2010 Saskatchewan Geological Survey Open House Poster

1. Fraser Lakes Zone B mineralized granitic pegmatites and their pelitic hosts: Mineral chemis- Selected Mineral Chemistry and Stoichiometry Fig. 18
Sample:
Pegmatites
WYL-10-61-190.3
Note: Mineral stoichiometry for all minerals was calculated using Andy Tindle’s mineral re-calculation Excel
try, stoichiometry, and geothermobarometry
Ilmenite (inclusion,
Mineral: Titanomagnetite primary)
spreadsheets (Tindle, 2010) SiO2 0.09 0.00
TiO2 17.84 49.79
AUSTMAN, Christine L.1, ANNESLEY, Irvine R.1,2, and ANSDELL, Kevin M.1 Pelitic gneisses Al2O3 9.12 0.01
Fig. 10. Arial view (looking
(1) Department of Geological Sciences, University of Saskatchewan, Saskatoon, SK Canada S7N 5E2 (E-mail: christine.austman@usask.ca); Sample: WYL-09-50-37.5 WYL-09-49-36.1 Fe2O3 0.00 0.00
NE) of the Fraser Lakes
(2) JNR Resources Inc., Saskatoon, SK, Canada S7K 0G6 Mineral (Core/ Bt Bt Bt (C adj. Gt (C; Gt (R; Pl (C; Pl (R; Bt (in Bt (adj. Gt (C; Gt Gt (R; PL (C; Pl (R;
Cr2O3 0.01 0.00
Zone B area. Rim; (matrix, (matrix, Gt; peak?) retro.) matrix) matrix) gt; Gt; peak) (C2, ?) retro.) matrix, matrix, FeO 70.56 44.81
interpretation) peak) peak) retrogr.) peak?) retro.) peak?) retro) MnO 2.08 4.04
SiO2 35.57 35.93 36.15 SiO2 37.89 38.27 SiO2 64.04 64.04 SiO2 36.32 35.80 SiO2 37.63 37.88 37.60 SiO2 60.78 61.47 MgO 0.08 0.00
Abstract Location of the study area Mineral Assemblages TiO2 4.77 4.77 3.96 TiO2 0.03 0.01 TiO2 0.00 0.00 TiO2 5.23 3.49 TiO2 0.03 0.00 0.03 TiO2 0.00 0.00 CaO 0.00 0.00
Al2O3 17.74 17.68 17.62 Al2O3 21.49 21.87 Al2O3 22.52 22.48 Al2O3 17.62 18.42 Al2O3 21.57 21.52 21.49 Al2O3 24.07 24.09 ZnO 1.43 0.00
The Fraser Lakes Zone B U-Th-REE mineralized granitic Fig.1 V2O3 0.05 0.06
Granitic Pegmatites Pelitic Gneisses FeO 17.09 17.73 17.13 FeO 34.09 32.91 FeO 0.06 0.05 FeO 16.41 18.23 FeO 34.06 34.04 34.02 FeO 0.04 0.02
NiO 0.04 0.00
pegmatites intruded into the highly deformed contact MnO 0.03 0.03 0.00 MnO 0.57 0.51 MnO 0.00 0.00 MnO 0.02 0.04 MnO 1.43 1.40 1.52 MnO 0.00 0.00
Fig. 19 TOTAL 101.30 98.71
between the Wollaston Group pelitic gneisses and  Major minerals  Metamorphic minerals: MgO 9.64 9.83 10.71 MgO 4.02 4.84 MgO 0.00 0.00 MgO 10.70 9.29 MgO 3.30 3.39 2.87 MgO 0.00 0.00
CaO 0.00 0.00 0.00 CaO 0.57 0.63 CaO 3.31 3.33 CaO 0.00 0.00 CaO 1.05 1.04 0.93 CaO 5.58 5.51 Si 0.03 0.00
Archean orthogneisses during the Trans-Hudson Orogen (primary): quartz, biotite, Plagioclase, quartz, biotite, Na2O 0.14 0.12 0.14 Na2O 0.02 0.02 BaO 0.00 0.00 Na2O 0.32 0.17 Na2O 0.01 0.01 0.02 BaO 0.01 0.00 Al 3.27 0.00
