The Johan Beetz Area is situated on the north shore of the Gulf of St. Lawrence and is bounded by latitudes 50°15'N and 50°30'N, and by longtitudes 62°3O'W and 63°00'W. It measures about 22 miles east-west and 17 miles north-south and is approximately 350 square miles in area. Johan Beetz, after which this area has been named, is a small settlement on the shore about midway between the east and west boundaries of the area.

In the Jasper Basin, Jasper National Park, Alberta, the late Frasnian Simla Member and Mount Hawk Formation comprise a shallow water carbonate platform (upper part of the Ancient Wall reef complex) and an adjacent slope and basin respectively. The Frasnian-Famennian paraconformity overlies the Simla Member everywhere within the study area. Basinward, this boundary becomes conformable where it overlies the Mount Hawk Formation. The F-F boundary forms the basal bounding surface for the Sassenach Formation. The early Famennian Sassenach Formation comprises mixed siliciclastic/carbonate strata that overlie, onlap and frequently toplap the underlying Mount Hawk Formation and Simla Member along the northeastern margin of the Jasper Basin. / The stratigraphic relationships within the study area are not unique and may be explained by different sequence stratigraphic and depositional models. Two end member models are considered and illustrate the difficulty in distinguishing between depositional systems where accommodation space is controlled mainly by sedimentation rate (Model 1) or mainly by sea-level (Model 2). Model 1 and Model 2 represent a minimum and maximum amount of relative sea-level fall across the F-F boundary respectively. (Abstract shortened by UMI.)

Devonian Winterburn strata in the Boule and Bosche Ranges of eastern Jasper National Park consist of two unconformity bounded, 45 m thick carbonate dominated depositional sequences, the Arcs Member (Nisku) and the Ronde Member (Calmar/Blue Ridge). Earliest Famennian clastics of the Sassenach Formation directly overlie the Ronde and this contact forms the Frasnian/Famennian boundary. Sampling for conodont biostratigraphy in three sections indicates that the Arcs and Ronde are Upper rhenana in age. / Arcs, Ronde, and Sassenach strata were deposited on a gently sloping carbonate ramp to platform ranging from shallow subtidal to peritidal depositional environments. Argillaceous limestones and shales are the dominate lithotype of the Mount Hawk Formation. Shallow subtidal limestones consisting of floatstones and rudstones interbedded with packstones and wackestones comprise most of the Arcs Member. Arcs strata consist of at least 4 depositional cycles and represent a shallowing upward sequence from outer shallow slope fossiliferous limestones to back reef lagoonal grainstones. Two previously undocumented Arcs patch reefs were described, the limestone Brule reef or bank in the southern Boule Range and the dolomitized Moosehorn reef in the central region of the Bosche Range. The Ronde Member is comprised of shallow subtidal limestones and siltstones with intertidal silty limestones occurring less frequently and predominately at the top. The Ronde consists of two carbonate shallowing upward cycles. FA 6 A intertidal limestones and fine grained sandstones comprise the Sassenach Formation which consists of two main depositional cycles and ranges from 20 m thick in the Bosche Range to less than 5 m thick in the Boule Range. (Abstract shortened by UMI.)

The Tabbernor Fault zone (TFZ) in Saskatchewan is a >1500km geophysical, topographic and geological lineament that trends approximately northward along the province's eastern boundary. Detailed field mapping and petrographic analyses, coupled with remote sensing and geophysical evidence have shown that the TFZ is a fundamental structure within the Trans-Hudson Orogen (THO), separating and offsetting several lithotectonic domains. / Earliest deformation preserved within the TFZ in the Wollaston Lake area is the transposition of a regional gneissic foliation onto a northeast-trending flattening plane, within north-trending sinistral shear zones. The transposed fabric is characterized by folded and attenuated remnants of the gneissic foliation, together with boudinaged leucogranitic sheets and dykes. Within these shear zones a shear fabric is developed parallel to the margins in several locations. The shear fabric offsets all earlier foliations with consistent sinistral offset. Adjacent to the shear fabric, structures are reoriented to lie dose to the shear plane. / The fault and its associated structures controlled the intrusion of granitic and pegmatitic dykes which were subsequently weakly deformed. / Brittle overprinting of ductile fault features is widespread. Sedimentary features, apatite fission track data, and uranium mineralogical studies all show that the TFZ was reactivated at least twice in Phanerozoic times. (Abstract shortened by UMI.)

