A Domain-Based Evolution Model for Red Sea: New Sea-Floor Spreading Evidence

A Domain-Based Evolution Model for Red Sea: New Sea-Floor Spreading Evidence | Research Square window.SnipcartSettings = { analytics: { enabled: false } }; (function() { var accessVector = localStorage.getItem('access_vector') || ''; window.dataLayer = window.dataLayer || []; if (accessVector) { window.dataLayer.push({ user: { profile: { profileInfo: { snid: accessVector } } } }); } })(); (function(w,d,s,l,i){w[l]=w[l]||[];w[l].push({'gtm.start':new Date().getTime(),event:'gtm.js'});var f=d.getElementsByTagName(s)[0],j=d.createElement(s),dl=l!='dataLayer'?'&l='+l:'';j.async=true;j.src='https://www.googletagmanager.com/gtm.js?id='+i+dl;f.parentNode.insertBefore(j,f);})(window,document,'script','dataLayer','GTM-K279D39R'); Browse Preprints In Review Journals COVID-19 Preprints AJE Video Bytes Research Tools Research Promotion AJE Professional Editing AJE Rubriq About Preprint Platform In Review Editorial Policies Our Team Advisory Board Help Center Sign In Submit a Preprint Cite Share Download PDF Article A Domain-Based Evolution Model for Red Sea: New Sea-Floor Spreading Evidence Khamis Farhoud, Ahmed El-Barkooky This is a preprint; it has not been peer reviewed by a journal. https://doi.org/ 10.21203/rs.3.rs-8819895/v1 This work is licensed under a CC BY 4.0 License Status: Posted Version 1 posted You are reading this latest preprint version Abstract The propagation of the Red Sea continental margin remains unevaluated. Despite the unanimous agreement that the southern Red Sea axial ridge valley is underlain by juvenile oceanic crust, there is a lack of such agreement for the central and northern Red Sea. Significant issues relating to Red Sea tectonics are whether the Arabian and Nubian plates have been completely separated (i.e., oceanic crust lies beneath the Red Sea from coast to coast) or if the oceanic crust is restricted to the Red Sea median valley. Here, we interpret a new spreading span of at least 12.5 Ma of magnetic anomaly stripes located in the Central Red Sea, which represent ancient seafloor spreading. We show that the Red Sea basement structure exhibits different fault trends, wherein the Red Sea crust is controlled by offshore inherited Precambrian suture zones. Both these infrastructure suture zones and the Dead Sea-Aqaba-transform faults control the Red Sea crustal evolution. Earth and environmental sciences/Ocean sciences Earth and environmental sciences/Solid earth sciences Red Sea Seafloor Spreading Magnetic Stripes Structural Inheritance Arabian-Nubian Shield Figures Figure 1 Figure 2 Figure 2 Figure 3 Figure 4 1. Introduction Considerable research has focused on the Red Sea continental margin and its crustal evolutionary sequence. Modern observations of the transition from continental breakup to the initiation of seafloor spreading have galvanized plate tectonics research. This study addresses salient topics, including the boundary between oceanic and continental crust, the possible seaward continuation of onshore Proterozoic sutures, and the long-standing dichotomy between previous crustal models. By reconciling inconsistencies through an integrated dataset of magnetic, gravity, bathymetry, seismic, and surface geology (Fig.1a-e), we propose a domain-based model for Red Sea development. Review of Evolutionary Models Early Foundations Positive gravity anomalies on the Red Sea shoreline (Fig. 1a) were first observed by Von Triulzi [1] and documented by pendulum observations [2]. Farquharson [3] and Owen [4] identified the axial trough as a belt of narrow, straight-sided troughs. This axial center was later interpreted as a large basic intrusion [5], which Tazieff [6] and Girdler and Harrison [7] linked to the axial deep (Fig. 1c and d). This activity was potentially related to the 107 km displacement of Arabia relative to Sinai [8, 9, 10]. Subsequent work by Drake et al. [11] and Girdler and Peter [12] confirmed these trough deeps and identified reversely magnetized rocks in the Gulf of Aden. Development of the Seafloor Spreading Hypothesis A pivotal discovery occurred when magnetic intensity lineations were first related to axial ridge valleys [13], then Vine [14] simulated magnetic profiles at the Red Sea axial depression with a spreading rate of 1 cm/yr for the past 5 Ma at latitudes 16° and 20°N. In the current study, the same concept of Magnetic Polarity Stripes will be used, where gravity and magnetic datasets (Fig. 1a and b) are not merely used for structural mapping but serve as the primary diagnostic tools for crustal differentiation and to delineate the boundaries of the Median Ridge Valley (MRV). Moreover, in the Red Sea, the axial trough exhibits seismic velocities between 6.7 and 7.3 km/s associated with distinct gravity and magnetic signatures [15]. While Wilson [16] noted that spreading directions require the mapping of coeval transform faults, Allan [17] provided a commendable amount of Red Sea regional data. Refined seismic data subdivided the trough into axial and marginal zones [18]. Girdler [19] suggested the axial crust formed over the last 3-5 Ma, where the basement exhibits velocities of 6.4 km/s at depths of 3.3 to 3.7 km [20]. Magnetic profiles at 19°N and 22°N suggested spreading over the last 2-4 Ma [21], reconcilable with the 150 km northward movement of Arabia relative to Africa along the Abu Masorib-Duwi and Wadi Alhamd-Wadi Hafafit shear zones [22]. Further mapping by Phillips and Ross [23] and Allan [24] delineated transform faults at 19°30'N. Divergent Views on Crustal Composition The nature of the northern Red Sea crust remains a central controversy. Girdler [25] suggested it consists of extremely faulted continental crust (Fig. 1d shows the profiles locations of previous work), whereas McKenzie et al. [26] argued the entire Red Sea is underlain by oceanic crust. Structural models emphasized the role of normal faulting [27] and the presence of NW-trending en-echelon active volcanics [28]. Although basalt recovered at Site 226 showed MORB affinities [29], the identification of the "S" seismic reflector suggested spreading was post-Miocene [30]. Conversely, Girdler and Styles [31] identified 41 Ma oceanic crust, while Roeser [32] identified 4-5 Ma anomalies, supported by gravity data at the Saudi margin [33]. An alternative school of thought suggests the presence of seafloor spreading in the northern province [34]. Regional Tectonics and Phase Evolution Tectonic complexities include the Danakil microplate blocking the Afar depression [35] and evidence for three phases of crustal development: 43-35.5 Ma, 23.5-16 Ma, and 4.5-0 Ma [36] based on the LaBrecque et al. [37] polarity scale. While a 1500 km gravity line suggested the entire sea is oceanic [38] (Fig. 1d), others identified "locked zones" like Zabargad Island [39]. The Red Sea was later divided into southern, central, and northern provinces [40]. Bonatti et al. [41] found MORB basalt at Nereus Deep (Fig. 1d) indicating spreading at 2-3 Ma. Girdler [42] proposed a three-phase evolution linked to the Aqaba-Dead Sea shear. Investigations at 22°N to 25°N identified quasi-oceanic crust [43], while Bicknell et al. [44] and Bonatti [45] debated the semantics of the controversy. Research continued to show varied initiation times, from 10–12 Ma [46] to a 200 km fracture rift phase [47]. Tectonic Inheritance and Integrated Structural Models Recent ESP data show oceanic-type velocities at 26°N despite thinned continental characteristics [48, 49]. Detailed mapping of Inter-Trough Zones (ITZ) and transverse structures [50, 51] attempted to resolve the validity of the three proposed models [52, 53]. Gravity studies emphasized crustal thickening [54], while the Najd Shear System and Onib-Hamisana/Baraka sutures (Fig. 1e) were identified as pre-existing infrastructure controlling the rift [55]. Bosworth et al. [56] noted the only known offshore pre-rift Zabargad Formation, while the northern province was found to be amagmatic during rifting [57, 58]. Early magmatism (29.9–28.7 Ma) was linked to the Afar plume [59, 60], with lithospheric thinning following at 15–12 Ma [61]. Recent data suggest rifting initiated in the south [62], involving transtensional structures [63] and oblique Mid-Ocean Ridges [64]. 2. Results 2.1. Geophysical Characterization of Structural Provinces The integration of georeferenced gravity, magnetic, and seismic datasets delineates three distinct structural provinces and four dominant structural trends (N-S, Precambrian Suture, Najd Shear, and Aqaba transform) within the Red Sea basin: Southern Province (13°30'N to 18°30'N) : Defined by elongated, laterally continuous magnetic and gravity lineations extending over 800 km (Fig. 3 e-f and Fig. 4 a-b). These lineations spatially coincide with a high-amplitude positive gravity anomaly (110 km width, Fig. 3 e) centered on the Median Ridge Valley (MRV). Seismic refraction profiles (Lines 170–178) record crustal velocities exceeding 6.4 km/s, consistent with a well-developed oceanic crustal structure. Central Province (18°30'N to 23°N) : Characterized by organized magnetic polarity patterns (Fig. 3 f). North of the Heya terrane (Fig. 4 a and b), these magnetic anomalies diverge from gravity signatures, where corresponding Bouguer anomalies diminish or are absent (Fig. 3 e). Seismic refraction velocities along the MRV remain high (6.76–6.97 km/s; Lines 179–181), while bathymetric data reveal increasingly irregular morphological features. Northern Province (23°N to 27°30'N) : In contrast to the southern and central provinces, the northern Red Sea exhibits characteristics of an amagmatic continental rift (Fig. 4 a-b). Pre-rift stratigraphic units, including the Zabargad Formation, are preserved, and seismic refraction velocities remain consistently below 6.4 km/s. Magnetic anomalies are discrete and low-amplitude, lacking laterally continuous lineation patterns. 2.2. Identification of Vine-Matthews Stripes and Structural Offsets Geospatial analysis identifies five clusters of linear magnetic anomalies within the Central and Southern provinces (Fig. 3 f). These elongated signatures features are interpreted as Vine-Matthews stripes, characterized by strike-parallel continuity with approximate lengths of 220 km, 220 km, 150 km, and 100 km for Groups 1 through 4, respectively. Group 5 is more fragmented, with magnetic lineations intersected and segmented by small-scale strike-slip structures. These Vine-Matthews-like stripes, representing organized seafloor spreading rather than discrete continental intrusions. A major structural discontinuity is observed at the Atlantis II Deep (20°30'N), where the gravity anomaly terminates abruptly at the Nakasib Suture Zone (Fig. 3 e). Across this crustal boundary, the magnetic anomaly axis is laterally offset by approximately 64 km between the northern and southern sub-zones Fig. 4 a). This offset aligns spatially with the offshore projection of the onshore Baraka left-lateral suture (Fig. 4 a and b). 