~1.8 Ga. The host pelitic gneisses and orthogneisses were plagioclase, and k-feldspar ± k-feldspar, ± garnet, ± K2O 10.02 10.21 10.04 ZnO 0.02 0.01 Na2O 11.13 11.08 K2O 9.93 9.98 ZnO 0.01 0.01 0.01 Na2O 9.66 9.63 Ti 4.08 1.94
BaO 0.00 0.03 0.08 Cr2O3 0.02 0.02 K2O 0.26 0.22 BaO 0.05 0.07 Cr2O3 0.03 0.02 0.03 K2O 0.26 0.18 Fe 17.95 1.94
metamorphosed to lower granulite facies, at a maximum  Other primary minerals: cordierite, ± sillimanite, ± Cs2O 0.00 0.00 0.00 Y2O3 0.03 0.04 TOTAL 101.33 101.20 Cs2O 0.01 0.00 Y2O3 0.00 0.01 0.10 TOTAL 100.41 100.90 Mn 0.54 0.18
temperature of about 765 °C and maximum pressure of ± titanomagnetite graphite, ± ilmenite, ± F 0.60 0.46 0.59 V2O3 0.00 0.02 F 1.24 1.16 V2O3 0.03 0.01 0.00 Mg 0.04 0.00
Cl 0.02 0.02 0.02 TOTAL 98.76 99.14 Si 11.23 11.24 Cl 0.08 0.07 TOTAL 99.14 99.34 98.61 Si 10.83 10.87 Zn 0.32 0.00
around 7.5 kbar, while the granitic pegmatites were (pegmatites in Archean spinel, ± kyanite, ± zircon, Li2O* 0.66 0.76 0.82 Al 4.66 4.65 Li2O* 0.87 0.72 Al 5.05 5.02 Ca 0.00 0.00
Cr 0.00 0.00
intruded at a temperature of 700- 800°C. The pelitic orthogneisses only), ±
H2O* 3.69 3.81 3.75 Si 3.02 3.02 Ti 0.00 0.00 H2O* 3.47 3.43 Si 3.01 3.02 3.02 Ti 0.00 0.00
± monazite, ± uraninite, ± O=F,Cl 0.26 0.20 0.25 Al iv 0.00 0.00 Fe 0.01 0.01 O=F,Cl 0.54 0.50 Al iv 0.00 0.00 0.00 Fe 0.01 0.00 Ni 0.01 0.00
gneisses later underwent at least one period of retrograde Fig. 4. Radioactive granitic pegmatite from drill hole V 0.01 0.00
ilmenite, ± pyrite, ± Fig. 11. Drill core from WYL-10-61 showing apatite, ± pyrite, ± other Total 99.71 101.20 100.76 Al vi 2.03 2.05 Mn 0.00 0.00 Total 101.73 100.37 Al vi 2.04 2.03 2.05 Mn 0.00 0.00
Total 26.24 4.06
metamorphism at approximately 700-730 °C (5.6-7.1 kbar WYL-09-44. Pegmatite shows zoning, from a compositional variation in the pelitic gneiss Ti 0.00 0.00 Mg 0.00 0.00 Ti 0.00 0.00 0.00 Mg 0.00 0.00
plagioclase-rich core through k-feldspar and quartz- chalcopyrite, ± rutile, ± sulphides and oxides Si 5.35 5.34 5.38 Cr 0.00 0.00 Ca 0.62 0.63 Si 5.33 5.37 Cr 0.00 0.00 0.00 Ca 1.07 1.05 Fig. 20
pressure). The similarity of intrusion temperatures to (including graphite-cordierite-sillimanite-rich
Al iv 2.65 2.66 2.62 Fe2+ 2.35 2.26 Na 3.78 3.77 Al iv 2.67 2.63 Fe2+ 2.35 2.34 2.38 Na 3.33 3.30
rich zones. titanite, ± fluorite, ± layers) and local boudinaged felsic melt pods.  Alteration assemblage: Fig. 21
metamorphic temperatures agrees with other evidence  Fraser Lakes Zones A and B are located in JNR Resource’s Way
Al vi 0.50 0.44 0.46 Mn 0.04 0.03 K 0.06 0.05 Al vi 0.39 0.63 Mn 0.10 0.09 0.10 K 0.06 0.04
which suggests that intrusion of the pegmatites was molybdenite, ± apatite, ± Fig. 12.
