Summary A series of eight high‐resolution seismic refraction profiles from the ultra‐slow spreading (16 mm yr− 1 full spreading rate) Mohns Ridge in the Norwegian–Greenland Sea has been treated with modern inversion methods. The profiles were shot parallel to the ridge at an off‐axis distance of 0–135 km corresponding to crustal ages of 0–22 Ma. The resulting models are constrained by synthetic seismograms and gravity modelling. The crustal thickness in all profiles is well below the global average for typical oceanic crust, and shows a high variability with a mean thickness of 4.0 ± 0.5 km. This is mainly due to a very thin and variable lower crustal layer (Layer 3). Generally, the crust is thicker beneath basement highs and thinner beneath basins, implying local isostatic compensation. The top of the basement (Layer 2a) consists of a zone with low P‐wave velocities (2.5–3.0 km s− 1). The mean thickness of this layer decreases with distance from the ridge. Beneath it lies a layer with slightly higher velocities (Layer 2b). Its thickness shows less variability along a given profile and an overall increase with age. The combined average thickness of the upper two layers remains nearly constant, indicating that the boundary between Layer 2a and 2b may represent an alteration front. Upper mantle velocities are generally slow, around 7.5 km s− 1. For the profile directly within the rift valley, a model without a third layer, incorporating a constant gradient up to upper mantle velocities, and a model with a Moho depth inferred from neighbouring profiles and upper mantle velocity as slow as 7.2 km s− 1 fit the seismic and gravity data equally well. The crustal structure is not mature below the ridge. These observations support previous models suggesting the presence of low densities and velocities at about 2 km below the rift axis. Poisson’s ratios determined from converted S‐wave modelling are incompatible with a Layer 3 consisting of purely serpentinized peridotite. However, a volume fraction of 10–40 per cent serpentinite cannot be ruled out.

Post-depositional remobilization and injection of sand can significantly change the geometry of deepwater clastic reservoirs. Features associated with these processes are particularly well developed in the lower Paleogene of the South Viking Graben of the UK and Norwegian North Sea. Seismic scale sandstone intrusions can be grouped in two classes. Class 1 comprises low-angle (20-40 degrees) tabular sandstone intrusions emanating from steep-sided in situ sand bodies within the Balder Formation. The intrusions may be 5-30+m thick and crosscut 120-250+m of compacted stratigraphic section. They terminate at an unconformity at the top of the Frigg interval where they may have extruded onto the palaeo-seafloor. Class 2 comprises conical sandstone intrusions that emanate some 50-300+m upward from distinct apexes located 400-700+m above the nearest depositional sand body. The conical intrusions may have been sourced from underlying sand bodies by clastic blow out pipes. Both types of intrusions seem to adopt their particular geometry independently of (but occasionally exploiting) polygonal faults within the encasing mudstones. Sandstone intrusions may be highly porous and permeable and are thus important both as reservoirs and as plumbing within thick mudstone sequences.

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