Journal of Geosciences, 60 (2015), 1–10

DOI: 10.3190/jgeosci.184

Original paper

Plášilite, Na(UO2)(SO4)(OH)·2H2O, a new uranyl sulfate mineral fromthe Blue Lizard mine, San Juan County, Utah, USA
Anthony R. Kampf1*, Anatoly V. Kasatkin2, Jiří Čejka3, Joe Marty4
1
Mineral Sciences Department, Natural History Museum of Los Angeles County, 900 Exposition Boulevard, Los Angeles, CA 90007,
USA; akampf@nhm.org
2
V/O “Almazjuvelirexport”, Ostozhenka str., 22, block 1, 119034 Moscow, Russia
3
Department of Mineralogy and Petrology, National Museum, Cirkusová 1740, 193 00 Prague 9, Czech Republic
45199 E. Silver Oak Rd., Salt Lake City, UT 84108, USA* Corresponding author

Plášilite (IMA 2014-021), Na(UO2)(SO4)(OH)·2H2O, is a new uranyl sulfate mineral from the Blue Lizard mine, San
Juan County, Utah, USA. The new mineral occurs in and on sandstone matrix in close association with atacamite, blödite,brochantite, calcite, chalcanthite, dickite, gerhardtite, gypsum, hexahydrite, johannite, manganoblödite, natrozippeite
and tamarugite. It is a low-temperature, secondary mineral formed by the post-mining weathering of uraninite. Plášilite
is monoclinic, with the space group P21/c, and unit cell parameters a = 8.7122(6), b = 13.8368(4), c = 7.0465(2) Å,
β = 112.126(8)°, V = 786.89(7) Å3 and Z = 4. Crystals are long, thin blades, elongated on [001] and flattened on {100};
rarely occur as prisms, also elongated on [001]. Crystals exhibit the forms {100}, {010} and {011}, and are commonly
twinned on {100}. Plášilite is greenish yellow, has a white streak and fluoresces bluish white under both long-wave
and short-wave UV. It is transparent with vitreous luster. The mineral has a Mohs hardness probably between 2 and3, brittle tenacity, even fracture and two perfect cleavages, {010} and {001}. The calculated density based on the empirical formula is 3.726 g/cm3. The mineral is optically biaxial (+), with α = 1.556(1), β = 1.581(1) and γ = 1.608(1)(measured with white light). The measured 2V is 88(1)° and the calculated 2V is 89°. Dispersion is moderate, r < v. The
mineral is pleochroic with X = nearly colourless, Y = very pale yellow, Z = pale yellow; X < Y < Z. The optical orientation is X = b, Y ^ c = 4° in obtuse β. The empirical formula of plášilite is Na0.94(UO2)(S1.01O4)(OH)(H2O)2 (based on 9
O apfu). Prominent features in the Raman spectrum include the symmetric stretching vibrations of the uranyl (UO22+)
group and sulfate tetrahedra and the O–H stretching and bending vibrations of the H2O molecules. The eight strongest
powder X-ray diffraction lines are [dobs Å(I )(hkl) ]: 6.90(100)(020), 5.85(99)(011,1̄11), 4.024(57)(200,130), 3.492(82)(1̄02,220,040), 3.136(40)(1̄22), 2.690(25)(141,102,2̄41,032), 2.618(34)(240,150,3̄02), 1.9212(30)(mult.). The crystal
structure of plášilite (R1 = 0.019 for 1603 reflections with Fobs > 4σF) contains uranyl sulfate sheets of composition[(UO2)2(SO4)2(OH)2]2– parallel to (010). Between the sheets and linking them to one another are chains of edge-sharing
NaO2(H2O)4 octahedra parallel to [001]. The uranyl sulfate sheet is based on the phosphuranylite anion topology. The
sheets in plášilite and deliensite are geometrical isomers.
Keywords: plášilite, new mineral, crystal structure, Raman spectroscopy, uranyl sulfate, Blue Lizard mine
Received: 25 June 2014; accepted: 23 November 2014; handling editor: F. Laufek
The online version of this article (doi: 10.3190/jgeosci.184) contains supplementary electronic material.