± chlorite, ± muscovite, ± Ti 0.54 0.53 0.44 Mg 0.48 0.57 Ba 0.00 0.00 Ti 0.58 0.39 Mg 0.39 0.40 0.34 Ba 0.00 0.00
Lake Property (Fig. 1 - modified map from JNR Resources Inc., Fe 2.15 2.20 2.13 Ni 0.00 0.00 Total 20.36 20.34 Fe 2.02 2.29 Ni 0.00 0.00 0.00 Total 20.34 20.29
related to regional metamorphism and migmatization of garnet, ± graphite, Boudinaged clay minerals, ± hematite, ±
2010) in northern Saskatchewan, ~ 25 km from the SE edge of the Mn 0.00 0.00 0.00 Zn 0.00 0.00 Mn 0.00 0.01 Zn 0.00 0.00 0.00
pyrrhotite, ± pentlandite felsic melt pods
the Wollaston Group in the Fraser Lakes area. Athabasca Basin and ~ 55 km from the Key Lake Uranium Mine with garnet
pyrite, ± fluorite, ± rutile Mg 2.16 2.18 2.38 Ca 0.05 0.05 An (%) 13.93 14.10 Mg 2.34 2.08 Ca 0.09 0.09 0.08 An (%) 23.89 23.82
Li* 0.40 0.45 0.49 Total 7.98 7.98 Ab (%) 84.75 84.77 Li* 0.51 0.44 Total 7.99 7.98 7.98 Ab (%) 74.77 75.28
 Radioactive accessory cores from Ca 0.00 0.00 0.00 Or (%) 1.33 1.12 Ca 0.00 0.00 Or (%) 1.34 0.90
Minerals (primary): ± WYL-09-37 Na 0.04 0.04 0.04 Almandine 80.62 77.49 Na 0.09 0.05 Almandine 80.24 79.97 81.90
Regional Geology (~190.0 m). K 1.92 1.94 1.90 Andradite 0.00 0.00 K 1.86 1.91 Andradite 0.00 0.00 0.00
 Area is underlain by Archean orthogneisses, uraninite, ± uranothorite, Sr 0.00 0.00 0.00 Grossular 1.60 1.77 Sr 0.00 0.00 Grossular 2.97 2.97 2.64
Ba 0.00 0.00 0.00 Pyrope 16.39 19.52 Ba 0.00 0.00 Pyrope 13.41 13.77 11.81
Wollaston Group metasedimentary rocks (pelitic ± zircon, ± monazite, ± Cs 0.00 0.00 0.00 Spessartine 1.32 1.16 Cs 0.00 0.00 Spessartine 3.29 3.23 3.55
gneisses ± graphite, psammopelitic gneisses, and allanite OH* 3.71 3.78 3.72 Uvarovite 0.07 0.05 OH* 3.40 3.43 Uvarovite 0.10 0.07 0.10 Fig. 18-21. Backscatter electron images of the pelitic gneiss samples showing the location of
calc-silicate gneisses), and Hudsonian intrusives  Alteration assemblage: ±
F 0.29 0.22 0.28 F 0.58 0.55 selected microprobe analysis points shown in the adjacent table. Fig. 18+ 19 are from
Cl 0.00 0.00 0.00 Cl 0.02 0.02
(Fig. 2) that were complexly deformed and sample WYL-09-50-37.5 while Figs. 20 + 21 are from sample WYL-09-49-36.1.
