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

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

36 Figure 2-8: Tectonic reconstruction of the Orpheus and Scotian basins on balanced-section techniques and Lithoprobe deep seismic line 86-5B across the Orpheus basin. The broad tract and basin depth are related to two levels of intracrustal detachment at 15-18 km and approximately 7km, restored to mid-Jurassic “breakup” unconformity datum to avoid effects of substantial and asymmetrical postrift subsidence. Top of basement reflector in red.
approximately 6 to 7 kilometers below the Early Jurassic breakup unconformity (Welsink et al., 1989) thus indicating that a common extensional system apparently links these landward-dipping basin-forming faults. Transfer fault zones are conspicuous off Nova Scotia where they accommodate distinct extensional tracts within the collective Scotian Basin, but are less predominant within subbasins. The lack of internal transfer trends and the en echelon arrangement of the major basin-forming faults suggest that extensional strain was transmitted across linked relay structures (Larson, 1988; Tankard and Welsink, 1989). 2.4.2 Thin Skin Deformation Within the Scotian Basin postrift structural modification was largely accommodated by seaward-dipping listric faults and associated synthetic and antithetic faults that detach within the sedimentary cover. Their occurrence is directly related to, but does not involve, underlying basement geometry. Two sets of postrift faults are recognized by Welsink et al. (1989); those restricted to the Jurassic postrift sequence and those that deform Cretaceous sediments (Figure 2-9). Although generally detaching at similar depths, these faults tend to extend to progressively higher stratigraphic levels in a seaward direction. Where syn-depositional, these faults are associated with rollover anticlines and growth strata. Syn-sedimentary growth faults set up one of the primary play types of the Scotian Shelf and are also predicted to play a similar role in the frontier Scotian Slope. 37
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 and 46: formation thickness consistently in
Page 47 and 48: 2.4 Structural Styles and Geometry
Page 49: and igneous rocks of the Meguma Ter
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
Page 97 and 98: NW SE Quaternary Miocene - Oligocen
Page 99 and 100: 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
Page 241 and 242:
Scotian Rise, Geological Survey of
Page 243:
Welsink, H.J., Dwyer, J.D., and Kni
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