Immobile elements are used to determine rock affinities, precursors, and mass changes that occur during hydrothermal alteration. / Altered rocks at the New Insco mine are calc-alkaline andesites (SiO$ sb2 / sim$ 60 wt%, Zr/Y = 6.5, La$ sb{ rm N}$/Yb$ sb{ rm N}$ = 5.3). A tholeiitic rhyolite (SiO$ sb2 / sim$ 77 wt%, Zr/Y = 3.4, La$ sb{ rm N}$/Yb$ sb{ rm N}$ = 2) is located 0.5 km south of the orebody. Net mass change of +11% resulted from additions of Fe$ sb2$O$ sb3$ (16%) and MgO (3%), and losses of Na$ sb2$O (3%) and CaO (3%). Three major alteration assemblages with up to 80% chlorite, 57% sericite and 50% quartz are identified. Mineral and cation plots outline chloritization, sericitization and silicification trends. / The Key Tuffite is at the contact of Watson Lake tholeiitic rhyolite and Wabassee mixed calc-alkaline and tholeiitic andesites. Pyroclastic components of the Tuffite are from both rock groups: a tholeiitic rhyolite component--Zr/Y = 2.8 and La$ sb{ rm N}$/Yb$ sb{ rm N}$ = 2.1, and a calc-alkaline andesitic component--Zr/Y = 8.9, La$ sb{ rm N}$/Yb$ sb{ rm N}$ = 6.4. During formation Fe$ sb2$O$ sb3$ (27%, total iron), SiO$ sb2$ (14%), CaO (8%), S and K$ sb2$O were added to the pyroclastic components. The Key Tuffite is composed of 33% quartz, 28% sulfide, 16% sericite, 8% carbonate, 6% chlorite and 9% others. / Geochemical and mineralogical trends in altered rocks and tuffites increase toward orebodies and can be used as mineral exploration guides.

The layered series of the Muskox Intrusion can be divided into four megacyclic units on the basis of field mapping, each beginning with a thick olivine cumulate and succeeded up section by a variety of pyroxenitic and gabbroic cumulates. A systematic change in the order of appearance of orthopyroxene in the pyroxenite units of the layered series is correlated with a decrease in Mg no. (Mg/Mg + $ Sigma$Fe in cation units) at which clinopyroxene joins olivine on the liquidus, and spike-like increases in LIL/HFS ratios, which require that the composition of the magma of the Muskox Intrusion changed through time across the layered series. Mixing of residual liquid with primary liquids replenishing the chamber can explain the upsection decrease in the Mg no. of clinopyroxene at the base of successive pyroxenite units, but this mechanism cannot account for increased ratios of LIL to HFS incompatible elements observed in the olwebsterite of Megacycle #3 and the first websterite of Megacycle #4, because these ratios are not significantly fractionated by closed-system crystal fractionation. Contamination of the parental magma with melts from the paragneiss country rocks can reproduce the observed increase in the ratios of K/Ti and K/Zr. The gabbroic layers of Megacycle #1, #2, and #3 are especially enriched in LIL/HFS ratios, indicating the presence of a highly contaminated magma layer above the uncontaminated magma which crystallized much of the ultramafic series. The spike-like enrichment in LIL/HFS ratios in the pyroxenites suggests that episodic events of mixing occurred between an evolving uncontaminated magma and a highly contaminated magma, accumulated at the roof of the magma chamber.

The Troilus gold-copper deposit lies within the northeastern part of the Archaean Frotet-Evans greenstone belt, in the Opatica sub-province of the Superior Province, northern Quebec, and contains total reserves of 51 Mt at 1.08 g/t gold, 0.11% copper, and 1.4 g/t silver. The largest orebody, Zone 87, has been mined by open pit methods since 1993. / Rocks of the Troilus domain include a coarse- to medium-grained metadiorite, a finer-grained amphibolite, a rock with a brecciated texture and felsic dykes, which crosscut the metadioritic pluton, the amphibolite and the breccia. The amphibolite, breccia, and felsic dykes all locally host ore. / Previous researchers have proposed a porphyry-type model for the genesis of the Troilus deposit. However, evidence that the breccia unit is not hydrothermal but a product of magma mixing, that the felsic dykes predate mineralization, and that mineralization and associated alteration occurred as two discrete events separated by a major episode of regional metamorphism (amphibolite facies), requires that alternative genetic models for the deposit be considered, such as orogenic gold model. (Abstract shortened by UMI.)

