Paleomagnetism and magnetic fabrics were determined for 2903 samples of the Akamas ophiolite, for comparison with the Troodos ophiolite, both located on the island of Cyprus.  The relationship between the ophiolites is inferred from the anisotropy of magnetic susceptibility (AMS), natural remnant magnetism (NRM) combined with low temperature demagnetization (LTD) and thermal demagnetization (TD), and paleopole studies.

From these data, it is determined that the ophiolites are of similar origin but produced at different times and locations.  Akamas is a Triassic slow spreading center from a rifted continental margin and Troodos is a Cretaceous slow spreading center from a suprasubduction zone.  The magnetic fabric from both Akamas and Troodos is that of an S-fabric, with a slightly continuity into the L-fabric field.  The AMS data for both ophiolites dips east-south-east, with two distinct regions of foliation, one steep and one shallow.  Principle component analysis determined two distinct magnetic polarities, both exhibiting a mild tectonic smearing.  The paleopole for these data points is determined to be 73 N, 95 W and 75 N, 85 E in a normal field and 27 S, 45 E and 10 S, 20 E in a reversed field.  The mean declination and inclination for these data is 159/-62 and 210/-47 in a normal field and 159/62 and 210/47 in a reversed field (a₉₅ = 10.6).  These data are plotted in the apparent polar wander path for Cyprus determined by Borradaile and Gauthier (in prep.).  It is concluded that the difference in magnetic polarity seen in the PCA analysis of the NRM (LTD, TD) results represent a reversal of the Earth's magnetic field.  This reversal is confirmed by magnetostratigraphy comparisons with Upper Triassic data.  The paleopole data also indicates a ~120° anticlockwise rotation of the Akamas ophiolite and the Mamonia terrain, prior to the documented 90° anticlockwise rotation of Cyprus.

Perovskite-type compounds in the series tausonite-lueshite, (SrTiO₃-NaNbO₃), were synthesized by solid-state reaction and analyzed using X-ray powder diffractometry.  The structures of several intermediate compositions were determined using the Rietveld refinement method.  In the compositional range 0≤ x ≤0.2, the series consists of an undistorted cubic structure in the space group Pm3m, with cell dimensions ranging from a≈3.905-3.916....  At the composition of x=0.9, a combination of the orthorhombic spaces groups Pbma and Pbnm is believed to occur (a ≈ 5.558, b ≈ 15.625, c ≈ 5.519 ...).  In the compositional range 0.95≤ x ≤1.00, the structure is orthorhombic and belongs to the space group Pbma.  In the series (SrTiO₃-NaNbO₃), the degree of structural distortion increases with x as a result of Na substituting into the A-site for Sr, and Nb substituting into the B-site for Ti.

The agate deposit at the TBAM is located 1 km northeast of Thunder Bay, Ontario in ferrodolomite of the Gunflint Formation.  The age of the agate deposit is delimited by the age of The Gunflint Formation and the age of the Logan sills which crown the Gunflint sediments to the west of the deposit.  The agate shows a consistent sequence of mineralization from nucleation against the host-host: dark amorphous silica (opal-A?), light amorphous silica (opal-CT?), translucent chalcedony, a-quartz, and vug-filling graphitic carbon.  The deposition of the agate appears to be related to pervasive, early silicification of the Gunflint and other Lake Superior-type iron formations.  Siliceous solutions from thermal springs located near the centre of the depositional basin were expelled to the margins by compaction.  At the site of agate deposition, the solutions encountered CO₂ from decaying organic matter.  The presence of CO₂ and organic material would create a pocket of decreased pH and temperature.  δ¹³C valves for vug-filling graphitic carbon show it is organic in origin.  Geochemical modeling demonstrates that the sequence of mineralization observed at the TBAM will precipitate from a solution in equilibrium with dolomite and atmospheric CO₂ as it experiences a decline in pH and temperature.

The carbonate sequence located in the upper most portion of the Paleoproterozoic Gunflint Formation was studied in detail, in an attempt to understand the ambient conditions that were present at the time of deposition and cementation.  The study included analyses of shore proximal sediments and structures using geochemical instrumentation, as well as qualitative interpretations of depositional environments based upon in-depth microscopic observations.  The carbonate sequence itself was located on the border between the sediments of the Gunflint Formation and the siliciclastic Rove Formation.  Moving up through the Gunflint Formation, through the carbonate and eventually into the Rove Formation one encounters major changes in the depositional environments in the surrounding area.  Indications of these major changes are drawn from the broad differences in compositions of the units.

Whole and partial rock geochemistries were acquired via the ICP-AES at Lakehead University (LUIL), as well as from the ICP-MS at the Ontario Geologic Survey, located in Sudbury.  Quantitative SEM analyses and qualitative SEM elemental mapping were conducted; as well the samples were subject to combustion reactions to determine H₂O and CO₂ content of samples via the LUIL.  Also, a vast amount of information was gained using a high-power Olympus petrographic microscope digital imaging system via the Lakehead University Geology Department.

