Journal of the Czech Geological Society, 42/4 (1997)

3

Secondary minerals of the Jáchymov (Joachimsthal) ore district
Sekundární minerály jáchymovského rudního revíru (Czech summary)
PETR ONDRUŠ1 - FRANTIŠEK VESELOVSKÝ1 - JAN HLOUŠEK2 - ROMAN SKÁLA1 - IVAN VAVěÍN1 - JIěÍ FRÝDA1 - JIěÍ ýEJKA3 - ANANDA GABAŠOVÁ1
1

Czech Geological Survey, Klárov 3, 118 21 Prague 1
U Roháþových kasáren 24, 100 00 Prague 10
3
National Museum, Václavské námČstí 68, 115 79 Prague 1
2

Two hundred and seven secondary mineral species are described and/or referenced. Approximately seventy secondary minerals were
known from the district before the present study. All known reliable data on the individual secondary minerals from Jáchymov are presented. New and more complete X-ray powder diffraction data for compreignacite, irhtemite, lavendulan, lindackerite, masuyite,mcnearite, metaschoepite, mottramite, rabbittite, rabejacite, richetite, sodium-zippeite, voglite, zellerite, zippeite, and zýkaite are presented. A list of secondary minerals arranged according to chemical composition and list of “non-secondary” minerals are included at
the end of this paper.
Key words: secondary minerals, new data, Jáchymov, encyclopaedia

MOTTO

OBSCURE LEGENDS UNSETTLING THE IMAGINATION OF MANY COLLECTORS.....
TALES OF A MYSTERIOUS GREEN URANIUM-BEARING MINERAL FROM ELIÁŠ MINE.....,NOT LEAVING IN PEACE THEIR LIVES.
STORIES WHICH FOR AGES STIMULATED THE MINDS OF RENOWNED MINERALOGISTS,CHEMISTS AND STRUCTURAL CRYSTALLOGRAPHERS REQUIRE US TO LOOK WITH HUMILITY
AT THE ONLY CHEMICAL QUANTITATIVE ANALYSISOF THE MINERAL VOGLITE CARRIED OUT
BY THE CHEMIST JOSEF LINDACKER
ALREADY IN 1853...
THE AUTHORS WITH DEEP RESPECT
DEDICATE THIS WORK TO THE MEMORY
OF AN OUTSTANDING MINERALOGIST,WHOSE WORK SECURED WORLD FAMEOF THE JÁCHYMOV DEPOSIT,JOSEF FLORIAN VOGLMINING OFFICER AND DIRECTOR OF THE WESTERNSECTION OF THE JÁCHYMOV MINESCORRESPONDING MEMBER OF THE IMPERIAL GEOLOGICAL INSTITUTE IN VIENNAHONORARY MEMBER OF THE NATURALIST GROUP "LOTOS" IN PRAGUECORRESPONDING MEMBER OF THE NATURALIST GROUP FOR HARZFULL MEMBER AND CURATOR OF THE MONTANISTIC GROUPIN THE KRUŠNÉ HORY (ERZGEBIRGE)

Acknowledgements
We are especially appreciating valuable advice and help
provided by cpt. J. Vajdák, Massapequa, N.Y., USA, andS. Vrána, Czech Geological Survey, Prague.

We wish to thank the Grant Agency of the Czech Republic for supporting our project by the grants Nos.
205/93/0900, 205/97/0491 and the Czech Geological
Survey for support of our research.
Our thanks go to the following specialists and institutions for allowing access to their collections:

4

Journal of the Czech Geological Society, 42/4 (1997)- in the Czech Republic: J. Litochleb, National Museum,
Prague, B. Kratochvíl, Institute of Chemical Techonology, Prague, P. Kašpar, Faculty of Science, Charles
University, Prague, A. Pfeifferová and M. H. Novák,
Moravian Museum, Brno, Z. Losos, Faculty of Science, Masaryk University, Brno
- in Austria: G. Niedermayr, Naturhistorisches Museum,
Vienna, and B. Moser, Landesmuseum Joaneum, Graz,- in Germany: K. Thalheim, Staatliches Museum fürMineralogie und Geologie, Dresden, Prof. M. Okrusch,
Mineralogisches Institut der Universität Würzburg, and
A. Massanek, TU Bergakademie Freiberg, Freiberg.
We are thankful also to other specialists and institutions for their help, particularly to those who have shown
us their specimens and in some instances allowed us totake small subsamples for our study.

Introduction.... PROGRESSIVE STEPS THAT ATTRACTED AND LED US TO THE MIDDLE OF KNOWN AND UNKNOWN HORIZONS,DEEPER AND DEEPER INTO THE DEPTHS OF NATURAL KNOWLEDGE, AND INDICATING THAT IT IS NATURAL FOR A MAN TOLEARN NOT ONLY ABOUT HIMSELF, BUT ALSO HIS MIRROR. THESE STEPS DEMANDED THAT WE TRIED TO LOOK TWO CENTURIES BACK AND RECOGNISE, AS HAS HAPPENED MANY TIMES IN THIS PERIOD, ONE SMALL, FOR SOMEONE MAYBE INSIGNIFICANT, BUT STILL SO FAMOUS AND BIG EPISODE OF SECONDARY MINERALS IN THE JÁCHYMOV ORE DISTRICT.
HAVING IN MIND ONLY A NEGLIGIBLE POSSIBILITY OF APPROACHING THESE INVISIBLE TOUCHES OF THE ENDLESSEXISTENCE OF THE UNIVERSE, WE PRESENT THIS WORK, IN HOPE THAT IT SHIFTS OUR KNOWLEDGE, ALBEIT INFINITESIMALLY,
AND, PERHAPS, OUR LONGING AND EMOTIONS....
The project of study of the secondary minerals in the
Jáchymov ore district was undertaken in the years 1993
to 1996, thanks to the support by the Grant Agency of
the Czech Republic [299].
The secondary minerals, usually of little interest formining economy, attracted in the past attention of mineralogists, often equipped only with modest instruments.
The present project aimed at obtaining new information
on topographic, systematic, and genetic mineralogy.
Special attention was paid to genetic aspects, which
could provide valuable information on conditions andprocesses of formation of the secondary minerals.
During work on the project it appeared that theamount of our own new work and data exceeded theoriginally expected extend, owing to ever increasing
number of newly identified mineral species, which were
new for this district. For this reason, only reliable information is included from the literature to gain space for
new data. In the limited time span, it was not possible tostudy in detail all the minerals identified; also, it was notpossible to characterise completely several newly discovered phases.
It was possible to confirm occurrence of a great majority of minerals previously reported from the Jáchymov district. New results and all available data are presented in a condensed form, as a data table. X-ray powder diffraction data are omitted in case of correspondence with values already published for a species fromthis district. Instead, newly measured and calculated
unit-cell dimensions are often included.
During this study of secondary minerals, the numberof primary and rock-forming minerals was also expanded (lists are included at the end of this paper).
Moreover, several new unknown natural phases wereidentified and thirty of them are described in more detailin a separate paper - see New naturally occurring phasesof secondary origin from Jáchymov in this issue.
Reference system by numbers in “[ ]” was used toreduce the length of the paper. Since all papers in thisissue refer to similar set of references, the literature ref-erences are presented as a single list at the end of thispaper. In the section Encyclopaedia of secondary minerals from Jáchymov ore district, all used references corresponding to individual mineral species are listed in reference row of data table.
The study of old literature often resulted in putting
together fragmentary information on type specimens andthe history of new minerals described from Jáchymov inthe past century. In view of the significant contributionof the district to systematic mineralogy, the old data,
which are of permanent interest, are grouped in the paper
History of secondary minerals discovered in Jáchymov.
Geology
Jáchymov is located on the southern slope of the Krušné
hory Mountains, approximately 20 km north of Karlovy
Vary. The Jáchymov ore district coincides with the immediate area of the town and its close surrounding. Elevation of the ore district ranges from 450 to 850 m a.s.l.
The region is underlain by a complex of metamorphosed sedimentary rocks of Cambrian and Ordivicianage, representing the mantle of granite pluton. The Variscan granitic rocks belong to the Karlovy Vary granite
pluton [100]. Metasedimentary rocks comprise biotite or
biotite-muscovite mica schists, often affected by albitization and pyritization; graphite and garnet are sometimes
present. Minor interlayers are represented by calcsilicate gneiss, quartzites, amphibolites and orthogneisses. According to Macourek and ýumrda [184],
the complex can be classified into two divisions, including the Jáchymov division with four horizons and theBarbora division with two horizons. Granitoids which
intruded this metasedimentary complex range in age
from 330 to 310 Ma [188]. The intrusive contacts are
dominantly subhorizontal with small undulations. The
older types of granitoids include mainly porphyritic biotite granodiorite with an elevated content of Th and U
and Th > U relation.

