## 3 Findings
### Geochemistry
The REE distributions of these serpentinites, which are rich in trace elements (U, K, Cs, Rb), are compatible with the characteristics of subduction zone serpentinites (\(\sim\)100 PM; Figure 4). In addition, serpentinites can be divided into abyssal, mantle wedge and subduction zone according to their formation environments. The amount of Ti is an important indicator for determining the protoliths of serpentinites. Another feature of subduction-zone serpentinites is high Ti (30-500 ppm), Yb (0.02-1 ppm) and Mg (\(>\)0.4 ppm) values [34,35]. These features are compatible with the analyzed Elazg serpentinites (Ti 30-66 ppm, Yb 0.1-0.3 ppm, Mg 0.70-0.83 ppm) (Table 1). LREE enrichment indicates that the serpentinites did not undergo partial melting but were formed by melt/rock interaction, and/or were enriched in the subduction zone by fluids during hydration [5,41,42,43,44,45,46,47,48]. At the same time, these serpentinites were rich in Pb. The fact that this feature, described by [PERSON] [49] in mantle wedge serpentinites  
Figure 4: Chondrite (**a**) and primitive mantle spider (**b**) diagrams of serpentinites [41]. and Tonga fore-arc peridotites, is also observed in subduction serpentinites shows that it originates from depleted basaltic magma, as well as abyssal and mantle wedge peridotites. Rock interactions led to a strong enrichment in U. Most of our examples indicated similar behaviors. In geology, chromatographic processes generally concern the separation and analysis of minerals and elements. This process, which is a laboratory technique, is used in the analysis of geological samples. It is important for the separation and analysis of minerals and elements, and the detection of contamination. The percolation of silicate melts through mantle peridotite, whether by reactive porous flow or the chromatographic process (fractionation), results in the enrichment of light rare earth elements (LREE), as well as incompatible elements such as Th and U [38]. Considering the incompatible elements, it can be said that the melt/rock interaction occurring before serpentinization affects the geochemical composition of serpentinites. Trace element enrichments probably originate from the passive continental margin [34]. This is because, at both passive margins, there are high incompatible trace element concentrations due to fluid remixing and smaller partial melting via metasomatizing melts before serpentinization [39; 50]. The MgO-SiO\({}_{2}\), MgO-Fe\({}_{2}\)O\({}_{3}\) and Ni-Ce diagrams show that the serpentinites examined are lizardite and chrysotile, and that these minerals are accompanied by talc (Figure 5). The serpentinites showed a mineral assemblage of olivine, chrysotil, lizardite, magnetite, brucite, chlorite, talc and carbonate. In the primitive mantle normalized trace element variation diagrams for forearc and MOR serpentinites, enrichments in U, Sb, Rb, Pb, Sr and Li, compared to elements with similar compatibility, characterize subduction zone serpentinites (Figure 4). Strong enrichments in large ion lithophile elements (LILE), especially Cs and Rb (Figure 4), are also similar to what is found in forearc serpentinites. At the same time, trace element patterns normalized to the flat primitive mantle with positive U, Rb, Sm and Ti anomalies indicate the interference of fluids in the subduction zone and forearc region (Figure 4b). Also, some MOR serpentinites show a positive Eu anomaly EuN/EuN* (0\(\cdot\)65\({}^{\circ}\)\(\times\) 9). However, most of the incompatible trace elements (Nb, Th and Ce) are present in extremely low amounts [36]. The compositional values of serpentinites depend on their characteristics, as shown in the literature [35; 36; 37; 38; 39; 40; 51] (Figure 5).