## 7 Discussion  
### Geotectonic Setting, Structural Control, and Magma Emplacement  
The magmatic complex at Vathi was emplaced during post-subduction tectonic extension. During the Miocene, several deep to shallow subvolcanic stocks, plugs, and dikes, which vary from intermediate to felsic compositions, intruded the metamorphic basement rocks in the Vathi area [16; 45]. Their emplacement was controlled by regional structures  
\begin{table}
\begin{tabular}{c c c c c c c} \hline \hline
**Sample** & **Vein Type** & **FI * Types** & **Th (\({}^{\circ}\)C)** & **Tm (ice) (\({}^{\circ}\)C)** & **Tm (NaCl)** & **Tm (KCI)** & **Salinity (wt \% NaCl** equiv *)** \\ \hline Vath 40 & Porphyr & 2 (L+V+H\(\rightarrow\)L) & 320 to \(>\)600 & - & 253–401 & 105–125 (\(n=2\)) & 34.6–47.2 \\  & A-type vein & 3 (L+V\(\rightarrow\)V) & 335–515 & \(-\)13.4—7.2 (\(n=23\)) & & 10.7–17.4 \\ \hline Vath 31c & Porphyr & 2 (L+V+H\(\rightarrow\)L) & 324–\(>\)600 & - & 220–374 & 112 (\(n=19\)) & 32.7–44.3 \\  & A-type vein & 3 (L+V\(\rightarrow\)V) & 405 to \(>\)600 & \(-\)14.1—6.4 (\(n=2\)) & - & - & 9.7–18.5 \\ \hline Vath 12a & Hydrothermal quartz in latite & 1 (L+V\(\rightarrow\)L) & 311–392 (\(n=7\)) & \(-\)7.6—5.4 (\(n=5\)) & - & - & 8.4–11.2 \\ \hline Vath 41 & Epithelial E-type vein & 1 (L+V\(\rightarrow\)L) & 205–255 (\(n=8\)) & \(-\)1.5—0.9 (\(n=3\)) & - & - & 1.6–2.6 \\ \hline Vath 42 & Epithelial E-type vein & 1 (L+V\(\rightarrow\)L) & 212–259 (\(n=5\)) & \(-\)1.7—0.8 (\(n=5\)) & - & - & 1.4–2.9 \\ \hline Vath 33 & Epithelial Catclasite & 1 (L+V\(\rightarrow\)L) & 211–251 (\(n=9\)) & \(-\)1.6—0.9 (\(n=9\)) & - & - & 1.6–2.7 \\ \hline \hline \end{tabular}  
* FI = fluid inclusion, L = liquid phase, V = vapor phase, H = halite, equiv = equivalent, \(n=\) number of microthermometric analyses.  
\end{table}
Table 3: Microthermometric data of the fluid inclusions in quartz of the A-type porphyry veins and the E-type epithermal veins from Vathi.  
Figure 18: Homogenization temperatures of the fluid inclusions from the A- and E-type veins at Vathi.  
including E-W, NW-SE, and NE-SW trending faults, which also favored the formation of the porphyry-style mineralization by localizing the magmatic-hydrothermal fluid circulation (Figure 3; inset map).  
The mineralization at Vathi is mainly hosted in latite, but it is genetically related to quartz monzonite, which intruded the older latite and the crystalline rocks of the Vertiskos Unit. The subvolcanic intrusion formed between 18 \(\pm\) 0.5 and 17 \(\pm\) 1 Ma, based on U-Pb zircon ages of Frei [16]. The microgranular and porphyritic texture and the elongate shape of the ore-related quartz monzonite are ascribed to fast ascending magma and subsequent crystallization at shallow depths set in an extensional regime. [PERSON] et al. [34] describe a similar mechanism for the origin of microgranite porphyry associated with the Maronia Cu-Mo deposit, NE Greece.  
The presence of the phreatic breccia intruding the latite at Ragain 1 Hill, its ESE-WNW orientation, and the minor presence of quartz monzonite fragments suggest that quartz monzonite intruded the latite. This breccia was possibly formed when magmatic fluids were mixed with surface meteoric water during the late stages of the quartz monzonite intrusion, at the upper and marginal parts of the porphyry system [50; 56].