Volcanic passive margin

The active rift model sees rupture driven by hotspot or mantle plume activity. Upwellings of hot mantle, known as mantle plumes, originate deep in Earth and rise to heat and thin the lithosphere. Heated lithosphere thins, weakens, rises, and finally rifts, Enhanced melting following continental breakup is very important in VPMs, creating thicker than normal oceanic crust of 20 to 40 km thick.[1] Other melts caused by convection related upwelling form reservoirs of magma from which dike swarms and sills eventually radiate to the surface, creating the characteristic seaward dipping lava flows. This model is controversial.[1][2][4][5]

The passive rift model infers that slab pull stretches the lithosphere and thins it. To compensate for lithospheric thinning, asthenosphere upwells, melts due to adiabatic decompression, and derivative melts rise to the surface to erupt. Melts push up through faults towards the surface, forming dikes and sills.[1][2][3][4][5][6]

Continued extension leads to accelerated igneous activity, including repeated eruptions. Repeated eruptions form a thick sequence of lava beds that can reach a combined thickness of up to 20 km. These beds are identified on seismic refraction sections as seaward dipping reflectors. It is important to note that the early phase of volcanic activity is not limited to the production of basalts. Rhyolite and other felsic rocks can also be found in these zones.[2][3][5]

Continued extension with volcanic activity forms transitional crust, welding ruptured continent to nascent ocean floor. Volcanic beds cover the transition from thinned continental crust to oceanic crust. Also occurring during this phase is the formation of high velocity seismic zones under the thinned continental crust and the transitional crust. These zones are identified by typical seismic velocities between 7.2 and 7.7 km/s and are usually interpreted as layers of mafic to ultramafic rocks that have underplated the transitional crust.[2][3][5] Asthenospheric upwelling leads to the formation of a mid-ocean ridge and new oceanic crust progressively separates the once-conjoined rift halves. Continued volcanic eruptions spread lava flows across transitional crust and onto oceanic crust. Due to the high rate of magmatic activity the new oceanic crust forms much thicker than typical oceanic crust. Some have theorized that the copious amounts of volcanic material also lead to the formation of oceanic plateaus at this time.

The final and longest phase is the continued thermal subsidence of the transitional crust and the accumulation of sediments. Continued seafloor spreading leads to the formation of oceanic crust of normal thickness. Over time this production of normal oceanic crust and sea floor spreading leads to the formation of an ocean.[2] This phase is of the most interest to the oil industry and sedimentary geologists.

The US Atlantic passive margin extends from Florida to southern Nova Scotia. This VPM was a result of the breakup of the supercontinent, Pangea, in which North America separated from northwestern Africa and Iberia to form the North Atlantic Ocean. This margin has a typical history of tectonic events that are representative of volcanic passive margins with rifting and passive margin formation occurring 225-165 million years ago. Like other VPMs the US East Coast Margin developed in two stages: First, rifting, initiated during the Middle to Late Triassic and continued into Jurassic time and, second, seafloor spreading, which began in Jurassic time and continues today. The US East Coast includes several components which are characteristic of VPM's including seaward-dipping reflectors, flood basalts, dikes, and sills.