1. Introduction
Uranyl sulfate minerals typically form by hydration–oxidation weathering of primary uranium minerals, mainly
uraninite, by acidic solutions derived from the decomposition of associated sulfides (Finch and Murakami 1999;
Krivovichev and Plášil 2013). They are found in mosturanium deposits world-wide.
Our mineralogical investigations of the Blue Lizard
mine over the last few years have revealed a remarkablesecondary assemblage of uranyl sulfates, the majorityof which are new to science. We have already described
the sodium uranyl sulfates meisserite (Plášil et al. 2013),
bluelizardite (Plášil et al. 2014a) and belakovskiite(Kampf et al. 2014), and herein we introduce plášilite, thefourth new sodium uranyl sulfate. In addition, six othernew uranyl sulfates from this mine, are currently understudy and all, except one, contain essential Na.
The discovery of such a wealth of new uranyl sulfates
at a single mine is unprecedented. The classic Jáchymov
deposit has yielded more uranyl sulfates (Ondruš et al.
1997; Tvrdý and Plášil 2010); however, they have been
described from several mines and over a lengthy time
period. Furthermore, it is remarkable that seven of the ten
new phases from the Blue Lizard mine feature only Na as
the additional cation and only one contains no essential
Na. The only sodium uranyl sulfate mineral known previously was natrozippeite (Frondel et al. 1976).
www.jgeosci.org

Anthony R. Kampf, Anatoly V. Kasatkin, Jiří Čejka, Joe Marty

Plášilite (‘pla: shil ait) is named for Jakub Plášil (born1984), a researcher in the Department of Structure Analysis at the Institute of Physics, Academy of Sciences of
the Czech Republic. His scientific research is focused on
the crystal chemistry of hydrated oxysalts and hexavalenturanium compounds. He is author or co-author of morethan 80 publications, including the descriptions of 23 newmineral species.
The new mineral and the name were approved by theCommission on New Minerals, Nomenclature and Classification of the International Mineralogical Association(IMA2014-021). The description is based on six cotype
specimens. Five of them are deposited in the collectionsof the Natural History Museum of Los Angeles County,
catalogue numbers 64126, 64127, 64128, 64129 and
64130. A sixth cotype specimen is housed in the collections of the Fersman Mineralogical Museum of the Russian Academy of Sciences, Moscow, Russia, registration
number 4548/1. Crystals from that specimen were used
for the chemical analyses.

2. Occurrence
Plášilite was found underground in the Blue Lizard Mine,
Red Canyon, White Canyon District, San Juan County,
Utah, USA (37°33'26"N 110°17'44"W) by one of theauthors (JM). The Blue Lizard mine is located c. 72 km
west of the town of Blanding, Utah, and c. 22 km southeast of Good Hope Bay on Lake Powell. It is on thenorthern side of Red Canyon and close to the Markey
mine. Information on the history and geology of the deposit is taken largely from Chenoweth (1993).
The deposit was first recognized in the summer of 1898
by John Wetherill, while leading an archeological expedition into Red Canyon. He noted yellow stains around apetrified tree. At that spot, he built a rock monument, inwhich he placed a piece of paper to claim the minerals.
Although he never officially recorded his claim, 45 years
later, in 1943, he described the spot to Preston V. Redd ofBlanding, Utah, who went to the site, found Wetherill’smonument and claimed the area as the Blue Lizzard claim(note alternate spelling). Underground workings to mineuranium were not developed until the 1950s.
Mineralized channels are found in the Shinarump
Member of the Chinle Fm. The Shinarump Member
consists of medium- to coarse-grained sandstone, conglomeratic sandstone beds and thick siltstone lenses. Ore
minerals were deposited as replacements of wood andother organic material and as disseminations in the enclosing sandstone. Since the mine closed in 1978, oxidation ofprimary ores in the humid underground environment has
produced a variety of secondary minerals, mainly sulfates,
as efflorescent crusts on the surfaces of mine walls.
Plášilite is a relatively widespread mineral in the secondary uranyl sulfate mineral assemblages at the Blue
Lizard mine. Other secondary minerals found in direct
association with plášilite include atacamite, blödite, brochantite, calcite, chalcanthite, dickite, gerhardtite, gypsum,hexahydrite, johannite, manganoblödite, natrozippeite andtamarugite. Primary quartz (sandstone) comprises the bulkof the matrix. Additional primary minerals include baryte,
bornite, chalcopyrite, covellite, feldspar, pyrite and uraninite. Other secondary minerals in the general assemblage
include belakovskiite, bluelizardite, boyleite, cobaltoblödite, copiapite, coquimbite, cyanotrichite, d’ansite(Mn), deliensite, ferrinatrite, halite, kröhnkite, lishizhenite,meisserite, metavoltine, pickeringite, pseudojohannite,rhomboclase, römerite and sideronatrite.
Plášilite has formed late in the secondary uranyl sulfate
mineral assemblages. Of the associated phases noted above,
only hexahydrite has been observed growing on plášilite.
Crystals of plášilite placed upon damp pH paper provide a
pH between 2 and 3, indicative of strongly to moderately
acidic conditions during the formation of the mineral.

