidha. However, the former hypothesis [START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF] that proposed clays from the Moni formation as a possible raw material for White Slip II ware production can definitively be discarded. The isotopic signature of the White Slip II ware pottery set from Hala Sultan Tekke corresponds well with a Sanidha source. Most likely the Sanidha and Hala Sultan Tekke material studied here share a similar origin, derived from the weathered gabbro, outcropping in the vicinity of Sanidha.

Two different origins can be proposed for White Slip II ware from Minet el-Beida. Some of the sherds share a common origin with White Slip II ware from Sanidha, and were most likely produced at Sanidha. Another group of sherd samples is most likely derived from another source, not yet identified. It should be searched for in the foothills of the Troodos Ophiolite or perhaps in the vicinity of Minet el-Beida.

This study also provides evidence for a grain-size selection and thus of a well defined and specific preparation of the clays prior to the White Slip II ware production. However, this grain size sorting and the selection of the finer fraction occurred without any major modification of the Pb isotopic composition.

The approach proposed here that includes Pb isotope analysis is indisputably efficient for identifying different groups within White Slip ware pottery, to link White Slip ware pottery to their clay sources and also to identify processes applied to clays prior to pottery making. The use of such an approach on further White Slip fragments and clays from the surroundings of the Troodos should allow a better understanding of this pottery ware production and distribution, which would improve knowledge on links and exchange between Cyprus and numerous regions in the Eastern Mediterranean. This type of approach is also encouraged at other similar archeological sites containing a variety of ceramics and different clay raw materials in the vicinity. This study confirms the utility of using Pb isotopic characterization for pottery provenance as well as the effectiveness and diagnostic significance of Pb isotopic analysis within multiproxy approaches.

Fig. 2 .

 2 Fig. 2. (a) 207 Pb/ 204 Pb vs 206 Pb/ 204 Pb three-isotope plot for Sanidha sherds. Open circles, White Slip II; dark green circles, Monochrome and light green circles, Coarse Monochrome; (b) 207 Pb/ 204 Pb vs 206 Pb/ 204 Pb three-isotope plot for White Slip II sherds from the three sites. Detail between 15.66 and 15.71 and between 18.80 and 19.00 for 207 Pb/ 204 Pb and 206 Pb/ 204 Pb, respectively. Green circles, White Slip II from Sanidha; brown squares, White Slip II from Hala Sultan Tekke and red triangles, White Slip II from Minet el-Beida. The two groups of White Slip II sherds from Minet el-Beida are surrounded by ellipses; (c) 207 Pb/ 204 Pb vs 206 Pb/ 204 Pb three-isotope plot for White Slip II sherds from the three sites, clays around Sanidha (this study), fresh gabbro (from Spooner and Gale (1982) and Hamelin et al. (1984)) and sulfides (from Spooner and Gale (1982), Hamelin et al. (1988) and Booij et al. (2000)). Green circles, White Slip II from Sanidha; brown squares, White Slip II from Hala Sultan Tekke; red triangles, White Slip II from Minet el-Beida; open squares, Moni formation; open diamond, Kannaviou formation; crosses, Perapedhi formation; Saint Andrews crosses, Upper Cretaceous Volcanic sequence and Intrusive sequence; open triangles, weathered gabbro; black circles, soils; open circles, fresh gabbro and dashes, sulfides. Samples C7 72a and C8 9b have very high 207 Pb/ 204 Pb and 206 Pb/ 204 Pb values and are not reported on the plot for clarity reasons. No leaching process was applied to clay samples measured in this study prior to analysis.

Fig. 3 .

 3 Fig. 3. (a) Factor loadings. In the PCA performed here, factor loadings represent correlation coefficients between the elements and the principal components; (b) communalities. The communality accounts for the proportion of each element's variance explained by the five extracted principal components. The total length of the bars is the communality of each element, while the sections represent the proportion of variance allocated in the principal components.

Fig. 4 .

 4 Fig. 4. (a) Factor scores of the five components in the different samples (pottery fragments and sediments); (b) C1-C2 projection showing the distribution of clays and sherds in the space defined by fine grain size content (C1) and mafic composition (C2). Open squares are Moni clays, light gray squares are weathered gabbros and soils, open triangles are White Slip II from Minet el-Beida, light gray diamonds are White Slip II from Sanidha and dark gray circles are White Slip II from Hala Sultan Tekke. Note that only clay KKP201 plots in the same compositional field of the sherds.

Fig. 5 .

 5 Fig. 5. Scattergram showing the isotopic composition vs the factor scores of C1 in clays and pottery fragments. Higher positive scores indicate enrichment in finer grains and thus a higher grain-size selection. Symbols as in Fig. 4.

Fig. 6 .