2.3. Stratigraphic Constrain and Magnetic Correlation Magnetic profile A–A′ reveals a sequence of organized polarity reversals extending ~ 250 km in width and ~ 220 km along strike beneath the Miocene S-reflector (Fig. 4 b, e). Assuming a half-spreading rate of ~ 1 cm/yr (Vine, 1966), the identified magnetic sequence corresponds to a spreading duration of approximately 12.5 Ma. When calibrated against the ~ 5 Ma age of the S-reflector, this yields a minimum crustal age of ~ 17.5 Ma. Correlation with the geomagnetic polarity timescale (GSA, 2022; Fig. 4 e) shows agreement over a ~ 12 Ma interval spanning chrons C20 to C24. Stratigraphic data from the Jeddah-1 well further document ~ 100 m of volcanic sequences within the Eocene interval. 3. Discussion The southern Red Sea axial ridge is characterized by straight-sided bathymetric troughs(Fig. 1 d). Although some models have proposed widespread oceanic crust extending back to ~ 40 Ma, such interpretations are difficult to reconcile with regional stratigraphic relationships, as they would require Jurassic formations to overlie Eocene oceanic crust. Synthesized potential-field data indicate that dense, high-gravity crustal material is confined to the Median Ridge Valley (Fig. 3 e). Southward-propagating oceanic crust terminates near 20°30′N, coincident with the Nakasib Suture Zone. This geometry suggests that active oceanization in the southern Red Sea is restricted to the axial trough and was strongly influenced by early plume-lithosphere interaction associated with Afar magmatism. Moving into the central province, the study provides key evidence for a domain-based evolutionary model. The presence of organized magnetic lineations beneath the undisturbed Miocene S-reflector indicates that oceanic crust formation predates the Pliocene. Application of spreading-rate constraints to profile A-A′ yields a minimum age of ~ 17.5 Ma, significantly older than the 2–3 Ma ages proposed for isolated “oceanization cells” in earlier models (Fig. 4 b and e). This province is laterally segmented by a ~ 64 km offset at the Atlantis II Deep (Fig. 4 a). The spatial correspondence between this offset and the offshore projection of the Baraka Suture suggests that inherited Precambrian structures exerted a first-order control on rift segmentation and lateral displacement during Red Sea evolution. Volcanic sequences encountered in the Jeddah-1 well likely reflect localized magmatic activity associated with this transitional domain. In contrast, the northern Red Sea retains the characteristics of an amagmatic continental rift. Preservation of pre-rift stratigraphy and seismic velocities below 6.4 km/s are consistent with continental basement rather than oceanic crust. Discrete, low-amplitude magnetic anomalies are interpreted as signatures of diffuse extension. Previous interpretations of oceanic crust based solely on seismic velocity and density are non-unique. Comparable velocity signatures could arise from the heterogeneous Neoproterozoic basement assemblages of the Egyptian Eastern Desert if submerged and imaged under similar acquisition conditions. Consequently, seismic velocity alone is insufficient to uniquely diagnose oceanic crust in the absence of organized magnetic lineations. Synthesizing these observations, the integrated geological and geophysical evidence indicates that Red Sea crustal evolution is segmented and strongly influenced by inherited Precambrian architecture (Fig. 4 c). Three distinct evolutionary domains are recognized: axial-restricted oceanic spreading in the South bounded by the Nakasib Suture; ancient oceanic crust (minimum ~ 17.5 Ma) in the Central province segmented by inherited sutures; and continental rifting in the North governed by Neoproterozoic basement grain and the Aqaba–Dead Sea transform system. Collectively, these findings indicate that the Red Sea behaves as a segmented rift in which the timing and geometry of crustal growth are strongly influenced by the inherited architecture of the Arabian–Nubian Shield. 4. Methodology To address inconsistencies among existing tectonic models, this study employs a multi-proxy geospatial integration workflow. Five independent datasets were compiled into a single, fully georeferenced database to enable consistent spatial comparison and identification of crustal domains across the Red Sea basin. 4.1. Potential Field Analysis Gravity and magnetic anomaly maps were analyzed to delineate the Median Ridge Valley (MRV) and to identify lateral offsets, lineations, and anomaly terminations (Figs. 1and b; Fig. 3 f; Fig. 4 a). Magnetic data were also examined for the presence of elongated anomaly patterns consistent with organized seafloor spreading. Criteria for Magnetic Stripe Identification Magnetic stripes were identified following the conceptual framework of [ 13 ] Stripe identification was based on three criteria: (1) linearity, (2) bilateral symmetry, and (3) organized polarity alternation (Fig. 3 f). On georeferenced magnetic intensity maps, these features appear as elongated, strike-parallel bands of alternating positive and negative anomalies. These patterns were distinguished from isolated magmatic intrusions, which typically present as discrete, high-amplitude, circular or irregular anomaly clusters with limited lateral continuity. Whereas intrusions represent localized magmatic events, magnetic stripes record successive geomagnetic polarity reversals during sustained crustal accretion. 4.2. Qualitative Geophysical Interpretation Gravity and magnetic datasets were interpreted qualitatively by examining lateral variations in anomaly character and their spatial correspondence with mapped tectonic domains and inherited structures (Fig. 3 a-f; Fig. 4 a). Interpretation was conducted within a comparative spatial framework, emphasizing anomaly continuity, termination, and offset, rather than through forward or inverse numerical modeling. 4.3. Seismic Velocity Compilation A ~ 1900 km composite seismic refraction profile was reconstructed from VEMA-Atlantis datasets (Fig. 1 c; Fig. 2 ). Crustal types were categorized based on velocities, with values exceeding 6.4 km/s classified as oceanic or intrusive crust and velocities below 6.4 km/s classified as continental crust. These seismic observations were used as independent constraints to evaluate interpretations derived from potential field data. 4.4. Bathymetric Analysis Bathymetric data were analyzed to characterize axial trough morphology, basin segmentation, and depth variations along the rift axis (Fig. 1 c-d). Bathymetry was incorporated into the geospatial database and evaluated alongside gravity and magnetic datasets to assess correspondence between surface morphology and subsurface geophysical signatures. 4.5. Tectonic Inheritance Mapping Onshore Precambrian suture zones, including the Nakasib and Sol Hamid sutures, were projected offshore to assess their spatial relationships with geophysical anomalies and rift segmentation patterns (Fig. 1 e; Fig. 4 a-b). A synthesized geological map was used to delineate inherited terranes, suture zones, and exposed crustal domains. 4.6. Magnetic Spreading Correlation A half-spreading rate of 1 cm/yr (Vine, 1966) was applied to a newly identified ~ 250 km magnetic profile (A-A′) in the central Red Sea (Fig. 4 b, e) to evaluate potential spreading durations represented by the observed anomaly sequences. 4.7. Stratigraphic Integration The Miocene S-reflector (~ 5 Ma) and stratigraphic data from the Jeddah-1 well (location shown in Fig. 1 c) were used as chronological reference horizons to calibrate the relative timing of the identified magnetic anomaly sequences (Fig. 3 f; Fig. 4 b). 4.8. Geospatial Integration Framework A central component of the methodology was the strict geospatial integration of all datasets within a high-resolution, unified coordinate system. This approach ensured spatial consistency among geological, geophysical, bathymetric, seismic, and stratigraphic observations, allowing systematic evaluation of spatial correspondence and mismatch across datasets. Figure 4 summarizes this integration framework and illustrates how dataset coherence was assessed without assuming uniform spreading along the rift axis. Declarations Competing interests The authors declare no competing interests. Funding: No funding. Author Contribution KF: Conceptualization, Methodology, Data Acquisition, Formal Analysis, and Writing-Original Draft. AE: Data Curation, Writing-Review \& Editing, and Technical Supervision. Acknowledgement We thank Mr. Dia Mahmoud, GEOPEX Ltd. and Dr. Hussein Hammouda, Ex-Chairman of Egyptian Mineral Resources Authority, for their help in digitizing the old Red Sea magnetic and gravity paper sheets. Special thanks to the late Dr. Wafik Mishrif for his support and encouragement in collecting most of magnetic and gravity sheets over Gulf of Suez and Red Sea. Thanks to The National Geophysical Data Center (NGDC) for delivering the copy of gravity and magnetic data acquired over Red Sea. Thanks to Dr. Hans A. Roeser for providing his own gravity and magnetic material of 1975, 1976 and 1980. Data Availability The regional geophysical datasets supporting the findings of this study are publicly available. Potential field and bathymetric data were integrated from the NOAA National Centers for Environmental Information (https://www.ngdc.noaa.gov), the UCSD Topographic/Bathymetric database (https://topex.ucsd.edu), and the World Digital Magnetic Anomaly Map (WDMAM v2.1) repository (http://www.wdmam.org). Specific processed datasets or geospatial integrations generated during the current study are available from the corresponding author upon reasonable request. References Von Triulzi, A. E. Denkschr Akad. Wiss Wien Math. -Nat Kl 65 , 131 (1898). Vening Meinesz, F. A. Gravity expeditions at sea, 1923–1932, Vol. II (Netherlands Geodetic Commission, 1934). https://doi.org/10.54419/3us2nj Farquharson, W. I. Topography, with an appendix on magnetic observations. Sci. Rep. John Murray Expedition . 1933-34 (1), 43–61 (1935). Owen, L. Origin of the Red Sea depression. AAPG Bull. 22 , 1217–1223. https://doi.org/10.1306/3d932fe0-16b1-11d7-8645000102c1865d (1938). Girdler, R. W. The relationship of the Red Sea to the East African Rift System. Q. J. Geol. Soc. Lond. 114 , 79–105. https://doi.org/10.1144/gsjgs.114.1.0079 (1958). Tazieff, H. Une recente campagne oceanographique dans la mer Rouge. Bull. Soc. Belge Geol. 61 , 84–90 (1952). Girdler, R. W. & Harrison, J. C. Submarine gravity measurements in the Atlantic, Indian Ocean, Red Sea and Mediterranean Sea. Proc. R. Soc. Lond. A 239, 202 (1957). https://doi.org/10.1098/rspa.1957.0033 Quennell, A. M. Tectonics of the Dead Sea rift. Int. Geol. Congr . 20 , 385–405 (1956). Quennell, A. M. Tectonics of the Dead Sea rift. Assoc Afr. Geol. Surv 385–408 (1959). Carey, S. W. A tectonic approach to continental drift. in Continental Drift: A Symposium 177–355University of Tasmania, Hobart, (1958). Drake, C. L., Girdler, R. W. & Landisman, M. Geophysical measurements in the Red Sea. Proc. Int. Oceanogr. Congr. 