- 124 -

Uranium Metallogenic Studies: II Rabbit Lake, Mineralogy and Geochemistry

by J. Hoeve*

The uranium metallogenic studies initiated in 1976 in formal cooperation with

the Saskatchewan Geological Survey were continued in 1977. The focus of attention was

again Rabbit Lake and material was also collected from other deposits for age dating

and mineralogical investigation.

Laboratory studies conducted on material collected from Rabbit Lake and its

illllllediate vicinity in 1976, include (1) mineralogy, paragenes~s and petrology of

ore and host rocks; (2) geochemistry of ore, regolith, altered and unaltered host

rocks; (3) micro-probe analysis of selected minerals; (4) fluid inclusions; (5)

stable isotopes; (6) radiometric age determination of ore and alteration minerals.

Most of these studies are still in an early stage and analytical data presently

available are too incomplete for definite conclusions to be made.

This preliminary report deals with the field work conducted during 1977 and

with the two fields of laboratory study in which most progress has been made, namely

(1) mineralogy, paragenesis and petrology and (2) geochemistry.

For information on geological background, reference should be made to earlier

reports (Hoeve and Sibbald, 1976; Sibbald 1976) and Sibbald (this volume).

General Relationships

The Rabbit Lake Thrust Fault recently exposed by mining in the northwestern wall

of the open pit, provided an interesting aspect of this summer's field work. In

the downthrown block the normally strongly hematitic basal conglomerates of the

Athabasca Formation, are seen to be affected by similar alteration and bleaching

effects as the host rocks of the ore in the upthrown block. These observations

present further evidence that the extensive alterations, characteristic for the

mineralized zone, post-date the Athabasca Formation.

The alteration zone has been divided into median and marginal subzones, (Hoeve

and Sibbald, 1976), the median subzone being more intensively altered, brecciated

and dolomitized. The dolomitization may be related to the proximity of a layer

of dolomitic marble which strikes into the alteration zone, where the marble is

recrystallized, possibly also remobilised (Sibbald, this volume) and influenced

by chloritization.

*Saskatchewan Research Council

- 125 -

Within the deposit an intimate relationship between mineralization, alteration,

and brecciation is observed. At least three stages of each are recognized.

The earliest alteration recognized is a dark green chloritization which either

predates initial mineralization or is associated with it.

The first stage of uraniUlll mineralization is represented by fracture and breccia

fillings of lustrous colloform pitchblende . The mineralized veins are often surrounded

by a hematite-stained, carbonatized (calcite) halo of wall-rock alteration, which

is superimposed upon the dark green chloritization.

The following episode of red chloritic alteration is characterized by extensive

silicification locally with formation of secondary quartzites, by some degree of

tourmalinization (dravite, magnesium-rich tourmaline) and in the vicinity of the

marble by extensive dolomitization, giving rise to zones of near-massive secondary

dolomite.

The red chloritic alteration must have been preceded or accompanied by brec­

ciation, because hematitic, coarse-grained breccia fillings in pseudomorphously altered

rocks are a common feature, particularly in the more intensively brecciated median

alteration zone.

The red alteration was terminated by renewed brecciation, which provided spaces

for the euhedral quartz veins that separate the red and the pale green alterations

and mark the transition from oxidizing to reducing conditions. These veins also

represent the second stage of mineralization, which is characterized by deposits

of massive lustrous pitchblende, coffinite and sulphides on top of euhedral quartz.

The pale green alteration represents a bleaching effect, which seems to have

been limited to the removal of hematite and the formation of some new sulphides.

Within the high-grade portion of the orebody pale green alteration is associated

with impregnations of sooty pitchblende and coffinite, which represent the third

stage in the sequence of mineralization. Reworking of the deposit is also recognized

to have taken place.

Most of the mineralized veins of the above mentioned stages are subjected to

oxidation as shown by the bright c oloured oxidized uranium minerals. In many cases,

"roll-front"-like phenomena can b e observed, where bodies of oxidized ore are fr inged

by black soo t y pitchblende at the contact with the pale green altered host r ock.

Oxygen-rich ground waters migrating downwards a long high-grade mineralized veins, may

have oxidized and remobilized uraniu.~ and precipitated it as sooty pitchblende. This

t ype of re-working could possibly be r e l a ted to Cretaceous , Tertiary or even Recent

meteoric regimes.