3. Physical and optical properties

Plášilite occurs as long, thin blades (Fig. 1), elongated on[001] and flattened on {100}; rarely as prisms (Fig. 2),
also elongated on [001]. Crystals exhibit the forms{100}, {010} and {011} (Fig. 3). Twinning is common on {100}; prismatic crystals show polysynthetic
twinning. Plášilite isgreenish yellow, has a
Tab. 1 Gladstone-Dale compatibilities of recently-described uranyl sulfate minerals
white streak and fluoCompatibility
resces bluish white
MineralReference
Ideal formulanav
Larsen*Mandarino**
under both long-wave
belakovskiite
Kampf et al. (2014)
Na7(UO2)(SO4)4(SO3OH)·3H2O 1.5113
0.023–0.005and short-wave UV.
beshtauite
Pekov et al. (2013)(NH4)2(UO2)(SO4)2·2H2O
1.57470.044
0.000
It is transparent withbluelizardite
Plášil et al. (2014a)
Na7(UO2)(SO4)4Cl·2H2O
1.53330.033
0.005
vitreous lustre. The
mathesiusite
Plášil et al. (2014b)
K5(UO2)4(SO4)4(VO5)∙4H2O
1.6217
0.070
0.011
Mohs hardness could
meisserite
Plášil et al. (2013)
Na4(UO2)(SO4)4·2H2O
1.53900.018–0.015not be measured, but
is probably between 2
plášilite
This study
Na(UO2)(SO4)(OH)·2H2O
1.58170.063
0.000
and 3, based upon thebased upon empirical formulae for k(UO3) = 0.134 (*Larsen 1921) and k(UO3) = 0.118 (**Mandarino 1976)
2

Plášilite, a new uranyl sulfate mineralFig. 1 Sprays of plášilite blades withtamarugite (white) on blödite andquartz. FOV 3 mm wide.

behavior of crystals when broken. The mineral exhibits
brittle tenacity, even fracture and two perfect cleavages,{010} and {001}. The mineral is easily soluble in roomtemperature H2O. The density was not measured because
plášilite is soluble in Clerici solution. The calculated
density based on the empirical formula is 3.726 g/cm 3.
The mineral is optically biaxial (+), with α = 1.556(1),β = 1.581(1) and γ = 1.608(1) (measured with whitelight). The 2V obtained by direct conoscopic observation
using a spindle stage is 88(1)° and the calculated 2V is89°. Dispersion is moderate, r< v. The mineral is pleochroic
with X = nearly colorless, Y= very pale yellow, Z = paleyellow; X < Y < Z. The opticalorientation is X = b, Y ^ c = 4°
in obtuse β.
The Gladstone-Dale compatibility, 1 – (K p/K c), is 0.0004
for the empirical formula and0.0029 for the ideal formula,in both cases in the range ofsuperior compatibility. Note thatthe compatibility was calculatedusing k(UO3) = 0.118 (Mandarino 1976), rather than k(UO3) =0.134, the value originally given
by Larsen (1921). Piret andDeliens (1989) recommended

the latter value for uranyl phosphates and arsenates andMandarino (1994) did so for selenites and selenates;
however, for uranyl sulfates, k(UO3) = 0.118 provides far
better compatibilities (See Tab. 1).

4. Chemical composition
The chemical composition of plášilite was determinedusing a CamScan4D scanning electron microscope

Fig. 2 Plášilite blades with chalcanthiteon quartz. FOV 1.8 mm.

3

Anthony R. Kampf, Anatoly V. Kasatkin, Jiří Čejka, Joe Marty

_
011

011

The empirical formula of plášilite, calculated on thebasis of 9 O apfu, is Na0.94(UO2)(S1.01O4)(OH)(H2O)2.
The ideal formula is Na(UO2)(SO4)(OH)·2H2O, which
requires (in wt. %) Na2O 7.01, UO3 64.70, SO3 18.11 andH2O 10.19, total 100.

