In extension, listric faults form rollover anticlines in their hanging walls.

Listric faults produce the correct model for this sufficient crustal extension needed to create the ocean basin.

A listric fault is a type of fault in which the fault plane is curved.

As rifting proceeds, listric fault systems form and further subsidence occurs, resulting in the creation of an ocean basin.

Accretionary wedges and listric faulting are characteristic of plate collisional conditions, and these terms now occur frequently in theses.

Periodic extension of the basin permitted release of the metal-bearing fluids up listric faults into the unlithified Carboniferous sediments.

Listric faults developed over suitably oriented lines of crustal weakness, giving rise to elongated zones of thickened sediment on their downthrown (generally southern) sides.

Fluid movement occurred during the Variscan orogeny aided by seismic pumping from the overpressured basins along listric faults (Plant and others, 1988).

This crustal uplift has created extension and horst and grabens and even listric faults which indicate a pre-oceanic basin structure.

The most prospective areas for Pennine-style mineralisation are in the concealed carbonate shelf adjacent to listric faults such as the area to the north-east of the Gainsborough Basin.

The depositional environment is thought to be a shoaling shallow sea in which the Hooggenoeg Formation has been deposited in a west-block down, listric faulted, synsedimentary setting."

As is also the case in the southern foreland of the Pyrenees, thrusts in the Southern Alps are oriented along listric fault planes with relatively shallow decollement horizons.

Moreover, these major faults tend to be discontinuous and curved in plan and it seems that main boundary listric faults alternate along rift valleys and are separated by transfer faults (Fig. 4.10).

Growth faults are also sometimes called "listric faults", implying that the fault is a concave-upward surface that transforms nearly vertical displacements at the surface into nearly horizontal ones at depth.

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.

Most significantly, the structure of many rifts examined by seismic methods has been shown to be asymmetric with most of the downthrow occurring along a major boundary listric fault on one side of the rift.

The main characteristic of Irish-style, Pb-Zn mineralisation is syn-diagenetic deposition of sulphides in shallow-water carbonate facies, adjacent to major listric faults, at early Dinantian sedimentary basin margins.

When a listric fault, which increases in dip upwards, reactivates the uppermost part of the fault may be too steep and new reverse faults typically develop in the footwall of the existing fault.

Reversal of the stress field at the end of the Cretaceous and culminating in the Miocene led to crustal shortening accommodated on the same listric faults, accentuating existing rollover anticlines and causing inversion.

Such rifts are said, therefore, to have a half-graben structure with the main boundary listric fault forming a footwall, and the opposing downwarped crust forming a hanging wall leading down from a roll-over zone (Fig. 4.9(B)).

Where the lithosphere undergoes horizontal extension at a normal fault or rifting center, the crust will stretch until faulting occurs, either by a system of normal faults (which creates horsts and grabens) or by a system of listric faults.

Russell (1986) prefers a model in which mineralising fluids were generated by Carboniferous seawater penetrating, and reacting with, the underlying Caledonian basement to increasing depths (up to 10 km) under a normal geothermal gradient during basin extension before being discharged up listric faults.