20 (1959). Girdler, R. W. & Peter, G. An example of the importance of natural remanent magnetization in the interpretation of magnetic anomalies. Geophys. Prospect. 8 , 474–483. https://doi.org/10.1111/j.1365-2478.1960.tb01730.x (1960). Vine, F. J. & Matthews, D. H. Magnetic anomalies over ocean ridges. Nature 199 , 947–949. https://doi.org/10.1038/199947a0 (1963). Vine, F. J. Spreading of the ocean floor: New evidence. Science 154 , 1405–1415. https://doi.org/10.1126/science.154.3755.1405 (1966). Drake, C. L. & Girdler, R. W. A geophysical study of the Red Sea. Geophys. J. 8 , 473–495. https://doi.org/10.1111/j.1365-246X.1964.tb06303.x (1964). Wilson, J. T. Transform faults, oceanic ridges and magnetic anomalies southwest of Vancouver Island. Science 150 , 482–485. https://doi.org/10.1126/science.150.3695.482 (1965). Allan, T. D. A Bathymetric Chart of the Red Sea. Int. Hydrogr. Rev. 43 , 33–36 (1966). Knott, S. T., Bunce, E. T. & Chase, R. L. Red Sea seismic reflection studies. Geol Surv. Can. Pap 66 – 14 . 33–61. https://doi.org/10.4095/103358 (1966). Girdler, R. W. Earth satellites, terrestrial heat flow, mantle convection and the location of extensional and compressional features on the Earth’s surface. Proc. Geol. Assoc. 78, 165–178 (1967). https://doi.org/10.1016/s0016-7878(67)80042-7 Tramontini, C. & Davies, D. Seismic refraction survey in the Red Sea. Geophys. J. 17 , 225–241. https://doi.org/10.1111/j.1365-246x.1969.tb02323.x (1969). Phillips, J. D., Woodside, J. & Bowin, C. O. Magnetic and gravity anomalies in the central Red Sea. in Hot Brines and Recent Heavy Metal Deposits in the Red Sea 98–113 (Springer, https://doi.org/10.1007/978-3-662-28603-6_10 (1969). Abdel-Gawad, M. Geological structures of the Red Sea area inferred from satellite pictures. in Hot Brines and Recent Heavy Metal Deposits in the Red Sea 25–37 (Springer, 1969). https://doi.org/10.1007/978-3-662-28603-6_5 Phillips, J. & Ross, D. A. Continuous seismic reflection profiles in the Red Sea. Philos. Trans. R Soc. Lond. A . 267 , 143–152. https://doi.org/10.1098/RSTA.1970.0029 (1970). Allan, T. D. Magnetic and gravity fields over the Red Sea. Philos. Trans. R Soc. Lond. A . 261 , 153–180. https://doi.org/10.1098/rsta.1970.0030 (1970). Girdler, R. W. A review of Red Sea heat flow. Philos. Trans. R Soc. Lond. A . 267 , 359–368. https://doi.org/10.1098/rsta.1970.0032 (1970). McKenzie, D. P., Davies, D. & Molnar, P. Plate tectonics of the Red Sea and East Africa. Nature 226 , 243–248. https://doi.org/10.1038/226243a0 (1970). Lowell, J. D. & Genik, G. J. Sea-floor spreading and structural evolution of the southern Red Sea. AAPG Bull. 56 , 247–259. https://doi.org/10.1306/819a3e56-16c5-11d7-8645000102c1865d (1972). Stieltjes, L. Evolution tectonique recente du rift d’Asal. Rev. Geogr. Phys. Geol. Dyn. 15 , 425–436 (1973). Stoffers, P. & Ross, D. A. Sedimentary history of the Red Sea. Woods Hole Oceanogr. Inst. Contrib. 3168, 849–865 (1974). https://doi.org/10.2973/dsdp.proc.23.123.1974 Roger, C., Searle, R. & Ross, D. A. Geophysical study of the Red Sea axial trough. Geophys. J. R Astron. Soc. 43 , 555–572. https://doi.org/10.1111/j.1365-246x.1975.tb00647.x (1975). Girdler, R. W. & Styles, P. Two-stage Red Sea floor spreading. Nature 247, 7–11 [Note: User provided 330, but 1974 article is Vol 247]. (1974). https://doi.org/10.1038/247007a0 Roeser, H. A. Detailed magnetic survey of the southern Red Sea. Geol. Jahrb . 13 , 131–153 (1975). Gettings, M. E. Delineation of the continental margin of the southern Red Sea from new gravity evidence. Saudi Arab. Dir. Gen. Min. Res. Bull. 2 , K1–K11 (1977). Girdler, R. W. & Southren, T. Structure and evolution of the northern Red Sea. Nature 330 , 716–721. https://doi.org/10.1038/330716a0 (1987). Le Pichon, X. & Francheteau, J. Plate tectonic analysis of the Red Sea–Gulf of Aden area. Tectonophysics 46 , 369–406. https://doi.org/10.1016/0040-1951(78)90214-7 (1978). Girdler, R. W., Brown, C., Noy, D. J. M. & Styles, P. Geophysical survey of the westernmost Gulf of Aden. Philos. Trans. R Soc. Lond. A . 298 , 1–43. https://doi.org/10.1098/rsta.1980.0239 (1980). LaBrecque, J., Kent, D. V. & Cande, S. C. Revised magnetic polarity time scale for Late Cretaceous and Cenozoic time. Geology 5 , 330–335. https://doi.org/10.1130/0091-7613(1977)5%3C330:rmptsf%3E2.0.co;2 (1977). Brown, C. & Girdler, R. W. Structure of the Red Sea at 20° N from gravity data and its implications for continental margins. Nature 298 , 51–53. https://doi.org/10.1038/298051a0 (1982). Courtillot, V. Propagating rifts and continental breakup. Tectonics 1 , 239–250. https://doi.org/10.1029/TC001i003p00239 (1982). Cochran, J. R. A model for development of Red Sea. AAPG Bull. 67 , 41–69. https://doi.org/10.1306/03B5ACBE-16D1-11D7-8645000102C1865D (1983). Bonatti, E., Colantoni, P., Della Vedova, B. & Taviani, M. Geology of the Red Sea transitional region (22° N–25° N). Oceanol. Acta . 7 , 385–398 (1984). Girdler, R. W. Problems concerning the evolution of oceanic lithosphere in the northern Red Sea. Tectonophysics 116 , 109–122. https://doi.org/10.1016/0040-1951(85)90224-0 (1985). LaBrecque, J. L. & Zitellini, N. Continuous seafloor spreading in the Red Sea. AAPG Bull. 69 , 513–524. https://doi.org/10.1306/AD46251F-16F7-11D7-8645000102C1865D (1985). Bicknell, J. D. et al. Tectonics of the Nereus Deep, Red Sea: A deep-tow investigation of a site of initial rifting. J. Geophys. Res. 91 , 131–148. https://doi.org/10.1007/bf00338225 (1986). Bonatti, E. Rifting or drifting in the Red Sea? Nature 330 , 962–963. https://doi.org/10.1038/330692a0 (1987). Izzeldin, A. Y. Seismic, gravity and magnetic surveys in the central part of the Red Sea. Tectonophysics 143 , 269–306. https://doi.org/10.1016/0040-1951(87)90214-9 (1987). Joffe, S. & Garfunkel, Z. Plate kinematics of the circum–Red Sea: A re-evaluation. Tectonophysics 141 , 5–23. https://doi.org/10.1016/0040-1951(87)90171-5 (1987). Gaulier, J. M. et al. Seismic study of the crust of the northern Red Sea and Gulf of Suez. Tectonophysics 153 , 55–88. https://doi.org/10.1016/0040-1951(88)90007-8 (1988). Martinez, F. & Cochran, J. R. Structure and tectonics of the northern Red Sea. Tectonophysics 150 , 1–32. https://doi.org/10.1016/0040-1951(88)90293-4 (1988). Izzeldin, A. Y. Transverse structures in the central Red Sea and implications for early oceanic accretion. Geophys. J. 96 , 117–129. https://doi.org/10.1111/j.1365-246X.1989.tb05254.x (1989). Guennoc, P., Pautot, G., Le Quentrec, M. F. & Coutelle, A. Structure of an early oceanic rift in the northern Red Sea. Oceanol. Acta . 13 , 145–155 (1990). Uchupi, E. & Ross, D. A. Springer,. The geologic enigma of the Red Sea rift. in Facets of Modern Biogeochemistry 52–61 (1990). Girdler, R. W. The case for oceanic crust beneath the Red Sea. Tectonophysics 198 , 275–278. https://doi.org/10.1016/0040-1951(91)90155-L (1991). Makris, J. & Rihm, R. Shear-controlled evolution of the Red Sea. Tectonophysics 198 , 441–466. https://doi.org/10.1016/0040-1951(91)90166-p (1991). Makris, J. & Henke, C. H. Pull-apart evolution of the Red Sea. J. Petrol. Geol. 15 , 127–134. https://doi.org/10.1111/j.1747-5457.1992.tb00958.x (1992). Bosworth, W. et al. Stratigraphic and structural evolution of Zabargad Island (Red Sea, Egypt) since the Early Cretaceous. Proc. 3rd Int. Conf. Geol. Arab World, Cairo Univ. 161–190 (1996). Bosworth, W. & McClay, K. R. Structural and stratigraphic evolution of the Gulf of Suez Rift, Egypt. in Peri-Tethys Memoir 6 567–606Springer, (2001). Cochran, J. R. Northern Red Sea: Nucleation of an oceanic spreading center within a continental rift. Geochem. Geophys. Geosyst. 6 , Q03006. https://doi.org/10.1029/2004gc000826 (2005). Bosworth, W. Geological evolution of the Red Sea: Historical background, review, and synthesis. Springer Earth Syst. Sci. 45–78. https://doi.org/10.1007/978-3-662-45201-1_3 (2015). Bosworth, W. & Stockli, D. F. Early magmatism in the greater Red Sea. Can. J. Earth Sci. 53 , 1158–1176. https://doi.org/10.1139/cjes-2016-0019 (2016). Blanchette, A. R., Klemperer, S. L., Mooney, W. D. & Zahran, H. M. Two-stage Red Sea rifting inferred from mantle earthquakes in Neoproterozoic lithosphere. Earth Planet. Sci. Lett. 497 , 92–101. https://doi.org/10.1016/j.epsl.2018.05.048 (2018). Bosworth, W., Khalil, S. M., Ligi, M., Stockli, D. F. & McClay, K. R. The northern Red Sea. in Geology of Egypt 344–369 (Springer, https://doi.org/10.1007/978-3-030-15265-9_9 (2020). Issachar, R., Ebbing, J. & Dilixiati, Y. New magnetic anomaly map for the Red Sea reveals transtensional structures associated with rotational rifting. Sci. Rep. 12 , 5757. https://doi.org/10.1038/s41598-022-09770-0 (2022). Delaunay, A. et al. Structure and morphology of the Red Sea, from the mid-ocean ridge to the ocean-continent boundary. Tectonophysics 849 https://doi.org/10.1016/j.tecto.2023.229728 (2023). Additional Declarations No competing interests reported. Cite Share Download PDF Status: Posted Version 1 posted You are reading this latest preprint version Research Square lets you share your work early, gain feedback from the community, and start making changes to your manuscript prior to peer review in a journal. As a division of Research Square Company, we’re committed to making research communication faster, fairer, and more useful. We do this by developing innovative software and high quality services for the global research community. Our growing team is made up of researchers and industry professionals working together to solve the most critical problems facing scientific publishing. Also discoverable on Platform About Our Team In Review Editorial Policies Advisory Board Help Center Resources Author Services Accessibility API Access RSS feed Manage Cookie Preferences © Research Square 2026 | ISSN 2693-5015 (online) Privacy Policy Terms of Service Do Not Sell My Personal Information {"props":{"pageProps":{"initialData":{"identity":"rs-8819895","acceptedTermsAndConditions":true,"allowDirectSubmit":true,"archivedVersions":[],"articleType":"Article","associatedPublications":[],"authors":[{"id":594922002,"identity":"ca6f3ec7-b418-4a03-8bc0-0f46d998ced7","order_by":0,"name":"Khamis Farhoud","email":"data:image/png;base64,iVBORw0KGgoAAAANSUhEUgAAAZAAAAAyAQMAAABI0h/eAAAABlBMVEX///8AAABVwtN+AAAACXBIWXMAAA7EAAAOxAGVKw4bAAAA7ElEQVRIiWNgGAWjYBACCQkGhg8MDAeAzORjYBE2dsJaGGdAtKSlMTAkALUwE68lxwyshYGQFsnZDYwNP/fckTM4nvPtwccf2+T5mBkYP3zMwa1FWuYAY2PPs2fGBmfebjeckXDbsI2ZgVly5jbcWuQkEtgf8Bw4nLjhRu42aZ6E24xALWzMvPi1MDb+AWvJeQbSYk9QizRQSzPElhw2kJZEglokZwC1yBw4bCx55pmZ5Iy028ltzIzNeP0icQPosDcHDsvxHU9+JvHB5rbt/Pbmgx8+4tHCwMD/AV2EsQGf+lEwCkbBKBgFRAAAaDFUJzYuS5EAAAAASUVORK5CYII=","orcid":"","institution":"Anton Oil","correspondingAuthor":true,"prefix":"","firstName":"Khamis","middleName":"","lastName":"Farhoud","suffix":""},{"id":594922007,"identity":"7262802c-25d9-480d-a85e-7e40eb1649f9","order_by":1,"name":"Ahmed El-Barkooky","email":"","orcid":"","institution":"Cairo University","correspondingAuthor":false,"prefix":"","firstName":"Ahmed","middleName":"","lastName":"El-Barkooky","suffix":""}],"badges":[],"createdAt":"2026-02-08 