Journal of the Czech Geological Society, 42/4 (1997)

5

Fig. 1. Sketch map of the Jáchymov ore district [187] with countours of the town (ruling pattern).

Vein clusters: A - Abertamy, B - Barbora-Eva, C - Rovnost, D - Svornost, E - Panoráma, F - Bratrství, G - Plavno.
Veins (from west to east): ý - ýertova, M - Mariánská, Fl - Fluther, Z - Ypsilon, ý - Nová ýervená, MK - Malá Krásná, G - Geister, B - Bergkittler,
SJ - Severní Jeroným, Š - Švýcar, E - Evangelista, HE - Heuerzecher, H - Hildebrand, F - Fundgrubner, G - Geschieber, AN - Anna, MT - MatČj, ZB - ZdaĜ BĤh, FR - Františka.

The younger granitoids are leucocratic, show a strong
predominance of U above Th and contain increased Nb,
Sn, and Be [76]. The apical parts of this granite are often
greisenized, featuring Sn mineralization and minor contents of topaz, fluorite and Li-bearing micas.
The immediate intrusive contact is marked by a biotite-rich zone about 10 cm thick.
The whole region contains abundant aplite, pegmatite, granite porphyry, lamprophyre dykes as well as
dykes of the Tertiary basalts and basaltic tufs.
In the framework of regional classification the
Jáchymov ore district belongs to the Saxothuringian
Zone [183] and to the Krušné hory metallogenetic unit.
The ore district coincides with the Gera-Jáchymov fault
zone trending NW-SE [293] which exhibits recurrent
activity during the Variscan and post-Variscan evolutionof this region. Deposition of majority of ore minerals
took place during the Variscan mineralization frommesothermal fluids.
The ore district is bound by several faults, including
the major northern fault zone. The fault pattern and location of mineral veins is shown in Fig. 1. The width of themost important faults and fault zones is variable, up to
300 m in case of the Krušné hory fault. For centuries,
mineralised veins were classified according their trend in
N-S trending veins ("midnight veins") and E-W trendingveins ("morning veins").The mineralization is irregular,barren parts of veins alternate with rich ore lenses andore pillars developed at places. The N-S trending veinstend to be richer and wider, the E-W trending veins show

more variation in trend and dip as well as thicknes. The
richest parts coincide with splitting of a vein in several
branches. Towards contact with granite, the veins become barren and disappear [116].
The mineralization of the deposit was classified byMrĖa and PavlĤ [126], [123] and Arapov et al. [76]. The
two classifications show many common features
1) Sn-W stage connected with autometamorphism of
younger granites, which according to MrĖa and PavlĤ
[126] underlay the metamorphic complex in the wholeore district.
2) quartz-sulphide stage is of minor importance andit is developed mainly at deeper levels of the eastern partof the district; it includes galena, sphalerite, chalcopyrite,
pyrite, arsenopyrite, pyrrhotite and dolomitic carbonates.
3) carbonate-pitchblende mineralization with fluorite.
4) carbonate-arsenide stage with native Ag and Bi,
skutterudite, nickeline, rammelsbergite, safflorite andminor pitchblende.
5) sulpharsenide stage
The most widespread stages in the district are thepitchblende, arsenide and sulpharsenide stages.
During the pitchblende stage, veins composed mainlyof dolomitic carbonate pigmented red by disseminatedhematite were deposited. Uraninite is accompanied by adark violet to black fluorite.
The sulpharsenide stage is characterized by dendritic
native silver, usually overgrown by zones of Niskutterudite, rammelsbergite and other Ni-minerals such

