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TitleQuaternary geology and till geochemistry of the western part of Cumberland county, Nova Scotia [Sheet 9]
AuthorStea, R R; Finck, P W; Wightman, D M
SourceGeological Survey of Canada, Paper 85-17, 1986, 58 pages (1 sheet),
PublisherNatural Resources Canada
MapsPublication contains 2 maps
Map Info.surficial geology, surficial geological, 1:100,000
Mediapaper; on-line; digital
RelatedThis publication contains Stea, R R; Finck, P W; (1986). (Sheet 9), Surficial Geology, Chignecto Peninsula, Nova Scotia, Geological Survey of Canada, "A" Series Map no. 1630A
File formatpdf
ProvinceNova Scotia
NTS21H/07; 21H/08NW; 21H/08SW; 21H/09NW; 21H/09SW; 21H/10; 21H/15; 21H/16NW; 21H/16SW
AreaChignego Peninsula
Lat/Long WENS-65.0000 -64.2500 46.0000 45.2500
Subjectsgeochemistry; surficial geology/geomorphology; tills; till geochemistry; clasts; lithology; till fabric; sandstones; coal; limestones; argillites; mudstones; intrusive rocks; sample preparation; grain size analyses; palynology; geochemical surveys; pebble lithology; deltaic sediments; ice movements; moraines; glacial features; Five Islands Formation; Quaternary
Illustrationsgeological sketch maps; charts; photographs; cross-sections
Released1986 05 01; 2015 08 20
AbstractThe area comprises two distinct physiographic regions, the Cumberland-Pictou Lowlands and the Cobequid Highlands. Bedrock, till, glaciojluvial, glaciomarine, alluvial, colluvial, marine, and organic sediments make up the sUJface materials. Large areas of mechanically and chemically weathered bedrock, residuum, on the Cobequid Highlands are believed to derive from a pre-Wisconsinan nonglacial interval. The first glacier flow recorded in the area, thought to be Early Wisconsinan in age, was eastward across Chignecto Bay, then southeastward. It formed the compact, calcareous M cCarron Brook Till. After this event there is some evidence for a brief nonglacial interval. Ice then.flowed southward and southwestwardfrom a centre over Prince Edward Island. The grey Joggins Till and the reddish-brown Eatonville Till were formed during this flow. The next glacial event was a pulse of southwestward.flow which created the bouldery Shu lie Lake Till and a moraine which blocks Parrsboro Gap. The Shu lie Lake Till terminates along an east to west line north of the Cobequid Highlands marked by Shulie and Welton lakes. This till limit represents a glacier marginal stand. These successive till-forming ice flows are termed the McCarron Brook, Eatonville and Shulie Lake phases. De glaciation probably occurred at the end of the Eatonville Phase about 14 000 years B .P. as glaciomarine deltas were being constructed along the north shore of Minas Basin. Meltwater was cut off to the deltas during Shulie Lake Phase when the moraine across Parrsboro Gap was constructed. Radiocarbon dates and pollen evidence from buried peat and basal organic sediments north of Shulie Lake Till limit suggest that ice persisted there until 12 000 BP and perhaps as recently as JO 500 BP. Marine limit decreases from 37 m above m.s.l. to 15 m northeastward along Chignecto Bay. Marine limit also decreases eastward in Minas Basin from 38 mat West Advocate to 22 mat Parrsboro. The decrease in marine limit along the.flow path of the Shulie Lake Phase suggests that the formation of raised marine features on the south coast of Chignecto Bay was delayed by ice in the bay. Pb and Zn geochemical anomalies in the locally-derived Shulie Lake Till suggest the presence of this type of mineralization in the Late Carboniferous Cumberland Group in the map area. Organic-rich channel-lagfacies may have been the focus for Pb-Zn precipitation within the Cumberland Group sandstones. Cu and As anomalies in residuum developed from the Devono-Carbon!ferous Greville River Formation correlate with chalcopyritearsenopyrite mineral occurrences along Glooscap Fault.