The Wabigoon subprovince in northwestern Ontario, Canada, is a Mesoarchean and Neoarchean greenstone-granite terrane, bounded to the north and south by the younger Neoarchean metasedimentary English River and Quetico subprovinces. The eastern Wabigoon subprovince includes the Onaman-Tashota Belt (OTB) and the Beardmore-Geraldton Belt (BGB). The OTB occupies the centre of the eastern Wabigoon subprovince where it consists of Mesoarchean (2975 Ma - 2922 Ma) and Neoarchean (2780 Ma - 2740 Ma) metavolcanic and metasedimentary assemblages, older tonalitic gneisses, and syn-volcanic and syn-tectonic Neoarchean plutons. Younger 2710 Ma – 2695 Ma metasedimentary sequence of interlayered sandstone, argillite and conglomerate are infolded with the metavolcanic rocks. The OTB has a dome-and-keel structural architecture characterized by tightly folded metavolcanic and metasedimentary rocks in between the Neoarchean Ombabika batholith and Onaman pluton, a steeply-dipping and northerly-striking foliation and down-dip stretching lineation wrapping around these intrusions, high strain zones along intrusion-volcanic rock contacts, and an overall younging of the metavolcanic rocks away from the intrusions. The BGB is located along the southern margin of the eastern Wabigoon subprovince and represents a transitional belt between the metasedimentary Quetico subprovince to the south and the Wabigoon subprovince to the north. It consists of E-trending and steeply-dipping, interleaved panels of 2700 Ma –2694 Ma metasedimentary and 2725 Ma metavolcanic rocks, which are bounded by thrust faults that were reactivated as transcurrent faults. It has a linear accretionary architecture that contrasts with the dome-and-keel architecture of the adjacent OTB to the north, although both are coeval and formed between 2700 Ma and 2690 Ma during closure of the Quetico basin and collision with a greenstone-granite terrane to the south. The OTB and BGB further differ in gold endowment. The OTB hosts few small gold deposits, past-producing mines, and early 20th century artisanal mines, which collectively produced less than 120,000 ounces of gold, whereas gold deposits in the BGB collectively produced 4.1 million ounces of Au. Gold is typically associated with early quartz-carbonate veins hosted by high strain zones and shear zones that formed during the downward flow of the supracrustal rocks between uprising granitic domes in the OTB and during accretion and imbrication of supracrustal rock panels in the BGB. Gold was further emplaced during the transcurrent reactivation of the panel-bounding shear zones in the BGB, which coincide with steeply-dipping zones of low reflectivity and resistivity that extend down to crustal depths of 15 km on the Metal Earth seismic and magneto-telluric transect across the eastern Wabigoon subprovince. The shear zones acted as conduits for the upward migration of hydrothermal fluids and possibly magmas, which altered the rocks and produced the geophysical responses observed on the Metal Earth transect. Thus, the presence of deeply penetrating reactivated structures in the BGB explains its preferential gold endowment and suggest that accretionary horizontal tectonics is more favorable for the formation of gold deposits than vertical dome-and-keel tectonics, although both may be coeval.