6

as nickeline or maucherite. Native silver was often
leached out, leaving hollow perimorphoses; the freespace was sometimes filled by argentite or quartz.
Skeletal crystals of native Bi are overgrown by arsenides carrying increased cobalt content, i.e., skutterudite and safflorite, less common are rammelsbergite andlöllingite. Gersdorffite a glaucodot may be also present;
millerite and bismuthinite are rare. Quartz and dolomite
constitute gangue material.
The sulpharsenide stage is characterized by the presence of native arsenic in botryoidal aggregates, which
can be up to 1 m long. Rare orange red realgar is deposited on native arsenic and proustite in small crystals occurs in a similar position or in hollow places in arsenic.
Finely disseminated pyrite and löllingite accompany theabove minerals.
Other silver-bearing minerals belonging to this stage
include equant acanthite and short prismatic stephanite
crystals. Less common are tabular crystals of polybasite
and pearceite. Sternbergite and argentopyrite are veryrare.
The younger sulphidic stage with pyrite, marcasite,
galena, sphalerite and chalcopyrite in calcite gangue isclosing the list of mineralization stages published byMrĖa and PavlĤ [33], [126]. Arapov et al. [76] consider
this stage as representing the final episode of the preceeding sulpharsenide stage and they proposed a still
younger quartz-hematite stage.
The intrusion of the autometamorphosed granites
took place in the Saale phase [304] , the pitchblendemineralization is dated to the Permian [303], the arsenide
and sulpharsenide stage mineralization took place during
the range Upper Carboniferous-Jurassic-Tertiary (?)[303].
The age of the uranium mineralization in Krušné
hory Mts. (Erzgebirge) is comparable to similar mineralization in other parts of the Variscan orogen in Europe.
The highest age obtained for the hydrothermal assemblage quartz-uraninite-calcite is 271 r 6 Ma (2V) [294].
Younger remobilization stages were dated to 190 r 4 Ma
(2 V) and 120 r 6 Ma (2 V). The U-Pb isotope system inuraninite was again disturbed and loss of radiogenic Pb
occurred in some samples by 80 r 8 Ma (2 V) and 0-40
Ma [294]. These ages correlate with reactivation of the
Earth's crust rather than with magmatic activity. The ageof 270 Ma corresponds to collapse of the Variscan orogen, the age of 190 Ma correlates with subsidence during
Jurassic and the age of 120 Ma may coincide with opening of the North Atlantic ocean. Younger events during
the Upper Cretaceous and Tertiary correspond to effectsof the Alpine orogen in the foreland [294]. The quoted
ages were measured on samples from the deposit AueNiederschlemma (in Germany), in the zone GeraJáchymov.
Legierski measured the following ages on uraninitefrom Jáchymov: 76, 140, 165, 202, 247, and 285 Ma[301]. The isotopic composition values of galena from
Jáchymov by Legierski are presented in the following
Table. The samples 224A and 22 belong to the young

Journal of the Czech Geological Society, 42/4 (1997)

polymetallic stage which followed the main stage of BiCo-Ni mineralization [301] [307].
The isotopic composition values of galena from Jáchymov [301], [307]
Pb206
Pb207
Pb208
Mine, locality, sample
Pb206/Pb204 Pb207/Pb204 Pb208/Pb204
Bratrství, 1. máj mine
Bratrství, gallery, 224A
Bratrství, sample 22
Eliáš
Rovnost, Bergkitler vein
Svornost

25.06
18.60
25.06
18.58
25.06
18.60
25.07
18.54
25.55
18.88
24.95
18.41

21.30
15.81
21.34
15.82
21.34
15.84
21.32
15.77
21.25
15.70
21.40
15.79

52.30
38.83
52.25
38.73
52.25
38.79
52.26
38.65
51.89
38.35
52.29
38.59

A thermometric measurement conducted on mediumgrained violet to violet blue and greenish fluorite yielded
homogenization temperatures of 190-198 qC for primary
inclusions having the shape of negative crystals. Primary
to secondary and secondary inclusions gave 158 qC and
105 to 145 qC [302].
The Jáchymov ore district can be described as consisting of six vein clusters: Rovnost, Barbora-Eva,
Bratrství, Svornost, Plavno, and Panoráma. The veinclusters bear names of the respective most importantmines. Position of these clusters is shown in Fig. 1.
Hydrogeology of the Jáchymov ore district is characterized by the presence of the following two systems ofwaters: (1) descending water and (2) ascendant water.
The descending water is bound to fractures and has alime-sulphate composition. Its composition evolved
during transport along veins and fractures, including
often portions with pyrite. Its median molar ratios are[HCO3-]/[SO42-]=0.18 and [Ca2+]/[Na+]=6.0 [120]. In
difference to this composition, ascendant water has acomposition influenced by the underlying granitoids,
median molar ratios: [HCO3-]/[SO42-] = 34 and[Ca2+]/[Na+] = 0.18.
It has a temperature near 30 oC and pressure between
1.9 and 4.0 MPa. The waters derived from granitoids
have an increased radioactivity which led to their curative utilization. The first springs used in such application
early in this century were the ŠtČpa's springs at the Daniel level of the Rovnost mine. In 1924, the spring Curie
at the 12th level of re-opened mine Svornost was
brought to use. The spring Becquerel was encountered in
1928 at the same level of this mine and in 1952 thesprings Evangelist and Prokop were taped.
Hydrogeological prospecting commenced in 1960,
which resulted in taping by underground boreholes ofsprings C1, HG1, and Academician F. BČhounek and intheir use in local spa. During the first part of the sixtees,
thick walls were built across all adits connecting with the
Rovnost and Bratrství mines and the neighbouring mining fields were flooded. These activities did not influence the discharge capacity of springs with radioactive
water or their chemical composition [185].

Localization of major mines of the Jáchymov ore district. Scale 1 : 50 000

Journal of the Czech Geological Society, 42/4 (1997)7

Projection revealing mutual relationship of individual levels in major shafts (horizontal labels) and adits (vertical labels) of the Jáchymov ore district

8
Journal of the Czech Geological Society, 42/4 (1997)

Journal of the Czech Geological Society, 42/4 (1997)

It is interesting that the two systems of water circulation behave as separate systems free of mutual influenceor mixing. There is lack of communication between respective conduits, though the underground springs (i.e.,
disruptions of the conduits by mine works) occur at various altitudes (personal communication by T. Paþes)Methods of study
In many cases, the quantity of pure mineral phase available for study was rather small. Separation of subsamples was done with the aim to preserve at least a portionof the mineral on the specimen, which is important for
any future study.
All separated samples, including also pure minerals(often only 0.1 to 1 mg in weight) were measured by Xray powder diffraction and their qualitative chemicalcomposition was studied with the electron microprobe.
The qualitative X-ray diffraction work was done withpowder Phillips X'pert System (Cu radiation, 40 kV/40
mA, step 0.01 - 0.05 q2T, time 1-10 s, graphite secondary
monochromator). To minimize complicated shape ofbackground due to classic glass sample holders, thesample studied was placed on the surface of flat siliconwafer from alcoholic suspension.
Data obtained were processed with the use of the Xray diffraction software, ZDS-system, version 6.01
[291]. The unit cell parameters were calculated from thepowder diffraction data using the ZDS-system (module
Gener). The samples were calibrated with an internal
standard, most frequently quartz, or using a calibration
procedure which corrects for eccentricity of the sample(correction term (cosTcotT)/O2). Data from publishedoriginal studies were used for indexing.
The qualitative, and in some cases quantitative,
chemical composition of minerals was measured with9