Although the carbonate sequence throughout the area was discontinuous, those outcrops sampled contained similar units in comparable order and could be correlated.  The majority of the outcrops sampled contained strata that placed them in a shore proximal environment that may have been sub-aerially exposed at some point in the Paleoproterozoic.  These features included a stromatolitic layer with an adjacent scoured fine carbonate sand, as well as upper and lower coarse carbonate sands.  Analyses of the units indicated that they are composed mainly of Fe-rich chlorite grains bounded in a calcite cement.  As well, some layers contained abundant dissolution and silica replacement.  Abundant V enrichment was associated with the Fe-rich chlorites throughout the shore proximal sediments.

As a comparison, outcrops located at a stratigraphically lower level in the carbonate sequence were sampled.  These samples represented more off-shore sediments deposited in the submarine environment at the time.  Analyses of these sediments indicated a much different composition to the more shore proximal sediments.  Not only did the samples not contain any of the shore proximal features, they were composed almost entirely of ankerite.  The submarine sediments also contain rare, highly silicified stromatolite fragments, as well as pressure solution features, such as styloites characteristic of the deep burial environment.

The fact that the shore proximal sediments contain cements that do not reflect the chemistry of the ocean during the Paleoproterozoic suggests that the calcitic cements were more reflective of the meteoric environment.  The large V enrichments also suggested the presence of a redox boundary, as well as suggesting an oxic atmosphere.  REE curves for the ankeritic marine precipitates show Ce anomalies that reflect an anoxic ocean, whereas those of the meteoric calcite cements reflect an oxic atmosphere, further reinforcing conclusions from other geochemical data.

The Thunder Bay Amethyst Mine Panorama boasts one of the largest occurrences of amethyst in the world with two distinct generations of veining.  These two generations of veins display vastly different colours, with the first generation veins being colourless and the second generation displaying a purple colour.  It is hypothesized within this thesis that the second-generation veins bleached the first generation veins during their deposition.

A series of heating experiments were conducted to determine how amethyst colour changed with respect to heat and time.  Amethyst samples used for experimentation were collected from the main fault and cut into 15 by 9mm slabs.  These samples were examined using a photospectrometer before and after each heating interval.  The results were then graphed by examining the absorbance of light against energy of light; spectral peaks representing colour centers known to cause amethysts purple colour were then fitted.

Samples were heated at temperatures of 350°C, 300°C and 250°C using a tube furnace attached to a digital temperature interface until colour was complete lost.  Samples heated at 350°C and 300°C became bleached quickly at periods of 1 and 3 hours respectively.  Extended heating of samples at 250°C resulted in no colour loss after a time period of 622 hours.  Peak fitted photospectropic  scans were then examined after each subsequent heating period and compared to the scans before colour loss occurred.  These results decreasing Fe⁴⁺ colour centers when samples lost colour and no change in colour centers when colour loss did not occur.

The stability of colour within amethyst at temperatures lower than 260°C can be attributed to a lack of energy required to overcome the activation energy barrier.  It has therefore been determined that the deposition of second-generation veins likely did not cause bleaching of the first generation veins.

This pegmatite occurrence is part of the Georgia Lake Rare-Element Pegmatite Field of the Quetico Subprovince, NW Ontario, and is related to Stype, peraluminous Georgia Lake granites. The Georgia Lake pegmatite field is approximately 32 by 105 km wide, and is hosted entirely within the clastic metasedimentary rock of the Quetico Subprovince.  There have been 38 rare element occurrences discovered, including 10 spodumene-bearing occurrences, with approximately 11.7 million tons averaging 1.14% lithium oxide.  The 2670 +/- 2 Ma Glacier Lake Batholith extends greater than 100 km NE into the Quetico Subprovince, and has been interpreted to be the result of partial melting, creating the associated S-type granites of the Georgia Lake pegmatite field.

The Rock Tech Li pegmatite occurrence fits into the classification of albite-spodumene-type pegmatite. The associated dykes and veinlets are not heavily fractionated or diverse from the pegmatite body.  The aplite veins represent a fine- grained assemblage of the Rock Tech Li pegmatite with no exotic mineralogy.  The veins emplaced and expanded pre-existing fractures.

The Sharpsand River IOCG prospect is located within the southern Algoma district, of the western Abitibi terrane, in the Archean Superior province.  This study integrates field mapping, petrography and x-ray diffraction analysis to determine; mineralogy, the controls on mineralization, the paragenesis of the prospect and to constrain an appropriate deposit model for the Sharpsand River prospect.  It has had previous exploration work completed in 1962 consisting of trenching, magnetometer surveys and 297 m of diamond drilling.  Assay results from the trenches and diamond drill holes averaged 1.18% Cu throughout, and a maximum value of 5.40%.

