ofm me 2005-111, geological map for part of nts 11e/07,
TRANSCRIPT
HORTON GROUP
WEST RIVER ST. MARYS FORMATION
CROSS BROOK FORMATION*
GRAHAM HILL, LOCHIEL*, BARRENS HILLS and LITTLE STEWIACKE RIVER FORMATIONS
((
((
((
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Chedabucto Fault
L@-E#Hwr
L@-E#Hgh
L@-E#Hbh/ls
Pictou County
Colchester County
Pictou County
Guysborough County
Colchester County
Halifax County
Guysbourgh County
Halifax County
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Tim Lake
Ben Lake
Mud Lake
Long Lake
Hood Lake
Fish Lake
Drug Lake
Dean Lake
Dunn LakeDuck Lake
Perch Lake
Round Lake
Elbow Lake
Grant Lake
Piper Lake
Black Lake
Moose Lake
Perch Lake
Roops Lake
Jenny Lake
Little Lake
Calder Lake
Forbes Lake
Sucker Lake
Little Lake
Barren LakeDunbar Lake
Nelson Lake
Hattie Lake
Pictou Lake
Gordon Lake
Dryden Lake
Dickey Lake
Sucker Lake
Sammys Lake
Meadow Lake
Island Lake
Archies Lake
Caribou Lake
MacLean Lake
The Millpond
Russell Lake
Johnson Lake
McIntosh Lake
McKinnon Lake
Gairloch Lake
Long John Lake
Speichts Lakes
Porcupine Lake
Cranberry Lake
East Loon Lake
West Loon Lake
MacDonald Lake
Cranberry Lake
South Loon Lake
Botany Bay Lake
MacPhersons Lake
West Branch Lake
Ellen Brown Lake
North River Lake
Otter Brook Lake
Black Brook Lake
Bottle Brook Lake
Grandfathers Lake
Little Ellen Brown Lake
Castley Pools
Bezanson Stillwaters
Bill Weir Stillwaters
Rhynos Landing Stillwater
Lime Brook
Drug B
rook
Fall Brook
Jack Brook
Black Brook
Black Brook
Black River
Otter B
rook
Grants Brook
Gor
man
Bro
ok
Holmes Brook
Fulton Brook
Johnny Brook
Glencoe B
rook
Cro
oked
Bro
ok
Doggett Brook
Tannery Brook
Cameron Brook
Gairloch
Brook
Mahailas Brook
Watervale Brook
Mill
stre
am B
rook
East Bryden B
rook
Sam C
ameron Brook
Scrub Grass
Brook
Bog
I sl a
n d L
a ke
Bk
Little
Bra
nch
Cox Bro
ok
South Brook
Nelson River
Mea
dow
Bro
ok
Castley B
rook
Ben
tley
Bro
ok
Calvary River
Bla
ncha
rd B
rook
Archibald Brook
Upper Bryden Brook
West R
iver of Pictou
BIG
BR
OO
K
NORTH NELSON RIVER
EAST RIVER OF PICTOU
WES
T BR
ANC
H EA
ST R
IVER
MID
DLE R
IVER O
F PIC
TOU
Moiche Hill
Drug Brook Hill
Kincaid Mountain
Mount Thom
Elgin
Lorne
Eureka
Glencoe
Rocklin
Concord
St Pauls
Pembroke
Burnside
SunnybraeIron Rock
Coromonie
Trafalgar
Marshdale
New Lairg
Lansdowne
Eastville
Watervale
Brookville
Millstream
Centredale
White Hill
Springside
Springville
Graham Hill
New Gairloch
Gordon Summit
Upper Burnside
Websters Corner
Lansberg Siding
Campbells Siding
Island East River
Glengarry Station
Lansdowne Station
West River Station
Hopewell
Bridgeville
8570
Duck Lake
Maple Lake
Crane Pond
Round Lake
Beaver Lake
Semple Lake
McQuarrie Lake
Big Brook Lake
Lansdowne Lake
Little Johnson Lake
Beaver Bk
Sucker B
rook
McDonald Brook
McLellans Brook
Middle Bryden Brook
Little Branch Stewiacke Rive
r
Cox Brook
Map
le B
rook
Bryden Brook
Pembroke River
Sutherland Brook
Big B
ranch Stew
iacke River
STEWIAC
KE R
IVER
WEST RIVER ST MARYS
500000mE
500000mE
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Jun 07, 2005
Descriptive Text
63°00'
45°15'
62°30'
45°15'
45°30'
63°00' 62°30'
45°30'
Bay of F
undy
Atlantic Ocean
Gulf ofSt. Lawrence
NewBrunswick
P.E.I.
