Description: The 3D seismic cube is in SEG-Y format with SP in byte 5, inline number in byte 25 and xline number in byte 17. Processing includes repositioning, time migration and depth conversion using a smoothed velocity field based on Berndt et al., 2019. Acquisition parameters are discussed in the SO227 cruise report (Berndt et al., 2013).

Description: The dataset contains the raw .segy files of the ocean bottom seismometers/hydrophones (OBS/H) that recorded wide-angle seismic data along 6 profiles in the Porcupine Basin. The active-source seismic survey was conducted by GEOMAR in 2004. The cruise report, navigation files for each profile, and geographical coordinates of each OBS/H are also included in this dataset.

Description: Hyperextension of continental crust at the Deep Galicia rifted margin in the North Atlantic has been accommodated by the rotation of continental fault blocks, which are underlain by the S reflector, an interpreted detachment fault, along which exhumed and serpentinized mantle peridotite is observed. West of these features, the enigmatic Peridotite Ridge has been inferred to delimit the western extent of the continent‐ocean transition. An outstanding question at this margin is where oceanic crust begins, with little existing data to constrain this boundary and a lack of clear seafloor spreading magnetic anomalies. Here we present results from a 160 km long wide‐angle seismic profile (Western Extension 1). Travel time tomography models of the crustal compressional velocity structure reveal highly thinned and rotated crustal blocks separated from the underlying mantle by the S reflector. The S reflector correlates with the 6.0–7.0 km s−1 velocity contours, corresponding to peridotite serpentinization of 60–30%, respectively. West of the Peridotite Ridge, shallow and sparse Moho reflections indicate the earliest formation of an anomalously thin oceanic crustal layer, which increases in thickness from ~0.5 km at ~20 km west of the Peridotite Ridge to ~1.5 km, 35 km further west. P wave velocities increase smoothly and rapidly below top basement, to a depth of 2.8–3.5 km, with an average velocity gradient of 1.0 s−1. Below this, velocities slowly increase toward typical mantle velocities. Such a downward increase into mantle velocities is interpreted as decreasing serpentinization of mantle rock with depth.