the scanning electron microprobe CamScan 4 with energy-dispersive analyser EDX system LINK eXL andwave-dispersive analyser WDX system Microspec 3PC.
For quantitative chemical analysis of mineral phasesin the system Ca-Cu-UO2-CO3-H2O the following standards were used: azurite (Cu, C, O), calcite (Ca, C, O),uranium (U). Operating voltage and sample current 20
kV and 40 nA respectively. Specimen beam size was
15u10 Pm. The samples for quantitative chemical analysis were usually coated with carbon; for measurement ofcarbon content, aluminium coating was used.
Correction procedures ZAF, Phi(rhouZ), and Quadrilateral were used for calculation of all quantitative analyses.
Mineral morphology was studied with the use of thescanning electron microscope TESLA BS 340, withmagnification in the range 75 to 3000. The samples were
coated with Au-Pd alloy, C, or Al.
TG, DTG curves were recorded simultaneously on
the thermobalance TG 750 Stanton Redcroft. The operating conditions: sample weight about 1-3 mg, heating rate
10 qC.min-1, dynamic air atmosphere 10 ml.min-1 andtemperature range 20-1000 qC.
Infrared absorption spectra in the 480-4000 cm-1
range were recorded with an FTIR spectrometer Nicolet
740 using KBr pellets and/or diffusion reflection mode.
In the case of rösslerite, program FullProf (version
3.2 for PC-compatibles - [284]) was used for the Rietveld refinement of crystal structure of this mineral fromexperimentally measured powder X-ray diffraction data.
Background was approximated via polynomial of thefifth order, corrections for sample displacement (cosineterm) and preferred orientation (in March-Dollase form)
were applied. Pseudo-Voigt profile shape function was
utilized. Peak base was set to 5.5 FWHM.

10

Journal of the Czech Geological Society, 42/4 (1997)

List of secondary minerals from the Jáchymov ore districtc Acanthite
AdamiteAgardite-(Y)z Albrechtschraufite
z Allophane
Alunogen
Andersonite
Anglesitec Annabergite
Antleritec Apatite
Apjohnitec Aragonite
c Arsenolite
Arsenuranospathitez Asbolan
Atelestitec Autunite
Bayldonite
Beaverite
Becquerelite
Beudantite
Beyeritec Bieberitec Bismitec Bismutite
Bismutoferrite
Brassite
Brochantite
c Calcite
Carbonate-fluorapatite
Cerussite
z Cervantite
c Chalcanthite
Chalcophyllite
Chenevixite
c Chlorargyritec Chrysocolla
Churchite-(Y)Chvaleticeite
Claudetite
Cobaltkoritnigite
Coffinite
Compreignacite
Copiapitec Copper
Coquimbite
CorkiteCornwallite
Coronadite
Cryptomelane
Cupritec Cuprosklodowskite
Curienite
Devilline
Dewindtite
z Diadochite
DuftiteEpsomitec Erythritec Eulytite
Ferrohexahydrite
FluckiteGeminite
Goethitez Goslarite
Goyazite
Guerinite
GunningiteSzomolnokite
c Gypsumc Haidingerite
Halotrichitec Hematitec Hemimorphite
Hexahydrite
Hidalgoitec Hörnesite
Hydronium jarosite
Hydrozincite
gz Isoclasite
Irhtemite
Jáchymovite
c Jarosite
c Johannite
Kaatialaite
Kahlerite
Kamotoite-(Y )KaĔkiteKasolitec Kermesite
Kettnerite
Koritnigite
Köttigite
Krautite
Langitec Lavendulan
Libethenite
c Liebigite
c Lindackerite
Magnesium-zippeite
Malachite
Masuyite
Mcnearite

Explanation of the symbols used in the table abovez{hno symbol

species known before this study - not confirmed
species known before this study - confirmed
doubtful mineral species
species newly found in this studyc Melanterite
Meta-autunite
Metalodevite
Metanováþekite
Metaschoepite
Metatorbernite
Metatyuyamunite
gz Meta-uranopilite
Meta-uranospinite
Metavoltine
Metazellerite
Metazeunerite
Mimetitec Mixite
Monohydrocalcite
Moorhouseitec Morenosite
Mottramite
Mrázekite
NamibiteNatrojarosite
c Neshquehonite
Nickelhexahydrite
Nickel-zippeiteNováþekite
Olivenite
Opal
Orpiment
Pararealgar
Parascorodite
Parasymplesite
Parnauite
Parsonsite
Petitjeanite
c Pharmacolite
Pharmacosiderite
Phosphuranylite
Picropharmacolitec Pitticite
Plumbojarosite
Posnjakite
Preisingerite
Proustite
Pseudomalachite
Psilomelane
Pucherite
Pyrolusite
c Pyromorphite
Rabbittite
Rabejacite
Rauenthalite
c Retgersite

c

c
c
z
z

c

z
z
c
z

z
c
c
c
z
z

z
c
c

c

c
c

Rhomboclase
Richetite
Römerite
Rösslerite
Rozenite
Sainfeldite
ScoroditeSchoepite
Schröckingerite
Schultenite
Silver
Sklodowskite
Smrkovecite
Soddyite
Sodium-zippeite
Strashimirite
Sulphur
Symplesite
Synchisite
Talc
Talmessite
Tenorite
Thenardite
Torbernite
Trögerite
Tyuyamunite
Urancalcarite
Uranocircite
Uranophane
Uranophane-beta
Uranopilite
Uranospathite
Uranosphaerite
Uranospinite
Valentinite
Vandendriesscheite
Villyaellenite
Vivianite
VogliteVochtenite
Walpurgite
Weeksite
WeiliteWidenmannite
Wölsendorfite
Wulfenite
Yingjiangite
Zellerite
Zeunerit
Zippeite
ZnucaliteZýkaiteJournal of the Czech Geological Society, 42/4 (1997)

Encyclopaedia of secondary minerals from Jáchymovore district

11

Lattice par. [Å]EDX, WDX
References

Acanthite Ag2S
Acanthite was described by Kenngott [221] using two
specimens collected in Jáchymov in the 18th century andkept in the Emeperror's collection in Vienna.
Kenngott [221] characterised acanthite as small,seemingly orthorhombic crystals terminated by a steep
pyramid, overgrowing argentite. The mineral is black,has a metallic lustre, it is malleable. Acanthite occurs inscattered radiating aggregates up to 2 mm long, rarely aslarger coatings. Individual crystals are platy, elongated in
one direction, with a rounded termination. It occurs inproximity of silver-bearing minerals, which provided Ag
for acanthite. The formation of acanthite is probably
taking place in the presence of sulphuric acid formed bydecomposition of pyrite and marcasite, in some cases
arsenic acid derived from arsenides was also involved.
Rarely, it overgrowth directly sulphidic minerals with
Ag. Native silver is often coated by scattered, minuteacicular acanthite crystals. It was observed in manyveins. Acanthite also forms on specimens after deposition in collection. Annabergite, gypsum, picropharmacolite, and pharmacolite are common associated minerals.
Hardness
1 < 2.5
Density [g.cm-3] 1 Dm = 7.31-7.36
References221