5. Raman spectroscopy
A Raman spectrum (Fig. 4) of plášilite crystal was collected using a DXR dispersive Raman spectrometer
100
010(Thermo Scientific) mounted on a confocal Olympus microscope (100× objective). The Raman signal was excitedby a 532 nm diode-pumped solid-state laser and detectedby a CCD detector. The experimental parameters were:
5s exposure time; 32 exposures, 400 lines/mm grating,
25 micron pinhole spectrograph aperture and 3.0 mW
laser power level. The instrument was calibrated by aFig. 3 Crystal drawing of plášilite;
software-controlled calibration procedure using multiple
clinographic projection in standard
neon emission lines (wavelength calibration), multipleorientation.
polystyrene Raman bands (laser frequency calibration)and standardized white light sources (intensity calibra(SEM) equipped with an Oxford Link ISIS energytion).
dispersive X-ray spectrometer. An operating voltage of
The foregoing interpretation of the Raman spectrum
20 kV was used with a beam current of 1 nA and a 1 μmof plášilite is based upon Nakamoto (1986), Volod’kobeam diameter. The EDS mode on the SEM was chosen
et al. (1981) and Čejka (1999, 2004, 2007). The crystal
for the analysis instead of the WDS mode on the elecstructure of plášilite contains one symmetrically distinct
tron microprobe because of the instability of plášilite
U6+, one symmetrically distinct S6+ and one symmetriunder the electron beam caused by high contents of bothcally distinct Na+. The free uranyl ion, (UO2)2+ with the
Na and H2O. Attempts to use the WDS mode were unpoint symmetry Dαh, exhibits three fundamental modes:
successful due to rapid and significant decomposition ofthe ν1 (Σg+) symmetric stretching vibration, Raman acthe mineral under the electron beam. Although plášilite
tive at 900–750 cm–1, the ν2 (δ) (Πu) doubly degenerate
is a relatively widespread mineral in the secondary
bending vibration, infrared active at 300–200 cm–1, anduranyl sulfate mineral assemblages at the Blue Lizard
the ν3 (Σu) antisymmetric stretching vibration, infraredmine, it is present in very small quantities, making it
active at 1000–850 cm–1. The symmetry decrease from
impossible to separate an adequate amount of pure maDαh to Cαv or C2v may cause the infrared activation of theterial for direct determination of H2O. Consequently,
ν1 vibration, Raman activation of the ν2 and ν3 vibrations
H2O was calculated by stoichiometry on the basis of 9 O
as well as splitting of the ν2 doubly degenerate bending
apfu as indicated by the crystal structure determination.
vibration. Sulfate anion, (SO4)2–, in Td symmetry, exhibits
Raman spectroscopy confirmed the absence of CO2 andfour fundamental modes: the ν1 (A1) symmetric stretchthe presence of H2O and OH in the mineral. Other thaning vibration, Raman active at ~983 cm–1, the ν2 (δ) (E)U, Na and S, no elements with atomic numbers higher
doubly degenerate bending vibration, Raman active atthan 8 were observed. Nine spot analyses provided the~450 cm–1, the ν3 (F2) triply degenerate antisymmetricdata reported in Tab. 2.
stretching vibration, infrared and Raman active at ~1105
cm–1, and the ν4 (δ) (F2) triply degenerate
Tab. 2 Analytical data for plášilite (wt. %)bending vibration, infrared and Raman active
at ~611 cm–1.
Constituent
Mean (n = 9)Range
SD
Probe standard
A band at 3600 cm–1 was assigned to the
Na2O
6.61
5.42–7.63
0.59
Chkalovite
ν(OH) stretching vibration of free or weakly
UO3
65.15
64.47–66.30
0.60
UO2hydrogen-bonded hydroxyl ions. Bands at
SO3
18.33
17.63–19.19
0.45
ZnS3530 and 3385 cm –1 are attributed to the
H 2O
10.24*
ν(OH) stretching vibrations of structurally
Total
100.33
nonequivalent hydrogen bonded water mol*
calculated from structure
ecules. According to Libowitzky (1999),
SD – standard deviation

4

Plášilite, a new uranyl sulfate mineral

O–H

Fig. 4 The Raman spectrum of plášilite.

