## 5 Paleomagnetic Mapping
### Paleomagnetic Mapping in Northern Israel
#### 5.1.4 Carmel Paleomagnetic Map  
The Mt. Carmel structure (see its location in Figure 3) differs from other coastal plain structures of the EMM by the essential tectonic amplitudes, vast development of magmatic formations (from Mesozoic to Cenozoic), geomorphological characteristics, high gravity-magnetic field gradients, and significant intensity of the seismic events [21]. Paleoteconically, the Carmel structure is located at the boundary between the Judea-Samaria and Galilee-Lebanon terranes [6]. The recent analysis indicates that this boundary is displaced a few km south of the Atlit fault branch zone (Figure 22A). Neotectonically, this boundary coincides with the seismic activity zone within the Yagur fault branch system. The boundary continues onshore and divides the area into the northern and southern sectors [102]. The Carmel tectonic node is crucial in estimating the space interaction of the continental and oceanic zones in the studied region. The oldest discovered deposits are the Triassic associations, an overlying series of the magmatic and sedimentary rocks of the Early Mesozoic (Asher Volcanoics) [103]. The last associations were covered by younger Mesozoic-Cenozoic deposits and affected by the extended complex deformation of the postaccretional tectonic stage (>130 Ma). Figure 22: (**A**) Geodynamic-paleomagnetic map of the Mt. Carmel–Galilee region (see its location in Figure 3) (modified and supplemented after [57]). (1) Cretaceous–Miocene basalts, (2) Miocene gabbroid intrusive, (3) Pliocene Cover basalts, (4) outcrops (a) and boreholes (b) with the Mesozoic-Cenozoic magmatic complexes, (5) radiometric age of magmatic rocks and minerals from K-Ar, Ar-Ar methods (a) and zircon geochronology (b), (6) thickness of the Lower Cretaceous traps (in m), (7) isolines of the Lower Cretaceous traps thicknesses (in m), (8) faults, (9) boundaries of terranes, (10) counterclockwise (a) and clockwise (b) rotation derived from tectonic and paleomagnetic data, (11) data of paleomagnetic measurements of magmatic rocks with normal (\(N\)) and reverse (\(R\)) polarities, (12–15) paleomagnetic zones: (12) Gissar, (13) Jalal-1, (14) Jalal-2, (15) Tuarkyr, (16) Sogdiana-2. (**B**) Paleomagnetic scale for the integrated paleomagnetic scheme for the Mt. Carmel–Galilee region. It was assumed earlier [103; 104] that the Early Mesozoic formation of the Asher Volcano was generated within the graben structure. [PERSON] et al. [105] proposed that the formations composing this graben have a primarily continental genesis since they include the soils and coal. Other data [106; 107] indicate that Asher Volcano relates to a deep basin with a possible ocean-like crust; the results of our investigations [20; 21; 22] partially coincide with the last proposition. In a series of numerous works, we have established that the concept of the Asher graben filled with volcanic rocks is initially tectonically and paleogeographically incorrect, e.g., [23]. A detailed analysis made it possible to determine that the Early and Middle Mesozoic igneous-sedimentary rocks underlying the Lower Cretaceous traps are a series of sheets of ophiolite melange. At the same time, the youngest of them, keratophyte melange, up to 164 million years old, lies at the base of the section. Furthermore, the oldest one, Mt. Carmel Upper ophiolites, is composed of an olivine-basalt melange with blocks of igneous rocks up to 222.4 Ma old [57]. In general, the association of allochthonous oceanic rocks of the Carmel-Lower Galilee is the thickest (up to 4 km) ophiolite complex in the EMM, detached from a block of oceanic crust, penetrated along transform faults from the northeast from the Neotethys zone towards the isolated oceanic basin of the Levant [21; 57]. The platform Triassic terrigenous-carbonate formations underlying the Carmel-Galilee ophiolite complex are of considerable thickness, up to 3000 m, and are intruded by Late Jurassic and Early Cretaceous trap sills.