metamorphosed during the Trans-Hudson
Fig. 5. Outcrop (Trench 2) of a typical radioactive chlorite, ± muscovite, ± TOTAL 19.72 19.79 19.86 TOTAL 19.80 19.80
granitic pegmatite showing coarse grain size and
Orogen ~1.8 Ga (Annesley et al. 2009) plagioclase- (Plag), biotite- (Bt), and quartz- (Qtz)
clay minerals, ± hematite,
 Two mineralized zones, A and B (see Fig. 2), are rich mineralogy. Abbreviations after Kretz (1983). ± pyrite, ± fluorite, ± Results of Initial Conventional Geothermobarometry Conclusions
hosted by NE-plunging regional fold structures  The host rocks to the Fraser Lakes granitic pegmatite-hosted U-Th-REE
Fig. 6. Granitic galena Fig. 14. Pelitic gneiss (WYL-09-50- Sample # Rock type Methods Maximum Retrograde Average max T°C Retrograde T° Max T°C of log10 f(O2)
adjacent to a 65 km long folded electromagnetic Pressure Pressures (rim) (core) C (rim) intrusion mineralization underwent regional metamorphism up to lower granulite
pegmatite Fig. 7. 37.5) with quartz, plagioclase,
(EM) conductor (Annesley et al. 2009) (WYL-10-61- (core) facies, based on the presence of key indicator minerals including spinel,
Biotite (Bt), biotite , spinel (Spl), sillimanite,
 At Zone B, the uranium and thorium 190.3) with zircon
Fig. 13. Pelitic gneiss (WYL-09-49-36.1) con-
WYL-09-49 Sill-Gt-Bt- Ti-Bt(T1), Gt-Bt ~7.2 kbar ~5.6 kbar (@ 765 °C (T1) ~ 700 °C (T1) n/a n/a sillimanite, and cordierite in the pelitic gneisses, and orthopyroxene in the
magnetite taining biotite, garnet, sillimanite, monazite, cordierite (Crd), graphite (Gr), and
mineralization is located in a ~500 m x 1500 m (Zrn), and monazite. This thin section also -36.1 bearing pelitic (T2), GASP (P1, (@ 765 °C, 702 °C, P1); Archean orthogneisses
(Mgt), ilmenite uraninite- quartz, and feldspar.
area NW of the Fraser Lakes in an antiformal gneiss P2) P1);
(Ilm), and rich
contains garnet and k-feldspar.  Relict kyanite in the pelitic gneisses indicates that the rock experienced
fold nose cross-cut by E-W ductile-brittle and uraninite (Urn) granitic conditions that enabled it to form during the prograde part of its P-T path
NNW- and NNE-trending brittle structures (Fig. 2, intrusive into pegmatite WYL-09-50 Sill-Crd-Spl-Gt- Ti-in-Bt(T1), Gt- ~7.6 kbar ~6.8 -7.1 kbar 750 °C (T1) 709 - 730 °C n/a n/a
Archean  The maximum pressure that the pelitic gneisses experienced during
(sample -37.5 Bt-Gr-bearing Bt(T2), GASP (@ 750 °C, (@709 °C - 730 (T1)
3, Annesley et al. 2009) orthogneisses. pelitic gneiss (P1, P2) P1) °C, P1) metamorphism was up to ~7.6 kbar at temperatures of up to ~ 760 °C
Trench 2-2).
