Non-volcanic passive margins (NVPM) constitute one end member of the transitional crustal types that lie beneath passive continental margins; the other end member being volcanic passive margins (VPM). Transitional crust welds continental crust to oceanic crust along the lines of continental break-up. Both VPM and NVPM form during rifting, when a continent rifts to form a new ocean basin. NVPM are different from VPM because of a lack of volcanism. Instead of intrusive magmatic structures, the transitional crust is composed of stretched continental crust and exhumed upper mantle. NVPM are typically submerged and buried beneath thick sediments, so they must be studied using geophysical techniques or drilling. NVPM have diagnostic seismic, gravity, and magnetic characteristics that can be used to distinguish them from VPM and for demarcating the transition between continental and oceanic crust.
Typical characteristics
NVPM are the result of rifting when a continent breaks up to form an ocean, producing transitional crust without volcanism. Extension causes a number of events to occur. First is lithospheric thinning, which allows asthenospheric upwelling; heating further erodes the lithosphere, furthering the thinning process. The extensional forces also cause listric faults and continentward dipping reflectors that help identify NVPM and distinguish them from VPM, characterized by seaward-dipping seismic reflectors. The main difference between NVPM and VPM is that in the latter case, the mantle is hot enough to melt and produce voluminous basalts, whereas in the former case the mantle doesn't melt and there is little or no volcanism. Instead, extension simply pulls the crust away, exposing or "unroofing" the mantle, exposing serpentinized peridotite. The mantle doesn't melt because it is cold or upwells slowly, so there are no igneous rocks like there are in VPM. The basalts and granites are replaced with serpentinized peridotite, accompanied by unique serpentothermal and hydrothermal activity. Increasing density of the lithosphere as it cools and sediment accumulation causes subsidence.
Geophysical properties
Seismic characteristics Seismic reflection lines across passive margins show many structural features common to both VPM and NVPM, such as faulting and crustal thinning, with the primary contra-indicator for volcanism being the presence of continent-ward dipping reflectors. NVPM also display distinct p-wave velocity structures that differentiate them from VPM. Typical NVPM exhibit a high velocity, high gradient lower crust (6.4-7.7 km/s) overlain by a thin, low velocity (4–5 km/s) upper crustal layer. The high velocity shallow layer is usually interpreted as the serpentinized peridotite associated with NVPM. In some cases, an extremely thick igneous underplating of a VPM will display similar P-wave velocity (7.2-7.8 km/s, but with a lower gradient). For this reason, velocity structure alone cannot be used to determine the nature of a margin.
Gravity properties Gravity data provides information about the subsurface density distribution. The most important gravity feature associated with any continent-ocean transition, including NVPM, is the free-air edge effect anomaly, which consists of a gravity high and a gravity low associated with the contrast between the thick continental and thin oceanic crust. There are also subsurface variations in density that cause significant variations across the continent-ocean transition. The crust, as well as the entire lithosphere, is thinned due to mechanical extension. The Moho marks a large density contrast between crust and mantle, typically at least 0.35 g/cm3. The highest amplitudes of the gravity anomaly occur seaward of the continent-ocean transition. High-density upper mantle material is elevated relative to the more landward crustal root. The oceanic crust density is then further enhanced with gabbros and basalts and additionally contributes to the regional gravity trend. Where the thickness of the crust and lithosphere varies, equilibrium must be reached. Isostatic compensation and gravity anomalies result from balance between mass excess of the extra mantle beneath the thinned lithosphere and the overlying low-density crust. Positive gravity anomalies result from the relatively low flexural strength of the lithosphere during the beginning of rifting. As the passive margin matures, the crust and uppermost mantle become colder and stronger, so that the compensating deflection in the base of the lithosphere is broader than the actual rift. Higher flexural strength results in a broadening of the gravity anomaly with time.
Magnetic properties The magnetic signature of a passive continental margin is influenced by the volume of material with a high magnetic susceptibility and the depth of the material below the surface. Large amplitude magnetic anomalies are associated with high magnetic susceptibility (~0.06 emu) igneous rocks of VPM. In contrast, NVPM exhibit only small amplitude anomalies associated with the edge effect at the boundary between the exhumed mantle (~0.003 emu) at the transition zone, and the true oceanic crust basalt (~0.05 emu). This anomaly can be used to locate the boundary between transitional crust and oceanic crust. The absence of large amplitude anomalies is a very strong indication that a margin is non-volcanic.
Formation
Passive rifting Passive rifting, unlike active rifting, occurs principally by extensional tectonic forces as opposed to magmatic forces originating from convection cells or mantle plumes. Isostatic forces allow mantle material to rise under the thinning lithosphere. Subsidence and sedimentation occur during both the initial rifting stage and the post rifting stages. Only after initial rifting does any mantle melting occur. Continued extension of the lithosphere will eventually lead to decompression melting of the mantle and the formation of a mid-ocean ridge. This process results in the creation of an ocean basin, and possibly conjugate NVPM.
Rifting models There are several models for forming NVPM. Passive rifting can follow McKenzie's pure shear model, Wernicke's simple shear model, or a composite model combining features of both, as observed at the Galicia bank NVPM.
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