Changes

==Geological Setting==

==Geological Setting==

The geology of the western [[Barents Sea]] is well known (Smelror et al., 2009<ref name=Smelroretal2009>Smelror, M., O. V. Petrov, G. B. Larsen, and S. Werner, eds., 2009, Atlas—Geological history of the Barents Sea: Geological Survey of Norway, Trondheim, 135 p.</ref>; Henriksen et al., 2011<ref name=Henriksenetal2001 />, and references therein). The geological description of the study area given here is largely constrained to the elements that are significant for the understanding of leakage from structural traps of the [[Jurassic]] play. The location of the study area and the main structural elements (from Gabrielsen et al., 1984<ref name=Gabrielsenetal1984>Gabrielsen, R. H., R. B. Faerseth, G. Hamar, and H. C. Rønnevik, 1984, Nomenclature of the main structural features on the Norwegian Continental Shelf north of 62nd parallel, in A. M. Spencer, S. O. Johnsen, A. Mørk, E. Nyséther, P. Songstad and Å. Spinnangr, Petroleum geology of the North European margin: Norwegian Petroleum Society, Graham & Trotman, London, p. 40–60.</ref>) are shown in [[:file:M114CH10FG01.jpg|Figure 1]. Ostanin et al. (2012<ref name=Ostaninetal2012a />) later separated the [[fault]]s in the area in four classes: first-order faults off-setting the Jurassic reservoir units and extending to the top of the [[Cretaceous]] and sometimes to the Upper Regional Unconformity (URU), second-order faults that offset [[reservoir]] rocks but do not extend to the top Cretaceous, the polygonal faults, and the [[Paleocene]] to [[Eocene]] faults that do not connect to the deeper faults.

The geology of the western [[Barents Sea]] is well known (Smelror et al., 2009<ref name=Smelroretal2009>Smelror, M., O. V. Petrov, G. B. Larsen, and S. Werner, eds., 2009, Atlas—Geological history of the Barents Sea: Geological Survey of Norway, Trondheim, 135 p.</ref>; Henriksen et al., 2011<ref name=Henriksenetal2001 />, and references therein). The geological description of the study area given here is largely constrained to the elements that are significant for the understanding of leakage from structural traps of the [[Jurassic]] play. The location of the study area and the main structural elements (from Gabrielsen et al., 1984<ref name=Gabrielsenetal1984>Gabrielsen, R. H., R. B. Faerseth, G. Hamar, and H. C. Rønnevik, 1984, Nomenclature of the main structural features on the Norwegian Continental Shelf north of 62nd parallel, in A. M. Spencer, S. O. Johnsen, A. Mørk, E. Nyséther, P. Songstad and Å. Spinnangr, Petroleum geology of the North European margin: Norwegian Petroleum Society, Graham & Trotman, London, p. 40–60.</ref>) are shown in [[:file:M114CH10FG01.jpg|Figure 1]]. Ostanin et al. (2012<ref name=Ostaninetal2012a />) later separated the [[fault]]s in the area in four classes: first-order faults off-setting the Jurassic reservoir units and extending to the top of the [[Cretaceous]] and sometimes to the Upper Regional Unconformity (URU), second-order faults that offset [[reservoir]] rocks but do not extend to the top Cretaceous, the polygonal faults, and the [[Paleocene]] to [[Eocene]] faults that do not connect to the deeper faults.

The western Hammerfest Basin was formed as a response to a Late Jurassic to Early Cretaceous rifting episode with a largely east–west extension in the western part of the study area. This rifting had an oblique stress component that resulted in local north–south extension in the eastern part of the basin (Berglund et al., 1986; Faleide et al., 2008). A Late Cretaceous–Early Tertiary megashear system developed along the margins of the Norwegian–Greenland Sea, which resulted in local transpression and transtension along restraining and releasing bends of this shear system. Some of the Jurassic to Early Cretaceous normal faults were rejuvenated at this time period in the Hammerfest Basin (Gabrielsen, 1984; Berglund et al., 1986).

The western Hammerfest Basin was formed as a response to a Late Jurassic to Early Cretaceous rifting episode with a largely east–west extension in the western part of the study area. This rifting had an oblique stress component that resulted in local north–south extension in the eastern part of the basin (Berglund et al., 1986; Faleide et al., 2008). A Late Cretaceous–Early Tertiary megashear system developed along the margins of the Norwegian–Greenland Sea, which resulted in local transpression and transtension along restraining and releasing bends of this shear system. Some of the Jurassic to Early Cretaceous normal faults were rejuvenated at this time period in the Hammerfest Basin (Gabrielsen, 1984; Berglund et al., 1986).