## 5 Results  
### Mineral Chemistry  
Electron microprobe analysis (EMPA) results of the examined olivine are listed in Table 1. They contain forsterite (Fo = 100 Mg/Mg + Fe) ranges from 91.94 to 98.13, with a mean value of 95.23 mol%. The Fo content of the examined olivine is higher than those reported in [21] (88-92 mol%), and similar to those of Egyptian ophiolitic peridotites (89-96 mol%) [22]. Moreover, they possess NiO and MnO contents (0.28-0.92; 0.087-0.92 wt.%) similar to olivine mantle array (plot in and close to mantle array field; Figure 4a). Unfortunately, pyroxene minerals are observed only in serpentine periodtites. Orthopyroxenes are typically enstatite (Supplementary Materials, Table S1), whilst clinopyroxenes (Supplementary Materials Table S2) are classified as augites based on nomenclature [23] (Figure 4b). Orthopyroxenes contain (En 89.65-93.18, Fs 6.13-9.23, Wo 0.59-2.62) and Mg# ranges from 89.65 to 93.18, with a mean value of 91.03, and low contents of Al\({}_{2}\)O\({}_{3}\) and TiO\({}_{2}\) (1.22-3.23; 0.01-0.04, respectively), similar to forearc periodicites [24]. Clinopyroxenes (En\({}_{49.89-61.71}\), Fs\({}_{1.94-5.33}\), Wo\({}_{34.89-46}\)) contain CaO ranges from 17.87 to 23.14 wt.% and low TiO\({}_{2}\) contents (0.02-0.08 wt.%), reflecting their non-alkaline affinity [25]; in addition, they have Al\({}_{2}\)O\({}_{3}\) contents of more than 1 wt.%, suggesting their magmatic affinity [26]. Orthopyroxenes and clinopyroxenes have Cr\({}_{2}\)O\({}_{3}\) less than 1 wt.%, similar to those in forearc  
\begin{table}
\begin{tabular}{l c c c c c c c c c c c c c c c c c c c} \hline \multicolumn{11}{c}{**Soperpentientized Periodicites**} \\ \hline
**No. ** & **1** & **2** & **3** & **4** & **5** & **6** & **7** & **8** & **9** & **10** & **  
Spinel is predominantly composed of opaque minerals, and reveals heterogeneities composition; it can be distinguished into Cr-spinel (Supplementary Materials, Table S3) and Al-spinel (Supplementary Materials, Table S4). Al-spinel is found in the picotitic field, whilst Cr-spinel straddles the chromite field, and both are related to ophiolitic spinels [29; 30] (Figure 5a). Furthermore, Cr-spinel can be classified into chromite and magneschormite, whereas Al-spinel is classified as spinel according to the Cr# versus Mg# binary discrimination diagram [31] (Figure 5b). Al-spinels contain high contents of Al\({}_{2}\)O\({}_{3}\) (33.55-38.55, av. 35.77 wt.%), MgO (12.37-16.12 av. 14.84 wt.%), and Mg# (Mg/Mg+Fe\({}^{2+}\)) (0.55-0.69, av. 0.64 wt.%), and low contents of FeO (11.98-20.16, av. 16.66 wt.%), Cr\({}_{2}\)O\({}_{3}\) (28.48-34.17, av. 31.46 wt.%), and Cr# (Cr/(Cr+Al) (0.34-0.39; av. 0.37), compared to those of Cr-spinel. In addition, they are found in the mantle array field, suggesting their magmatic nature (Figure 5c). The Cr# contents of Cr-spinel are similar to those of the Egyptian Eastern Desert [32]. Cr-spinels contain YCr (Cr/(Cr+Al+Fe\({}^{+3}\)), YAl (Al/(Al+Cr+Fe\({}^{+3}\)) and YFe\({}^{+3}\) (Fe\({}^{+3}\)/(Fe\({}^{+3}\)+Al+Cr), similar to forearc peridotites [32], whilst the contents of Al-spinel are similar to those of abyssal peridotites, which may be formed during inanition of subduction processes in proto-forearc environments (Figure 5d). Figure 4: (**a**) Fo vs. NiO binary variation of olivines. Fields of olivine mantle array [27], ophiolite [22], forearc peridotite (FAP) [24], and layered intrusions [7]. (**b**) Enstatite (En)–ferrosilite (Fs)–wollastonite (Wo) nomenclature diagram of pyroxene minerals [23]. (**c**) Na\({}_{2}\)O vs. Al\({}_{2}\)O\({}_{3}\) and (**d**) Cr\({}_{2}\)O\({}_{3}\) vs. Al\({}_{2}\)O\({}_{3}\) binary diagrams [24]. Field of forearc peridotite (FAP) and abyssal basin peridotite (ABP) obtained from [24], and back-arc peridotite (BAP) [28]. EPMA results of serpentine minerals are shown in the Supplementary Materials (Table S5).