SableIsland
Nova Scotia
11F/0511E/0811E/0711E/06
Regional Key Map
Scale 1:50 0001 0 1 2 3 km
© Her Majesty the Queen in Right of the Province of Nova Scotia 2005
Halifax, Nova Scotia
62°45'
62°45'
45°22.5' 45°22.5'
100 0 100 km
The St. Marys Basin, central mainland Nova Scotia, is dominated by a Late Devonian(?) - Early
Carboniferous intracontinental alluvial fan-fluviatile-lacustrine basin-fill sequence that occupies the current
boundary between the Meguma and Avalon terranes of the Canadian Appalachians. The Basin rocks
belong to the Horton Group which is divided into six, partially laterally equivalent, formations. The
stratigraphically lowest rocks are predominantly exposed in the central part of the Basin in a series of en
echelon anticlinal closures (11E/06-08). These clastic rocks were deposited in a longitudinal drainage
system represented by a lacustrine (Little Stewiacke River Formation) and an overlying braided fluvial
(Barrens Hills, Lochiel and Graham Hill formations) environment, which are in turn overlain by the Cross
Brook and West River St. Marys formations. These rocks unconformably overly the Meguma Group,
reflecting a decrease in accommodation space and implying that the St. Marys Basin is underlain, at
least in part, by Meguma basement.
This map is predominantly underlain by the Little Stewiacke River and Barrens Hills formations. The
contact between these formations is exposed on this map on the Stewiacke River about 100 m south of
its intersection with highway 289. Facing directions in the vicinity of this contact clearly show that the
Barrens Hills Formation overlies the Little Stewiacke River Formation. However, contact relationships
between these formations are still being mapped out, so they are presented as an undivided unit on this
map. The Little Stewiacke River Formation, which consists of interstratified, thinly bedded, bioturbated
mudstone, fissile, light to dark grey and black shale and slate, and light to dark grey sandstone,
frequently contains abundant comminuted plant debris. Coarsening- and thickening-upward cycles,
2-25 m thick, occur with individual beds ranging in thickness from 2 mm to 15 cm. In some localities the
sandstones display soft sediment deformation. In many sections, the finer grained lithologies display a
slaty cleavage. Siltstone/shale-sandstone contacts are either sharp or transitional, or, less commonly,
erosional. Sandstones are typically grey or dark grey weathering, very fine- to fine-grained and micaceous,
and in some locations, moderately feldspathic. Primary and penecontemporaneous sedimentary features
include normal grading, parallel lamination, ripple crosslamination, loading features and bioturbation.
Sandstone strata generally vary from millimetres to decimetres in thickness. As the contact with the
overlying Barrens Hills Formation is approached, the upper member lithologies are coarser, erosionally
amalgamated with channel scours and possible swaley cross-stratification, and display large scale
(10-20 cm) trough cross-stratification. Fine, organic debris is often abundant in these sandstones and
their weathering colour darkens accordingly.
The Barrens Hills Formation is characterized by resistant intervals of light grey to grey-white
weathering, fine- to very coarse-grained sandstone, monomict or polymict granulestone and conglomerate
interstratified with recessive intervals of micaceous, grey to dark grey weathering shale and/or siltstone.
