Originally claimed in 2011 and covering 517 sq/km and 920 claims. An airborne survey was flown in 2012 and followed in 2013 by a soil survey to determine the sectors with potentiel.
These surveys brought us to divided the In Between into four distinct blocks: the Landry block, the Wares block, the MacNeil block and the McDonald block that now consists of 200 sq/km and 315 mining claims.
The properties are part of NTS 22A13 and 22H04.
- Focus work on targets defined by the Geophysics airborne (Mag and Spectro)
- 436 targets 141 priority target
- Generate targets using CARDS system from Diagnos (TSX-V : ADK)
- Surface exploration (team of prospectors and mapping)
- Soil geochemistry survey
- First program 3000 samples
- Second program 1000 samples
- Preparation of future drilling
The Gaspé Peninsula is a segment of the Canadian Appalachians that formed as a result of terrane accretion to the North American craton during the Paleozoic (Bourque et al. 1995). The Gaspé Peninsula consists of two principal lithotectonic assemblages(Williams 1979):
• The Humber zone is the vestiges of a passive continental margin sequence of Cambro- Ordovician age (544 My to 440 My to today).
• The Dunnage zone represents an assemblage of oceanic terrains of Silurian-Devonian age (440 My to 360 My to today).
The contact between the Humber and Dunnage zones is a linear zone of discontinuous serpentinites, dismembered ophiolites and called the Brompton-Baie Verte Line. The InBetween property is located at the contact between the Humber and Dunnage zones, in the northern part of Gaspé Peninsula within the Silurian-Devonian rocks of the Dunnage zone. The Silurian-Devonian rocks of the Gaspé Peninsula are divided into three major structural zones (Malo and Bourque 1993):
1. The Connecticut Valley Gaspe Synclinorium
2. The Aroostock-Percé Anticlinorium
3. The Chaleurs Bay Synclinorium
The Connecticut Valley-Gaspé Synclinorium lies between the Cambro-Ordovician allochtonous rocks of the Taconian Orogen to the northwest and the Aroostook-Percé Anticlinorium to the southeast. It is bounded to the north by the Schick Schock-South fault, a dextral strike-slip fault (Malo and Bourque 1993), and by the Grand Pabos Fault to the south. The stratigraphic succession in the Connecticut Valley-Gaspé Synclinorium consist of shallow marine clastic, carbonate and minor volcanic rocks assigned to the Chaleurs Group. The Chaleurs Group is overlain by the Upper Gaspé Limestone Group, which consists of shallow- to deep-water shelf carbonates deposited on a stable platform (Bourque et Al. 1995). The Upper Gaspé Limestone group is overlain by the Gaspé Sandstones Group, which represents a gradually shallowing basin in an intra-arc extensional setting, and is accompanied by increasing bimodal volcanic activity(Bellehumeur and Valiquette 1993). The Siluro-Devonian rocks of the Connecticut Valley-Gaspé Synclinorium are intruded by dikes and plutons associated with Acadian faults. The epigenetic deposits of the Gaspe Peninsula (Mines Gaspe, Sullipek, Mines Madeleine, Reboul, Patapédia and Ste-Marguerite) are related to the hydrothermal activity generated by these Acadian intrusions. The hydrothermal activity of intrusions produced skarn in the carbonated surrounding sediments and porcellanite in the pellitic surrounding sediments. The skarn and porcellanite are mainly mineralized in copper. Along the faults and breaks in the rocks, hydrothermal activity produced quartz-carbonate veins principally mineralized in copper, gold and silver.