approximate O–H···O hydrogen bond lengths are > 3.2
Å/3599 cm–1, 2.96 Å/3532 cm–1 and 2.79 Å/3385 cm–1. Nobands were observed in the region of bending vibrationsof water molecules (~1600 cm–1).
Bands at 1180, 1069 and 1035 cm–1 are assigned to thesplit triply degenerate ν3(SO4)2– antisymmetric stretchingvibrations and a strong band at 997 cm–1 to the ν1(SO4)2–
symmetric stretching vibration. A shoulder at 986.5 cm–1
may be assigned to the δU–OH bending vibration or theν1(SO4)2– vibration.
A weak band at 905 cm –1 is connected with the
ν3(UO2)2+ antisymmetric stretching vibration. A very strong
band at 838 cm–1 was attributed to the ν1(UO2)2+ symmetricstretching vibration, while a shoulder at 824 cm–1 may be
assigned to the same vibration or to the δ U–OH bending
vibration. According to Bartlett and Cooney (1989), approximate U–O bond lengths in the uranyl ion are 1.78
Å/904 cm–1, 1.78 Å/838 cm–1 and 1.79 Å/824 cm–1. All
these U–O bond lengths are close to those inferred by
Burns (2005) for uranyl pentagonal dipyramidal coordination polyhedra and agree with U–O bond lengths in the
plášilite structure determined by X-ray diffraction.

Bands at 645 and 603 cm–1 are connected with triply
degenerate ν4(δ)(SO4)2– bending vibrations, and bands at
480 and 445 cm–1 to the doubly degenerate ν2(δ)(SO4)2–
bending vibrations. A band at 349 cm–1 may probably
be assigned to ν(U–Oequatorial) stretching vibrations. The
doubly degenerate ν 2(δ)(UO 2) 2+ bending vibration ischaracterized by a band at 243 cm–1. Remaining bands
at 210, 186, 170, 137, 88 and 70 cm–1 may be assigned
to lattice modes.

6. X-ray crystallography and structure
determination

6.1.	Powder diffraction
Powder X-ray diffraction data for plášilite were obtainedusing a Rigaku R-Axis Rapid II curved imaging plate
microdiffractometer utilizing monochromatized MoKα
radiation (Gandolfi method). Observed powder dhkl values and intensities were derived by profile fitting using
JADE 2010 software (Materials Data Inc.). Data (in Å)
5Anthony R. Kampf, Anatoly V. Kasatkin, Jiří Čejka, Joe Marty
Tab. 3 Powder X-ray diffraction data for plášilite
Iobs