- 126 -

Mineralogy, Paragenesis and Petrology

Mineralization, Stage I. The oldest mineralization occurs as fracture and breccia

fillings in r e latively ~naltered rocks that show evidence of dark green chloritization

(Hoeve and Sibbald, 1976). The mineralized veins comprise predominant pitchblende,

euhedral quartz and calcite, accompanied by adularia, chlorite, sulphides, coffinite

and some hematite.

The pitchblende consists of two types: pitchblende(l) and pitchblende(2).

Pitchblende (1) occurs as colloform encrustration of the wall-rock, is relatively

hard, and white-grey, has high reflectivity and looks homogeneous. Pitchblende (2)

tends to be massive, has low variable reflectivity, and is often associated with

coffinite and intergrown with sulphides (galena, pyrite , arsenopyrite, chalcopyrite,

bornite, chalcocite , covellite and several others including Ni-, Co- sulphides ) and

arsenides. Micro-probe analysis is being performed on the sulphide phases for

proper identification.

Pitchblende (2) replaces pitchblende (1) along fractures and concentric and

radiating growth lines and generally includes small euhedral crys tals of galena,

which may r epresent radiogenic lead originally contained in pitchblende (1) .

Pitchblende (2) being of low reflectivi ty is probably in a higher oxidation state

then pitchblende (1) from which it may have formed through oxidation.

The idealized paragenetic sequence is shown in figure 1 . Paragensis (la):

mineralization started with deposition of pitchblende (1) on the walls of fractures

and breccia f ragments and was followed by growth of euhedral quart z . Pitchblende (1)

and euhedral quartz were then locally fractured. Paragenesis (lb): mineralization

continued with replacement of quart z by adularia, followed by deposition of chlorite.

Quartz and adularia were both replaced in turn by calcite, which also fo rmed

complicated, sometimes zonal, inter-growths with chlorite.

Finely divided hematite outlines and impregnates quartz, adularia and chlorite .

Hematite also occurs as thin crystallographically oriented films in some calcites.

However the majority of calcite has inclusions of the same s ulphides as are associated

with pitchblende (2) . Thus , pitchb l ende (2) and the s ulphides enter the paragenesis

af ter the deposition of hematite. The formation of hematite probably indicates

oxidizi ng conditions during which uranium was remob i lized; pit chb l ende (1 ) was

corroded and converted into pitchblende (2). Coffinite belongs t o paragenesis

(lb), but its exact place in the sequence is uncertain.

Mineralization , Stage II. The second stage of mine r a l i zation opens with the

emplacement of euhedr al quartz veins. The paragen~sis includes drav ite (magnesium

- 127 -

lo lb

i I I

I I

I I I pitchblende ( ! ) - I I Poragenesis /

lo \ I I euhedrol quartz - I I

Fracturln; I I

I I I odulorio -- I I I

I I I / chlorlte

I ~ I

hema1 lte LJ Pora;enesl1 ; I I

lb \ colclte \

\ pitchblende ( 2 )/ coffinite I I

\ I I \ . \ sulphides I I

I I

Fig. 1. Idealized paragenetic scheme for Stage J of mi neral i za t ion .

rich tourmaline), euhedral quartz, dolomite rhombohedrons, calcite, siderite, pitch­

blende, coffinite, chlorite, geothite, psilomelane, kaolinite, sulphides (pyrite,

arseno-pyrite, chalcopyrite, chalcocite, bornite, covellite, galena, sphalerite,

and Ni-, Co- sulphides) arsenides, native copper and glassy "buttons" of carbon.

As these minerals are seldom present together and many show replacement relationships,

the paragenesis is complex . This complexity is influenced by local control in the

sense that dolomite bearing veins are r6stricted to the areas of carbonate alteration .

Although the euhedral quartz veins are extremely abundant, few are mineralized

with uranium and these are all concentrated in the high-grade portion of the ore

body. Most of the euhedral quartz veins have a very simple mineralogy which includes

dravite, euhedral quartz and a few other phases.

The idealized scheme in figure 2, shows the complete paragenesis. Fracture

filling started with deposition of white, very fine- grained, s pherulit ic dravite,

followed by colourless euhedral quartz locally accompanied by pyrite and chalcopyrite.