07:53:16","currentVersionCode":1,"declarations":{"humanSubjects":false,"vertebrateSubjects":false,"conflictsOfInterestStatement":false,"humanSubjectEthicalGuidelines":false,"humanSubjectConsent":false,"humanSubjectClinicalTrial":false,"humanSubjectCaseReport":false,"vertebrateSubjectEthicalGuidelines":false},"doi":"10.21203/rs.3.rs-8819895/v1","doiUrl":"https://doi.org/10.21203/rs.3.rs-8819895/v1","draftVersion":[],"editorialEvents":[],"editorialNote":"","failedWorkflow":false,"files":[{"id":103247147,"identity":"070c36b8-70dd-4846-bee6-e8ad95b5ba01","added_by":"auto","created_at":"2026-02-23 15:19:37","extension":"png","order_by":1,"title":"Figure 1","display":"","copyAsset":false,"role":"figure","size":2589949,"visible":true,"origin":"","legend":"\u003cp\u003eSee image above for figure legend\u003c/p\u003e","description":"","filename":"AllFigures1.png","url":"https://assets-eu.researchsquare.com/files/rs-8819895/v1/009fa500f35aa57620419f72.png"},{"id":103505946,"identity":"d69ecb17-a3d1-4281-bb29-1f1d5c8083e9","added_by":"auto","created_at":"2026-02-26 13:33:35","extension":"png","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":1182679,"visible":true,"origin":"","legend":"\u003cp\u003eSee image above for figure legend\u003c/p\u003e","description":"","filename":"AllFigures2.png","url":"https://assets-eu.researchsquare.com/files/rs-8819895/v1/de3e61f90ff69f3683aa8acb.png"},{"id":103365303,"identity":"f0effe74-a84f-40a2-919e-da9abea16b2d","added_by":"auto","created_at":"2026-02-24 22:52:13","extension":"png","order_by":2,"title":"Figure 2","display":"","copyAsset":false,"role":"figure","size":1182679,"visible":true,"origin":"","legend":"\u003cp\u003eSee image above for figure legend\u003c/p\u003e","description":"","filename":"AllFigures2.png","url":"https://assets-eu.researchsquare.com/files/rs-8819895/v1/d07d45dbf333b717690ae67a.png"},{"id":103247148,"identity":"7341da9b-c96f-4dec-b0b2-eb2bc2672fa0","added_by":"auto","created_at":"2026-02-23 15:19:37","extension":"png","order_by":3,"title":"Figure 3","display":"","copyAsset":false,"role":"figure","size":3146156,"visible":true,"origin":"","legend":"\u003cp\u003eSee image above for figure legend\u003c/p\u003e","description":"","filename":"AllFigures3.png","url":"https://assets-eu.researchsquare.com/files/rs-8819895/v1/2d685eb8c7fc386e0574972a.png"},{"id":103247150,"identity":"cea8d45e-49a4-49a6-b475-8f3d4b0323c7","added_by":"auto","created_at":"2026-02-23 15:19:37","extension":"png","order_by":4,"title":"Figure 4","display":"","copyAsset":false,"role":"figure","size":2297938,"visible":true,"origin":"","legend":"\u003cp\u003eSee image above for figure legend\u003c/p\u003e","description":"","filename":"AllFigures4.png","url":"https://assets-eu.researchsquare.com/files/rs-8819895/v1/c62c3e371ab4b0d619ea7ad3.png"},{"id":104405266,"identity":"1324b1b4-ee55-4361-ba09-d0af6d95d7bf","added_by":"auto","created_at":"2026-03-11 12:22:21","extension":"pdf","order_by":0,"title":"","display":"","copyAsset":false,"role":"manuscript-pdf","size":14011165,"visible":true,"origin":"","legend":"","description":"","filename":"manuscript.pdf","url":"https://assets-eu.researchsquare.com/files/rs-8819895/v1/1aef6032-f0c6-468b-937a-e8b2472c38d8.pdf"}],"financialInterests":"No competing interests reported.","formattedTitle":"A Domain-Based Evolution Model for Red Sea: New Sea-Floor Spreading Evidence","fulltext":[{"header":"1. Introduction","content":"\u003cp\u003eConsiderable research has focused on the Red Sea continental margin and its crustal evolutionary sequence. Modern observations of the transition from continental breakup to the initiation of seafloor spreading have galvanized plate tectonics research. This study addresses salient topics, including the boundary between oceanic and continental crust, the possible seaward continuation of onshore Proterozoic sutures, and the long-standing dichotomy between previous crustal models. By reconciling inconsistencies through an integrated dataset of magnetic, gravity, bathymetry, seismic, and surface geology (Fig.1a-e), we propose a domain-based model for Red Sea development.\u003c/p\u003e\n\u003ch2\u003eReview of Evolutionary Models\u003c/h2\u003e\n\u003cp\u003e\u003cstrong\u003eEarly Foundations\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003ePositive gravity anomalies on the Red Sea shoreline (Fig. 1a) were first observed by Von Triulzi [1] and documented by pendulum observations [2]. Farquharson [3] and Owen [4] identified the axial trough as a belt of narrow, straight-sided troughs. This axial center was later interpreted as a large basic intrusion [5], which Tazieff [6] and Girdler and Harrison [7] linked to the axial deep (Fig. 1c and d). This activity was potentially related to the 107 km displacement of Arabia relative to Sinai [8, 9, 10]. Subsequent work by Drake et al. [11] and Girdler and Peter [12] confirmed these trough deeps and identified reversely magnetized rocks in the Gulf of Aden.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eDevelopment of the Seafloor Spreading Hypothesis\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eA pivotal discovery occurred when magnetic intensity lineations were first related to axial ridge valleys [13], then Vine [14] simulated magnetic profiles at the Red Sea axial depression with a spreading rate of 1 cm/yr for the past 5 Ma at latitudes 16\u0026deg; and 20\u0026deg;N. In the current study, the same concept of Magnetic Polarity Stripes will be used, where gravity and magnetic datasets (Fig. 1a and b) are not merely used for structural mapping but serve as the primary diagnostic tools for crustal differentiation and to delineate the boundaries of the Median Ridge Valley (MRV). Moreover, in the Red Sea, the axial trough exhibits seismic velocities between 6.7 and 7.3 km/s associated with distinct gravity and magnetic signatures [15]. While Wilson [16] noted that spreading directions require the mapping of coeval transform faults, Allan [17] provided a commendable amount of Red Sea regional data.\u003c/p\u003e\n\u003cp\u003eRefined seismic data subdivided the trough into axial and marginal zones [18]. Girdler [19] suggested the axial crust formed over the last 3-5 Ma, where the basement exhibits velocities of 6.4 km/s at depths of 3.3 to 3.7 km [20]. Magnetic profiles at 19\u0026deg;N and 22\u0026deg;N suggested spreading over the last 2-4 Ma [21], reconcilable with the 150 km northward movement of Arabia relative to Africa along the Abu Masorib-Duwi and Wadi Alhamd-Wadi Hafafit shear zones [22]. Further mapping by Phillips and Ross [23] and Allan [24] delineated transform faults at 19\u0026deg;30\u0026apos;N.\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eDivergent Views on Crustal Composition\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eThe nature of the northern Red Sea crust remains a central controversy. Girdler [25] suggested it consists of extremely faulted continental crust (Fig. 1d shows the profiles locations of previous work), whereas McKenzie et al. [26] argued the entire Red Sea is underlain by oceanic crust. Structural models emphasized the role of normal faulting [27] and the presence of NW-trending en-echelon active volcanics [28]. Although basalt recovered at Site 226 showed MORB affinities [29], the identification of the \u0026quot;S\u0026quot; seismic reflector suggested spreading was post-Miocene [30].\u003c/p\u003e\n\u003cp\u003eConversely, Girdler and Styles [31] identified 41 Ma oceanic crust, while Roeser [32] identified 4-5 Ma anomalies, supported by gravity data at the Saudi margin [33]. An alternative school of thought suggests the presence of seafloor spreading in the northern province [34].\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eRegional Tectonics and Phase Evolution\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eTectonic complexities include the Danakil microplate blocking the Afar depression [35] and evidence for three phases of crustal development: 43-35.5 Ma, 23.5-16 Ma, and 4.5-0 Ma [36] based on the LaBrecque et al. [37] polarity scale. While a 1500 km gravity line suggested the entire sea is oceanic [38] (Fig. 1d), others identified \u0026quot;locked zones\u0026quot; like Zabargad Island [39].\u003c/p\u003e\n\u003cp\u003eThe Red Sea was later divided into southern, central, and northern provinces [40]. Bonatti et al. [41] found MORB basalt at Nereus Deep (Fig. 1d) indicating spreading at 2-3 Ma. Girdler [42] proposed a three-phase evolution linked to the Aqaba-Dead Sea shear.\u003c/p\u003e\n\u003cp\u003eInvestigations at 22\u0026deg;N to 25\u0026deg;N identified quasi-oceanic crust [43], while Bicknell et al. [44] and Bonatti [45] debated the semantics of the controversy. Research continued to show varied initiation times, from 10\u0026ndash;12 Ma [46] to a 200 km fracture rift phase [47].\u003c/p\u003e\n\u003cp\u003e\u003cstrong\u003eTectonic Inheritance and Integrated Structural Models\u003c/strong\u003e\u003c/p\u003e\n\u003cp\u003eRecent ESP data show oceanic-type velocities at 26\u0026deg;N despite thinned continental characteristics [48, 49]. Detailed mapping of Inter-Trough Zones (ITZ) and transverse structures [50, 51] attempted to resolve the validity of the three proposed models [52, 53].\u003c/p\u003e\n\u003cp\u003eGravity studies emphasized crustal thickening [54], while the Najd Shear System and Onib-Hamisana/Baraka sutures (Fig. 1e) were identified as pre-existing infrastructure controlling the rift [55]. Bosworth et al. [56] noted the only known offshore pre-rift Zabargad Formation, while the northern province was found to be amagmatic during rifting [57, 58].\u003c/p\u003e\n\u003cp\u003eEarly magmatism (29.9\u0026ndash;28.7 Ma) was linked to the Afar plume [59, 60], with lithospheric thinning following at 15\u0026ndash;12 Ma [61]. Recent data suggest rifting initiated in the south [62], involving transtensional structures [63] and oblique Mid-Ocean Ridges [64].\u003c/p\u003e"},{"header":"2. Results","content":"\u003cdiv id=\"Sec3\" class=\"Section2\"\u003e \u003ch2\u003e2.1. Geophysical Characterization of Structural Provinces\u003c/h2\u003e \u003cp\u003eThe integration of georeferenced gravity, magnetic, and seismic datasets delineates three distinct structural provinces and four dominant structural trends (N-S, Precambrian Suture, Najd Shear, and Aqaba transform) within the Red Sea basin:\u003c/p\u003e \u003cp\u003e \u003cul\u003e \u003cli\u003e \u003cp\u003e \u003cb\u003eSouthern Province (13\u0026deg;30'N to 18\u0026deg;30'N)\u003c/b\u003e: Defined by elongated, laterally continuous magnetic and gravity lineations extending over 800 km (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ee-f and Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ea-b). These lineations spatially coincide with a high-amplitude positive gravity anomaly (110 km width, Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ee) centered on the Median Ridge Valley (MRV). Seismic refraction profiles (Lines 170\u0026ndash;178) record crustal velocities exceeding 6.4 km/s, consistent with a well-developed oceanic crustal structure.