 6 Fig. 6. (a) Relationship between part of the total Pb content (Pbres) and C5 factor scores (indicative of a Cu-Zn sulfide bearing phase); (b) relationship between part of the isotopic composition ( 206 Pb/ 204 Pbres) and C5 factor scores. Symbols as in Figs. 4 and 5, except for the light gray triangles showing White Slip II sherds from Minet el-Beida that have a similar isotopic composition to White Slip II sherds from Sanidha. Pbres: since the regression of C4 scores vs Pb accounts for Pb in felsic minerals (64% of Pb variance), the residual term is calculated by detrending total Pb concentration from C4: obtaining for every sample the difference between the observed (concentration in the sample) and expected (estimated based on the linear equation of the regression function) values. Residuals (Pbres) are assumed to represent the fraction of Pb related to non-felsic sources. 206 Pb/ 204 Pbres: in a similar way, the residual isotopic signal is obtained in two steps (since it has two major controls, C1 and C3): first it is detrended from C1, and then the obtained residuals are detrended from the effect of C3. The high correlation of Pbres and 206 Pb/ 204 Pbres with C5 scores point to a residual dominant effect of a sulfide phase.

Table 2

 2 Major element composition obtained from SEM-EDX analysis of White Slip II from Sanidha. Total Fe as FeO. Values in wt.%. Traces of P 2 O 5 , Cr 2 O 3 , NiO and As 2 O 3 were detected in some samples and are reported where they are above detection limits (0.15 wt.% for elements above Na).

	Sample	SiO 2	TiO 2	Al 2 O 3	FeO	MnO	MgO	CaO	Na 2 O	K 2 O	P 2 O 5	Cr 2 O 3	NiO	As 2 O 3
	San 24	53.06	0.36	24.47	12.02	0.00	3.20	5.00	1.45	0.43	0.00	0.00	0.00	0.00
	San 24	54.35	0.49	22.31	12.04	0.00	6.21	3.25	0.77	0.58	0.00	0.00	0.00	0.00
	San 24	56.22	0.00	26.65	2.83	0.49	0.00	9.09	3.58	0.29	0.00	0.00	0.00	0.86
	San 24	51.03	0.94	4.08	17.34	0.78	14.14	10.61	0.88	0.19	0.00	0.00	0.00	0.00
	San 24	53.97	0.00	33.00	0.00	0.00	8.38	1.94	0.45	2.26	0.00	0.00	0.00	0.00
	San 24	52.38	0.36	6.88	15.31	0.00	13.73	11.17	0.00	0.18	0.00	0.00	0.00	0.00
	San 24	51.88	5.39	23.72	11.77	0.00	2.16	3.91	0.81	0.35	0.00	0.00	0.00	0.00
	San 24	55.73	0.36	26.10	11.06	0.00	3.68	2.02	0.60	0.44	0.00	0.00	0.00	0.00
	San 27	55.95	3.41	17.64	12.73	0.00	4.04	4.06	1.05	1.13	0.00	0.00	0.00	0.00
	San 27	63.85	0.00	19.70	3.45	0.00	1.25	9.10	1.44	1.20	0.00	0.00	0.00	0.00
	San 27	54.43	0.57	25.89	9.53	0.00	4.88	1.99	0.66	2.04	0.00	0.00	0.00	0.00
	San 27	54.72	0.00	6.08	18.85	0.00	17.43	2.55	0.00	0.37	0.00	0.00	0.00	0.00
	San 27	57.65	0.00	24.73	7.84	0.00	4.37	4.56	0.86	0.00	0.00	0.00	0.00	0.00
