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Naust Formation

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Back-stripped model for Cape Vulture after removal of the Naust Formation. (a) Results of 1D back-stripping showing change in burial depths and increased water depths. (b) Revised geomechanical model. (c) Detailed pressure v. depth plot showing estimated aquifer pressure for Cape Vulture give reduction in pressure of 150 bar. (d) Predicted oil column height trapped using hydrodynamic seal model compared with static seal model.
Published: 19 December 2023
Fig. 17. Back-stripped model for Cape Vulture after removal of the Naust Formation. ( a ) Results of 1D back-stripping showing change in burial depths and increased water depths. ( b ) Revised geomechanical model. ( c ) Detailed pressure v. depth plot showing estimated aquifer pressure for Cape
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Figure 2. Seismic stratigraphy of upper ∼0.5 m.y. of Naust Formation deposited on mid-Norwegian shelf. Sediment thickness is calculated using sound velocity of 2000 m s−1. Seismic line (IKU B81–208) is located as N-S in Figure 3. Note erosion of underlying units by recent ice-stream flow in Traenadjupet and older ice-stream channels within sediments of Traenabanken to south (red lines labeled paleo-trough). Red arrows indicate presence of streamlined bedforms on buried paleotrough surfaces. Three-dimensional survey is NLGS-95 and survey B is NNE-2000
Published: 01 April 2006
Figure 2. Seismic stratigraphy of upper ∼0.5 m.y. of Naust Formation deposited on mid-Norwegian shelf. Sediment thickness is calculated using sound velocity of 2000 m s −1 . Seismic line (IKU B81–208) is located as N-S in Figure 3 . Note erosion of underlying units by recent ice-stream flow
Journal Article
Published: 01 January 2007
Journal of the Geological Society (2007) 164 (1): 129–141.
... of the overlying Naust Formation (upper Pliocene–Present). The faults abruptly terminate upward below a thick interval of debris flows. We propose a dynamic model in which: (1) the development of polygonal faults discontinues temporarily as a result of a change in regional sedimentation, leading to inactive...
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Series: Geological Society, London, Special Publications
Published: 01 January 2002
DOI: 10.1144/GSL.SP.2002.196.01.09
EISBN: 9781862394445
... geohazards, including slides. At the Vøring margin in the north, there has been the build-out of a huge prograding wedge of sediment in Plio-Pleistocene times. The sediments of the wedge are assigned to the Naust Formation, which has been subdivided into eight units (A-H), and includes only a few...
Journal Article
Journal: Geology
Published: 01 January 2010
Geology (2010) 38 (1): 3–6.
...Julian A. Dowdeswell; Dag Ottesen; Leif Rise Abstract Sediment delivery rates through an entire ice age are investigated using seismic records of glacial erosion products from the Fennoscandian Ice Sheet deposited offshore of mid-Norway in the 2.7 m.y. old Naust Formation (volume 100,000 km 3...
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Best-fitting exponential porosity–depth trends for the Cretaceous mudrocks after subtracting the thickness of the Naust Formation in each well (i.e. depths are relative to the base of the Naust Formation). Colours of trend lines for the respective wells are as for Figure 6.
Published: 18 December 2014
Fig. 15. Best-fitting exponential porosity–depth trends for the Cretaceous mudrocks after subtracting the thickness of the Naust Formation in each well (i.e. depths are relative to the base of the Naust Formation). Colours of trend lines for the respective wells are as for Figure 6 .
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Section through 10 wells. The line of section is shown in Figure 7. N, Naust Formation; K, Kvitnos Formation; L, Lange Formation. The unlabelled interval between the Kvitnos and Naust formations comprises the whole sequence from the Late Cretaceous Nise Formation to the Miocene–Pliocene Kai Formation. Density porosity values (%) on the best-fitting exponential trends for the Kvitnos and Lange mudstones at 2700 m depth below seafloor are given along the bottom of the figure.
Published: 18 December 2014
Fig. 8. Section through 10 wells. The line of section is shown in Figure 7 . N, Naust Formation; K, Kvitnos Formation; L, Lange Formation. The unlabelled interval between the Kvitnos and Naust formations comprises the whole sequence from the Late Cretaceous Nise Formation to the Miocene–Pliocene
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Three interpreted seismic sections (locations shown in Fig. 4) with positions of nearby wells projected onto the line of section. Interpreted horizons are: cream, base of Naust T (unconformity); blue, base of Naust A; green, base of Naust N unit and of Naust Formation; and yellow, base of Molo Formation. The vertical scale is two-way time in seconds.