\u003c/p\u003e \u003c/li\u003e \u003cli\u003e \u003cp\u003e \u003cb\u003eCentral Province (18\u0026deg;30'N to 23\u0026deg;N)\u003c/b\u003e: Characterized by organized magnetic polarity patterns (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ef). North of the Heya terrane (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ea and b), these magnetic anomalies diverge from gravity signatures, where corresponding Bouguer anomalies diminish or are absent (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ee). Seismic refraction velocities along the MRV remain high (6.76\u0026ndash;6.97 km/s; Lines 179\u0026ndash;181), while bathymetric data reveal increasingly irregular morphological features.\u003c/p\u003e \u003c/li\u003e \u003cli\u003e \u003cp\u003e \u003cb\u003eNorthern Province (23\u0026deg;N to 27\u0026deg;30'N)\u003c/b\u003e: In contrast to the southern and central provinces, the northern Red Sea exhibits characteristics of an amagmatic continental rift (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ea-b). Pre-rift stratigraphic units, including the Zabargad Formation, are preserved, and seismic refraction velocities remain consistently below 6.4 km/s. Magnetic anomalies are discrete and low-amplitude, lacking laterally continuous lineation patterns.\u003c/p\u003e \u003c/li\u003e \u003c/ul\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec4\" class=\"Section2\"\u003e \u003ch2\u003e2.2. Identification of Vine-Matthews Stripes and Structural Offsets\u003c/h2\u003e \u003cp\u003eGeospatial analysis identifies five clusters of linear magnetic anomalies within the Central and Southern provinces (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ef). These elongated signatures features are interpreted as Vine-Matthews stripes, characterized by strike-parallel continuity with approximate lengths of 220 km, 220 km, 150 km, and 100 km for Groups 1 through 4, respectively. Group 5 is more fragmented, with magnetic lineations intersected and segmented by small-scale strike-slip structures. These Vine-Matthews-like stripes, representing organized seafloor spreading rather than discrete continental intrusions.\u003c/p\u003e \u003cp\u003eA major structural discontinuity is observed at the Atlantis II Deep (20\u0026deg;30'N), where the gravity anomaly terminates abruptly at the Nakasib Suture Zone (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ee). Across this crustal boundary, the magnetic anomaly axis is laterally offset by approximately 64 km between the northern and southern sub-zones Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ea). This offset aligns spatially with the offshore projection of the onshore Baraka left-lateral suture (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ea and b).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec5\" class=\"Section2\"\u003e \u003ch2\u003e2.3. Stratigraphic Constrain and Magnetic Correlation\u003c/h2\u003e \u003cp\u003eMagnetic profile A\u0026ndash;A\u0026prime; reveals a sequence of organized polarity reversals extending\u0026thinsp;~\u0026thinsp;250 km in width and ~\u0026thinsp;220 km along strike beneath the Miocene S-reflector (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003eb, e). Assuming a half-spreading rate of ~\u0026thinsp;1 cm/yr (Vine, 1966), the identified magnetic sequence corresponds to a spreading duration of approximately 12.5 Ma. When calibrated against the ~\u0026thinsp;5 Ma age of the S-reflector, this yields a minimum crustal age of ~\u0026thinsp;17.5 Ma.\u003c/p\u003e \u003cp\u003eCorrelation with the geomagnetic polarity timescale (GSA, 2022; Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ee) shows agreement over a\u0026thinsp;~\u0026thinsp;12 Ma interval spanning chrons C20 to C24. Stratigraphic data from the Jeddah-1 well further document\u0026thinsp;~\u0026thinsp;100 m of volcanic sequences within the Eocene interval.\u003c/p\u003e \u003c/div\u003e"},{"header":"3. Discussion","content":"\u003cp\u003eThe southern Red Sea axial ridge is characterized by straight-sided bathymetric troughs(Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ed). Although some models have proposed widespread oceanic crust extending back to ~\u0026thinsp;40 Ma, such interpretations are difficult to reconcile with regional stratigraphic relationships, as they would require Jurassic formations to overlie Eocene oceanic crust. Synthesized potential-field data indicate that dense, high-gravity crustal material is confined to the Median Ridge Valley (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ee). Southward-propagating oceanic crust terminates near 20\u0026deg;30\u0026prime;N, coincident with the Nakasib Suture Zone. This geometry suggests that active oceanization in the southern Red Sea is restricted to the axial trough and was strongly influenced by early plume-lithosphere interaction associated with Afar magmatism.\u003c/p\u003e \u003cp\u003eMoving into the central province, the study provides key evidence for a domain-based evolutionary model. The presence of organized magnetic lineations beneath the undisturbed Miocene S-reflector indicates that oceanic crust formation predates the Pliocene. Application of spreading-rate constraints to profile A-A\u0026prime; yields a minimum age of ~\u0026thinsp;17.5 Ma, significantly older than the 2\u0026ndash;3 Ma ages proposed for isolated \u0026ldquo;oceanization cells\u0026rdquo; in earlier models (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003eb and e). This province is laterally segmented by a\u0026thinsp;~\u0026thinsp;64 km offset at the Atlantis II Deep (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ea). The spatial correspondence between this offset and the offshore projection of the Baraka Suture suggests that inherited Precambrian structures exerted a first-order control on rift segmentation and lateral displacement during Red Sea evolution. Volcanic sequences encountered in the Jeddah-1 well likely reflect localized magmatic activity associated with this transitional domain.\u003c/p\u003e \u003cp\u003eIn contrast, the northern Red Sea retains the characteristics of an amagmatic continental rift. Preservation of pre-rift stratigraphy and seismic velocities below 6.4 km/s are consistent with continental basement rather than oceanic crust. Discrete, low-amplitude magnetic anomalies are interpreted as signatures of diffuse extension. Previous interpretations of oceanic crust based solely on seismic velocity and density are non-unique. Comparable velocity signatures could arise from the heterogeneous Neoproterozoic basement assemblages of the Egyptian Eastern Desert if submerged and imaged under similar acquisition conditions. Consequently, seismic velocity alone is insufficient to uniquely diagnose oceanic crust in the absence of organized magnetic lineations.\u003c/p\u003e \u003cp\u003eSynthesizing these observations, the integrated geological and geophysical evidence indicates that Red Sea crustal evolution is segmented and strongly influenced by inherited Precambrian architecture (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ec). Three distinct evolutionary domains are recognized: axial-restricted oceanic spreading in the South bounded by the Nakasib Suture; ancient oceanic crust (minimum\u0026thinsp;~\u0026thinsp;17.5 Ma) in the Central province segmented by inherited sutures; and continental rifting in the North governed by Neoproterozoic basement grain and the Aqaba\u0026ndash;Dead Sea transform system. Collectively, these findings indicate that the Red Sea behaves as a segmented rift in which the timing and geometry of crustal growth are strongly influenced by the inherited architecture of the Arabian\u0026ndash;Nubian Shield.\u003c/p\u003e"},{"header":"4. Methodology","content":"\u003cp\u003eTo address inconsistencies among existing tectonic models, this study employs a multi-proxy geospatial integration workflow. Five independent datasets were compiled into a single, fully georeferenced database to enable consistent spatial comparison and identification of crustal domains across the Red Sea basin.\u003c/p\u003e \u003cdiv id=\"Sec8\" class=\"Section2\"\u003e \u003ch2\u003e4.1. Potential Field Analysis\u003c/h2\u003e \u003cp\u003eGravity and magnetic anomaly maps were analyzed to delineate the Median Ridge Valley (MRV) and to identify lateral offsets, lineations, and anomaly terminations (Figs.\u0026nbsp;1and b; Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ef; Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ea). Magnetic data were also examined for the presence of elongated anomaly patterns consistent with organized seafloor spreading.\u003c/p\u003e \u003cp\u003e \u003cb\u003eCriteria for Magnetic Stripe Identification\u003c/b\u003e \u003c/p\u003e \u003cp\u003eMagnetic stripes were identified following the conceptual framework of [\u003cspan citationid=\"CR13\" class=\"CitationRef\"\u003e13\u003c/span\u003e] Stripe identification was based on three criteria: (1) linearity, (2) bilateral symmetry, and (3) organized polarity alternation (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ef). On georeferenced magnetic intensity maps, these features appear as elongated, strike-parallel bands of alternating positive and negative anomalies. These patterns were distinguished from isolated magmatic intrusions, which typically present as discrete, high-amplitude, circular or irregular anomaly clusters with limited lateral continuity. Whereas intrusions represent localized magmatic events, magnetic stripes record successive geomagnetic polarity reversals during sustained crustal accretion.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec9\" class=\"Section2\"\u003e \u003ch2\u003e4.2. Qualitative Geophysical Interpretation\u003c/h2\u003e \u003cp\u003eGravity and magnetic datasets were interpreted qualitatively by examining lateral variations in anomaly character and their spatial correspondence with mapped tectonic domains and inherited structures (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ea-f; Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ea). Interpretation was conducted within a comparative spatial framework, emphasizing anomaly continuity, termination, and offset, rather than through forward or inverse numerical modeling.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec10\" class=\"Section2\"\u003e \u003ch2\u003e4.3. Seismic Velocity Compilation\u003c/h2\u003e \u003cp\u003eA\u0026thinsp;~\u0026thinsp;1900 km composite seismic refraction profile was reconstructed from VEMA-Atlantis datasets (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ec; Fig.\u0026nbsp;\u003cspan refid=\"Fig4\" class=\"InternalRef\"\u003e2\u003c/span\u003e). Crustal types were categorized based on velocities, with values exceeding 6.4 km/s classified as oceanic or intrusive crust and velocities below 6.4 km/s classified as continental crust. These seismic observations were used as independent constraints to evaluate interpretations derived from potential field data.