	San 27	54.73	0.00	26.08	9.70	0.00	5.12	1.91	0.79	1.67	0.00	0.00	0.00	0.00
	San 27	56.19	0.41	18.30	12.11	0.00	8.90	2.03	0.60	1.46	0.00	0.00	0.00	0.00
	San 27	40.96	0.43	26.67	14.12	0.00	5.55	12.27	0.00	0.00	0.00	0.00	0.00	0.00
	San 27	60.15	0.29	21.11	7.11	0.00	5.53	4.45	0.78	0.58	0.00	0.00	0.00	0.00
	San 27	50.96	0.00	15.96	11.58	0.00	11.35	9.47	0.67	0.00	0.00	0.00	0.00	0.00
	San 27	56.70	0.00	10.84	13.66	0.00	13.35	3.98	0.84	0.64	0.00	0.00	0.00	0.00
	San 27	65.69	0.00	20.72	2.38	0.00	0.00	6.27	2.52	1.12	0.00	0.00	0.00	1.28
	San 27	53.48	0.42	7.07	17.14	0.00	15.48	5.81	0.28	0.00	0.00	0.00	0.32	0.00
	San 27	48.86	1.66	11.48	13.68	0.00	15.28	7.94	0.00	0.00	0.00	1.11	0.00	0.00
	San 28	52.83	1.26	11.58	29.73	0.57	0.95	1.59	0.73	0.77	0.00	0.00	0.00	0.00
	San 28	59.74	0.00	24.60	5.32	0.00	2.76	5.73	1.34	0.51	0.00	0.00	0.00	0.00
	San 28	66.03	0.00	20.30	5.17	0.00	2.57	4.35	1.41	0.16	0.00	0.00	0.00	0.00
	San 28	48.72	0.00	30.66	2.44	0.00	1.20	15.84	0.88	0.26	0.00	0.00	0.00	0.00
	San 28	61.41	0.00	21.65	5.29	0.00	1.61	6.16	2.25	1.63	0.00	0.00	0.00	0.00
	San 28	63.52	0.00	20.76	7.15	0.00	3.34	3.99	1.03	0.21	0.00	0.00	0.00	0.00
	San 28	58.53	0.61	8.62	16.57	0.00	10.50	4.32	0.85	0.00	0.00	0.00	0.00	0.00
	San 28	57.03	0.00	25.19	9.88	0.00	4.99	1.60	0.78	0.24	0.29	0.00	0.00	0.00
	San 28	48.56	0.45	26.30	14.90	0.00	4.89	3.72	0.98	0.19	0.00	0.00	0.00	0.00
	San 28	66.29	0.00	22.42	5.63	0.00	2.47	1.80	1.03	0.36	0.00	0.00	0.00	0.00
	San 28	51.95	0.50	28.59	8.83	0.00	4.32	3.49	1.66	0.66	0.00	0.00	0.00	0.00
	San 28	54.91	0.00	36.54	3.05	0.00	0.76	1.62	1.89	1.23	0.00	0.00	0.00	0.00
	San 28	55.92	0.00	25.55	9.71	0.00	4.25	3.07	1.07	0.43	0.00	0.00	0.00	0.00
	San 30	62.80	0.00	20.84	10.51	0.00	3.76	1.50	0.59	0.00	0.00	0.00	0.00	0.00
	San 30	60.71	0.54	20.10	14.17	0.00	2.58	1.27	0.43	0.21	0.00	0.00	0.00	0.00
	San 30	46.84	0.43	24.76	22.78	0.00	3.08	1.51	0.00	0.60	0.00	0.00	0.00	0.00
	San 30	57.71	0.54	21.95	11.22	0.00	2.92	1.87	1.15	2.63	0.00	0.00	0.00	0.00
	San 30	54.11	0.00	25.91	8.83	0.00	4.63	2.59	2.16	1.78	0.00	0.00	0.00	0.00
	San 30	54.42	0.59	24.90	12.00	0.00	4.07	1.04	1.42	1.55	0.00	0.00	0.00	0.00
	San 30	48.20	0.53	26.28	17.43	0.00	3.49	1.51	0.51	2.05	0.00	0.00	0.00	0.00
	San 30	60.41	0.00	17.77	7.48	0.00	5.81	6.54	1.15	0.84	0.00	0.00	0.00	0.00
	San 30	50.34	0.00	5.08	24.85	0.00	13.73	5.61	0.39	0.00	0.00	0.00	0.00	0.00
	San 30	56.27	1.40	22.80	14.02	0.00	4.63	0.55	0.33	0.00	0.00	0.00	0.00	0.00
	San 30	57.74	0.00	4.52	19.76	0.00	16.21	0.61	0.48	0.69	0.00	0.00	0.00	0.00
	San 30	53.46	0.91	22.61	13.07	0.00	3.59	5.70	0.65	0.00	0.00	0.00	0.00	0.00