Buildup interior cycle stacking patterns and buildup margin geometries of Frasnian Fairholme Group reef complexes suggest that deposition and buildup stratigraphy were controlled by short-term and long-term fluctuations in relative sea-level. Correlation of these stacking patterns, and regional trends in buildup margin morphology, reveal a hierarchy of fifth, fourth, and third order sea-level changes driven by an allocyclic mechanism. / The Caim Formation consists of shallowing upward hemicycles (fifth order). These are grouped into larger, broadly shallowing upward trends (fourth order). The Caim Formation and the overlying Peechee Member represent a single third order depositional sequence deposited during an overall period of sea-level rise. The dominantly retrograding buildup margins of the Peechee Member also reflect the influence of rising sea-level, punctuated by relative stillstands. Reciprocal siliciclastic basin sedimentation and buildup carbonate sedimentation characterized Peechee buildup margins. / The dominantly retrograding buildup margins of the Fairholme Group are characteristic of transgressive systems tracts. Buildup margins developed progradational or vertically aggradational geometries due to prevailing circulation patterns and the manner of basin filling.

The stratigraphy of the sediments on the Riviere-du-Loup platform consists in a thin layer ( 8 phi), deposited between 5,800 y B.P. and 4,400 y B.P. The underlying pelitic sediments are made out of series of silt and clay microlaminations ($ approx$1 mm), separated by thin layers (2 to 5 mm) of fine sand (2 $<$ $ phi$ $<$ 3) originating either from ice rafted materials or turbid flows along the bottom during the spring thaw. Variations in the size composition of the material entering the estuary or fluctuations in currents during tidal cycles, could explain the formation of the series of microlaminations. / At present, the circulation pattern of the residual current is modulated by the fornightly tidal cycle. During the spring freshet, from mid-May to mid-June, the circulation pattern is altered, and the vector of the residual current is oriented upstream whereas it is usually oriented downstream. The solid discharges of the spring freshet (4,104 t.d$ sp{-1}$), neap tide (1,800 t.d$ sp{-1}$) and spring tide (2,592 t.d$ sp{-1}$), are sufficient to transport in 12 days, 28 days and 19 days respectively, the amount of sediment dredged annually in the riviere-du-Loup harbor (50 * 10$ sp3$ t). / The TSM fluctuations are mainly controlled by the resuspension of sediments deposited during slack tide (2,250 t at neap tide and 3,735 t at spring tide). Advection of TSM from the MTZ explains the variations in turbidity observed on the outer edge of the platform. Downstream of the study area, fluctuations of turbidity are controlled by advection of a turbid plume located at the mouth of the riviere du Loup.

The regional distribution of Holocene sediments of eastern Hudson Bay off the Great Whale River mouth was mapped using a grid of reflection seismic lines over 60 km long and covering an area of approximately 800 km$ sp2$ and data from eight piston cores. A larger data base and a greater area of study than that used in previous studies significantly increases our understanding of the sedimentation and deglaciation processes that have occurred in the area since the last deglaciation. Based on the seismic records and piston cores, four stratigraphic units overlying the Proterozoic bedrock (unit 1) were defined and interpreted: unit 2, glacial till deposited by a westward flowing ice sheet; unit 3, glaciolacustrine stratified muds deposited in glacial Lake Ojibway; unit 4, postglacial marine muds deposited in Tyrell Sea; unit 5, distal fluvio-deltaic sediments from the Great Whale River. Textural and geochemical analyses of individual laminae suggest that unit 3 rhythmites are true varves; dark "summer" laminae were deposited mainly by underflows during the open water season, and light "winter" laminae were deposited by overflows-interflows under a seasonal ice cover. Unit 5 covers approximately 400 km$ sp2$ and occurs as a deltaic constructional wedge which reaches 11 km offshore of the Great Whale River entrance. It was deposited between 3500 BP and 2800 BP from material supplied by the erosion of the Sakami Moraine and of glaciolacustrine and marine muds exposed along the river banks.