 Multiple generations of pegmatites including
WYL-09-61 Magnetite- Mgt-Ilm (T2, n/a n/a n/a n/a ~ 831 °C (T2); ~ -1.92 relative to  Pegmatite crystallization began at 750 - 830 °C with the oxide minerals, and
syn-tectonic (subcordant to gneissosity, often Fig. 8. Quartz- rich,
-190.3 bearing Granitic T3), f(O2) (1, 2) NNO (f1); feldspars and quartz crystallizing later at lower temperatures (>500 °C for
radioactive granitic 706 - 828°C
radioactive) and post-tectonic (discordant, non- Pegmatite (T3) -17.99 to -15.18 (f2) similar pegmatites in the Grenville Province (Lentz 1992))
pegmatite (outcrop sample).
mineralized) pegmatites intrude the Archean- Note the radiation cracks
Fig. 2 Regional geological map of the Fraser Lakes area. Modified from Ray (1980). Models:  Similarity of pegmatite intrusion temperatures to maximum metamorphic
Wollaston Group contact (Austman et al. 2009) surrounding the altered
uraninite (Urn) grain.
T1: Titanium-in-Bt T2, f(O2)1: T3, f(O2)2: P1: GASP1.EXE program available from Ganguly temperatures agrees with other evidence (Austman et al. 2009, 2010 a, b)
 Pegmatites in the western part of the fold nose are geothermometer of Henry Magnetite-Ilmenite geother- Magnetite-ilmenite geothermometer (2010), which uses thermodynamic properties from
that the mineralized granitic pegmatites formed by partial melting of pelitic
U and Th-enriched (Th/U ~1; up to 0.242% U3O8 with Fig. 9 Biotite- and monazite- (2005); applied to non-graphitic mometer and f(O2) geobarometer and f(O2) geobarometer of Anderson Berman (1988) and experimental data from Koziol and
0.254% ThO2 over 0.5 m in drill core), while those in rich pegmatite (WYL-09-46 Fig. 15. Pelitic Gneiss (WYL-10-61-78.1) Fig. 16. Pelitic gneiss (WYL-09-49-) pelites by Eric (2009). of Ghiorso and Evans (2008); f and Lindsley (1985) calculated using Newton (1988) for the pure end-member GASP reaction. gneisses ± orthogneisses during regional metamorphism
-83.0) with thorite (Thr) and with altered cordierite, biotite, sillimanite, contains sillimanite after kyanite, (O2) is relative to NNO of O'Neill ILMAT (Lepage 2003). The large Thermodynamic solution models are from Ganguly et al.  Future work will include additional microprobe analyses of pegmatites
the eastern part are Th + LREE-enriched with vari- zircon (Zrn). feldspar, and quartz with some remnant sillimanite left. and Pownceby (1993). range of temperatures is due to (1996) (garnet) and Elkins and Grove (1990)
able U (Th/U ~ 2-20; up to 0.109% ThO2 with 0.013% (biotite, magnetite-ilmenite, feldspar) and pelitic gneisses (cordierite, spinel,
differences in the calculation of the (Plagioclase). Ti-in-biotite temperatures (T1) from
U3O8 over 7.0 m in drill core) (JNR Resources Inc., molecular fraction of ulvospinel and co-existing biotite were used in the calculations. garnet, biotite) in order to further constrain pressures and temperatures of
ilmenite. regional metamorphism and pegmatite crystallization
2010) Observed Mineral Reactions in Pelitic Gneisses
 The presence of migmatites, melt-textures in thin
section, geochemical trends between the pegmatites and References
Fig. 17. Qualitative P-T
pelitic gneisses, and initial U-Th-Pb chemical age 1. Bt + Sil +Qtz = Grt +Kfs + melt diagram for the pelitic Andersen, D.J., and Lindsley, D.H., 1985. New (and final!) models for the Ti-magnetite/ilmenite geothermometer and oxygen barometer: Abstract AGU 1985 Spring Meeting Eos Transactions. American Geophysical Union 66 (18), 416.
dating of the pegmatites (1795 ± 15 Ma, Annesley et al. Annesley, I.R., Madore, C. and Portella, P., 2005, Geology and thermotectonic evolution of the western margin of the Trans-Hudson Orogen: evidence from the eastern sub-Athabasca basement, Saskatchewan: Canadian Journal of Earth Sciences, 42, 573-597.