Table 3

 3 Elemental compositions measured by XRF. Results are given in % for major elements and in mg/g for trace elements. Values below detection limits are reported as <DL. Detection limits, standard deviation, accuracy and reproducibility are reported for each element.

	Sample		Si	Ti	Al	Fe	Mn	Mg	Ca	Na	K	P	S	V	Ni	Cu	Zn	Rb	Sr	Pb
			%	mg/g	%	%	mg/g	%	%	%	%	mg/g	%	mg/g	mg/g	mg/g	mg/g	mg/g	mg/g	mg/g
	DL		0.028	0.015	0.012	0.007	0.005	0.01	0.005	0.007	0.002	0.2	0.002	0.004	0.002	0.003	0.003	0.002	0.003	0.004
	STDEVA		1.56	0.00002	0.28	0.14	0.052	0.053	0.072	0.011	0.062	0.181	0.23	0.008	0.004	0.005	0.02	0.009	0.017	0.003
	Acc. (%)		4	5	7	4	5	7	7	5	3	26	36	3	8	4	10	11	9	4
	Repr. (%)		90	92	91	92	92	93	90	92	90	88	99	90	82	78	91	93	93	88
	Clays
	C7 63	UC Moni form.	27	6.3	3.2	4.5	0.79	1.6	1.7	0.79	1.72	0.9	0.08	0.154	0.092	0.052	0.10	0.062	0.19	0.022
	C8 34	UC Moni form.	30	2.8	2.6	3	1.28	1.27	2.1	0.46	0.95	0.9	0.13	0.097	0.048	0.076	0.082	0.043	0.18	0.019
	C8 35a	UC Moni form.	21.1	3.3	3.3	3.6	0.25	1.7	0.63	0.56	1.23	0.7	0.08	0.137	0.060	0.076	0.089	0.057	0.14	0.023
	C8 35b	UC Moni form.	23.1	4.1	2.8	3.7	0.5	1.4	1.8	0.38	1.39	0.5	0.09	0.099	0.069	0.042	0.078	0.000	0.025	0.017
	C9 34	UC Moni form.	22.7	3	2.6	2.7	1.13	1.33	0.66	0.54	0.82	0.6	0.1	0.103	0.039	0.048	0.067	0.030	0.078	<DL
	C9 36	UC Moni form.	18.1	3	2.4	2.47	0.56	1.01	0.55	0.59	0.88	0.28	0.13	0.069	0.031	0.020	0.050	0.027	0.058	<DL
		Average	24	3.8	2.8	3.3	0.75	1.4	1.3	0.6	1.2	0.6	0.1	0.110	0.057	0.052	0.077	0.037	0.11	0.014
		Stand. Dev.	4.2	1.34	0.4	0.8	0.39	0.2	0.7	0.1	0.3	0.23	0.0	0.0310	0.022	0.021	0.017	0.023	0.068	0.010
	C8 8a	Weather. gabbro	15.7	0.67	3.8	3.1	0.60	4.2	3.3	0.37	0.12	<DL	0.05	0.054	0.083	0.019	0.090	<DL	0.087	<DL
	C8 8b	Weather. gabbro	20.9	1.84	3.8	4.4	0.84	5.6	4.4	0.5	0.18	0.25	0.06	0.134	0.21	0.024	0.054	<DL	0.066	<DL
	C8 70	Weather. gabbro	21.7	1.43	4.7	4.2	0.84	6.1	5.5	0.85	0.03	0.29	0.05	0.100	0.091	0.019	0.053	0.062	0.12	0.011
	KKP201	Weather. gabbro	20.2	3.9	5.5	6.0	0.53	2.1	2.1	0.72	0.33	0.38	0.07	0.236	0.059	0.139	0.052	0.011	0.083	0.006
	C9 42	Soil	22	3.5	3.8	5.5	1.66	3.5	6.2	0.51	1.15	0.28	0.06	0.174	0.056	0.089	0.079	0.029	0.19	0.008
	C9 44	Soil	25	1.16	1.5	6.7	1.44	9.4	6.2	0.12	0.06	0.25	0.06	0.121	0.61	0.000	0.060	0.015	0.023	0.010
		Average	21	2.1	3.9	5	0.98	5.2	4.6	0.51	0.31	0.27	0.06	0.137	0.18	0.048	0.065	0.020	0.095	0.006
		Stand. Dev.	3	1.31	1.3	1.3	0.46	2.5	1.7	0.26	0.42	0.07	0.01	0.063	0.22	0.054	0.016	0.023	0.056	0.004
	Sherds
	Hala Sultan Tekke
	HST 4d	White Slip II	19.9	3.2	4.1	5.7	0.68	2.5	1.5	0.89	0.39	0.24	0.05	0.174	0.059	0.047	0.046	0.006	0.075	<DL
	HST 13	White Slip IIA	20.5	3.9	4.9	6.2	0.78	2.6	2.5	0.49	0.3	0.5	0.06	0.251	0.055	0.098	0.048	0.004	0.19	0.009