Five lithologies were identified within the study area, consisting of Algoma monzogranite, Keweenawan diabase intrusives, quartz veins, silicified breccia and quartz/diabase breccia.  The Algoma monzogranite is the host rock in the study area and is comprised of weakly foliated, coarse- to medium-grained plagioclase, microcline, quartz and minor biotite.  The Keweenawan diabase dikes consist of 5 to 50 m vertical dikes intruding the monzogranite at a northwest-southeast trend, and are related to the Mackenzie dike swarm.  The dikes are comprised of fine-grained, massive plagioclase, pyroxene and finely disseminated magnetite.  After the intrusion of the Keweenawan dikes, the area underwent regional greenschist metamorphism, altering pyroxenes to clincochlore, forming selectively pervasive sericite alteration and causing recrystallization of primary quartz and magnetite.  The quartz veins occur in a northeast-southwest trending fault zone through the topographic low in the middle of the study area.  Silicification of the fault zone occurred penecontemporaneously to faulting.  The quartz veins consist of coarse-grained, euhedral quartz with minor clinochlore and chalcopyrite, with common open filling textures.  The silicified breccia unit represents the area between the intersections of diabase dikes and the barren quartz vein, characterized by 60-90% quartz by modal composition, with strongly altered diabase fragments and shear textures.  The quartz/diabase breccia occurs at the intersections of the diabase dikes and quartz veins, and is comprised of equal proportion of vein fill, dominated by quartz, and angular diabase clasts.  This unit hosts the strongest chalcopyrite and hematite mineralization.  The chalcopyrite and hematite mineralization was precipitated by late stage hydrothermal fluids, which intruded the fractured quartz veins and through oxidation of primary magnetite in the Keweenawan dikes, concentrated the mineralization in the quartz/diabase breccia unit.  Controls on the mineralization have been determined to be the presence of magnetite bearing diabase dikes, the northeast-southwest trending fault zone, silicification of the fault zone and the hydrothermal fluids to concentrate the mineralization.

The IOCG deposit model in the broadest sense is applicable to the Sharpsand River prospect.  The prospect fits the IOCG deposit model due to: (1) presence of copper and trace gold, (2) hydrothermal ore styles and strong structural controls, (3) abundant magnetite and hematite and (4) no clear spatial associations with igneous intrusions.  To constrain a specific IOCG deposit subtype, more research should be conducted through geochemical analysis to determine (1) the presence of LREE enrichment and low S sulphides, (2) the range in depth of formation of the prospect and (3) the Fe/Ti ratios of the Fe oxides.  Further exploration work would also be required to determine if the copper and gold are present in economic quantities.

The Hindon prospect is located on two leucocratic to mesocratic gabbro sills located 185 km north of Toronto Ontario. The sill has been interpreted as having evolved in the central gneiss belt during the Grenville orogeny. The Hindon property has historically been described as a folded gabbro sill, this is hard to reconcile due to an obvious lack of metamorphic texture. Since copper sulfides were discovered on the property in the 1950’s various work has been performed with in the property. Assays have shown a mix of promising copper results as well as possible PGE mineralization. Little is known about the structure and genesis of the gabbro; however, the two zones of the property show distinctly similar characteristics and therefore most likely share the same genesis. Copper mineralization is abundant but disseminated throughout the property. It is likely that the historically accepted mode of genesis for the gabbro with in the Hindon property is inaccurate, it is very likely that the gabbro intrusion occurred after the Grenville Orogeny. 

The Dickenson-Campbell diorite (DCD) is a lithological unit that is exposed at surface on and around the Red Lake Gold Mines (RLGM) near the town of Red Lake, Ontario.  The DCD has had an uncertain past with geologists using a variety of naming schemes for these rocks since their initial description in the 1940’s.  The goal of this thesis was to properly classify the DCD using modern geochemical methods combined with mapping and petrography.  Mapping was undertaken on all exposed DCD within Balmertown where structure and lithology were noted in detail.  Samples of the outcrop, as well as near-surface intersections of drill core were taken for geochemistry and petrography.  Analysis of the data that was obtained showed that the DCD is not an intermediate intrusive lithology.  Petrographic analysis revealed an abundance of glass and / or very fine-grained silica and carbonate mineralogy.  Not only was the very fine grain size an indicator of petrogenesis but the resemblance to the regional and underground basalts also helped refute the diorite theory.  Major and trace element geochemistry showed that all DCD outcrop and drill core samples were tholeiitic basalts and basaltic-andesites, with MORB-like signatures.  Mapping of the area provided an idea as to the stratigraphic relationship between the pillowed basalts and the DCD exposed at surface on the mine site.  Only one unit had well preserved pillows these showed evidence of south-western topping direction (towards the DCD).  The presence of narrow shear zones and conjugate fractures led to the conclusion that there has been an effect of pure shear on these rocks, likely due to regional scale deformation.  Samples taken from various areas in the Balmertown area revealed that there is a variation in the degree of alteration affecting the DCD.  The alteration is the most extreme near the base of the unit, where it is in contact with the underlying basalts.  The black ilmenitic flecks, commonly used as an identifier for the DCD, are the coarsest and most obvious where carbonatization and silicification of the rocks is the strongest.  This has led to the conclusion that the DCD is a rock type that is contiguous with the underlying Balmar assemblage basalts.