Deposition of white or somewhat greenish dolomite rhombohedrons occurred t oward the

end of quartz emplacement. Hematite entered the paragenesis during t he final growth

of quartz appearing at first as thin parallel films in t he outer zones of t he quartz

crystals . Where dolomite has grown on top of colourless quartz , the hematite fi l ms

I i

DRAY I TE

EUHEDRAL QUARTZ

HEMATITE

DOLOMITE

SIDER1TE

CHL..ORITE

PITCHBLENDE

COFFINlTE

SULPHIDES

NATIVE COPPER

CARBON "BUTTONS"

GOE TH I TE

CALCITE

I

- 128 -

Reducing Oxidizing Reducing ! . [Oxid.: Reduc. t

color less '. red

dust spherules ------. white: red

---~

:white

-- t

t 1----~ -

-' t ----

Fig. 2. Paragenetic sequence in euhedral quartt veins.

are present in the dolomite and occasionally the dolomite is intergrown with coarse

spherulitic aggregates of specular hematite. Dolomite crystallized after the

oxidising period indicated by the hematite generally carries inclusions of or is

capped by sulphides including pyrite, arsenopyrite, chalcopyrite, chalcocite, and

galena. Finally, white dolomite is capped by white calcite, accompanied by the

sulphides and occasionally glassy "buttons" of carbon.

In dolomite-free veins, spherulitic hematite deposited directly upon red-stained

euhedral quartz is locally overgrown by siderite and/or calcite. Overlying chlorite

is followed in mineralized veins by pitchblende and coffinite embedded in a calcite

matrix. The pitchblende and coffinite are intimately intergrown, often forming

concentric, rhythmically zoned aggregates, which include sulphides (pyrite, arsenopy­

rite, galena, sphalerite, chalcopyrite, bornite, chalcocite, covellite) and several

others among which Ni-, Co- minerals and clausthalite appear (cf. Rimsaite, 1977).

The deposition of pitchblende, coffinite and sulphides was briefly interruped, by

- 129 -

precipitation of geothite and calc ite.

Glas sy "buttons" of carbon enter the para genesis toge ther with s ulphides,

pitchblende, coffin i te and calcite. Deposits of kaolinite and psilomelane have been

observed directly on euhedral quartz, but their position in the paragenetic sequence

i s uncertain.

Reducing conditions mus t have prevai l e d throughout the stage II mineralization

except for the oxidizing periods during which hematite and goethite were introduced.

Mi nerali zat ion, Stage III. The third s tage of mineralization is as sociated wit h t he

pale green alteration and appears as a re-working r ather t han as a discrete mineral­

izing episode . Where pale green alteration encroa ches upon mineralized veins of

stage II, the lustrous pitchblende i s transformed to sooty pitchblende and coffinite,

often accompanied by s ome galena . Spherulitic and earthy hematite of the euhedral

quartz veins is replaced by fine- grained, pale green chlor i te . Within t he high­

grade part of the ore body, pale green altered rocks of t en contain impregnat ions of

pitchblende and coffinite, which are no t associated with euhedral quartz veins.

This s uggest s that disp ersion of uranium t ook place in conjunction wi th pal e green

al teration.

Dark Green Chloritic Alteration. Rocks affected by thi& type of chloritization

appear relative l y fresh in hand specimen and original metamorphic t extures are pre­

served.

Mi croscopic examination shows that biotite- amphibole-pyroxene aggregates of

t he original rocks a r e completely altered to aggregates of green chlorit e associated

with some anatase. The composition of this chlor i t e is as yet unknown, but its

dark gr een col our suggest it t o be r icher i n iron t han t he near-colourless magnesium

r ich chlorites associated wi th the red and pale green alterations. Anat ase i s a l so

present as aggregates that are pseudomorphous afte r iron-titanium oxides . Small

r elicts of feldspar and pyroxene are occas ionally observed as inclusions in

l arge , irregular quartz grains, which show undulose extinct ion and are t ransected

by closely spaced , parallel sutures lined with an abundance of fluid inclusions .

Within the wall-rock alteration ha l o of stage I mineral i zed veins, some

l arger fractures are present transect i ng chlori te aggregates and quartz alike.

These fractures are filled with chl orite and calci t e and normally show hemati t e­

rich margins . They are also occasionally mineralized, with pitchb l ende (2),

coffinite and s ulphides, an assemblage similar to paragenesis (lb) . The chlorite­

calcite veinlet s post- date the micro- fractures lined with fluid inclusion, in that

they cross- cut them. They become more widespread and wider nearer the stage I

- 130 -

mineralized veins until the wall-rock is almost permeated. Similarly the hematite

pigmentation sho··,.f a progressive increase.