a = 13.52(1)major elements:
Cu, As, Y
88, 99, 110, 143

c= 5.86(1)minor elements:
TR

Albrechtschraufite MgCa4F2[(UO2)(CO3)3]2 . 17H2OThis phase was proposed as a new mineral to the Commission on New Minerals and Mineral Names (IMA) by
Mereiter in 1983. Data for albrechtschraufite based on asingle sample from Jáchymov were not published, except
an abstract indicating that the crystal structure was studied [62].
The abstract gives the following information: the newmineral occurs on a specimen of schröckingerite. The
crystal structure and chemical composition were derived
using single-crystal X-ray study. Albrechtschraufite has atriclinic cell, space group P 1 , Z=2. It contains two independent complex anions [(UO2)(CO3)3]4-. Colour is yellow green, hardness 2 to 3.
It is possible that Mereiter had an insufficient amountof the new phase, which could explain why he refrained
from publication of the data. During our work, no phasecorresponding to albrechtschraufite was encountered.
Lattice par.
[Å, °]

1 a=13,562(3) b=13,406(3) c=11,636(3)D=115,75(2) E=107,66(2) J 92,86(2)Density [g.cm-3] 1 Dm = 2.6, Dx=2.67
References
12, 62
1 – Albrechtschraufite, Jáchymov. Mereiter [62]1 - Acanthite, Jáchymov. Kenngott [221]Adamite Zn2(AsO4)(OH)

Allophane (amorphous alunimium silicates)

Adamite occurs sparsely in small spherical aggregates up
to 2 mm in diameter. The spheres are largely isolated,rarely coalesce to larger aggregates. Small-scale facetson the spheres, seen at magnification near to 1000, correspond to termination of individual crystals. The aggregates are pale pinkish in colour.
Adamite was determined in specimens from the
Geschieber vein, deposited on wallrock together withköttigite showing a striking colour banding (pale grey
brown and buff white). Adamite accompanies whitish
köttigite only and crystallised mainly in small fractures
while köttigite coated surfaces of larger free cavities.

Allophane was described [118] as strong blue spheroidal
aggregates. The present study did not confirm presenceof allophane.

Lattice par. [Å]EDX, WDX
Referencesa = 8.329(3) b = 8.530(5) c = 6.061(3)major elements:
minor elements:
Zn, As248

Agardite-(Y) (Y,Ca)Cu6(AsO4)3(OH)6 . 3H2O
This mineral was identified in a single specimen only as
glassy crust with a smooth and lustrous surface and withan intense emerald green colour. The crust is 1 mm thickcoating with area of several cm2.

Alunogen Al2(SO4)3 . 17 H2O
Alunogen occurs in a mixture with halotrichite in widelydispersed clusters of thin acicular crystals. The crystals
are white, greenish or bluish. Alunogen occurs in porous
quartz gangue, being deposited on pyrite and on minutecrystals of proustite together with other secondary minerals, which show the following succession: gypsum halotrichite + alunogen - melanterite + Mo-phase - metavoltine + copiapite.
The specimens originate from the Geschieber vein.
Andersonite Na2Ca[(UO2)(CO3)3] . 6H2O
Andersonite belongs to the most rare uranyl-carbonates
in Jáchymov. It occurs in coherent, yellow, irregularaggregates (up to 3 mm) on pieces of wallrock in old
workings. Andersonite occurs with schröckingerite andliebigite. In the ultraviolet light, it fluoresces an intenselight green.

12

Journal of the Czech Geological Society, 42/4 (1997)

Lattice par. [Å]a = 7.912(6)c = 23.36(4)Z = 18
EDX, WDX
major elements:
minor elements:
U, Ca, CNa
IR
1 215,254,272,286,300,320,347,425,475,
545,701,728,795,849,854,(880),903,915,[cm-1]
1081,1091,1378,1417,1522,1560,1578,(1662),2620,(3220),(3430),3563
Therm. analysis 1 50-185 (release of 4 H2O), 185-315 (release of 1.6 H2O), 315-450 (release of[qC]
1.5 CO2), 450-725 a 725-860 (release ofa rest of CO2)
endothermic reaction: 145, 365
References
12, 17, 56
1 - andersonite, Jáchymov. ýejka et al. [17]Anglesite PbSO4
It occurs in isometric or slightly elongated rounded crystals with adamantine lustre, up to 3 mm long. Its transparent, pale yellow or partly rusty crystals were found inminor open fractures in weathered pitchblende, among
remains of a dump from the Schweizer vein. Anglesite
was also identified, free of accompanying minerals, inopen fractures in wallrock near the Geister vein. Blackmaterial coating fractures in two specimens designatedpateraite (sample Nos. NM 45173 and NM 16899) in the
National Museum, Prague, was also identified as anglesite.

Lattice par. [Å]Referencesa = 8.261(2) b=12.030(8) c = 6.039(3)275

Apatite Ca5(PO4)3(F,Cl,OH)
Apatite was found as microscopic, short prismatic crystals embedded in goethite coating cavities in vein quartz.
This mineral was listed by Kratochvíl [118] from wallrock gneisses, but he mentioned also apatite occurrencein an ore vein.
Apjohnite MnAl2(SO4)4 . 22 H2OApjohnite occurs as whitish to light pink aggregatescomposed of very fine acicular crystals in radiating clusters. The aggregates are deposited on compact crusts ofsulphur-yellow copiapite. Central parts of some of theradiating aggregates are filled by compact, light pinkchvaleticeite. Apjohnite occurs in paragenesis with copiapite, chvaleticeite, whitish epsomite and gypsum on
specimens from the Geschieber vein.

Annabergite Ni3(AsO4)2 . 8 H2OAnnabergite forms mainly powdery coating or fragile
crusts on weathered Ni-Co ores. It is typically pale blue
green in colour, grading to grey green and greyish white.
The aggregates consist of microcrystals 1 to 10 m long.
Although annabergite is often earthy in appearance,
green glassy and botryoidal coatings or spheroidal aggregates with radiating texture were also observed.
Chemical analyses show variable proportions of Ni, Co,
Zn, Fe, and Mg; pure Ni member was not encountered.
Lattice par.
[Å,°]
EDX, WDX
IR[cm-1]
Referencesa = 10.20(3) b = 13.27(3) c = 4.68(2)E=104.61(2)major elements:
minor elements:
As, NiZn, Ca, Mn, Mg
440,470,515,595,795,865,(920),1120,
1625,3050,3200,3450
27, 91

Antlerite Cu3(SO4)(OH)4Antlerite forms glassy, very thin coatings of a strong
green colour, deposited on tabular aggregates of zeunerite. Coatings up to several cm2 in size were observed.
Antlerite was analysed in a single sample, representing a
mixture with langite and in paragenesis with zeunerite,richetite, and an unknown phase of the type “UO3H2O(1)”.