\u003c/p\u003e \u003cp\u003e \u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec11\" class=\"Section2\"\u003e \u003ch2\u003e4.4. Bathymetric Analysis\u003c/h2\u003e \u003cp\u003eBathymetric data were analyzed to characterize axial trough morphology, basin segmentation, and depth variations along the rift axis (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ec-d). Bathymetry was incorporated into the geospatial database and evaluated alongside gravity and magnetic datasets to assess correspondence between surface morphology and subsurface geophysical signatures.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec12\" class=\"Section2\"\u003e \u003ch2\u003e4.5. Tectonic Inheritance Mapping\u003c/h2\u003e \u003cp\u003eOnshore Precambrian suture zones, including the Nakasib and Sol Hamid sutures, were projected offshore to assess their spatial relationships with geophysical anomalies and rift segmentation patterns (Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ee; Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003ea-b). A synthesized geological map was used to delineate inherited terranes, suture zones, and exposed crustal domains.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec13\" class=\"Section2\"\u003e \u003ch2\u003e4.6. Magnetic Spreading Correlation\u003c/h2\u003e \u003cp\u003eA half-spreading rate of 1 cm/yr (Vine, 1966) was applied to a newly identified\u0026thinsp;~\u0026thinsp;250 km magnetic profile (A-A\u0026prime;) in the central Red Sea (Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003eb, e) to evaluate potential spreading durations represented by the observed anomaly sequences.\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec14\" class=\"Section2\"\u003e \u003ch2\u003e4.7. Stratigraphic Integration\u003c/h2\u003e \u003cp\u003eThe Miocene S-reflector (~\u0026thinsp;5 Ma) and stratigraphic data from the Jeddah-1 well (location shown in Fig.\u0026nbsp;\u003cspan refid=\"Fig1\" class=\"InternalRef\"\u003e1\u003c/span\u003ec) were used as chronological reference horizons to calibrate the relative timing of the identified magnetic anomaly sequences (Fig.\u0026nbsp;\u003cspan refid=\"Fig2\" class=\"InternalRef\"\u003e3\u003c/span\u003ef; Fig.\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003eb).\u003c/p\u003e \u003c/div\u003e \u003cdiv id=\"Sec15\" class=\"Section2\"\u003e \u003ch2\u003e4.8. Geospatial Integration Framework\u003c/h2\u003e \u003cp\u003eA central component of the methodology was the strict geospatial integration of all datasets within a high-resolution, unified coordinate system. This approach ensured spatial consistency among geological, geophysical, bathymetric, seismic, and stratigraphic observations, allowing systematic evaluation of spatial correspondence and mismatch across datasets. Figure\u0026nbsp;\u003cspan refid=\"Fig3\" class=\"InternalRef\"\u003e4\u003c/span\u003e summarizes this integration framework and illustrates how dataset coherence was assessed without assuming uniform spreading along the rift axis.\u003c/p\u003e \u003c/div\u003e"},{"header":"Declarations","content":" \u003ch2\u003eCompeting interests\u003c/h2\u003e \u003cp\u003eThe authors declare no competing interests.\u003c/p\u003e \u003c/p\u003e\u003ch2\u003eFunding:\u003c/h2\u003e \u003cp\u003eNo funding.\u003c/p\u003e\u003ch2\u003eAuthor Contribution\u003c/h2\u003e\u003cp\u003eKF: Conceptualization, Methodology, Data Acquisition, Formal Analysis, and Writing-Original Draft. AE: Data Curation, Writing-Review \\\u0026amp; Editing, and Technical Supervision.\u003c/p\u003e\u003ch2\u003eAcknowledgement\u003c/h2\u003e \u003cp\u003eWe thank Mr. Dia Mahmoud, GEOPEX Ltd. and Dr. Hussein Hammouda, Ex-Chairman of Egyptian Mineral Resources Authority, for their help in digitizing the old Red Sea magnetic and gravity paper sheets. Special thanks to the late Dr. Wafik Mishrif for his support and encouragement in collecting most of magnetic and gravity sheets over Gulf of Suez and Red Sea. Thanks to The National Geophysical Data Center (NGDC) for delivering the copy of gravity and magnetic data acquired over Red Sea. Thanks to Dr. Hans A. Roeser for providing his own gravity and magnetic material of 1975, 1976 and 1980.\u003c/p\u003e\u003ch2\u003eData Availability\u003c/h2\u003e\u003cp\u003eThe regional geophysical datasets supporting the findings of this study are publicly available. Potential field and bathymetric data were integrated from the NOAA National Centers for Environmental Information (https://www.ngdc.noaa.gov), the UCSD Topographic/Bathymetric database (https://topex.ucsd.edu), and the World Digital Magnetic Anomaly Map (WDMAM v2.1) repository (http://www.wdmam.org). Specific processed datasets or geospatial integrations generated during the current study are available from the corresponding author upon reasonable request.\u003c/p\u003e"},{"header":"References","content":"\u003col\u003e\u003cli\u003e\u003cspan\u003eVon Triulzi, A. E. \u003cem\u003eDenkschr Akad. Wiss Wien Math. -Nat Kl\u003c/em\u003e \u003cb\u003e65\u003c/b\u003e, 131 (1898).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eVening Meinesz, F. A. \u003cem\u003eGravity expeditions at sea, 1923\u0026ndash;1932, Vol. II\u003c/em\u003e (Netherlands Geodetic Commission, 1934). \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.54419/3us2nj\u003c/span\u003e\u003cspan address=\"10.54419/3us2nj\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eFarquharson, W. I. Topography, with an appendix on magnetic observations. \u003cem\u003eSci. Rep. John Murray Expedition\u003c/em\u003e. \u003cb\u003e1933-34\u003c/b\u003e (1), 43\u0026ndash;61 (1935).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eOwen, L. Origin of the Red Sea depression. \u003cem\u003eAAPG Bull.\u003c/em\u003e \u003cb\u003e22\u003c/b\u003e, 1217\u0026ndash;1223. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1306/3d932fe0-16b1-11d7-8645000102c1865d\u003c/span\u003e\u003cspan address=\"10.1306/3d932fe0-16b1-11d7-8645000102c1865d\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1938).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGirdler, R. W. The relationship of the Red Sea to the East African Rift System. \u003cem\u003eQ. J. Geol. Soc. Lond.\u003c/em\u003e \u003cb\u003e114\u003c/b\u003e, 79\u0026ndash;105. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1144/gsjgs.114.1.0079\u003c/span\u003e\u003cspan address=\"10.1144/gsjgs.114.1.0079\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1958).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eTazieff, H. Une recente campagne oceanographique dans la mer Rouge. \u003cem\u003eBull. Soc. Belge Geol.\u003c/em\u003e \u003cb\u003e61\u003c/b\u003e, 84\u0026ndash;90 (1952).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGirdler, R. W. \u0026amp; Harrison, J. C. Submarine gravity measurements in the Atlantic, Indian Ocean, Red Sea and Mediterranean Sea. \u003cem\u003eProc. R. Soc. Lond. A\u003c/em\u003e 239, 202 (1957). \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1098/rspa.1957.0033\u003c/span\u003e\u003cspan address=\"10.1098/rspa.1957.0033\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eQuennell, A. M. Tectonics of the Dead Sea rift. \u003cem\u003eInt. Geol. Congr\u003c/em\u003e. \u003cb\u003e20\u003c/b\u003e, 385\u0026ndash;405 (1956).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eQuennell, A. M. Tectonics of the Dead Sea rift. \u003cem\u003eAssoc Afr. Geol. Surv\u003c/em\u003e 385\u0026ndash;408 (1959).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eCarey, S. W. A tectonic approach to continental drift. in \u003cem\u003eContinental Drift: A Symposium\u003c/em\u003e 177\u0026ndash;355University of Tasmania, Hobart, (1958).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eDrake, C. L., Girdler, R. W. \u0026amp; Landisman, M. Geophysical measurements in the Red Sea. \u003cem\u003eProc. Int. Oceanogr. Congr.\u003c/em\u003e 20 (1959).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGirdler, R. W. \u0026amp; Peter, G. An example of the importance of natural remanent magnetization in the interpretation of magnetic anomalies. \u003cem\u003eGeophys. Prospect.\u003c/em\u003e \u003cb\u003e8\u003c/b\u003e, 474\u0026ndash;483. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1111/j.1365-2478.1960.tb01730.x\u003c/span\u003e\u003cspan address=\"10.1111/j.1365-2478.1960.tb01730.x\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1960).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eVine, F. J. \u0026amp; Matthews, D. H. Magnetic anomalies over ocean ridges. \u003cem\u003eNature\u003c/em\u003e \u003cb\u003e199\u003c/b\u003e, 947\u0026ndash;949. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1038/199947a0\u003c/span\u003e\u003cspan address=\"10.1038/199947a0\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1963).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eVine, F. J. Spreading of the ocean floor: New evidence. \u003cem\u003eScience\u003c/em\u003e \u003cb\u003e154\u003c/b\u003e, 1405\u0026ndash;1415. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1126/science.154.3755.1405\u003c/span\u003e\u003cspan address=\"10.1126/science.154.3755.1405\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1966).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eDrake, C. L. \u0026amp; Girdler, R. W. A geophysical study of the Red Sea. \u003cem\u003eGeophys. J.\u003c/em\u003e \u003cb\u003e8\u003c/b\u003e, 473\u0026ndash;495. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1111/j.1365-246X.1964.tb06303.x\u003c/span\u003e\u003cspan address=\"10.1111/j.1365-246X.1964.tb06303.x\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1964).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eWilson, J. T. Transform faults, oceanic ridges and magnetic anomalies southwest of Vancouver Island. \u003cem\u003eScience\u003c/em\u003e \u003cb\u003e150\u003c/b\u003e, 482\u0026ndash;485. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1126/science.150.3695.482\u003c/span\u003e\u003cspan address=\"10.1126/science.150.3695.482\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1965).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eAllan, T. D. A Bathymetric Chart of the Red Sea. \u003cem\u003eInt. Hydrogr. Rev.\u003c/em\u003e \u003cb\u003e43\u003c/b\u003e, 33\u0026ndash;36 (1966).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eKnott, S. T., Bunce, E. T. \u0026amp; Chase, R. L. Red Sea seismic reflection studies. \u003cem\u003eGeol Surv. Can. Pap 66 \u0026ndash; 14\u003c/em\u003e. 33\u0026ndash;61. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.4095/103358\u003c/span\u003e\u003cspan address=\"10.4095/103358\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1966).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGirdler, R. W. Earth satellites, terrestrial heat flow, mantle convection and the location of extensional and compressional features on the Earth\u0026rsquo;s surface. \u003cem\u003eProc. Geol. Assoc.