Red Chloritic Alteration. Red-altered rocks are composed essentially of magnesium

rich chlorite as a replacement product of feldspars and mafics, accompanied by

tourmaline. Titanite and iron-titanium oxides are replaced by fine-grained aggre­

gates of anatase. Relict grains of orange-brown tourmaline often have colourless

border zones, representing secondary overgrowth of dravite (magnesium rich tourma­

line), which also occurs as spherulitic aggregates in the chloritic groundmass.

The red colouration stems from pervasive finely divided hematite. In silicified

zones, the red altered rocks tend to be vuggy and secondary quartz is present on

radiating encrustations of chlorite that outline the vugs. The silicification must

have taken place concurrently with the red alteration, because the quartz is hematite

stained.

In some parts of the alteration zone, dolomitization is represented by fracture

fillings and diffuse impregnation zones, which in extreme cases may grade into

massive secondary dolomite. The crystals of this generation of dolomite are

disc-shape with spindle-like cross-sections. Hematite is generally present, often

as films in crystallographic planes and growth zones.

Breccia matrix containing fragments of pseudomorphously altered red rocks is

composed of coarse-grained hematite-stained chlorite, with secondary quartz and

spherulitic dravite. The dravite may amount to 10-15 percent by volume.

Hematite staining indicates that conditions must have been generally oxidizing

during this episode of red alteration.

Pale Green Alteration. The pale green alteration is superimposed upon red chloritic

alteration as well as on hematitic rego1ith, and forms bleached halos on the margins

of fractures and veins of euhedral quartz. In places, pale green alteration is

pervasive and only small red altered spots remain.

The mineralogical composition of the pale green altered rocks is similar to that

of the red, except that the chlorites are not hematite-stained and that small

amounts of newly formed sulphides, including pyrite, chalcocite and galena, are often

present. Secondary quartz and dolomite retain their hematite, thus bearing evidence

of formation during previous red alteration. Similarly, radiating spherulitic

aggregates of dravite may consist of a hematite-stained core, surrounded by hematite­

free borders. This suggests that the formation of dravite continued during pale

green alteration.

- 131 -

Ill-defined s ilicified zones a re locally present. As the quartz crystals of t hese

zones are not hematite-stained they may post-date the r ed alteration. Moreover,

these silicified zones often contain sulphides (pyrite, chalcocite, and ga lena) and

occas ionally dolomite. They possibly correlate with the euhedral quartz veins.

In some places, pale green altered rocks contain aggregat es of graphite and

galena which seem t o be n ewl y formed.

Conditions at this time must have been reducing, because of the removal of

hematite and the deposition of sulphides and graphite.

Geochemistry

In order to establish the behaviour of elements for various types of alteration

encountered, whole rock chemical analyses have been p erformed on pairs of (1)

unaltered and red altered rocks; (2) red and pale green altered rocks; (3) unaltered

and weathered rocks; (4) weathered rocks and weathered rocks that are affected by

pale green chloritic alteration.

In stud ies of rock alteration, the behaviour of elements cannot be directly

inferred by comparison of the chemical analyses as volume changes may have accom­

panied alteration. However, comparisons can be made by examination of compos ition -

volume r elationships as outlined by Gresens (1976).

Applying Gresens procedure to analyses of the rock pairs above the behaviour

of elements in various alteration situations is s ummarized below and in Table 1 . A

de tailed interpretation and discussion of the r esults will be given in a report,

upon completion of the analytical program.

Weathering . The f ormation of the regolith is characterized by immobility of A12o

3,

TiO? and total Fe?O , probably also Band by leaching of nearly all other constituents, - - 3

except for H2o, which is introduced, This behaviour of elements is similar to that

observed in present day lateritic soil formation . X-ray identification of c lay

minerals showed the regolith to be characterized by kaolinite and sericite .

Red Chloriti c Alteration. Red alteration is typified by immobility of Al2o3 and

Ti02

and by introduction of MgO , and t otal Fe2

o3

, H2

0 and pr obabl y also B. The

alkali metals, Si02

and CaO are thoroughly leached . The behaviour of elements is

cons istent with the observed mineralogical changes; f ormation of magnesi um-ri ch

ch lorite, magnesium-rich tourmaline and pervasive hematite staining .