dobs

100

6.90

99

5.85

15

4.72

57

4.024

21

3.731

dcalc

Icalc

hkl

6.9184100020

5.903642011

5.7981
4.747942
71̄ 1 1
021

Iobs

dobs

5

1.9620

dcalc

Icalc

hkl

1.96792033

1.96313

232

1.93701.93444
3

420
1̄ 4 3

1.92906350

1.92301.91992
92̄ 4 3170

4.69248

1̄ 2 14.14004.0353

6
37

111
200

4.004523130

1.91693

4̄ 3 2

3.76683.739088031
1̄ 3 11.90801.8630

5
4

113
341

1.85536

4̄ 1 3

1.8396
1.82123
2

4̄ 4 1261

30

1.9212

3.67574121

3.59973.52176
27

2̄ 2 1
1̄ 0 23.492

3.4857

34

220

40

3.136

3.4592
3.1385
3.1115

20
33
2

040
1̄ 2 22̄ 3 1  9

3.050

3.05656041

1.74293440

3.04164

1̄ 4 11.7367

5

411

14

2.898

2.902517211

1.73483

4̄ 3 313

2.841

2.840115

3̄ 1 11.72852

5̄ 0 22.70482.69362.6740

4
18
3

141
102
2̄ 4 1

1.7182
1.7124
1.70733
6
2

322
5̄ 1 1252

2.66422032

1.70644

2̄ 2 42.62632.6177

8
7

240
150

1.69081.680755072
2̄ 7 22.614816

3̄ 0 2

1.67694

5̄ 2 22.53922.51012
9

1̄ 5 1122

1.67191.66942
2081
1̄ 8 12.49622.46782.45622.44592.32382.3008

5
5
7
7
4
4

231
1̄ 4 23̄ 3 13̄ 2 2
330
1̄ 1 31.6402
1.63671.6333
1.63191.6163
1.6066

4
3
2
3
3
2

1̄ 6 3431
2̄ 6 3004
5̄ 3 1181

2.28185

2̄ 1 31.6001

3

2̄ 8 12.21102.18342.174432
5

1̄ 2 3311
061

1.59601.59291.5883

5
4
3

361
370
024

2.1690

6

1̄ 6 1

1.58262063

2.14942.1253

4
7

013
142

1.5812
1.57844
2

4̄ 6 1342

2.11072.1062

3
2

052
321

1.5692
1.56413
2

2̄ 4 43̄ 6 31.55563

4̄ 2 41.5103
1.46793
2

190
5̄ 4 3

82

25

34

2.690

2.618

14

2.509

18

2.457

10

2.293

15

14

20

18

2.173

2.122

2.084

2.021

2.10383

3̄ 1 32.09122.08593
7

2̄ 5 2
3̄ 4 22.07252

4̄ 2 12.06792

2̄ 3 32.03642.02422.0231

4
2
6

161
251
2̄ 6 12.01775400

2.00272

3̄ 5 1

Only calculated lines with Icalc ≥ 2 are shown

6

11

3

8

11

13

14

1.85381.81951.76671.73501.70881.677113

1.631520

1.592591.56532

1.50566

1.466951.445991.38741.81292

3̄ 4 31.77761.77381.7608

3
3
6

133
302
2̄ 0 4

1.46114272

1.44952

4̄ 4 4

1.44181.4384
1.397932
2

4̄ 7 2313
6̄ 1 31.39082092

1.38523

2̄ 9 2are given in Tab. 3. Unit-cell parameters refined from the powder datawith whole-pattern fitting are: a =8.697(2), b = 13.827(2), c = 7.065(2)Å, β = 112.118(7)° and V = 787.1(3)Å 3.

6.2. Single-crystal X-ray   diffraction and structure   solution
Single-crystal data for plášilite werecollected on a Rigaku R-Axis Rapid
II curved imaging plate microdiffractometer using monochromatized
MoK α radiation. The CrystalClearsoftware package (Rigaku Corp.) was
employed for processing structure
data, including the application ofan empirical multi-scan absorption
correction using ABSCOR (Higashi2001). The structure was solved bydirect methods using SIR2004 (Burlaet al. 2005). SHELXL-2013 (Sheldrick 2008) was utilized for the refinement of the structure. A difference
Fourier synthesis located all H atom
positions, which were then refinedwith soft restraints of 0.82(3) Å on
the O–H distances and 1.30(3) Åon the H–H distances and with the
Ueq of each H set to 1.2 times that ofthe donor O atom. Data collection andrefinement details are given in Tab. 4,
atom coordinates and displacement
parameters in Tab. 5, selected bonddistances in Tab. 6, and a bond-valence analysis in Tab. 7.

6.3. Description of the crystal   structure
The U site in the structure of plášilite
is surrounded by seven O atom sites
forming a squat pentagonal bipyramid. This is a typical coordination
for U6+ in which the two short apicalbonds of the bipyramid constitute theuranyl group. The observed uranyl
bond-lengths in plášilite (U–O5 =1.779 and U–O6 = 1.781Å; Tab 5)
closely match the typical value for theuranyl bond-length given by Burns

Plášilite, a new uranyl sulfate mineral

Tab. 4 Data collection and structure refinement details for plášilite
Temperature
Structural formulaSpace group
Unit-cell dimensions

298(2) K
Na(UO2)(SO4)(OH)(H2O)2
P21/c
a = 8.7122(6) Å
b = 13.8368(4) Åc = 7.04650(17) Å
β = 112.126(8)°V
786.89(7) Å3
Z
4
Density (for above formula) 3.723 g cm–3
Absorption coefficient20.965 mm–1
F(000)
780
Crystal size
80 × 20 × 5 µm
θ range
3.45 to 27.48°
Index ranges–11 ≤ h ≤ 11, –15 ≤ k ≤ 17, –7 ≤ l ≤ 9
Reflections collected/unique 7709/1794; Rint = 0.0295
Reflections with Fo > 4σ(F) 1609
Completeness to θ = 27.48° 99.4%
Refinement method
Full-matrix least-squares on F2Parameters refined
124
GoF
1.081
Final R indices [Fo > 4σ(F)] R1 = 0.0194, wR2 = 0.0446
R indices (all data)
R1 = 0.0231, wR2 = 0.0462
Largest diff. peak/hole+3.07/–0.70 e A–3
2
2
2*Rint = Σ|Fo –Fo (mean)|/Σ[Fo ]. GoF = S = {Σ[w(Fo2–Fc2)2]/(n–p)}1/2.
R 1 = Σ||F o |–|F c ||/Σ|F o |. wR 2 = {Σ[w(F o 2 –F c 2 ) 2 ]/Σ[w(F o 2 ) 2 ]} 1/2 ;w = 1/[σ 2(F o2) + (aP) 2 + bP] where a is 0.026, b is 0.4537 and
P is [2Fc2 + Max(Fo2,0)]/3.