	HST 16	White Slip II	26	4	4.8	7.9	1.56	2.6	2.2	0.92	0.5	0.30	0.06	0.252	0.075	0.188	0.14	0.027	0.14	0.012
	HST 17	White Slip II	20.5	3.2	3.7	5.7	1.28	2.4	1.5	0.69	0.61	0.5	0.05	0.167	0.044	0.141	0.13	0.013	0.12	<DL
	HST 20	White Slip II late	10.3	1.34	2.1	2.2	0.22	1.19	1.04	0.35	0.14	<DL	0.05	0.064	0.013	0.007	0.021	0.003	0.12	<DL
	WS 17	White Slip II	25	3.9	5.1	8	0.91	2.5	2.2	1.31	0.55	0.5	0.06	0.224	0.061	0.080	0.064	0.019	0.098	0.012
	WS 27	White Slip II	22.4	3.2	4.6	6	0.83	2.6	2	1.31	0.38	0.33	0.06	0.191	0.054	0.031	0.050	0.012	0.081	0.004
	WS 28	White Slip II	25	3.1	5.2	5.7	0.69	3.4	3.1	0.86	0.55	0.4	0.06	0.167	0.113	0.008	0.050	0.029	0.090	0.013
	WS 33	White Slip II	19.3	2.1	4.3	4.5	0.60	3.2	2.1	0.63	0.35	0.27	0.06	0.128	0.097	0.003	0.039	0.010	0.062	0.005
	WS 35	White Slip II	21.7	3.9	4	6.3	1.34	2.4	1.5	1.39	0.28	<DL	0.06	0.191	0.052	0.29	0.144	0.014	0.081	<DL
	WS 36	White Slip II	19.9	2.3	4.6	4.8	0.63	3.3	2.3	0.67	0.37	0.20	0.06	0.141	0.108	<DL	0.042	0.013	0.065	0.005
	WS 58	White Slip II	26	4.1	5.1	7.3	1.03	2.5	2.3	1.48	0.61	0.4	0.06	0.239	0.067	0.089	0.068	0.026	0.098	0.011
	WS 59	White Slip II	23.5	4.1	4.9	7.6	0.97	2.5	2.2	1.21	0.55	0.28	0.06	0.223	0.069	0.065	0.063	0.021	0.097	0.009
	WS 61	White Slip II	24.6	3.1	5.2	6	0.92	3.4	2.8	0.83	0.5	0.33	0.06	0.183	0.12	0.016	0.051	0.021	0.080	0.010
	WS 65	White Slip II	20.5	3.4	4.5	7.7	0.68	2.3	1.7	0.81	0.44	0.29	0.05	0.181	0.059	0.027	0.050	0.016	0.076	0.007
	WS 66	White Slip II	23.7	3.7	5	7.7	0.87	2.7	2.2	1.31	0.52	0.4	0.06	0.210	0.064	0.089	0.059	0.017	0.096	0.011
	WS 69	White Slip II	22.3	2.9	5	5.3	0.59	3.1	2.3	0.85	0.81	0.33	0.05	0.195	0.067	0.011	0.042	0.008	0.094	0.005
	WS 70	White Slip II	19.6	3.3	4	6.1	0.85	2.3	1.8	0.9	0.27	0.29	0.05	0.167	0.045	0.32	0.43	0.015	0.083	0.006
		Average	22	3.3	4.5	6.2	0.86	2.65	2.07	0.94	0.45	0.32	0.06	0.186	0.068	0.084	0.085	0.015	0.097	0.007
		Stand. Dev.	4	0.75	0.75	1.45	0.31	0.53	0.51	0.33	0.16	0.11	0.00	0.046	0.027	0.095	0.094	0.008	0.031	0.004
	Sanidha
	San 13	White Slip II late	24.3	3.6	5.1	6.8	1.28	3.3	2.8	0.56	0.54	0.29	0.06	0.232	0.15	0.030	0.047	0.014	0.094	0.006
	San 14	White Slip II late	23.1	3.1	5.2	6	0.74	2.4	2.4	0.66	0.35	<DL	0.06	0.185	0.14	0.022	0.049	0.013	0.103	0.009
	San 16	White Slip II	22.6	3.5	5.5	5.9	0.87	3.2	2.8	0.66	0.71	0.5	0.06	0.195	0.097	0.011	0.046	0.018	0.085	0.012
	San 18	White Slip II	23	3.3	5.3	5.7	0.64	3	2.4	1.04	0.84	0.22	0.06	0.225	0.064	0.011	0.044	0.019	0.11	0.007
	San 20	White Slip II	25	3.3	5.8	6.6	0.90	3.3	2.5	0.53	0.61	0.38	0.06	0.193	0.092	0.008	0.044	0.026	0.072	0.009
	San 23	White Slip II	23.5	3.7	5.4	6.1	0.95	3.2	2.6	0.6	0.52	0.32	0.06	0.196	0.15	0.036	0.056	0.032	0.068	0.011
	San 24	White Slip II	19.7	3.6	4.7	5.5	0.74	2.1	1.9	0.8	0.3	0.22	0.05	0.214	0.057	0.044	0.049	0.009	0.063	<DL