Pale Green Alteration. Pale green alteration is characterized by immobility of

Al203 , Ti02 , Cao, alkali me tal s and H20. Tot al Fe

2o

3 is removed and the behaviour

- 132 -

of Si 02 is uncertain. There is some introduction of uranium. vanadium and possibly

boron and magnesium.

ln comparison to red alteration no dramatic changes have taken place, except

for removal of total Fe2o

3. This behaviour is consistent with petrographic

observations; removal of hematite and continued growth of magnesium rich tourmaline .

Table 1 - Whole-rock analyses of unaltered, altered and weathered rocks

Si02 62. 1 52 . 9 64.6 63.0 55 . 6 51. 8

Al2

03

15.5 28 . 8 17 .8 16. 0 15 .9 19.0

Ti02

.57 1.14 .63 . 69 .78 .87

FeO 1. 27 .21 . 28 1. 71 .28 . 56

Fe2o3 2.26 6.70 1.07 .so 3 . 19 . 60

Na20 7.20 .09 . 09 7.29 .18 .09

CaO 4 . 60 .09 .37 2.26 .33 .47

MgO 4.88 . 88 8.00 4.98 16.30 18.00

K20 1. 00 . 59 1. 62 1. 71 .25 .25

MnO .02 .02 . 01 . 03 .02 .03

H2o . 70 6.50 5.47 1.03 7 . 22 7 . 42

co2 .12 .10 .02 1. 20 .07 .02

Total 100.22 98.02 100 . 25 100 .40 100.12 99.11

1. Unaltered plagioclasite F/22/191' - 192'

2. Weathered plagioclasite F/22/45' - 46'

3. Pale green alteration superimposed upon weathering F/22/83' - 84'

4. Unaltered plagioclasite R76 - 15 - 3

5. Red altered plagioclasite R76 - 28 - 1

6 . Pa l e green plagioclasite R76 - 28 - 6

The increase of uranium and vanadium is not surprising in view of the reducing

conditions during pale green alteration.

The major chemical changes accompanying the chloritic alteration within the

alteration zone were brought about during red alteration, which was characteri zed

by introduction of large amount of magnesium and probably boron and, hence, could

be described as magnesium-boron metasomatism. The f ormation of the regolith by

contrast was characterized by leaching of magnesium and probably by immobility of

boron, and is thus similar to l aterit ic weathering .

- 133 -

Table 2 - Geological history of t he Rabbit Lake deposit

1. Weathering of basement rocks; regolith - 1350 ± 50 m. y .

2, Athabasca Formation - 1350 ± 50 m. y .

3. Brecciation

4. Stage I of mineralization; dark green chloritization - 1100 m.y.

S. Brecciation - Rabbit Lake fault

6. Red chloritic alteration; silicification; dolomitization; tourmalinization

7, Brecciation

8. Euhedral quartz veins; stage II of mineralization

9. Pale green alteration; some silicification; dispersion of earlier

mineralization: . Stage III

10. Younger reworking of deposit

Discussion and Conclusions

The general sequence of events as listed by Hoeve and Sibbald (1976) is now

essentially confirmed and expanded (Table 2). Two parageneses separated by a

brecciation event are recognized in veins of stage I mineralization. Pitchblende (1)

of paragenesis (la) is corroded and replaced by pitchblende (2) reflecting remobilization

and redeposition of uranium in connection with the hematite-producing oxidising

phase of paragenesis (lb).

The paragenesis of stage II shows such close similarities to paragenesis (lb)

of stage I that they may be one and the same. In this case paragenesis (la) only

is stage I and paragenesis (lb) i s the imprint of stage II.

The precipitation of uranium took place after oxidizing episodes. Stage II

mineralization, associated wi th the euhedral quartz veins, took place between the

red and pale green alterations during a transition from oxidizing to reducing

conditions . Similarly, in more detail, uranium deposition followed the oxidizing

intervals in the paragenesi s of stage II mi neralization (Fig. 2). These relationships

indicate that oxida tion - reduction reactions played a major role in shaping the final

deposit . Uranium of stage I was probably remob i lized during the oxidizing episode

of red chloritic alteration and redepos i ted as stage II mineralization when conditions

changed to reducing. However, as sulphides, arsenides and selenides of various metals

are part of the par agenes i s, an influx of new compounds must also have taken place.

Dispersion of stage II mineralization t ook pl ace in connection with pale green

alteration.