Acicular crystals of apjohnite. Magnification 250

Aragonite CaCO3
Aragonite occurs in thin coatings 1 to 2 cm2 in size andspheres up to 2 mm in diameter. The coatings are lightbluish grey, non-lustrous, while the spheres are always
grey green with a variable intensity of green shade.
There are also paragenetic differences - the coatings
occur with Ca and Mg arsenates and in the Kryštof veinon carbonate gangue with disseminated skutterudite,while the spheres associate with lavendulan and pinkköttigite overgrowing quartz and chalcopyrite crystals incavities of the Geister vein.
Arsenolite As2O3
It occurs mainly with native arsenic or in its proximity inthe form of colourless crystalline or powdery coating.
Individual octahedral crystals 2 to 3 mm long are lesscommon. In rare cases of arsenic covered by powdery
dickite, arsenolite octahedrons are up to 6 mm long,
however, large arsenolite crystals do not accompany
massive, hard dickite aggregates. The arsenolite crystals
have cleavage along {111}, conchoidal fracture, andremarkably strong glassy lustre.

Journal of the Czech Geological Society, 42/4 (1997)

Arsenolite often accompanies arsenates, in particularpharmacolite and sometimes annabergite. In one sample,
arsenolite formed together with gypsum, pharmacolite,
and lavendulan after altered Co-Ni arsenide, probably
skutterudite.
Lattice par. [Å]EDX, WDX
Density [g.cm-3]
References

a =11.051(3)major elements:
minor elements:As
Dm = 3.798 (determined by pycnometer)
27

Arsenuranospathite HAl(UO2)4(AsO4)4 . 40 H2OArsenuranospathite forms inconspicuous planar to spheroidal aggregates of light green to light yellow green
colour, composed of fine rose-shaped groups of tabular
tetragonal crystals. The crystals show a strong pearly
lustre. Arsenuranospathite aggregates are deposited directly on partly weathered uraninite or on unidentified,very thin coating of a strong yellow colour.
It was observed in paragenesis with uranospathite,whitish to transparent anglesite, nováþekite a white green
metatorbernite.
The semiquantitative chemical analyses suggest thatin the specimens studied there are members of a continuous series uranospathite-arsenuranospathite. The
specimens were collected on dumps of the Eliáš mine.
EDX, WDX
References

major elements:
U, As, Al289

13

Autunite Ca(UO2)2(PO4)2 . 10-12 H2OAutunite was described by Kratochvíl [118] as yellow,
tetragonal tabular crystals, which are rare in the Eliáš
mine and occur in small crystals in the Hohe Tane mine.
The present study did not confirm autunite in Jáchymov.
All specimens designated previously as autunite were redefined as meta-autunite.
Bayldonite PbCu3(AsO4)2(OH)2 . H2OBayldonite minute crystals form thin coatings strong
green or pale yellow in colour. They are deposited onlimonite in vugs of vein quartz. On its turn, bayldonite isovergrown by zeunerite, metazeunerite, hidalgoite, andmimetite
Lattice par.
[Å, °]
EDX, WDX
Referencesa = 14.06(2) b = 5.893(8) c = 10.15(1)E=105.75(1)major elements:
minor elements:
Pb, Cu, As
231

minor elements:
P

Asbolan (Co,Ni)1-y (Mn4+O2)2-x(OH)2-2y-2x . n H2O
Asbolan was described in the past as psilomelane, cobalt
black, or as cobalt-manganese ore. It forms largely minor botryoidal or powdery coatings. Massive material isblack, with waxy lustre. Asbolane occurs in cavities of
the Geister and Eliáš veins, in part mixed with silver
black ore [118].
Atelestite Bi8(AsO4)3O5(OH)5Atelestite was observed only as mixture with preisingerite. The mixture forms compact aggregates or irregular veinlets with total surface of several cm2, intergrown in quartz gangue. The aggregates are rather hard,
they have a pitch-like lustre (similar to that of mimetite)and grey yellow to dark grey colour. Some poorly
formed crystals up to 3 mm long, with a waxy yellow
colour, crystallised in a cavity in quartz.
Atelestite, always mixed with preisingerite, is associated with bismuth, beyerite and walpurgite. The material analysed was collected in the Rovnost I shaft.
Lattice par.
[Å,°]
EDX, WDX
References

a=10.896(7) b = 7.431(6) c = 6.978(5)E=107.45(1)major elements:
minor elements:
Bi, AsP
274

Crust of bayldonite crystals in vug of vein quartz. Magnification 1000

Beaverite Pb2(Cu,Fe,Al)6(SO4)4(OH)12
It has been found in a mixture with anglesite and metatorbernite as a fine-grained crust up to 3 mm thick. Its
colour ranges from light green to brown yellow. The
crust developed on a matrix of quartz vein with pyrite.
Jarosite, anglesite, limonite and gypsum occur as a coating on the specimen or as fill of minor fractures.
The specimen originated in the Eliáš mine.
Becquerelite

Ca(UO2)6O4(OH)6 . 8 H2O

Becquerelite occurs as spheroidal aggregates up to 0.5
mm in diameter, consisting of very fine acicular crystals
with a silky lustre. The light yellow aggregates have amatte surface. They occur as coating on fractures in thevein or in country rock close to the vein. Becquerelite
tends to be covered by spheres of compreignacite.
The specimens originate in the Geschieber vein.

14

Lattice par.
[Å]
EDX, WDX
References

Journal of the Czech Geological Society, 42/4 (1997)

a=13.835(7) b=12.378(5) c= 14.924(9)major elements:
U200, 262, 270

minor elements:
Ca

Beudantite PbFe3(AsO4)(SO4)(OH)6
Beudantite is rarely coating quartz crystals in vugs ofsome veins. It has honey yellow brown colour, glassy towaxy lustre. Beudantite is overgrown by a mixture ofnováþekite and metanováþekite. The mineral was foundin vuggy vein quartz enclosing sphalerite and bismuthinite on the dump of the Eliáš mine.
Lattice par. [Å]EDX, WDX
Referencesa = 7.351(1)major elements:
Fe, Pb, As
270

c=17.057(3)minor elements:
Ca, P,(Si)Bismite Bi2O3
Bismite in white grey grains with a high waxy lustre invein quartz forms pseudomorphs after isolated grains of
native bismuth, which is often preserved in part in thecore of the pseudomorph. The increase in volume, accompanying this replacement, resulted in radial fracturesin quartz around altered native bismuth.
Bismite is accompanied by yellow powdery bismutite
coating, remnants of native bismuth, and dispersed acicular crystals of bismuthinite, which is altered in part into
yellow material. These products were too scarce for
identification. Bismite was identified in samples fromdumps of the Eliáš mine.
Sejkora [193] reported on bismite associated withwhite powdery bismutite, walpurgite, younger bismutoferrite and bismutite.
Lattice par.
[Å, °]
References