Interbeds of minor red siltstone and sandstone also occur. The sandstones are dominated by quartz and
feldspar, although grey sedimentary lithic clasts are common near the base of the Formation. Feldspars
are generally intensely weathered to clay minerals. Locally, the sandstones may be slightly micaceous,
moderately feldspathic, and contain varying, but significant amounts of dark grey sedimentary lithic
clasts of schist and sandstone, some with a fabric, that are probably derived from the Meguma Terrane
south of the St. Marys Basin. The Barrens Hills Formation underlies large areas of both the central and
eastern Basin where it outcrops along a broad, regional, northeastward-trending anticlinal axis. To the
west of the Stewiacke River region the Formation thins dramatically and passes into the laterally
equivalent Graham Hill Formation. To the east of this map sheet, it passes into the laterally equivalent
Lochiel Formation.
The basal contact of the Barrens Hills Formation is positioned where sand- to granule-sized quartz-rich
clastic sediment starts to predominate over the darker and more thinly bedded lithologies of the Little
Stewiacke River Formation. This contact is exposed in the Stewiacke River region (11E/07) where it is
transitional over 1 m. It is recognized by the abrupt occurrence of thin (10-20 cm) lenses of small pebble
conglomerate at the base of the Barrens Hills Formation.
In the western portion of the map, the Graham Hill Formation consists of 1220 m of red and
maroon weathering, finer grained litharenite to feldspathic litharenite and siltstone with thick intervals of
grey weathering, interstratified, coarser grained sandstone, pebbly sandstone and granule to pebble
conglomerate. Clasts include quartz, mica, intraformational siltstone (0.5-1 cm), and flow-banded rhyolite.
Regional relationships indicate that the Graham Hill Formation is also a lateral facies equivalent of the
Barrens Hills Formation. In separate stratigraphic sections, both formations conformably overlie the Little
Stewiacke River Formation. In the eastern portion of 11E/06, the Graham Hill Formation is complexly
interstratified with both the Barrens Hills and Little Stewiacke River formations. This indicates that the three
formations are, at least in part, time equivalents. This style of interfingering is thought to characterize the
stratigraphic relationships between formations throughout the Basin.
The Cross Brook Formation consists of grey-green weathering sandstone interstratified with less
abundant grey-green weathering siltstone, shale and conglomerate and rare limestone. The Cross Brook
Formation is not exposed in this map area, but further east it occurs along the southern flank of the Basin.
The sandstones are typically fine- to coarse-grained, micaceous, variably feldspathic, and locally contain
varying amounts of granule-sized quartz and sedimentary/metasedimentary lithic fragments. They generally
are thinly bedded and commonly display ripple crosslamination, and trough cross-stratification in sets up
to 1 m thick. Pebble conglomerates are polymict, poorly sorted and framework supported. Dominant clast
types in the sandstones and conglomerates include psammite, pelite, micaceous granite, vein quartz and
muscovite. Less abundant, sedimentary clasts include laminated carbonaceous mudstone (possibly of
algal origin), siltstone, sandstone, carbonate and organic debris, all of which are interpreted as intrabasinal
detritus. Most clasts are subangular to subrounded. Siltstone and shale beds are grey weathering,
micaceous and display parallel lamination and ripple crosslamination.
The West River St. Marys Formation consists of reddish-brown to grey-brown weathering conglomerate
interstratified with grey-brown weathering sandstone. The Formation outcrops along the southern flank of
the central and eastern portions of the Basin. The red-brown to grey-brown weathering conglomerate
contains clasts ranging from pebbles to boulders. The rock is dominantly framework- to locally matrix-
supported with a roughly 80:20 framework to matrix ratio. It is very poorly to poorly sorted, may contain
imbricated pockets, or display crude inverse- to normal-grading. The conglomerate contains numerous,
major scour surfaces and fines upward to large pebble-size in the top of the measured section. Basal
contacts with sandstone lenses are erosional. Clast shape and size vary with composition. Sedimentary
clasts are largest (sandstone to 90 cm, shale/siltstone to 6 cm) and are subrounded to subangular.