  and between 18.812 and 18.926 for 207 Pb/ 204 Pb and 206 Pb/ 204 Pb, respectively. The isotopic values of the bentonitic clay from the Kannaviou formation are 15.662 and 18.812. Values for the umbers and shales from the Perapedhi formation range between 15.592 and 15.629 and between 18.516 and 18.724, while values for the bentonitic clay of this formation are 15.665 and 18.834. Clays and rock from the Upper Cretaceous Volcanic sequence display values that range from 15.601 to 15.612 and from 18.829 to 18.904. Values for the sample derived from the weathering of the Upper Cretaceous Intrusive sequence are 15.640 and 19.274. The weathering products of the gabbros (Upper Cretaceous Plutonic sequence) have values that range from 15.573 to 15.713 and from 18.526 to 21.531. The values for the soil samples are between 15.593 and 15.684 and between 18.846 and 18.878, for 207 Pb/ 204 Pb and 206 Pb/ 204 Pb ratios, respectively. Finally, for sample C7 72a, a pure chlorite, the 207 Pb/ 204 Pb and 206 Pb/ 204 Pb ratios are 15.957 and 25.275.

  have already reported the greenschist facies mineralogy. These observations also agree well with the results

	0.009	0.017	0.006	0.009	0.004		<DL	0.009	0.014	0.012	<DL	0.017	0.012	0.008	0.01	0.006
	0.100	0.073	0.070	0.084	0.016		0.053	0.11	0.073	0.094	0.085	0.14	0.068	0.086	0.089	0.027
	0.022	0.019	0.016	0.019	0.007		0.005	0.039	0.022	0.017	0.015	0.019	0.013	0.012	0.018	0.010
	0.045	0.061	0.044	0.049	0.006		0.029	0.056	0.054	0.066	0.053	0.081	0.049	0.063	0.056	0.015
	0.018	0.052	0.034	0.027	0.015		0.013	0.045	0.007	0.083	0.066	0.101	0.157	0.077	0.069	0.049
	0.082	0.084	0.062	0.098	0.036		0.068	0.15	0.17	0.18	0.15	0.112	0.066	0.074	0.12	0.045
	0.215	0.202	0.208	0.207	0.0150		0.091	0.170	0.168	0.194	0.155	0.198	0.167	0.188	0.166	0.034
	0.06	0.05	0.05	0.06	0.00		0.06	0.06	0.06	0.08	0.06	0.06	0.06	0.06	0.06	0.01
	0.26	0.36	0.28	0.30	0.10		<DL	0.38	0.35	0.4	0.33	0.6	0.26	<DL	0.33	0.15
	0.69	0.3	0.31	0.52	0.20		0.2	0.35	0.46	0.36	0.3	0.24	0.23	0.28	0.30	0.08
	0.96	0.69	0.84	0.73	0.17		0.46	0.63	0.69	0.42	0.39	0.55	0.51	0.83	0.56	0.15
	2.4	2.6	2	2.44	0.30		1.8	3.3	2.9	2.8	2.4	3	2.1	3	2.67	0.52
	2.9	3	2.4	2.88	0.43		2.5	3.4	3.9	3	2.8	2	1.8	2.7	2.76	0.69
	0.68	0.96	0.79	0.86	0.184		0.45	0.86	1.01	0.82	0.66	0.78	0.62	0.75	0.74	0.171
	6.1	6.5	5.7	6.1	0.42		3.4	6.1	5.8	6	5.1	5.8	4.7	5.8	5.3	0.92
	5.4	6.3	4.7	5.3	0.48		3.3	5.1	4.9	4.8	4.1	4.8	4.3	5.4	4.6	0.66
	3.5	2.9	3.8	3.4	0.28		1.83	3.3	2.9	3	2.7	3.6	3	3.3	3	0.54
	22.9	24.2	21.7	23	1		16.6	25	25	22.4	18.3	23	16.9	23	21	4
	San 27 White Slip II	San 28 White Slip II	San 29 White Slip II	Average	Stand. Dev.	Minet el-Beida	MeB 2 White Slip II	MeB 3 White Slip II	MeB 4 White Slip II	MeB 5 White Slip II	MeB 6 White Slip II	MeB 10 White Slip II late	MeB 16 White Slip II late	MeB 17 White Slip II late	Average	Stand. Dev.

of petrographic analysis of Sanidha sherds made by Xenophontos

Table 4

 4 Lead isotope ratios of Sanidha and Minet el-Beida sherds. 2se refers to 2 standard errors (internal error).