Beyerite Ca(BiO)2(CO3)2

1 a = 5.835(8) b = 8.138(6) c = 7.482(8)E= 67.04(8)38, 89, 193

1 - bismite, Jáchymov, Sejkora [193]Bismutite (BiO)2CO3
Beyerite occurs in coatings on quartz and eulytite crystals, powdery material filling small vugs and aggregatesof very minute crystals with an adamantine lustre. It is
usually lemon yellow, grass green, and pale yellow orgrey green. It is accompanied by eulytite, namibite,
pucherite, kettnerite, native bismuth, and yellow or white
powdery bismutite, which usually replace bismuthinite.
Beyerite occurs in Bi vein fill in the Eliáš and Rovnost mines.
Lattice par. [Å] 1 a=3.7780(8)c= 21.756(6)EDX, WDX
major elements:
minor elements:
As, Cu, Fe, Mn, Si
Bi, Ca, Pb, C as
(CO3)2IR
1 572,678,701,862,1065,1138,1194,1428,
1481,2392,2452,2520,2850,2940,2980,[cm-1]
3400
References27, 49, 81,111, 193
1 - beyerite, Jáchymov, Sejkora [193]Bismutite occurs as powdery coating and earthy crusts,
white, grey, or pale yellow in colour. It formed by replacement of bismuthinite. Bismutite, accompanied bykettnerite and beyerite, occurs in brown pseudomorphs
after eulytite. Bismutite with preisingerite compose
pseudomorphs after native bismuth in a quartz veinlet. It
also replaces skeletal crystals of native bismuth. Bismutite is often accompanied by bismutoferrite and represents the most abundant oxidic mineral of bismuth.
Lattice par. [Å]a = 3.877(2)1 a = 3.871(2)EDX, WDX
major elements:
Bi, C as (CO3)2-3
Density [g.cm ] 1 Dx = 8.15
References
27, 38, 81, 190

c = 13.75(1)c = 13.87(1)minor elements:
Fe, Ca, As, Si

1 - bismutite, Jáchymov. Sejkora et al. [190]Bismutoferrite BiFe2(OH)(SiO4)2Bieberite CoSO4 . 7 H2OBieberite forms minute skeletal crystals, mainly orthorhombic tablets with uneven edges. It has a buff pinkcolour and a weak glassy lustre. Bieberite overgrowths
koritnigite and it is accompanied by pink köttigite andpicropharmacolite. The secondary minerals crystallisedon fractured quartz-carbonate gangue. It occurs inGeschieber and Evangelista veins.
Spontaneous dehydration of bieberite results in alteration to moorhouseite.
Bieberite was also described [118] as crystalline efflorescence grey buff to reddish or brownish, coating
skutterudite, pateraite, native bismuth, and on cobalt ore
minerals. It was found on the Geister vein.

It is a yellow, yellow green or olive green mineral in soft
coatings and crusts. Bismutoferrite is a common component of the so-called bismuth ochres and in western partof the district, it accompanies almost invariably native
bismuth. It is often accompanied by yellow white powdery bismutite, while association with beyerite and walpurgite is rare.
Sejkora [193] described bismutoferrite as bright yellow, small tabular crystals filling minor vugs in veinquartz and accompanied by mixite. He documented bismutoferrite also from the 6th level of the Geister vein
(Rovnost mine). Sejkora [193] gave the following
chemical analysis: Bi2O3 42.34, SiO2 23.73, Fe2O3 29.64,
H2O 1.68, Total 97.39 wt. %. Recalculation on the basisof 9(O,OH) results in the formula:

Journal of the Czech Geological Society, 42/4 (1997)

Bi0.95(Fe1.95Si0.08)2.03Si2O8(OH)
Lattice par.
[Å,q]EDX, WDX
IR[cm-1]
Referencesa = 5.220(3) b = 9.007(3) c = 7.731(4)E=101.63(5)major elements:
minor elements:
Bi, Fe, Si
Mg, Ca1 461, 489, 568, 673, 759, 797, 999, 1022,
1069, 3545

15

mineral is pale green. The mineral is biaxial, negative,
weakly pleochroic in green to blue green colours. It is
accompanied by gypsum, devilline, langite, andposnjakite, often in proximity of primary chalcopyrite
and tennantite.
Lattice par.
[Å, °]
EDX, WDX

45, 49, 52, 97, 118, 193

1 - bismutoferrite, Jáchymov. Sejkora [193]References

a =13.445(4) b=9.856(6)c =6.024(3)E=103.42(1)major elements:
minor elements:
Cu, S
Ca
27

Brassite MgHAsO4 . 4 H2O
Calcite CaCO3
The first description of the mineral, known at present as
brassite, was presented by Haidinger [225] and Turner[226] as early as 1825. Turner reported contents of As2O5
50.1 and H2O 31.6 wt. %. In 1867, Tschermak [224]published a very good description of brassite, without
suggesting a name for this species. It is a paradox that
only about a century later (1973) brassite was describedby Fontan et al. [210] using museum specimens from
Jáchymov.
Brassite forms monoclinic, pseudo-orthorhombic
crystals with a glassy lustre. The white crystals are veryfragile, with a good {100} cleavage. Tschermak [224]gave the following chemical analysis: As2O5 49.1, MgO
17.0, H2O 34.7, Total 100.8 wt. %. Only a trace of Ca
was found by a recent spectral analysis.
Brassite forms in a dry environment by dehydrationof rösslerite. Rösslerite deposited in collections readily
whitens and alters to brassite in a few weeks. The alteration starts at certain sites distributed at random throughout the crystal. Surprisingly, some rösslerite crystals,
kept in collections, resist alteration for over 20 years.
Possibly, small amounts of sulphuric or arsenic acidpresent in the latter specimens may account for a sufficient content of water. X-ray analysis of some whitenedrösslerite crystals shows that the original structure ispreserved.
Fontan et al. [210] gave the following analysis:
As2O5 48.1, MgO 15.6, CaO 0.9, H2O (calculated to100%) 35.4 wt. %. This mineral is identical with a synthetic phase crystallised from solutions at pH 2 to 4[210].
In view of the above relations, the paragenesis ofbrassite and rösslerite is analogous. The old museum
specimens with brassite show more visible haidingeriteand other minerals, which remained transparent, butwere unnoticed by the old time mineralogists.