Published: 18 December 2014
Fig. 9. Three interpreted seismic sections (locations shown in Fig. 4 ) with positions of nearby wells projected onto the line of section. Interpreted horizons are: cream, base of Naust T (unconformity); blue, base of Naust A; green, base of Naust N unit and of Naust Formation; and yellow, base
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A: Map of mid-Norwegian margin, including source catchment area of glacial erosion (yellow dashed line) and area of offshore deposition (isopach map of thickness of Naust Formation in milliseconds of two-way traveltime, where 1 ms is ∼1 m). White box in isopach map locates Figure 2; red box is area of C. Blue line marks present shelf edge. B: Interpretation of seismic profile of Naust stratigraphy (orange dashed line in A), showing sequences N, A, U, S, and T, and Molo Formation (M) across Norwegian margin and schematic of previous surfaces indicating depth of erosion on inner shelf, coastal zone, and land areas (dashed parabolic lines). Light-brown shaded formations underlying Naust Formation are mainly Tertiary, Cretaceous, and Jurassic sedimentary rocks. C: Development of Naust depocenter over past 2.7 m.y., demonstrating seaward progradation. Area of coverage is located by red box in A.
Published: 01 January 2010
Figure 1. A: Map of mid-Norwegian margin, including source catchment area of glacial erosion (yellow dashed line) and area of offshore deposition (isopach map of thickness of Naust Formation in milliseconds of two-way traveltime, where 1 ms is ∼1 m). White box in isopach map locates Figure 2
Journal Article
Journal: Geology
Published: 01 April 2007
Geology (2007) 35 (4): 359–362.
... features on high-latitude continental shelves. Our examples come mainly from the mid-Norwegian shelf, where there are many 3-D seismic blocks available and the seismic stratigraphy of the 2.7 Ma Naust Formation is relatively well understood (e.g., Ottesen et al., 2005 ; Rise et al., 2005 ). We...
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Series: Geological Society, London, Special Publications
Published: 15 March 2024
DOI: 10.1144/SP525-2023-25
EISBN: 9781786209573
... ). However, the Kai Formation is absent in large extents of the study area ( Dalland 1988 ; Eidvin et al. 2007 ; Dybkjær et al. 2021 ), forming a big unconformity from the Naust Formation (see below) into the Brygge Formation. The spreading in the Norwegian–Greenland Sea, the opening of the Fram Strait...
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Map showing the 100 wells from the mid-Norwegian shelf included in this study (outlined by dotted circles). The eight wells used as local comparison to the Tulipan well are highlighted in yellow. The Tulipan well is outlined in yellow and red. An isopach map (two-way traveltime in ms) of the Pliocene/Pleistocene Naust Formation (modified from Rise et al., 2005) is displayed in the background. The Naust Formation was formed by westward prograding glaciogenic debris flows along the entire mid-Norwegian margin (Hjelstuen et al., 2005). The most voluminous of these debris flow sequences, the North Sea Fan, is outlined by the thick dotted line.
Published: 01 June 2008
) of the Pliocene/Pleistocene Naust Formation (modified from Rise et al., 2005) is displayed in the background. The Naust Formation was formed by westward prograding glaciogenic debris flows along the entire mid-Norwegian margin (Hjelstuen et al., 2005). The most voluminous of these debris flow sequences, the North
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Figure 2. A: Seismic-stratigraphic section (GMNR-94–105) across shelf and slope on the mid-Norwegian margin showing sedimentary wedge making up the glacier-influenced 2.7 Ma Naust Formation (twt—two-way traveltime; 1 s is ∼1000 m of sediment thickness). Letters represent five sequences within formation. B: Location of seismic line on Norwegian margin. Td—Traenadjupet; Tb—Traenabanken. C: Subdivisions and proposed ages for Naust Formation (Rise et al., 2005). Boundaries between units are color coded and shown in A. Interpreted parts of the seismic section in A show truncation of prograding wedges (marked in red) and removal of paleoshelf surfaces (D) and preservation of prograding wedges and their buried shelf surfaces (E; marked in red).
Published: 01 April 2007
Figure 2. A: Seismic-stratigraphic section (GMNR-94–105) across shelf and slope on the mid-Norwegian margin showing sedimentary wedge making up the glacier-influenced 2.7 Ma Naust Formation (twt—two-way traveltime; 1 s is ∼1000 m of sediment thickness). Letters represent five sequences within
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Figure 3. Streamlined sedimentary bedforms produced beneath paleo–ice streams on mid-Norwegian continental shelf. A: Buried surface ∼100 m deep within upper Naust Formation (three-dimensional [3D] seismic block NLGS-95). B: ∼200 m deep within upper Naust Formation (3D seismic block NNE-2000). C: Late Weichselian sediments at modern seafloor of Traenadjupet (3D seismic block ST-9404). D: Seafloor of Vestfjorden (EM1002 swath bathymetry). E: Map of changing ice-stream flow directions inferred from orientation of streamlined bedforms on mid-Norwegian shelf (located in Fig. 1A). Red lines are Elsterian–Saalian and white lines are Weichselian ice-stream flow directions, respectively. TS—Traenadjupet Slide, NS—Nyk Slide. Locations of surfaces in A–D are shown in E (labeled a–d), together with seismic line from Figure 2 (labeled N-S). Black boxes locate two 3D seismic blocks
Published: 01 April 2006
Figure 3. Streamlined sedimentary bedforms produced beneath paleo–ice streams on mid-Norwegian continental shelf. A: Buried surface ∼100 m deep within upper Naust Formation (three-dimensional [3D] seismic block NLGS-95). B: ∼200 m deep within upper Naust Formation (3D seismic block NNE-2000). C
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Schematic sections from sink to source along profiles A and B in Figure 1. Sediment geometry indicates missing cover rocks in land area. Reworking of Molo and Utsira Formations into base of Naust Formation is indicated by dashed yellow lines. Jurassic outliers are shown schematically; approximate thickness of missing overburden is indicated by vitrinite reflectance (Bøe et al., 2008).