Metasedimentary clasts are similar in shape, but generally smaller in size. Granite and quartz clasts are
rounded to well-rounded, the latter reaching 30 cm in diameter. Sandstone clasts are dominantly
grey-green weathering, fine- to medium-grained, micaceous and feldspathic. In some instances they exhibit
postdepositional en echelon tension fractures. Clast counts also indicate that metasedimentary clasts are
marginally more dominant in the west and sedimentary clasts are more dominant in the east.
Metasedimentary clasts are dominantly dark grey weathering pelite, commonly with an inherited tectonic
fabric. The matrix is grey-brown weathering, medium- to very coarse-grained, feldspathic, lithic sandstone.
Conglomerates further upsection are finer grained and better organized, displaying imbrication and
trough cross-stratification. In the eastern portion of the Basin, these conglomerates contain a significant
amount of plant debris including fragments up to 30 cm long. Sandstone occurs as trough-shaped lenses
up to approximately 2 m thick, characteristically 30-80 cm thick, with a minimum lateral extent of 15 m.
The lenses are grey-green weathering, medium- to very coarse-grained, feldspathic and micaceous.
Occasional interstratified pebbly or granulestone horizons occur. Scours, trough cross-stratification
(sets to 30 cm), ripple cross-stratification and normal grading all occur in the sandstone. The number of
sandstone lenses increases upsection.
The deposition of coarse conglomerates occurs along the southern flank of the Basin suggesting a
strong tectonic influence on sedimentation where subsidence along this Basin margin occurs along
northerly dipping listric normal faults. In contrast, the character of the sediments does not vary with
proximity to the northern margin (Chedabucto Fault) suggesting that the Fault does not constitute the
J. B. Murphy and R. J. Rice
Recommended Citation
Map Notes
Universal Transverse Mercator Projection (UTM), Zone 20, Central Meridian 63°00' West.
Base and digital data derived from the Nova Scotia Topographic Database (NSTDB). The NSTDB is
available from Service Nova Scotia and Municipal Relations (SNSMR), Land Information Services
Division (LIS), Nova Scotia Geomatics Centre (NSGC), Amherst, Nova Scotia.
We acknowledge the support of the Geological Survey of Canada, Natural Sciences and Engineering
Research Council, Caledonia Mining Corporation and the Nova Scotia Department of Natural Resources.
We are grateful to David Dowe, Samantha Evans, Lorne Jennex, Fraser Keppie, Jon Malone, Sarah
Jane Mosher, Cashel Meagher, Alex Nazck, Jacquie Stevens, Tim Stokes and Tim Webster for
assistance in the field.
Map production funded by Natural Resources Canada and Nova Scotia Department of Natural
Resources under the Targeted Geoscience Initiative (Phase 2) Project: Geological Mapping and
Resource Evaluation in Central Nova Scotia, 2004-2005.
Cartography and reproduction by Nova Scotia Department of Natural Resources, Geoscience
Information Services Section, 2004-2005.
North American Datum (NAD) 1927.
Disclaimer
The information on this map may have come from a variety of government and nongovernment
sources. The Nova Scotia Department of Natural Resources does not assume any liability for
errors that may occur.
±
LEGEND
CARBONIFEROUS
LATE DEVONIAN - EARLY CARBONIFEROUS
undivided
reddish-brown to grey-brown weathering, pebble to boulder conglomerate interstratified with grey-brown weathering sandstone. Abundant clasts derived from the Meguma Terrane.
grey-green weathering sandstone, interbedded grey-green weatheringsiltstone, shale, conglomerate and rare limestone. Abundant clasts derived from the Meguma Terrane.
Map Area..................
NTS Map Sheets......
Study Area................
