Abstract Reactivated Paleozoic faults provided accommodation of rift and synrift basin fill in the Triassic Fundy Basin and Orpheus Graben of the Scotian Margin. Age data (Williams, 1985) suggests that the Minas Subbasin opened as early as the Anisian (242–247.2 ma) while the Orpheus Graben opened as early as the Rhaetian (201.3–208.5 ma). The Minas Fault Zone (MFZ) defines the boundary between the Avalon and Meguma terranes in the Canadian Appalachians and is exposed along mainland Nova Scotia (Murphy et al. , 2011). This series of faults mark the northern flank of the Minas subbasin (Fundy basin) and Orpheus graben (Scotian basin), and were reactivated during Mesozoic regional extension. Faults nearest the highlands accommodated the coarsest material (alluvial) while faults toward the basin center accommodated relatively finer grained fluvial, aeolian, and lacustrine sediments (Wade and MacLean, 1990 ; Leleu et al. , 2009). The Wolfville Formation comprises alluvial facies and generally fines upward into the Blomidon Formation aeolian sediments (Fig. 1), only found along the northern boundary of the basin. Is this facies present due to local deposition within the Minas subbasin in an arid, dry zone or do aeolian sediments persist along all footwalls of eastern North American synrift basins? Figure 1. Schematic transect through the Minas Subbasin showing the structural and stratigraphic elements of this basin during rifting. Alluvial fan facies are found along the northern faulted flank of the basin, with minor occurrence of Aeolian facies. Fluvial facies are found along the entirety of the basin. Lacustrine facies are also found along the entirety of the basin but are dominantly deposited in the central areas of the basin. The Orpheus graben is an oblique trending Mesozoic extensional basin. At outcrop on the western edge of the basin, facies comprise fine to coarse-grained sandstone containing pebble to cobble clasts and having a minor mud and conglomeratic facies. These are interpreted to have been deposited in an alluvial braided channel complex nearest the mouth of the river system (Tanner and Brown, 1999). To the east, more distal facies representing evaporites, playa lake and marginal marine environments are present in cores of the Eurydice Formation and represent initial opening of the Atlantic Ocean. Paleoflow indicators suggest axial rivers once existed between the two basins along the MFZ (Tanner and Brown, 1999 ; Leleu et al. , 2009). Could the “Broad Terrane Hypothesis” of Russell (1879) be applicable? Was there a single connected basin which was separated into two subbasins through uplift and erosion of conjoining strata (alluvial deposits along the axial trend of the MFZ)? During basin inversion (Withjack et al. , 1995 ; Withjack et al ., 2009 ; Withjack et al ., 1998) sediments deposited along the Minas Fault Zone have been uplifted and eroded. This is most likely the reason for the lack of alluvial facies present along the northern edge (footwall) of the Minas Subbasin. Facies associations of surface and subsurface synrift sediments are being characterized to discern sediment distribution patterns and sediment provenance (outcrop, thin section) and subsurface (core, cuttings, thin section).

Abstract The contemporary rifted margin off Nova Scotia was formed over the Meguma and Avalon Appalachian terranes in response to plate motions between Africa and North America (Figs. 1 and 2; Williams and Hatcher, 1983; Haworth, 1981). Rifting began in the Late Triassic and produced rift basins beneath the present continental shelf. Of these basins, the Orpheus sub-basin which lies on the Avalon-Meguma boundary is a prominent example. Regionally the rift basins are not uniformly distributed throughout the Nova Scotian margin and southern Grand Banks region. Most are found in the Avalon terrane, rather than the Meguma terrane. Evidence of Triassic mafic volcanism is exemplified by the North Mountain basalts and the Shelburne dike in Nova Scotia, and most of the known occurrences of volcanic rocks appear to lie well inland of the present ocean-continent transition (Poole, 1970; Papezik and Barr, 1981). Triassic rifting was accompanied by the deposition of non-marine clastics within the rift basins. During the Early Jurassic, thick salt beds developed beneath much of the present shelf and slope (Jansa and Wade, 1975). In Early-Middle Jurassic time a deepening, less restricted marine environment led to the construction of carbonate platforms (Jansa, 1981). It was during this time that sea-floor spreading began east of the rifted North American continent. This rift-drift transition does not appear to be marked by a period of uplift, erosion, or by the development of a clear breakup unconformity After the onset of sea floor spreading, the margin subsided and over 10 km of Jurassic