the stratigraphy and structural history of the mesozoic and cenozoic ...

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$A marine wide angle reflection/refraction profile adjacent Nova ...$

Figure 2-6: Top; index map of Scotian Slope showing lease blocks, wells, and area of multibeam bathymetric survey. Bottom; multibeam bathymetric image of central Scotian Slope. Note, M.Sc study area shown in red (modified from Pickerill et. al., 2001) 32
2.4 Structural Styles and Geometry The rifted margin off Nova Scotia is the best understood of the rifted margins of eastern Canada. The margin was formed within the Appalachian Meguma Zone as the result of Late Triassic to Early Jurassic rifting was between Africa and North America. Normal faulting accompanied this rifting (Keen et. al., 1990). The margin has a well- developed hinge line, a thick sedimentary wedge consisting of both syn- and post-rift sediments, numerous salt diapirs (particularly beneath the slope) and carbonate build-ups that probably represent the position of an earlier Jurassic shelf edge. After the rift phase, both fault and thermally controlled subsidence occurred as the basin settled through Mid- Jurassic to Recent. Two principal classes of faults are recognized within the Scotian Basin: (1) those that involve basement (thick skin); and (2) those that detach within the cover sequence (thin skin). Both styles contribute to the gross structural framework of northeast trending normal faults, and subordinate northwest trending transfer faults (Welsink et al., 1989). 2.4.1 Thick Skin Deformation Basin forming faults of the composite Scotian Basin are long and sinuous. Large amounts of extension were accommodated by dip-slip and oblique slip movement along a system of en echelon and intersecting faults and relay ramps (Tankard and Welsink, 1989; Figure 2-7). The distribution and geometries of Mesozoic Scotian rift basins are controlled largely by tensional stress fields within pre-existing crustal structure. Metasedimentary 33
Page 1 and 2: THE STRATIGRAPHY AND STRUCTURAL HIS
Page 3 and 4: The integration of seismic stratigr
Page 5 and 6: leaving his door open and helping m
Page 7 and 8: 3.3.4 Tr2 Sequence Boundary 57 3.3.
Page 9 and 10: List of Figures (Short Titles) 1-1
Page 11 and 12: 3-22 Time structure map of the T1 S
Page 13 and 14: 5-17 End member geometries of alloc
Page 15 and 16: Chapter 1 Introduction 1.1 Introduc
Page 17 and 18: developed in the western part of th
Page 19 and 20: Areomagnetic surveys of the North A
Page 21 and 22: y Mukhopadhyay and Wade (1990), Wil
Page 23 and 24: 9 Figure 1-2: Comparative stratigra
Page 25 and 26: Naskapi N-30 Figure 1-3: Map showin
Page 27 and 28: SE NW 0 6 12 Kilometers 13 Figure 1
Page 29 and 30: converted using velocity informatio
Page 31 and 32: to date the effects of salt tectoni
Page 33 and 34: A 19 A’ Figure 2-1: Bathymetry an
Page 35 and 36: Within the area of the Scotian Basi
Page 37 and 38: 23 Figure 2-3: Generalized lithostr
Page 39 and 40: the landward extensions of regularl
Page 41 and 42: marine shales of the Misaine Member
Page 43 and 44: and positive relief structures on t
Page 45: formation thickness consistently in
Page 49 and 50: and igneous rocks of the Meguma Ter
Page 51 and 52: approximately 6 to 7 kilometers bel
Page 53 and 54: 4.2.3 Halotectonics In addition to
Page 55 and 56: 41 Figure 2-10: Scotian Margin base
Page 57 and 58: NW SE 6126 m 43 Figure 3-1: Represe
Page 59 and 60: TGS Base Tertiary Unconformity 45 T
Page 61 and 62: 47 Figure 3-3: Lithoprobe seismic r
Page 63 and 64: (Member Good DS9 Good Good Excellen
Page 65 and 66: NW SE Onlap Downlap 0 6 12 Kilomete
Page 67 and 68: 3.3.1. Top Basement Marker Within t
Page 69 and 70: 3.3.2. Tr1 Sequence Boundary The Tr
Page 71 and 72: 3.3.3 Depositional Sequence 1 Depos
Page 73 and 74: Glooscap C-63 E Moheida P-15 D TWT
Page 75 and 76: NW SE D D’ Eurydice Figure 3-9: S
Page 77 and 78: Formation consists of a series of m
Page 79 and 80: These reflections may represent int
Page 81 and 82: Anomalous highs Sequence boundary i
Page 83 and 84: in shape, 1 to 12 kilometers in dia
Page 85 and 86: Intersection with salt structure Fa
Page 87 and 88: 62, also intersected the Abenaki Fo
Page 89 and 90: marker in a landward direction (Fig
Page 91 and 92: south (slope-parallel) direction. T
Page 93 and 94: 3.3.13 Depositional Sequence 5 Depo
Page 95 and 96: Thickness TWT (ms) D D’ Thick Int
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NW SE Quaternary Miocene - Oligocen
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Due to the consistently high amplit
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Correlation with the Shubenacadie H
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3.3.17 Depositional Sequence 7 Depo
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3.3.18. T2 Sequence Boundary The T2
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Reflections within DS8 are commonly
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3.3.20 T3 Sequence Boundary The T3
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3.3.21 Depositional Sequence 9 Depo
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3.3.22 Water Bottom The uppermost r
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4.1 Introductory Remarks Chapter 4
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A (TWT ms) Basin-Bounding Fault Fam
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A A’ NW SE 105