GRAHAM HILL FORMATION (L@-E#Hgh): red and maroonweathering, finer grained litharenite to feldspathic litharenite and siltstone with thick intervals of grey weathering, interstratified, coarsergrained sandstone, pebbly sandstone and granule to pebble conglomerate. Clasts include quartz, mica, intraformational siltstone (0.5-1 cm), and flow-banded rhyolite. LOCHIEL FORMATION* (L@-E#Hl): grey or green, fine- to very coarse-grained, micaceous and feldspathic sandstones, interbedded minor granulestone, dark grey siltstone.
E#W
L@-E#Hcb
L@-E#Hwr
Nova Scotia Department of Natural ResourcesMineral Resources Branch
Murphy, J.B. and Rice, R.J. 2005: Geological map for part of NTS 11E/07, Hopewell
area, Nova Scotia; Nova Scotia Department of Natural Resources, Mineral Resources Branch,
Open File Map ME 2005-111, scale 1:50 000.
original Basin margin, and that an unknown portion of the Basin and its Meguma basement have been
tectonically removed and may be found north of the Fault.
The St. Marys Basin is an example of basin development and evolution adjacent to an intracontinental
fault zone associated with oblique convergence during orogenesis. Its evolution provides constraints on
the potential relationship between the termination of the mid-Paleozoic Acadian Orogeny, subsequent
basin development and the ongoing interactions between the Avalon and Meguma terranes, and between
Laurentia and Gondwana during the assembly of Pangea. More generally, because the relationship
between fabric development and motion along intracontinental strike-slip faults in continental zones is
difficult to interpret, the sedimentology and structural geology in basins developed along these fault
zones may preserve a less ambiguous record of the main tectonic events.
The evolution of the St. Marys Basin preserves evidence of protracted dextral shear along an
intracontinental fault zone during collisional orogenesis and the assembly of Pangea. The origin and
evolution of the Basin are attributed to either discrete or progressive dextral strike-slip tectonics along the
Minas Fault Zone (MFZ) between the Late Devonian and Late Carboniferous. Evidence for the Late
Devonian origin of the Basin is recorded along its southern flank by the fabrics of the deformed
ca. 370 Ma granites, the overall sedimentary facies distribution and some syndepositional features
within the clastic rocks. The most intense deformation within the Basin is concentrated in a narrow
east-northeastward-trending zone, in which predominantly fine grained clastic rocks are deformed into
periclinal folds and related reverse faults. The orientation of this zone, relative to the MFZ, is consistent
with dextral shear. At least some of this deformation occurred after the deposition of the overlying
Viséan Windsor Group (11E/06). The style of deformation along the present northern margin of the
Basin (the Chedabucto Fault) is also consistent with regional dextral shear.
Benson, D.G. 1967: Geology of the Hopewell map area, Nova Scotia; Geological Survey of Canada,
Memoir 343, 58 p. and Map 1215A, scale 1:63 360
Benson, D.G. 1974: Geology of the Antigonish Highlands, Nova Scotia; Geological Survey of Canada,
Memoir 376, 92 p.
Fletcher, H. and Faribault, E.R. 1887: Geological surveys and explorations in the counties of
Guysborough, Antigonish, Pictou, Colchester and Halifax, Nova Scotia from 1882-1886; Geological
Survey of Canada, Annual Report, v. II, 1886, pt. P, p. 5-128.
Jennex, L.C. 1998: Geological and geophysical investigation of the western St. Mary's Basin,
central mainland Nova Scotia: implications for paleoplacer gold potential; unpublished M.Sc.
thesis, St. Francis Xavier University, Nova Scotia, 286 p.
Jennex, L.C., Murphy, J.B. and Anderson, A.J. 2000: Post-orogenic exhumation of an auriferous
terrane: the paleoplacer potential of the Early Carboniferous St. Marys Basin, Canadian Appalachians;
Mineralium Deposita, v. 35, p. 776-790.