	Sample		208 Pb/ 204 Pb	2se	207 Pb/ 204 Pb	2se	206 Pb/ 204 Pb	2se
	Sanidha
	San 1	Coarse Monochrome	39.0148	0.0030	15.6773	0.0011	18.9568	0.0013
	San 2	Coarse Monochrome	39.0212	0.0017	15.6814	0.0006	18.9511	0.0007
	San 3	Coarse Monochrome	39.0176	0.0020	15.6864	0.0007	18.9453	0.0008
	San 4	Coarse Monochrome	39.0160	0.0023	15.6860	0.0008	18.9396	0.0008
	San 5	Monochrome	39.0164	0.0022	15.6792	0.0008	18.9330	0.0008
	San 6	Monochrome	39.0239	0.0020	15.6810	0.0007	18.9368	0.0007
	San 7	Monochrome	39.0232	0.0020	15.6842	0.0006	18.9538	0.0006
	San 8	Monochrome	39.0050	0.0025	15.6823	0.0008	18.9132	0.0008
	San 9	Monochrome	38.9323	0.0024	15.6714	0.0008	18.8718	0.0009
	San 10	Monochrome	39.0012	0.0023	15.6798	0.0008	18.9234	0.0008
	San 11	Monochrome	38.9278	0.0019	15.6725	0.0006	18.8610	0.0006
	San 12	White Slip II late	39.0301	0.0018	15.6850	0.0006	18.9354	0.0006
	San 13	White Slip II late	39.0718	0.0025	15.6846	0.0009	18.9450	0.0009
	San 14	White Slip II late	39.0252	0.0025	15.6813	0.0009	18.9351	0.0010
	San 15	White Slip II	39.0149	0.0027	15.6786	0.0010	18.9444	0.0010
	San 16	White Slip II	39.0393	0.0024	15.6821	0.0008	18.9381	0.0009
	San 17	White Slip II	39.0362	0.0021	15.6835	0.0007	18.9440	0.0008
	San 18	White Slip II	39.0298	0.0021	15.6831	0.0007	18.9761	0.0008
	San 19	White Slip II	39.0336	0.0024	15.6808	0.0008	18.9288	0.0009
	San 20	White Slip II	39.0673	0.0027	15.6827	0.0009	18.9359	0.0009
	San 21	White Slip II	39.0553	0.0027	15.6843	0.0009	18.9455	0.0009
	San 22	White Slip II	39.0449	0.0028	15.6839	0.0010	18.9257	0.0010
	San 23	White Slip II	39.0180		15.6798		18.8981
	San 24	White Slip II	38.9579	0.0027	15.6743	0.0009	18.8529	0.0009
	San 25	White Slip II	39.0490	0.0025	15.6816	0.0008	18.9473	0.0009
	San 26	White Slip II	39.0733		15.6850		18.9588
	San 27	White Slip II	39.0338	0.0025	15.6830	0.0008	18.9591	0.0008
	San 28	White Slip II	39.0395	0.0019	15.7039	0.0006	18.9772	0.0007
	San 28 *		39.0443	0.0030	15.7039	0.0011	18.9788	0.0011
	San 29	White Slip II	39.0729	0.0028	15.6811	0.0010	18.9302	0.0009
	San 30	White Slip II	39.0414	0.0024	15.6844	0.0008	18.9449	0.0008
	Minet el-Beida
	MeB 2	White Slip II	38.9999	0.0024	15.6818	0.0008	18.9142	0.0010
	MeB 3	White Slip II	39.0006	0.0026	15.6827	0.0009	18.9199	0.0009
	MeB 4	White Slip II	39.0111	0.0024	15.6817	0.0009	18.9105	0.0010
	MeB 5	White Slip II	38.9516	0.0019	15.6813	0.0008	18.8769	0.0010
	MeB 5 *		38.9508	0.0023	15.6809	0.0009	18.8758	0.0010
	MeB 6	White Slip II	38.9589	0.0032	15.6830	0.0012	18.8845	0.0013
	MeB 9	White Slip II late	38.9766	0.0023	15.6838	0.0008	18.8976	0.0008
	MeB 9 **		38.9768	0.0020	15.6843	0.0007	18.8979	0.0008
	MeB 10	White Slip II late	38.9859	0.0024	15.6897	0.0009	18.9188	0.0013
	MeB 11	White Slip II late	38.9746	0.0027	15.6844	0.0010	18.8936	0.0011
	MeB 15	White Slip II late	38.9938	0.0032	15.6922	0.0012	18.9162	0.0013
	MeB 16	White Slip II late	39.0331	0.0025	15.6972	0.0009	18.9607	0.0011
	MeB 17	White Slip II late	38.9563	0.0021	15.6836	0.0007	18.8723	0.0009