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4.2.1 Slope Basin-Bounding Fault Fa
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Figure 4-3: Seismic Profile B-B’
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Wernicke (1981) or “second-order
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a) 2.0 3.0 4.0 5.0 6.0 7.0 8.0 b) D
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T3 T2 T1 T0 K1 J2 J1 Tr2 Tr1 NW SE
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thickening, resulting in distinct w
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Tertiary. In the northwest some maj
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SE NW Minor Faults 3076 m Major Fau
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NE SW 3075 m Pock-Marks ? Erosion E
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Chapter 5 Salt Tectonics 5.1 Mechan
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as a pressurized fluid with differe
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shales related to rapid progradatio
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131 Figure 5-3: Tectono-stratigraph
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Shelf N 0 15 30 Kilometers Moheida
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Shelf N 0 15 30 Kilometers Upper Sl
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A) NW SE B) Swells Normal basement-
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Salt Detachment Association includi
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formed shortly after autochthonous
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and Vendeville (1994) shows that th
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Allochthonous Stock “Finger” Di
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A’ SE A Folding of strata from T0
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Diapirs commonly intersect the K1 S
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D’ SE NW D 0 3 6 Strata folded fr
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Figure 5-14: Diapir rejuvenation du
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5.3.4 The Secondary Weld Associatio
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NW SE 0 3 6 Kilometers Inclined Sec
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An allochthonous salt structure is
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Salt Stocks A salt stock is charact
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F’ NE SW F 0 6 12 Kilometers Coal
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G (A) (B) G’ Figure 5-20: (A) Nor
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Figure 5-21: Schematic evolution of
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listric fault, causing the developm
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egardless of depositional setting a
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growth will continue until the sour
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Salt structures with onlapping syn-
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the base of post-kinematic stratigr
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SE NW 4093 m 179 Offset of paleo-de
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NE SW 6 km 181 Turtle Structure Pos
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NE SW 183 0 3 6 Turtle Structure Ki
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Figure 6-1: Seismic profile from th
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Figure 6-2: Tectono-stratigraphic c
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Ordovician metasedimentary rocks of
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191 Figure 6-3: Schematic block dia
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etween the location of salt swells
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On the slope, the Late to Middle Ju
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Listric growth faults typically tip
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this diapiric region. However, it w
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characteristically concordant with
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typical of passive margins modified
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Slope Basin: Kidston et al. (2002)
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~ Present day 100 C ~ Present day 1
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area can be divided into three slop
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Pre-Mesozoic structures are not con
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eservoir. The well locations were c
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7.2 Key Conclusions Geological Evol
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exclusively deform Late Triassic to
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• A reservoir of Cretaceous to Te
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References Alsop, G. I., Brown, J.P
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Gauley, B. J., 2001, Lithostratigra
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Keen, C. E., and Potter, D. P., 199
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Scotian Rise, Geological Survey of
Page 243:
Welsink, H.J., Dwyer, J.D., and Kni
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