Murphy, J.B. and Rice, R.J. 1998: Stratigraphy and depositional environment of Horton Group rocks in
the St. Mary’s Basin, central mainland Nova Scotia; Atlantic Geology, v. 34, p. 1-26.
Murphy, J.B., Rice, R.J., Stokes, T.R. and Keppie, D.F. 1995: The St. Mary's Basin, central mainland
Nova Scotia: Late Paleozoic basin formation and deformation along the Avalon-Meguma terrane
boundary, Canadian Appalachians; in New Perspectives in the Caledonian-Appalachian
Orogen, eds. J. Hibbard, C. Van Staal and P. Cawood; Geological Association of Canada, Special Paper,
p. 409-420.
Murphy, J.B., Stokes, T.R., Meagher, C. and Mosher, S.J. 1994: The geology of the eastern St. Mary's
Basin; in Eastern Canada and National and General Programs; Geological Survey of Canada,
Current Research 1994-D, p. 95-102.
Webster, T. 1996: Digital imagery and geology of the St. Mary's Basin, Nova Scotia; Acadia University,
Nova Scotia.
Webster, T., Murphy, J.B. and Barr, S.M. 1998: Anatomy of a terrane boundary: an integrated structural,
GIS, and remote sensing study of the Avalon-Meguma terrane boundary, mainland Nova Scotia, Canada;
Canadian Journal of Earth Sciences, v. 35, p. 787-801.
BARRENS HILLS AND LITTLE STEWIACKE RIVER FORMATIONS (L@-E#Hbh/ls): undivided BARRENS HILLS FORMATION: resistant grey to grey-whiteweathering, fine- to very coarse-grained sandstone, monomict or polymict granulestone and conglomerate interstratified with recessive micaceous, grey to dark grey weathering shale and/or siltstone, minor red siltstone and sandstone. LITTLE STEWIACKE RIVER FORMATION: interstratified, thinly bedded, bioturbated mudstone, fissile, light to dark grey and black shale and slate, and light to dark grey sandstone containing comminuted plant debris.
Selected References
Open File Map ME 2005-111
Geological Mapfor Part of NTS 11E/07,
Hopewell Area, Nova Scotia
WINDSOR GROUP
Outcrop data from Benson (1967), although not illustrated, were used locally tohelp support map interpretation. Map users should refer to Benson (1967) foradditional outcrop locations and structural measurements.
L@-E#Hbh/lsL@-E#Hgh L@-E#Hl
Acknowledgments
Bedrock units are not mapped in this map area*
Geological Symbols
Interfingering contact, approximate (units of approximately similar age, units of differing age) . . . . . . . . . . . . . . . . . . . . .
!(
!(
!( !(
!(
!( (( (
(
(
Geological boundary (defined, approximate, assumed) . . . . . . . .
Major fault (defined) . . . . . . . . . . . . . . . . . .
Minor fault . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Anticline and syncline (approximate) . . . ®®
®
®
Minor fold axis . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Cleavage or foliation, 1st generation (inclined, vertical) . . .
Intersection lineation, 1st generation . . . . . . . . . . . . . . . . . . . . .
Bedding, tops unknown (inclined, vertical, horizontal) . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Bedding, tops known (inclined,overturned, vertical, horizontal) . . . . . . . . . . . . . . . .
Outcrop . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Legend
County Boundary . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Railway Inactive . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Railway . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Trail/Footpath . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
VehicleTrack . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Loose Surface/Resource Access Road . . . . . . . . . . . . . . . . .
Road Under Construction . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Hard Surface Road . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Collector Highway . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Trunk Highway . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Trans-Canada Highway . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
100 Series Highway . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Lakes, Single-line Rivers, Streams . . . . . . . . . . . . . . . . . . . . .
333
4
104
102
Coastline . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Index Depression Contour . . . . . . . . . . . . . . . . . . . . . . . . . . .
Depression Contour . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Index Contour . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
Contour . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . . .
*