## 2 Geological Setting  
The Serbo-Macedonian Massif (SMM) in Greece is represented by the Vertiskos Unit that is composed of the following: (i) a sequence of migmatities, engisses, schists, and thin marble intercalations, and (ii) a sequence of metagabbros, metadiabases, and amphibolites, intercalated with engisses [17; 21; 22; 23; 24]. Mafic to ultramafic rocks which belong  
Figure 3: (**a**) Geological map of the Vathi porphyry system. The locations of the legacy drill holes are also shown. Inset map shows the location of the Vathi magmatic rocks in respect to local geological settings; (**b**) Schematic cross-section A-A’ of Ragan 1 Hill, defined by Institute of Geology and Mineral Exploration (IGME) drillings and drill core interpretation. Drill holes D2 and D3 were inclined; (**c**) Schematic cross-section B-B’ of Ragan 1 Hill. Interpretation was based on field mapping held during this study and on observations made by [PERSON] (1968) and [PERSON] (1970). to the Thermes-Volvi-Gomati complex, are tectonically emplaced in these sequences [25] (Figure 1). [PERSON] et al. [26] describes three pre-Alpine pulses and one Cenozoic magmatic pulse related to the igneous evolution of the Vertiskos Unit. Neoproterozoic and middle Or-dovician granitoids metamorphosed into orthogneisses, and A-type granites (so-called Arnea-type granites) characterize the pre-Alpine igneous evolution [22]. The Cenozoic magmatism is subdivided into four magmatic events [16,22,26] (Figure 1). These magmatic events include I-type plutonic rocks, and related subvolcanic and volcanic rocks with calc-alkaline to high K-calc-alkaline and shoshonitic affinities, which intruded the SMM and the neighboring Rhodope Massif mainly as late-stage intrusions [27, 28, 29]. The first Cenozoic magmatic event (Early to Middle Eocene) is characterized by intrusions unrelated to metallic mineralization [16,20,28,29,30]. The second event formed during the Oligocene, and it is associated with mineralized intrusions. During this event, calc-alkaline magmatism was produced following an E-W trend [29] (Figure 1). The third event started in the Early Miocene (22-17 Ma) and is characterized by the intrusion of several subvolcanic rocks that host porphyry-style mineralization (e.g., Vathi, Gerakario, Skouries, and Fisoka) [16,20,31]. The last magmatic event (Pliocene to Pleistocene) is not related to mineralized intrusions and it is mostly restricted to the Strymoniko hryolitic dome [19]. The rocks of the Vertiskos Unit were affected by two metamorphic events: (i) a Cretaceous amphibitic facies and (ii) a Cretaceous to Early Paleogene event related to local retrograde greenschist facies [17,22]. Two extensional events were reported by [PERSON] et al. [21]. The oldest is contemporaneous with the Cretaceous amphibite facies metamorphic event and exhibits an ENE-WSW extensional trend and eastward-trending shears. The youngest extensional event occurred during the Late Cretaceous and Middle Eocene (68.5 \(\pm\) 3.8 to 46.6 \(\pm\) 3.6 Ma) and continued through to the Miocene [21,32,33]. The faults of this event structurally controlled the intrusions related to the second and the third Cenozoic magmatic events [19,20]. Oligocene-Miocene Ore Deposits and Prospects of the Serbo-Macedonian Metallogenic Province (SMMP) in Greece  
The SMMP and Rhodope metallogenic provinces contain several ore deposits and prospects of Cenozoic age [5,6,8,34,35,36,37,34]. According to [PERSON] et al. [19], 48 ore deposits (e.g., porphyry, epithermal and replacement types) occur in the Vertiskos Unit and the adjacent Kerdylion Unit that are genetically associated with the Oligocene-Miocene magmatism (Figure 2). These deposits and prospects occur mainly in the Kilks ore district to the north and in the Kassandra district (NE Chalkidiki) to the south [6,19,20,38,39]. The Kilks district hosts porphyry (e.g., Pontokerasia, Vathi, Gerakario), skarn/carbonate replacement (e.g., East and West Myriofyto), and epithermal-type (Rodemas) mineralization (Figure 2).