et al. (1997), based on a large-number of well-refined
crystal structures. In the structure, pairs of pentagonal
bipyramids share a common edge, forming dimers. The
dimers are linked by sharing corners with SO4 groups,
yielding a [(UO2)2(SO4)2(OH)2]2– sheet parallel to (010)(Fig. 5). Between the sheets are NaO2(H2O)4 octahedra,
which link by sharing trans H2O–H2O edges to form
chains along [001]. Sodium octahedra link the sheets in
the [010] direction; each Na octahedron shares one O
corner with an SO4 group in the sheet and the opposite
O corner with a uranyl group. The framework thereby
created is further linked via relatively weak hydrogenbonds (Fig. 6).
The [(UO 2 ) 2 (SO 4 ) 2 (OH) 2 ] 2– sheet is based on thephosphuranylite anion topology (Burns 2005), with aring symbol 61524232 (Krivovichev and Burns 2007). The
sheets in johannite, Cu[(UO2)2(OH)2(SO4)2](H2O)8, (Mereiter 1982) and deliensite, Fe(UO2)2(SO4)2(OH)2·7H2O,(Plášil et al. 2012) are topologically identical to that inplášilite; however, the sheets are geometrical isomers,
differing in the orientation of the SO 4 groups (Fig. 5).
It is worth noting that plášilite and johannite occur indirect association at the Blue Lizard mine, and deliensite
has been found in the general assemblage. None of theother uranyl sulfates recorded at the Blue Lizard mine(e.g. belakovskiite, bluelizardite, meisserite and several

Tab. 5 Atom coordinates and displacement parameters (Å2) for plášilite
U
S
Na
O1
O2
O3
O4
O5
O6
OH7
H7
OW8
H8A
H8B
OW9
H9A
H9B

x/a
y/b
z/c
0.23417(2) 0.46715(2)0.12219(2)0.32042(13) 0.50289(8)0.66758(15)0.2793(3) 0.73085(15) 0.6584(3)0.1796(4) 0.5684(2)0.6139(5)0.4914(4)0.3124(4) 0.4419(2)0.4736(4) 0.5623(2)0.7334(5)0.3242(4) 0.4368(2)0.8366(4)0.1168(4)0.1933(4) 0.3410(2)0.2856(4) 0.5921(2)0.1325(5)–0.0008(4) 0.5113(3)0.1785(5)–0.002(8)0.483(4)0.276(7)–0.0797(5) 0.2716(3)0.6917(6)0.006(5)0.242(3)0.702(9)–0.044(7)0.328(2)0.719(9)0.5186(5) 0.2503(3)0.0025(6)0.296(3)–0.063(8)0.475(7)0.448(6)0.210(3)–0.020(8)

Ueq
U11
U22
U33
U23
0.01131(7) 0.00812(10) 0.01565(10) 0.00985(10) –0.00007(5)0.01204(19) 0.0089(5)0.0173(5)0.0097(5)0.0013(4)0.0305(5)0.0401(12) 0.0251(10) 0.0272(10) –0.0035(8)0.0187(6)0.0107(15) 0.0222(15) 0.0231(16) 0.0033(13)0.0205(7)0.0261(18) 0.0238(16) 0.0104(15) –0.0004(12)0.0186(6)0.0076(15) 0.0242(15) 0.0208(16) 0.0025(13)0.0173(6)0.0236(17) 0.0207(15) 0.0099(14) 0.0047(12)0.0229(7)0.0236(18) 0.0204(16) 0.0229(17) –0.0032(13)0.0225(7)0.0179(16) 0.0186(16) 0.0309(18) –0.0006(13)0.0240(7)0.0120(16) 0.048(2)0.0127(16) 0.0048(15)0.029
0.0326(8)0.028(2)0.034(2)0.035(2)–0.0005(18)
0.039
0.039
0.0319(8)0.033(2)0.0272(18) 0.034(2)–0.0076(17)
0.038
0.038