- 134 -

The exact position in sequence of the dark green chloritization is unknown,

although it predates the hematite stained wall-rock alteration of paragenesis (lb).

Hence this chloritization may represent wall-rock alteration of paragenesis (la),

or be much older, possibly even late metamorphic.

With respect to the nature of the agents responsible for the foregoing para­

genetic events much remains unknown. However, the glassy carbon "buttons" of stage

II mineralization and graphite in the pale green altered rock, suggest the action of

reducing agents capable of precipitating native carbon.

Pagel (1975) reports the presence of hydrocarbons in fluid inclusions in quartz

from Rabbit Lake and from the 'D' zone at Cluff Lake. His observations indicate that

volatile hydrocarbons (natural gas) might have acted as a reducer and precipitator.

Even at present, the 1D1 zone is fairly rich in hydrocarbons because cutting of the

samples on a diamond saw produces a strong odor of these compounds. However, their

source remains unknown.

Adler (1974) describes the origin of certain types of roll-fronts in sandstone

deposits at Rifle, Colorado, in terms of diffusion of cations across a stationary

redox interface formed by two bodies of water, one oxidizing and containing uranium,

vanadium and other cations, the other reducing and containing petroleum and H2s.

Assuming that hydrocarbons might have acted as the reducing agent at Rabbit

Lake, the oscillations between oxidizing and reducing conditions may also have arisen

through the interaction of bodies of oxidizing and reducing waters.

Reduced or bleached zones are not restricted to the Rabbit Lake ore body, but

also occur in the regolith and in the basal conglomerates and sandstones throughout

the Athabasca Basin (cf. Fahrig, 1961). X-ray identification of clay minerals shows

in all cases that bleaching is not accompanied by major mineralogical change other

than removal of hematite. These observations suggest that at some stage in the

evolution of the Athabasca Basin, reduction processes operated on a basin wide scale.

Knipping (1974), proposes a supergene origin for the Rabbit Lake deposit and

equates the development of the regolith with the chloritic alterations in the ore

zone. Evidence presented in the present report shows that, at least in the Rabbit

Lake area, the regolith and the alterations are characterized by contrasting miner­

alogy and behaviour of elements. As the alterations are superimposed upon the regolith,

they are thought to have been formed by unrelated processes.

The general coincidence of the deposits in the Athabasca basiP. with the uncon­

formity has been the main argument for the supergene hypothesis (Knipping, 1974;

Langford, 1974). The author believes that this coincidence can be more satisfactorily

- 135 -

explained by a diagenetic - hyarothermal model as outlined by Hoeve and Sibbald (1976).

References

Adler, H.H. (1974): Concepts of uranium-ore formation in reducing environments in sandstones and other sediments; Symposium : Formation of uranium deposits; IAEA, Vienna.

Fahrig, W. F. (1961): The geology of the Athabasca Formation; Geol. Surv. Can . Bull.68.

Gresens, R.L. (1967): Composition - volume relationships of metasomatism, Chem. Geol., 2.

Hoeve, J, and Sibbald, T.I.l. (1976): Rabbit Lake Uranium Deposit; In: Uranium in Saskatchewan; Ed. Dunn, C.E., Sask. Geol. Soc. Spec. Puhl. 3.

Knipping, H.D. (1974 ) : The concepts of supergene versus hypogene emplacement of uranium at Rabbit Lake, Saskatchewan, Canada; Symposium: Formation of uranium depos i ts; IAEA, Vienna .

Langford, F.F. (1974): Origin of Australian uranium deposits; a universal process that can be applied to deposits in Saskatchewan; in Fuels; a geol ogical appraisal; Ed. Parslow, G.R.; Sask. Geol. Soc. Spec. Publ. 2.

Pagel, M. (1975) : La Diagenese des gres et les gisements d'uranium dans le bassin Athabasca (Canada); In "Rapport de'activite 1975" Equipe de recherche sur les equilibres entre fluides et mineraux; Centre de Recherches Petro­graphique et Geochimiques; Nancy , France.

Rimsaite, J. (1977): Mineral assemblages at the Rabbit Lake uranium deposit, Saskatchewan; a preliminary report ; In: Report of Activities, Part B; Geol. Surv. Can., Paper 77-lB.

Sibbald, T.I.I. (1976): Uranium me tallogenetic studies - Rabbit Lake; In Sununary of Investigations 1976, Sask. Geol. Surv.; Ed. Christopher, J.E. and Macdonald, R.