## 6 Discussion
The paleomagnetic mapping contributed to the finding of an ophiolite complex in the southern framing of the EMM, an area topologically replaced by the MTB in the southern margin of the Neotethys Ocean. The 3D magnetic field modeling [21] indicates that the thickness of the ophiolite complex to the south of the Makhtesh Ramon area reaches 500 m (Figure 11B). The paleomagnetic data studies in the Carmel area (22A) made it possible to show in a new way that the Triassic-Jurassic ophiolite complex underlying the Aptian-Albian traps of the Mt. Carmel within the Galilea-Lebanon terrane contrasts sharply with the Mesozoic and sedimentary rocks penetrated by traps. These traps' regional Late Jurassic-Neocomian age precedes the Late Jurassic-Neocomian phase of joining the MTB to the Gondwana. The paleomagnetic analysis of the oceanic crust of the EMM, where the oldest Kiama hyperzone of inverse polarity was identified [21; 22], was cartographically implemented (Figure 17). The map development was based mainly on the correlation with the ophiolites of the neighboring areas of the Galilea-Antilebanon terrane, with the ophiolite platesof the Illawarra, Omolon, and Gissar superzones immediately following in the general paleomagnetic scale after the Kiama superzone. Such an ancient crust has an allochthonous origin, which is evident due to (1) the presence of the Cretaceous ophiolites dominating in the Alpine belt of this junction of Eurasia and Gondwana, and (2) the development of the Noetethys oceanic crust in the very Late Paleozoic (Kiama paleomagnetic chron) to the east of the studied region. These studies open new aspects of the development of the terrane belts in plate tectonics, where both the continental and oceanic terranes are present. During paleomagnetic mapping, we revealed the phenomenon of changing the strike of magnetoactive bodies of different ages. These bodies represent single linearly oriented structures, i.e., sills, dikes, and their swarms, and larger zones of coeval trap formation. A difference in the strike of dikes of different ages was revealed in the Antilebanon terrane near Hermon Mt. (Figure 21B) and in the south of the Negev terrane, the Makhtesh Ramon subterrane (Figure 23B). A common feature for both regions is that the older dikes of intrusive traps extend submeridionally. In comparison, the younger dikes extend sublatitudinally, thus fixing the rotation of the terranes counterclockwise by more than 90\({}^{\circ}\). In Carmel and Galilee, in the junction zone of the Galilee-Lebanon, Antilebanon, Judea-Samaria, and Pleshet terranes (see Figure 1), a rotation of the magnetization zones of the Early, Late Cretaceous, and Late Cenozoic was revealed (Figure 22A). In general, the older traps of the Hissar and Halal-1 superzones of the Late Jurassic-Early Cretaceous extend in the NNE-SW direction, while the younger Halal-2 traps of the Late Cretaceous extend in the direction of NE-SSE. The youngest traps of the Sogdiana-2 zone of the late Cenozoic extend in the direction WNW-ESE, as well as the largest trap zone in the Eastern Mediterranean, Harrat Ash Shaam, to which it belongs. The final moment of the regional paleomagnetic mapping of the Carmel-Galilee region is the fact that from the Early Cretaceous to the Late Cenozoic, this vast zone of the Mesozoic terrane belt was rotated for about 140 Ma by at least 90\({}^{\circ}\) counterclockwise. According to the paleomagnetic mapping, the Cenozoic stage of development in the region observes contrast in terms of discordance of the paleomagnetic structures of the Mesozoic and Cenozoic. This discordance was explained in the light of the latest combined geodynamic studies [14], according to which the axis of the deep mantle structure in the middle of the Cenozoic began to turn more intensively in the counterclockwise direction, which caused the lithospheric plate disruption development, and the formation of the topologically displaced zones of the dike complexes and younger effusive traps.