gneisses from the Fraser Annesley, I., Cutford, C., Billard, D., Kusmirski, R., Wasyliuk, K., Bogdan, T., Sweet, K., and Ludwig, C., 2009, Fraser Lakes Zones A and B, Way Lake Project, Saskatchewan: Geological, geophysical, and geochemical characteristics of basement-hosted mineralization: Proceedings of the 24th International Applied Geochemistry
(2010)) suggests that the pegmatites formed by partial Lakes Zone B area Symposium (IAGS), Fredericton, NB. Conference Abstract Vol.1. p. 409-414.
melting of pelitic gneisses ± Archean orthogneisses in
2. Bt + Sil +Qtz = Grt +Crd +Kfs + melt showing an approximate Annesley, I.R., Creighton, S., Mercadier, J., Bonli, T., and Austman, C.L., 2010, Composition and U-Th-Pb chemical ages of uranium and thorium mineralization at Fraser Lakes, northern Saskatchewan, Canada: GeoCanada 2010, Calgary, Canada, May 2010, Extended Abstract.
Austman, C.L., Ansdell, K.M., and Annesley, I.R., 2009, Granitic pegmatite- and leucogranite-hosted uranium mineralization adjacent to the Athabasca Basin, Saskatchewan, Canada: A different target for uranium exploration: Geological Society of America Abstracts with Programs, Vol. 41, No. 7, p. 83.
the middle to lower crust during the Trans-Hudson Fig. 3. Geological map of the Fraser Lakes Zone B area showing the presence of multiple clockwise metamorphic P Austman, C.L., Ansdell, K.M., and Annesley, I.R., 2010a, Petrography and geochemistry of granitic pegmatite and leucogranite- hosted uranium & thorium mineralization: Fraser Lakes Zone B, northern Saskatchewan, Canada: GeoCanada 2010, Calgary, Canada, May 2010, Extended Abstract.
-T path based on mineral Austman, C.L., Ansdell, K.M., and Annesley, I.R., 2010b, Mineralogy, geochemistry and economic potential of granitic pegmatite- and leucogranite-hosted uranium, thorium and REE mineralization adjacent to the Athabasca Basin, Saskatchewan, Canada: SEG 2010, Keystone, CO, USA, October 2010, Extended Abstract.
Orogen (Austman et al. 2009, 2010 a, b) pegmatites (red and blue) at/near the contact between Archean orthogneisses (orange and
purple) and Wollaston Group metasedimentary rocks (green). Modified from Ko, 1971.
3. Bt + Sil + Qtz = Pl + Grt + Kfs + melt assemblages and
Berman, R.G., 1988, Internally-Consistent Thermodynamic Data for Minerals in the System Na2O-K2O-CaO-MgO-FeO-Fe2O3-Al2O3-SiO2-TiO2-H2O-CO2: J. Petrology, 29, 445-522.
Elkins, L.T., and Grove, T.L., 1990, Ternary feldspar experiments and thermodynamic models: Amer. Min., 75, 544-559
reactions observed in Eric, S., Logar, M., Milovanovic, D., Babic, D., and Adnadeic, B.,2009, Ti-in-biotite geothermometry in non-graphitic, peraluminous metapelites from Crni vrh and Resavski humovi (Central Serbia): Geologica Carpathica, 60, 3-14.
Ganguly, J., Cheng, W. and Tirone, M. (1996) Thermodynamics of aluminosilicate garnet solid solution: new experimental data, an optimized model, and thermometric applications. Contrib.. Mineral. Petrol., 126, 137-151 (pdf file)
Purpose: to obtain estimates of the pressures and temperatures of regional metamorphism in the area 4. Bt + Sil + Qtz + Pl = Grt + Crd ± Kfs +melt thin section. Numbers
Ganguly, J., 2010, Index of /~ganguly/pub/P-T_Calc: Viewed: November 15, 2010, <http://geo.arizona.edu/~ganguly/pub/P-T_Calc/>
on the diagram Ghiorso, M.S., and Evans, B.W., 2008, Thermodynamics of rhombohedral oxide solid solutions and a revision of the Fe-Ti two-oxide geothermometer and oxygen-barometer: Amer. Jour. Sci., 308, 957–1039.
and determine the relationship of regional metamorphism to pegmatite intrusion. correspond to the Henry, D. J., Guidotti, C.V., and Thomson, J.A., 2005, The Ti-saturation surface for low-to-medium pressure metapelitic biotites: Implications for geothermometry and Ti-substitution mechanisms: Amer. Min., 90, 316-328.