Table 5

 5 Lead isotope ratios and coordinates of clay samples. 2se refers to 2 standard errors (internal error). UC for Upper Cretaceous. Values in italics refer to data previously published in[START_REF] Renson | Lead isotopic analysis for the identification of Late Bronze Age pottery from Hala Sultan Tekke (Cyprus)[END_REF].

	Sample		Geological unit/formation	208 Pb/ 204 Pb	2se	207 Pb/ 204 Pb	2se	206 Pb/ 204 Pb	2se	Lat. N	Long. E
	C7 63	Clay	UC Moni form.	39.0638	0.0025	15.6812	0.0009	18.9258	0.0011	34°44 0 23.94 00	33°13 0 51.24 00
	C8 34	Clay	UC Moni form.	38.8761	0.0010	15.6658	0.0004	18.8476	0.0004	34°44 0 35.52 00	33°07 0 42.36 00
	C8 35a	Clay	UC Moni form.	38.9315	0.0011	15.6840	0.0004	18.8249	0.0005	34°44 0 15.24 00	33°07 0 41.64 00
	C8 35a *	Clay	UC Moni form.	38.9326	0.0010	15.6842	0.0004	18.8254	0.0004	34°44 0 15.24 00	33°07 0 41.64 00
	C8 35a **	Clay	UC Moni form.	38.9308	0.0010	15.6840	0.0004	18.8247	0.0004	34°44 0 15.24 00	33°07 0 41.64 00
	C8 35a **	Clay	UC Moni form.	38.9293	0.0011	15.6837	0.0004	18.8249	0.0005	34°44 0 15.24 00	33°07 0 41.64 00
	C8 35b	Clay	UC Moni form.	38.9858	0.0009	15.6890	0.0003	18.8139	0.0004	34°44 0 15.24 00	33°07 0 41.64 00
	C9 34	Clay	UC Moni form.	38.9214	0.0028	15.6787	0.0012	18.8780	0.0012	/	/
	C9 36	Clay	UC Moni form.	38.9713	0.0022	15.6871	0.0007	18.8116	0.0009	34°43 0 39.80 00	33°10 0 04.50 00
	KKP 204	Clay	UC Kannaviou form.	38.8453	0.0028	15.6615	0.0010	18.8118	0.0011	/	/
	C8 63a	Umber	UC Perapedhi form.	38.7387	0.0011	15.6292	0.0004	18.7241	0.0005	34°48 0 0.42 00	33°16 0 47.28 00
	C8 63b	Shale	UC Perapedhi form.	38.6792	0.0011	15.6160	0.0004	18.6610	0.0005	34°48 0 0.42 00	33°16 0 47.28 00
	C8 76a	Umber	UC Perapedhi form.	38.6417	0.0011	15.6123	0.0004	18.6368	0.0005	34°46 0 32.46 00	33°15 0 41.10 00
	C8 76b	Shale	UC Perapedhi form.	38.5202	0.0010	15.5918	0.0004	18.5157	0.0004	34°46 0 32.46 00	33°15 0 41.10 00
	KKP 202	Bentonitic clay	UC Perapedhi form.	38.8649	0.0023	15.6645	0.0009	18.8340	0.0010	/	/
	KKP 202 **	Bentonitic clay	UC Perapedhi form.	38.8616	0.0030	15.6641	0.0013	18.8332	0.0014	/	/
	C7 O 2 Alt	Clay	UC Volcanic seq.	38.9039	0.0043	15.6007	0.0012	18.8910	0.0014	34°55 0 38.46 00	33°23 0 34.74 00
	C7 O 2 Alt *	Clay	UC Volcanic seq.	38.9193	0.0031	15.6022	0.0012	18.9042	0.0014	34°55 0 38.46 00	33°23 0 34.74 00
	C7 O 2 Rock	Rock	UC Volcanic seq.	38.9415	0.0052	15.6065	0.0021	18.8841	0.0023	34°55 0 38.46 00	33°23 0 34.74 00
	C7 O 12	Clay	UC Volcanic seq.	38.8791	0.0018	15.6124	0.0007	18.8294	0.0008	34°55 0 47.94 00	33°23 0 48.36 00
	C8 11	Clay	UC Intrusive seq.	38.9618	0.0018	15.6401	0.0007	19.2742	0.0011	34°47 0 30.00 00	33°13 0 56.40 00
	KKP201	Weather. gabbro	UC Plutonic seq.	38.9673	0.0016	15.6799	0.0005	18.9096	0.0006	/	/
	KKP201 **	Weather. gabbro	UC Plutonic seq.	38.9662	0.0021	15.6794	0.0008	18.9097	0.0010	/	/
	C8 7	Weather. gabbro	UC Plutonic seq.	38.7954	0.0030	15.6013	0.0012	18.9580	0.0012	34°48 0 45.84 00	33°11 0 56.16 00
	C8 8a	Weather. gabbro	UC Plutonic seq.	38.8224	0.0022	15.5780	0.0008	19.0510	0.0009	34°48 0 43.38 00	33°11 0 54.24 00
	C8 8b	Weather. gabbro	UC Plutonic seq.	38.9820	0.0019	15.6735	0.0007	18.8984	0.0008	34°48 0 43.38 00	33°11 0 54.24 00
	C8 9b	Weather. gabbro	UC Plutonic seq.	40.2163	0.0044	15.7128	0.0015	21.5311	0.0019	34°48 0 35.52 00	33°11 0 44.64 00
	C8 70	Weather. gabbro	UC Plutonic seq.	38.7284	0.0024	15.5725	0.0007	18.8886	0.0010	34°48 0 44.70 00	33°09 0 14.16 00
	C8 71	Weather. gabbro	UC Plutonic seq.	39.4792	0.0083	15.6901	0.0032	19.6286	0.0041	34°48 0 44.70 00	33°09 0 14.16 00
	C8 71 *	Weather. gabbro	UC Plutonic seq.	39.4858	0.0072	15.6892	0.0021	19.6233	0.0033	34°48 0 44.70 00	33°09 0 14.16 00
	C9 49	Weather. gabbro	UC Plutonic seq.	38.4291	0.0019	15.6108	0.0010	18.5162	0.0008	34°48 0 45.80 00	33°11 0 55.30 00
	C7 72a	Clay	UC Plutonic seq.	40.6408	0.0049	15.9574	0.0019	25.2754	0.0029	34°48 0 26.40 00	33°11 0 20.64 00
	C8 69a	Soil		38.9611	0.0012	15.6529	0.0004	18.8775	0.0005	34°51 0 16.14 00	33°12 0 29.10 00
	C9 40	Soil		38.6932	0.0020	15.5926	0.0008	18.8698	0.0009	34°47 0 49.00 00	33°16 0 45.40 00
	C9 42	Soil		38.8036	0.0026	15.6278	0.0010	18.8457	0.0011	34°48 0 10.30 00	33°16 0 46.40 00
	C9 44	Soil		38.9487	0.0027	15.6838	0.0012	18.8591	0.0011	34°48 0 58.40 00	33°12 0 04.10 00

Acknowledgements

This study is supported by the Research Foundation Flanders (FWO Grants KN137 to Karin Nys and G.0585.06 to Philippe Claeys and Frank Vanhaecke) and the Research Council of the Vrije Universiteit Brussel (Grant HOA11 to Karin Nys and Philippe Claeys). The WD-XRF acquisition, set-up and optimisation, was made possible through a research grant from the Kempe Foundation to Richard Bindler, which also provided a post doc fellowship to F.D.V. Additional support was provided by the Swedish Research Council (grant to Richard Bindler). We warmly thank the Musée d'Archéologie Nationale de Saint-Germain-en-Laye for allowing the sampling of material from Ugarit and for providing room in the laboratory during the sampling. We are grateful to Alison South and Ian Todd for providing pottery samples from Sanidha and to the late Professor Paul Åström for the White Slip sherds from Hala Sultan Tekke. Thank you to Claude Maerschalk, Jeroen De Jonge and Vinciane Debaille from Université Libre de Bruxelles and Kris Latruwe from University of Gent for their help during the laboratory work and the measurements at the MC-ICP-MS, to Nathalie Fagel (University of Liège) for spending time on some XRD spectra interpretation, to Oscar Steenhaut (Vrije Universiteit Brussel) for his assistance during the measurements on the SEM-EDX and to