Published: 01 December 2013
Figure 4. Schematic sections from sink to source along profiles A and B in Figure 1. Sediment geometry indicates missing cover rocks in land area. Reworking of Molo and Utsira Formations into base of Naust Formation is indicated by dashed yellow lines. Jurassic outliers are shown schematically
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Schematic illustration of formation of injectites and extrudites in the northern North Sea with interpreted fluid pressure (F1 and F2) and lithostatic pressure (L1 and L2) below points P1 and P2 at the time of sand extrusion (E2). Differential loading of the prograding Naust Formation causes fluid pressure build-up in a parent sand (PS) below the thick glaciomarine package and the low-permeability smectite-rich Hordaland Group. The fluid pressure (line F1) builds up towards lithostatic pressure in the sand (line L1). Differential loading of the prograding shelf generates a lateral fluid pressure gradient in the parent sand and fluids move towards lower pressure where the overburden is thinnest, which is at the toe of the slope. Here the fluid pressure is reduced from that of F1, indicated by the dotted line F1’, but owing to the reduced thickness of the Naust Formation the fluid pressure (F2) is above lithostatic pressure within the parent sand and hydro-fractures form in the overburden. Water and fluidized sand flow through the fractures and finally reach the seafloor as extrusive sand (arrows). Thick sand also deposits within large fractures (I2) at the transition from the smectite- to the ooze-rich claystones. A noteworthy feature is the kink in the lithostatic curve in the low-density ooze-rich sediments, which is why most injectites form near the base of the low-density layer. I1 and E1 indicate respectively intrusive and extrusive sands formed during an earlier phase of high fluid pressure. Once the fractures are filled with sand, the water–sand slurry will continue to flow, as it also does after the fluid pressure drops below lithostatic pressure.
Published: 25 November 2015
Fig. 1. Schematic illustration of formation of injectites and extrudites in the northern North Sea with interpreted fluid pressure (F1 and F2) and lithostatic pressure (L1 and L2) below points P1 and P2 at the time of sand extrusion (E2). Differential loading of the prograding Naust Formation
Journal Article
Published: 18 December 2014
Petroleum Geoscience (2015) 21 (1): 17–34.
...Fig. 15. Best-fitting exponential porosity–depth trends for the Cretaceous mudrocks after subtracting the thickness of the Naust Formation in each well (i.e. depths are relative to the base of the Naust Formation). Colours of trend lines for the respective wells are as for Figure 6 . ...
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NW–SE-striking seismic section crossing the position of well 34/8-3A (location shown in Fig. 5) and showing the late Cenozoic stratigraphic subdivision above the Visund Field. The stratigraphic position of the base of the lower Miocene unit, top Hordaland Group unconformity, top glauconitic sand and base of the glaciomarine prograding Naust Formation are shown as interpreted by Eidvin & Rundberg (2001). Much of the lower Miocene unit is eroded west of the escarpment.
Published: 01 January 2013
glauconitic sand and base of the glaciomarine prograding Naust Formation are shown as interpreted by Eidvin & Rundberg (2001) . Much of the lower Miocene unit is eroded west of the escarpment.
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 Seismic profile CD produced from the 3D seismic dataset. The Kai Formation throughout the Vøring Basin is characterized by numerous polygonal faults with small offsets (5–20 m) and an average spacing of 100–500 m. The polygonal faults affect an interval with an average thickness of 500 ms TWT (from Horizon C to Horizon D). Although the base of the Naust Formation (below the debris-flow interval and over Horizon C) does not seem affected by such faulting on the seismic profile, polygonal faults have been clearly identified on Horizons A and B, using curvature maps.
Published: 01 January 2007
ms TWT (from Horizon C to Horizon D). Although the base of the Naust Formation (below the debris-flow interval and over Horizon C) does not seem affected by such faulting on the seismic profile, polygonal faults have been clearly identified on Horizons A and B, using curvature maps.
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 Curvature maps of Horizons A–D. Concave-up and concave-down structures are represented in black and white, respectively. Using this attribute, polygonal faults are highlighted in black. They have been counted and measured, and the results are reported in rose diagrams. This statistical analysis of faults helps to define two main intervals of faults. The lower interval (top of Kai Formation) is affected by faults oriented N50, N110 and N170, whereas the upper interval (base of Naust Formation) is affected by faults oriented N20, N80 and N140. However, Horizons B and C are affected by both populations, but at opposite concentrations. This suggests that faults of the lower and upper intervals are interpenetrating.
Published: 01 January 2007
analysis of faults helps to define two main intervals of faults. The lower interval (top of Kai Formation) is affected by faults oriented N50, N110 and N170, whereas the upper interval (base of Naust Formation) is affected by faults oriented N20, N80 and N140. However, Horizons B and C are affected by both