\u003c/em\u003e 78, 165\u0026ndash;178 (1967). \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/s0016-7878(67)80042-7\u003c/span\u003e\u003cspan address=\"10.1016/s0016-7878(67)80042-7\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eTramontini, C. \u0026amp; Davies, D. Seismic refraction survey in the Red Sea. \u003cem\u003eGeophys. J.\u003c/em\u003e \u003cb\u003e17\u003c/b\u003e, 225\u0026ndash;241. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1111/j.1365-246x.1969.tb02323.x\u003c/span\u003e\u003cspan address=\"10.1111/j.1365-246x.1969.tb02323.x\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1969).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003ePhillips, J. D., Woodside, J. \u0026amp; Bowin, C. O. Magnetic and gravity anomalies in the central Red Sea. in Hot Brines and Recent Heavy Metal Deposits in the Red Sea 98\u0026ndash;113 (Springer, \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1007/978-3-662-28603-6_10\u003c/span\u003e\u003cspan address=\"10.1007/978-3-662-28603-6_10\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1969).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eAbdel-Gawad, M. Geological structures of the Red Sea area inferred from satellite pictures. in \u003cem\u003eHot Brines and Recent Heavy Metal Deposits in the Red Sea\u003c/em\u003e 25\u0026ndash;37 (Springer, 1969). \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1007/978-3-662-28603-6_5\u003c/span\u003e\u003cspan address=\"10.1007/978-3-662-28603-6_5\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003ePhillips, J. \u0026amp; Ross, D. A. Continuous seismic reflection profiles in the Red Sea. \u003cem\u003ePhilos. Trans. R Soc. Lond. A\u003c/em\u003e. \u003cb\u003e267\u003c/b\u003e, 143\u0026ndash;152. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1098/RSTA.1970.0029\u003c/span\u003e\u003cspan address=\"10.1098/RSTA.1970.0029\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1970).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eAllan, T. D. Magnetic and gravity fields over the Red Sea. \u003cem\u003ePhilos. Trans. R Soc. Lond. A\u003c/em\u003e. \u003cb\u003e261\u003c/b\u003e, 153\u0026ndash;180. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1098/rsta.1970.0030\u003c/span\u003e\u003cspan address=\"10.1098/rsta.1970.0030\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1970).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGirdler, R. W. A review of Red Sea heat flow. \u003cem\u003ePhilos. Trans. R Soc. Lond. A\u003c/em\u003e. \u003cb\u003e267\u003c/b\u003e, 359\u0026ndash;368. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1098/rsta.1970.0032\u003c/span\u003e\u003cspan address=\"10.1098/rsta.1970.0032\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1970).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eMcKenzie, D. P., Davies, D. \u0026amp; Molnar, P. Plate tectonics of the Red Sea and East Africa. \u003cem\u003eNature\u003c/em\u003e \u003cb\u003e226\u003c/b\u003e, 243\u0026ndash;248. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1038/226243a0\u003c/span\u003e\u003cspan address=\"10.1038/226243a0\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1970).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eLowell, J. D. \u0026amp; Genik, G. J. Sea-floor spreading and structural evolution of the southern Red Sea. \u003cem\u003eAAPG Bull.\u003c/em\u003e \u003cb\u003e56\u003c/b\u003e, 247\u0026ndash;259. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1306/819a3e56-16c5-11d7-8645000102c1865d\u003c/span\u003e\u003cspan address=\"10.1306/819a3e56-16c5-11d7-8645000102c1865d\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1972).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eStieltjes, L. Evolution tectonique recente du rift d\u0026rsquo;Asal. \u003cem\u003eRev. Geogr. Phys. Geol. Dyn.\u003c/em\u003e \u003cb\u003e15\u003c/b\u003e, 425\u0026ndash;436 (1973).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eStoffers, P. \u0026amp; Ross, D. A. Sedimentary history of the Red Sea. \u003cem\u003eWoods Hole Oceanogr. Inst. Contrib.\u003c/em\u003e 3168, 849\u0026ndash;865 (1974). \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.2973/dsdp.proc.23.123.1974\u003c/span\u003e\u003cspan address=\"10.2973/dsdp.proc.23.123.1974\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eRoger, C., Searle, R. \u0026amp; Ross, D. A. Geophysical study of the Red Sea axial trough. \u003cem\u003eGeophys. J. R Astron. Soc.\u003c/em\u003e \u003cb\u003e43\u003c/b\u003e, 555\u0026ndash;572. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1111/j.1365-246x.1975.tb00647.x\u003c/span\u003e\u003cspan address=\"10.1111/j.1365-246x.1975.tb00647.x\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1975).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGirdler, R. W. \u0026amp; Styles, P. Two-stage Red Sea floor spreading. \u003cem\u003eNature\u003c/em\u003e 247, 7\u0026ndash;11 [Note: User provided 330, but 1974 article is Vol 247]. (1974). \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1038/247007a0\u003c/span\u003e\u003cspan address=\"10.1038/247007a0\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eRoeser, H. A. Detailed magnetic survey of the southern Red Sea. \u003cem\u003eGeol. Jahrb\u003c/em\u003e. \u003cb\u003e13\u003c/b\u003e, 131\u0026ndash;153 (1975).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGettings, M. E. Delineation of the continental margin of the southern Red Sea from new gravity evidence. \u003cem\u003eSaudi Arab. Dir. Gen. Min. Res. Bull.\u003c/em\u003e \u003cb\u003e2\u003c/b\u003e, K1\u0026ndash;K11 (1977).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGirdler, R. W. \u0026amp; Southren, T. Structure and evolution of the northern Red Sea. \u003cem\u003eNature\u003c/em\u003e \u003cb\u003e330\u003c/b\u003e, 716\u0026ndash;721. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1038/330716a0\u003c/span\u003e\u003cspan address=\"10.1038/330716a0\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1987).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eLe Pichon, X. \u0026amp; Francheteau, J. Plate tectonic analysis of the Red Sea\u0026ndash;Gulf of Aden area. \u003cem\u003eTectonophysics\u003c/em\u003e \u003cb\u003e46\u003c/b\u003e, 369\u0026ndash;406. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/0040-1951(78)90214-7\u003c/span\u003e\u003cspan address=\"10.1016/0040-1951(78)90214-7\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1978).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGirdler, R. W., Brown, C., Noy, D. J. M. \u0026amp; Styles, P. Geophysical survey of the westernmost Gulf of Aden. \u003cem\u003ePhilos. Trans. R Soc. Lond. A\u003c/em\u003e. \u003cb\u003e298\u003c/b\u003e, 1\u0026ndash;43. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1098/rsta.1980.0239\u003c/span\u003e\u003cspan address=\"10.1098/rsta.1980.0239\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1980).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eLaBrecque, J., Kent, D. V. \u0026amp; Cande, S. C. Revised magnetic polarity time scale for Late Cretaceous and Cenozoic time. \u003cem\u003eGeology\u003c/em\u003e \u003cb\u003e5\u003c/b\u003e, 330\u0026ndash;335. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1130/0091-7613(1977)5%3C330:rmptsf%3E2.0.co;2\u003c/span\u003e\u003cspan address=\"10.1130/0091-7613(1977)5%3C330:rmptsf%3E2.0.co;2\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1977).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eBrown, C. \u0026amp; Girdler, R. W. Structure of the Red Sea at 20\u0026deg; N from gravity data and its implications for continental margins. \u003cem\u003eNature\u003c/em\u003e \u003cb\u003e298\u003c/b\u003e, 51\u0026ndash;53. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1038/298051a0\u003c/span\u003e\u003cspan address=\"10.1038/298051a0\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1982).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eCourtillot, V. Propagating rifts and continental breakup. \u003cem\u003eTectonics\u003c/em\u003e \u003cb\u003e1\u003c/b\u003e, 239\u0026ndash;250. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1029/TC001i003p00239\u003c/span\u003e\u003cspan address=\"10.1029/TC001i003p00239\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1982).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eCochran, J. R. A model for development of Red Sea. \u003cem\u003eAAPG Bull.\u003c/em\u003e \u003cb\u003e67\u003c/b\u003e, 41\u0026ndash;69. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1306/03B5ACBE-16D1-11D7-8645000102C1865D\u003c/span\u003e\u003cspan address=\"10.1306/03B5ACBE-16D1-11D7-8645000102C1865D\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1983).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eBonatti, E., Colantoni, P., Della Vedova, B. \u0026amp; Taviani, M. Geology of the Red Sea transitional region (22\u0026deg; N\u0026ndash;25\u0026deg; N). \u003cem\u003eOceanol. Acta\u003c/em\u003e. \u003cb\u003e7\u003c/b\u003e, 385\u0026ndash;398 (1984).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGirdler, R. W. Problems concerning the evolution of oceanic lithosphere in the northern Red Sea. \u003cem\u003eTectonophysics\u003c/em\u003e \u003cb\u003e116\u003c/b\u003e, 109\u0026ndash;122. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/0040-1951(85)90224-0\u003c/span\u003e\u003cspan address=\"10.1016/0040-1951(85)90224-0\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1985).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eLaBrecque, J. L. \u0026amp; Zitellini, N. Continuous seafloor spreading in the Red Sea. \u003cem\u003eAAPG Bull.\u003c/em\u003e \u003cb\u003e69\u003c/b\u003e, 513\u0026ndash;524. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1306/AD46251F-16F7-11D7-8645000102C1865D\u003c/span\u003e\u003cspan address=\"10.1306/AD46251F-16F7-11D7-8645000102C1865D\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1985).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eBicknell, J. D. et al. Tectonics of the Nereus Deep, Red Sea: A deep-tow investigation of a site of initial rifting. \u003cem\u003eJ. Geophys. Res.\u003c/em\u003e \u003cb\u003e91\u003c/b\u003e, 131\u0026ndash;148. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1007/bf00338225\u003c/span\u003e\u003cspan address=\"10.1007/bf00338225\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1986).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eBonatti, E. Rifting or drifting in the Red Sea? \u003cem\u003eNature\u003c/em\u003e \u003cb\u003e330\u003c/b\u003e, 962\u0026ndash;963. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1038/330692a0\u003c/span\u003e\u003cspan address=\"10.1038/330692a0\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1987).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eIzzeldin, A. Y. Seismic, gravity and magnetic surveys in the central part of the Red Sea. \u003cem\u003eTectonophysics\u003c/em\u003e \u003cb\u003e143\u003c/b\u003e, 269\u0026ndash;306. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/0040-1951(87)90214-9\u003c/span\u003e\u003cspan address=\"10.1016/0040-1951(87)90214-9\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1987).