U13
0.00306(6)0.0033(4)0.0136(9)0.0062(12)0.0055(13)0.0018(12)0.0090(13)0.0069(14)0.0092(14)0.0053(13)U120.00043(6)0.0011(4)0.0062(9)0.0038(13)0.0040(14)0.0012(12)0.0065(13)0.0072(14)0.0015(13)0.0057(15)0.0121(16) 0.0040(16)0.0115(16) 0.0021(17)Tab. 6 Selected bond distances (Å) and angles (°) for plášilite
U–O5
U–O6
U–OH7
U–OH7
U–O3
U–O2
U–O4
<U–O>

1.779(3)1.781(3)2.310(3)2.338(3)2.394(3)2.454(3)2.456(3)
2.289

Na–O1
Na–OW9Na–OW8Na–OW8Na–OW9
Na–O6<Na–O>

2.387(4)2.389(4)2.417(4)2.425(4)2.442(4)2.459(4)
2.420

S–O1
S–O2
S–O3
S–O4
<S–O>

1.456(3)1.481(3)1.485(3)1.492(3)1.479

Hydrogen bonds (D = donor, A = acceptor)
D–H
d(D–H) d(H…A)<DHA
OH7–H70.80(3)2.10(5)137(6)
OW8–H8a0.82(3)2.26(3)161(5)
OW8–H8b0.84(3)2.32(3)
166(5)
OW9–H9a0.79(3)2.31(3)
162(6)
OW9–H9b0.80(3)2.43(3)161(5)

d(D…A)
2.739(5)3.050(5)3.141(5)3.066(5)3.193(5)

A
O1
O5
O7
O4
O2

<HDH

101
120

7

Anthony R. Kampf, Anatoly V. Kasatkin, Jiří Čejka, Joe Marty

c
b
c

c
b

a

U

U

S

plášilite

U

S

S

johannitedeliensite

Fig. 5 Sheets in the structures of plášilite, deliensite and johannite. The unit is cell shown by dashed lines. For plášilite, H atoms are represented
by white spheres. O–H bonds are drawn as sticks.
Tab. 7 Bond-valence analysis for plášilite (in valence units)
O1
U
Na
S
H7
H8a
H8b
H9a
H9b
Σa

0.18
1.57
0.10

O2
0.46

O3
0.52

O4
0.46

1.47

1.46

1.43

O5
1.69

O6
1.68
0.15

OH7
0.61, 0.58

OW8

OW9

0.17, 0.16

0.18, 0.16

0.90
0.08
0.07

0.92
0.93

Σc
5.99
1.00
5.93
1.00
1.00
1.00
1.00
1.00

0.07
0.93
0.06
0.94
1.86
1.99
1.97
1.96
1.77
1.83
2.15
2.18
2.21
Bond strengths are as follows:*S6+–O from Brown and Altermatt (1985); Na+–O from Wood and Palenik (1999); U6+–O from Burns et al. (1997); hydrogen based on H…O bondlengths from Brown and Altermatt (1985).

others under study) have structures that contain uranyl
dimers.

U
Na

S

b
a

8

Acknowledgements. Reviewer Stuart Mills, an anonymous reviewer and handling editor František Laufek arethanked for their constructive comments on the manuscript. Ken Krahulec of the Utah Geological Survey isthanked for providing information about the genesis of
the U deposits in the area. The recording of the plášilite
Raman spectrum by Ladislav Lapčák (Institute of Chemical Technology, Prague) is highly appreciated. A portionof this study was funded by the John Jago Trelawney
Endowment to the Mineral Sciences Department of the
Natural History Museum of Los Angeles County. Further support was provided by long-term project DKRVO
Fig. 6 The crystal structure of plášilite. The unit is cell indicated bydashed lines. Hydrogen atoms are shown as white spheres; O–H bonds
are drawn as sticks. Hydrogen bonds are shown as thin lines. Note thechains of [NaO2(H2O)4] octahedra running along [001].

Plášilite, a new uranyl sulfate mineral

2014/02 of the Ministry of Culture of the Czech Republic(National Museum 000232782) to J. Č.
Electronic supplementary material. Supplementary crystallographic data for this paper are available online at the
Journal web site (http://dx.doi.org/10.3190/jgeosci. 184).

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