JNR Resources Inc., 2010, —Home Page—Nov. 20, 2010: JNR Resources Inc., Saskatoon, SK Canada, <http://www.jnrresources.com>, Last accessed: Nov. 20, 2010.
5. Bt + Sil + Qtz + Pl = Crd ± Kfs + melt numbered reactions in Ko, C.B., 1971, Geological Report on Dynamic Petroleums Products Ltd . CBS 1837, Sask. N.T.S.: 74H-2-SW, Assessment Report, Great Plains Development Company of Canada, Ltd., 1-23.
the adjacent table of Koziol, A.M., and Newton, R.C., 1988, Redetermination of the anorthite breakdown reaction and improvement of the plagioclase-garnet-Al2SiO5-quartz geobarometer: Amer. Min., 73, 216-233.
Methodology observed reactions. Kretz, R., 1983, Symbols for rock-forming minerals: American Mineralogist, 68, 277-279.
Lentz, D. 1992, Petrogenesis of U-, Th-, Mo- and REE-bearing Pegmatites, Skarns, and Veins in the Central Metasedimentary Belt of the Grenville Province, Ontario and Quebec. Ph.D. thesis, University of Ottawa, Ottawa, Ontario.
Several samples of Fraser Lakes Zone B drill core and outcrop were prepared for petrological studies. Of these samples, one 6. Grt + Sil = Crd + Qtz ± Kfs (Diagram is modified Lepage, L, 2003, ILMAT: an Excel worksheet for ilmenite–magnetite geothermometry and geobarometry: Comp. and Geosci., 29, 673-678.
from Fig. 5 of Annesley O’Neill, H. St.C., and Pownceby, M. L., 1993, Thermodynamic data from redox reactions at high temperatures. I. An experimental and theoretical assessment of the electro-chemical method using stabilized zirconia electrolytes, with revised values for the Fe-―FeO‖, Co-CoO, Ni-NiO, and Cu-Cu2O oxygen buffers, and new data for the
granitic pegmatite (WYL-10-61-190.3) and two pelitic gneiss thin sections (WYL-09-49-36.1; WYL-09-37.5) were W-WO2 buffer: Cont. to Min. and Pet., 114, 296–314.
et al. 2005).
selected for initial electron microprobe analysis and conventional geothermobarometry. All microprobe analyses were com- 7. Grt + Sil = Crd + Spl + Ilm Ray, G.E., 1980, Geology of the Parker Lake-Nelson Lake Vicinity: Map 190A to accompany Sask. Geol. Surv. Rept. No. 190.
Tindle, A.G., 2010, Andy Tindle - Free Software (Mineral Recalculation Software): Available from: <http://www.open.ac.uk/earth-research/tindle/AGTWebPages/AGTSoft.html>, Last accessed: November 19, 2010
pleted at Saskatchewan Research Council’s Geoanalytical Laboratories using a Cameca SX-100 electron microprobe. Pres-
sure and temperature constraints are given by a combination of mineral assemblage data and conventional Acknowledgements
The authors acknowledge the financial support of JNR Resources Inc., NSERC (Discovery Grant to Ansdell) and the University of Saskatchewan (Department Heads Research Grant to Ansdell and Graduate Scholarship to Austman). Thanks to Blaine Novakovski for preparing the thin sections, to Kimberly Bradley from JNR Re-
geothermobarometry. sources Inc. for her assistance with petrography, and Steven Creighton for his assistance with the electron microprobe work.