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eJoffe, S. \u0026amp; Garfunkel, Z. Plate kinematics of the circum\u0026ndash;Red Sea: A re-evaluation. \u003cem\u003eTectonophysics\u003c/em\u003e \u003cb\u003e141\u003c/b\u003e, 5\u0026ndash;23. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/0040-1951(87)90171-5\u003c/span\u003e\u003cspan address=\"10.1016/0040-1951(87)90171-5\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1987).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGaulier, J. M. et al. Seismic study of the crust of the northern Red Sea and Gulf of Suez. \u003cem\u003eTectonophysics\u003c/em\u003e \u003cb\u003e153\u003c/b\u003e, 55\u0026ndash;88. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/0040-1951(88)90007-8\u003c/span\u003e\u003cspan address=\"10.1016/0040-1951(88)90007-8\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1988).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eMartinez, F. \u0026amp; Cochran, J. R. Structure and tectonics of the northern Red Sea. \u003cem\u003eTectonophysics\u003c/em\u003e \u003cb\u003e150\u003c/b\u003e, 1\u0026ndash;32. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/0040-1951(88)90293-4\u003c/span\u003e\u003cspan address=\"10.1016/0040-1951(88)90293-4\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1988).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eIzzeldin, A. Y. Transverse structures in the central Red Sea and implications for early oceanic accretion. \u003cem\u003eGeophys. J.\u003c/em\u003e \u003cb\u003e96\u003c/b\u003e, 117\u0026ndash;129. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1111/j.1365-246X.1989.tb05254.x\u003c/span\u003e\u003cspan address=\"10.1111/j.1365-246X.1989.tb05254.x\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1989).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGuennoc, P., Pautot, G., Le Quentrec, M. F. \u0026amp; Coutelle, A. Structure of an early oceanic rift in the northern Red Sea. \u003cem\u003eOceanol. Acta\u003c/em\u003e. \u003cb\u003e13\u003c/b\u003e, 145\u0026ndash;155 (1990).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eUchupi, E. \u0026amp; Ross, D. A. Springer,. The geologic enigma of the Red Sea rift. in \u003cem\u003eFacets of Modern Biogeochemistry\u003c/em\u003e 52\u0026ndash;61 (1990).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eGirdler, R. W. The case for oceanic crust beneath the Red Sea. \u003cem\u003eTectonophysics\u003c/em\u003e \u003cb\u003e198\u003c/b\u003e, 275\u0026ndash;278. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/0040-1951(91)90155-L\u003c/span\u003e\u003cspan address=\"10.1016/0040-1951(91)90155-L\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1991).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eMakris, J. \u0026amp; Rihm, R. Shear-controlled evolution of the Red Sea. \u003cem\u003eTectonophysics\u003c/em\u003e \u003cb\u003e198\u003c/b\u003e, 441\u0026ndash;466. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/0040-1951(91)90166-p\u003c/span\u003e\u003cspan address=\"10.1016/0040-1951(91)90166-p\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1991).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eMakris, J. \u0026amp; Henke, C. H. Pull-apart evolution of the Red Sea. \u003cem\u003eJ. Petrol. Geol.\u003c/em\u003e \u003cb\u003e15\u003c/b\u003e, 127\u0026ndash;134. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1111/j.1747-5457.1992.tb00958.x\u003c/span\u003e\u003cspan address=\"10.1111/j.1747-5457.1992.tb00958.x\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (1992).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eBosworth, W. et al. Stratigraphic and structural evolution of Zabargad Island (Red Sea, Egypt) since the Early Cretaceous. \u003cem\u003eProc. 3rd Int. Conf. Geol. Arab World, Cairo Univ.\u003c/em\u003e 161\u0026ndash;190 (1996).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eBosworth, W. \u0026amp; McClay, K. R. Structural and stratigraphic evolution of the Gulf of Suez Rift, Egypt. in \u003cem\u003ePeri-Tethys Memoir 6\u003c/em\u003e 567\u0026ndash;606Springer, (2001).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eCochran, J. R. Northern Red Sea: Nucleation of an oceanic spreading center within a continental rift. \u003cem\u003eGeochem. Geophys. Geosyst.\u003c/em\u003e \u003cb\u003e6\u003c/b\u003e, Q03006. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1029/2004gc000826\u003c/span\u003e\u003cspan address=\"10.1029/2004gc000826\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (2005).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eBosworth, W. Geological evolution of the Red Sea: Historical background, review, and synthesis. \u003cem\u003eSpringer Earth Syst. Sci.\u003c/em\u003e 45\u0026ndash;78. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1007/978-3-662-45201-1_3\u003c/span\u003e\u003cspan address=\"10.1007/978-3-662-45201-1_3\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (2015).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eBosworth, W. \u0026amp; Stockli, D. F. Early magmatism in the greater Red Sea. \u003cem\u003eCan. J. Earth Sci.\u003c/em\u003e \u003cb\u003e53\u003c/b\u003e, 1158\u0026ndash;1176. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1139/cjes-2016-0019\u003c/span\u003e\u003cspan address=\"10.1139/cjes-2016-0019\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (2016).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eBlanchette, A. R., Klemperer, S. L., Mooney, W. D. \u0026amp; Zahran, H. M. Two-stage Red Sea rifting inferred from mantle earthquakes in Neoproterozoic lithosphere. \u003cem\u003eEarth Planet. Sci. Lett.\u003c/em\u003e \u003cb\u003e497\u003c/b\u003e, 92\u0026ndash;101. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/j.epsl.2018.05.048\u003c/span\u003e\u003cspan address=\"10.1016/j.epsl.2018.05.048\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (2018).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eBosworth, W., Khalil, S. M., Ligi, M., Stockli, D. F. \u0026amp; McClay, K. R. The northern Red Sea. in Geology of Egypt 344\u0026ndash;369 (Springer, \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1007/978-3-030-15265-9_9\u003c/span\u003e\u003cspan address=\"10.1007/978-3-030-15265-9_9\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (2020).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eIssachar, R., Ebbing, J. \u0026amp; Dilixiati, Y. New magnetic anomaly map for the Red Sea reveals transtensional structures associated with rotational rifting. \u003cem\u003eSci. Rep.\u003c/em\u003e \u003cb\u003e12\u003c/b\u003e, 5757. \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1038/s41598-022-09770-0\u003c/span\u003e\u003cspan address=\"10.1038/s41598-022-09770-0\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (2022).\u003c/span\u003e\u003c/li\u003e \u003cli\u003e\u003cspan\u003eDelaunay, A. et al. Structure and morphology of the Red Sea, from the mid-ocean ridge to the ocean-continent boundary. \u003cem\u003eTectonophysics\u003c/em\u003e \u003cb\u003e849\u003c/b\u003e \u003cspan class=\"ExternalRef\"\u003e\u003cspan class=\"RefSource\"\u003ehttps://doi.org/10.1016/j.tecto.2023.229728\u003c/span\u003e\u003cspan address=\"10.1016/j.tecto.2023.229728\" targettype=\"DOI\" class=\"RefTarget\"\u003e\u003c/span\u003e\u003c/span\u003e (2023).\u003c/span\u003e\u003c/li\u003e\u003c/ol\u003e"}],"fulltextSource":"","fullText":"","funders":[],"hasAdminPriorityOnWorkflow":false,"hasManuscriptDocX":true,"hasOptedInToPreprint":true,"hasPassedJournalQc":"","hasAnyPriority":false,"hideJournal":true,"highlight":"","institution":"","isAcceptedByJournal":false,"isAuthorSuppliedPdf":false,"isDeskRejected":"","isHiddenFromSearch":true,"isInQc":false,"isInWorkflow":false,"isPdf":false,"isPdfUpToDate":true,"isWithdrawnOrRetracted":false,"journal":{"display":true,"email":"[email protected]","identity":"researchsquare","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":true,"externalIdentity":"","sideBox":"","snPcode":"","submissionUrl":"/submission","title":"Research Square","twitterHandle":"researchsquare","acdcEnabled":true,"dfaEnabled":false,"editorialSystem":"","reportingPortfolio":"","inReviewEnabled":false,"inReviewRevisionsEnabled":true},"keywords":"Red Sea, Seafloor Spreading, Magnetic Stripes, Structural Inheritance, Arabian-Nubian Shield","lastPublishedDoi":"10.21203/rs.3.rs-8819895/v1","lastPublishedDoiUrl":"https://doi.org/10.21203/rs.3.rs-8819895/v1","license":{"name":"CC BY 4.0","url":"https://creativecommons.org/licenses/by/4.0/"},"manuscriptAbstract":"\u003cp\u003eThe propagation of the Red Sea continental margin remains unevaluated. Despite the unanimous agreement that the southern Red Sea axial ridge valley is underlain by juvenile oceanic crust, there is a lack of such agreement for the central and northern Red Sea. Significant issues relating to Red Sea tectonics are whether the Arabian and Nubian plates have been completely separated (i.e., oceanic crust lies beneath the Red Sea from coast to coast) or if the oceanic crust is restricted to the Red Sea median valley. Here, we interpret a new spreading span of at least 12.5 Ma of magnetic anomaly stripes located in the Central Red Sea, which represent ancient seafloor spreading. We show that the Red Sea basement structure exhibits different fault trends, wherein the Red Sea crust is controlled by offshore inherited Precambrian suture zones. Both these infrastructure suture zones and the Dead Sea-Aqaba-transform faults control the Red Sea crustal evolution.\u003c/p\u003e","manuscriptTitle":"A Domain-Based Evolution Model for Red Sea: New Sea-Floor Spreading Evidence","msid":"","msnumber":"","nonDraftVersions":[{"code":1,"date":"2026-02-23 15:19:11","doi":"10.21203/rs.3.rs-8819895/v1","editorialEvents":[{"type":"communityComments","content":0}],"status":"published","journal":{"display":true,"email":"[email protected]","identity":"researchsquare","isNatureJournal":false,"hasQc":true,"allowDirectSubmit":true,"externalIdentity":"","sideBox":"","snPcode":"","submissionUrl":"/submission","title":"Research Square","twitterHandle":"researchsquare","acdcEnabled":true,"dfaEnabled":false,"editorialSystem":"","reportingPortfolio":"","inReviewEnabled":false,"inReviewRevisionsEnabled":true}}],"origin":"","ownerIdentity":"baa84087-6f85-496f-9b77-88945b2e63e1","owner":[],"postedDate":"February 23rd, 2026","published":true,"recentEditorialEvents":[],"rejectedJournal":[],"revision":"","amendment":"","status":"posted","subjectAreas":[{"id":63312234,"name":"Earth and environmental sciences/Ocean sciences"},{"id":63312235,"name":"Earth and environmental sciences/Solid earth sciences"}],"tags":[],"updatedAt":"2026-03-16T14:12:58+00:00","versionOfRecord":[],"versionCreatedAt":"2026-02-23 15:19:11","video":"","vorDoi":"","vorDoiUrl":"","workflowStages":[]},"version":"v1","identity":"rs-8819895","journalConfig":"researchsquare"},"__N_SSP":true},"page":"/article/[identity]/[[...version]]","query":{"redirect":"/article/rs-8819895","identity":"rs-8819895","version":["v1"]},"buildId":"XKTyCvWXoU3ODBz1xrDgd","isFallback":false,"isExperimentalCompile":false,"dynamicIds":[84888],"gssp":true,"scriptLoader":[]}