## 4 Discussion and Conclusions  
Residual mantle peridotites or ultramafic cumulates protooliths serpentinites is located in orogenic zones. These serpentinites consist of abyssal periodtites and mantle wedge periodtites; the protoolith of Guleman serpentinites contains traces of primary orthopyroxene and olivine [45]. These residual minerals (olivine and orthopyroxene in Figure 3) indicate that the protooliths of the serpentinites were mantle peridotite dunite or harzburgite. Serpentine group minerals are formed by the hydration of silica poor olivine/pyroxene minerals at relatively low temperatures. Figure 8: Whole-rock X-Ray diffraction (XRD) spectra of selected samples. Figure 7: SEM images of the serpentinite samples. (**a**) Sample 2, (**b**) Sample 5, (**c**) Sample 6. In serpentinites, there is a linear relationship between alteration mineralogy and texture. One of the specific features demonstrating this relationship is the bastite texture (in harzburgite) formed by the serpentinization of orthopyroxene [46]. Another feature is the lizardite vein networks with relict olivine cores, which are also observed in the Gulleman serpentinites (Figure 3). When examining the results of whole-rock analyses presented in Table 1, the LOI (loss on ignition; wt.%) values of the serpentine samples range from 8% to 11% (Sp1-Sp9), indicating a high degree of serpentinization, which is consistent with the observed excessive serpentinization and the presence of mesh texture (Table 1, Figure 3). Gulleman serpentinites are refractory serpentinites; high MgO (usually >35 wt.%; Table 1), high Mg# (78-82), low Al\({}_{2}\)O\({}_{3}\)/SiO\({}_{2}\) (<0.01) and high MgO/SiO\({}_{2}\) (0.6-0.95) show that it is high. Major element compositions show that the examined serpentinites are similar to the major element compositions of forearm/mantle wedge serpentinites and abyssal plate serpentinites, except for their refractory properties [54], because abyssal plate serpentinites exhibit higher FeO, lower SiO\({}_{2}\), MgO and Al\({}_{2}\)O\({}_{3}\) contents compared to forearc/mantle wedge serpentinites. According to studies [5; 6; 7; 8; 9; 10; 26], a high MgO value indicates lizardite, while chrysotile develops along the cracks. In a geological environment, Mg/Si varies between 1.18 and 1.38 (-1.33 ppm), the Mg# [Mg/(Mg + Fe)] values vary around 78-82, and the Ti value is >100 ppm, indicating the presence of subduction-zone serpentinites [30]. The \(\Sigma\)REE values in the analyzed serpentinites are 1-44 ppm, while the \(\Sigma\)LREE values are 0.8-6.22 ppm and \(\Sigma\)HREE values are 0.6-38 ppm. The \(\Sigma\)LREE/\(\Sigma\)HREE ratios are 0.16-4 ppm. Additionally, the negative Ce anomaly (0.1-12 ppm) and the weakly positive Eu anomaly (0.1-0.3 ppm) are caused by the interaction between fluids and rock. Highly incompatible elements are an indication of fluid integration into the system during subduction [23]. In particular, elements such as U, K, Cs, and Rb are highly present in these serpentinites (-100 PM). The \(\Sigma\)REE values of the samples are between 1-44, the \(\Sigma\)LREE value is between 0.8-6.22, and the \(\Sigma\)HREE contents are between 0.6-38. The \(\Sigma\)LREE/\(\Sigma\)HREE ratios are 0.16-4 and high Ce (0.1-12) shows a weakly positive Eu anomaly (0.1-0.3). These features indicate fluid intrusion into the rock structure during serpentinization, during which highly incompatible elements (HIEs) are gradually introduced into the serpentinization process. Additionally, as regards LREE enrichment, it was found that serpentinites do not undergo partial melting and structural changes with melt/rock interactions, and that the Pb content is high in serpentinites exhibiting this feature. All data show that the compositions of the examined samples are quite similar to the compositions of the mantle wedge/back rocks, but are contaminated by subduction components.