Calcite forms up to 2 cm thick coatings on mine walls.
They are snow white, grey to brown or rusty, depending
on colouring admixture. Calcite stalagmites have thesame colour as accumulations on floor; up to 20 cm longtubes, 3 mm in diameter occur, often showing twisted
and irregular shape. Some of these odd shapes result
from coating of algae fibres by calcite.
Carbonate-fluorapatite Ca5(PO4, CO3)3F
It occurs as crystalline crusts deposited on fractures andsmall cavities in mineralised vein. The crusts are up to 1
mm thick, with short prismatic crystals on its surface.
The mineral is white or rusty, if containing limonite admixture. Crystal faces show glassy or pearly lustre. Carbonate-fluorapatite occurred in the Geschieber vein.
EDX, WDX

major elements:
minor elements:
Ca, P, C as (CO3)2-

Cerussite PbCO3
Vogl [20] described white cerussite coatings on galena in
the Geister vein. The present study confirmed cerussite
on a specimen from the same vein as minute equant orlong dipyramidal crystals of white grey colour andgreasy adamantine lustre, grown on bismutoferrite.
Cervantite Sb3+Sb5+O4
Cervantite was also described under the name of antimony ochre. According to Vogl, it accompanies stibnite
and pyrargyrite as a coating on sphalerite [118] on samples from the Geister vein.
Cervantite was not confirmed during the present
study.

Lattice par. [Å]a = 7.472(1) b=10.891(1) c=16.585(5)Z=8Density [g.cm-3] 1 Dm = 2.28, Dx = 2.326
References
107, 210, 224, 225, 226
1- Brassite, Jáchymov. - [210]Brochantite Cu4(OH)6SO4
Brochantite occurs in green to emerald green crusts ofminute crystals with a high glassy lustre. Powder of the

Chalcanthite CuSO4 . 5 H2O
Chalcanthite occurs as dark blue crystalline aggregatesin gangue impregnated by melanterite from the Kaiser
Josef mine [118].
Recently it was found in light blue aggregates composed of fine crystals, together with lindackerite anderythrite on samples collected in the Geister vein.

16

Lattice par.
[Å, °]
EDX, WDX
References

Journal of the Czech Geological Society, 42/4 (1997)

a = 7.149(1) b=10.701(7) c =5.956(1)D=97.677(4) E=125.26(4) J 94.331(3)major elements:
minor elements:
Cu, S
118, 275

Chlorargyrite was considered as a very rare mineralin reports from the 19th century [46], [63]. A specimen
kept in the mineral collection of the Faculty of Science,
Masaryk University in Brno (sample No.: 4947a), contains 1 cm wide argentite veinlet in quartz, carrying
chlorargyrite in small crevices. The cubes are up to 1
mm long and violet-brown in colour.

Chalcophyllite Cu9Al(AsO4)2(SO4)1.5(OH)12 . 18H2O
Chrysocolla (Cu,Al)2H2Si2O5(OH)4 . n H2O
Chalcophyllite associated with parnauite was identified
as a coating of light green spherical aggregates up to 2
mm in diameter. The X-ray diffraction pattern with diffuse lines indicates an imperfect crystallinity and probably a rapid deposition from weakly acid to neutral solutions.
The associated minerals include parnauite, brochantite, and malachite. The specimen is from the Geschieber
vein.
EDX, WDX

major elements:
Cu, As, S

minor elements:

Chenevixite Cu2Fe2(AsO4)2(OH)4 . H2O
Chenevixite forms earthy aggregates of a green-olive
colour. It was analysed in a single specimens only.
X-ray powder diffraction pattern with diffuse lines
indicates an imperfect crystallinity.
The mineral was identified on specimen from theWerner main.
EDX, WDX

major elements:
Cu, Fe, As

It was mentioned by an anonymous author [213] as accompanying waltherite in the Geister vein. Its identity
was confirmed by Fischer [108] in the course of revisionof the waltherite specimens.
Churchite-(Y) YPO4 . 2 H2O
Churchite occurs as minute, exceptionally 1 mm large
spheres with a rough surface and composed of radiating
acicular crystals. The mineral is white with a glassy lustre, but the surface of aggregates is usually slightly rusty
coloured. It is deposited on small quartz crystals in vugsof vein quartz, being accompanied by yellow or yellow
green spheroidal aggregates of parsonsite, ferruginous
pseudomorphs after autunite, and by anglesite. Minutecrystals of zeunerite were observed on some churchite
spheres. The mineral was identified on specimens fromthe Geister vein.

minor elements:
S, Si, Ca

Chlorargyrite AgCl
Chlorargyrite was found during the early stages ofmining, probably in shallow mines as white hexahedral
crystals. Later on, it was recorded in an altered porphyryin the Barbora adit [118], [51].
Lattice par. [Å]EDX, WDX

5.5514(2)major elements:
Ag, Clminor elements:
Br

Churchite-(Y) in radiating aggregates of minute crystals. Magnification 250

Lattice par.
[Å, °]
EDX, WDX
Referencesa = 5.61(2) b = 15.18(7) c = 6.22(1)E=115.17(5)major elements:
minor elements:
P,Dy,Ca, Y
Nd,Sm,Gd,Tm
77

Chvaleticeite (Mn, Mg)SO4 . 6 H2OHexahedral crystals of chlorargyrite. Magnification 200

Chvaleticeite forms earthy fill of light pink colour
among radiating crystals of apjohnite. The latter mineralcrystallised on compact crust of sulphur-yellow copiapite. Chvaleticeite occurs with fine acicular apjohnite,
copiapite, whitish epsomite and gypsum on specimensfrom the Geschieber vein.

Journal of the Czech Geological Society, 42/4 (1997)17

Cobaltkoritnigite (Co, Zn)(AsO3)OH . H2O
The type of occurrence is similar as for koritnigite, except for the dark violet red colour, characteristic for thecobalt-dominated species. The cobalt/zinc ratio varies
from specimen to specimen and the composition correlates with intensity of violet colour. Other physical andmineralogical properties of cobaltkoritnigite and koritnigite are nearly identical
Cobaltkoritnigite forms rare isolated radiating aggregates of minute crystals with glassy lustre on open fractures of the Geschieber vein.
Lattice par.
[Å, °]

Equant crystals of chvaleticeite constitute matrix covered by acicular
crystals of apjohnite. Magnification 250

D = 90.30(2) E =96.12(2) E = 89.77(1)major elements:
minor elements:
As, Co, Ni
Mg
43, 277

EDX, WDX

Claudetite As2O3

References

It was observed as individual acicular crystals up to 2
mm long, sometimes in radiating groups. It is transparent, highly lustrous; the latter property makes it distinct
from gypsum. Elasticity of the crystal is characteristic. It
overgrows native arsenic together with the other polymorph of As2O3 - arsenolite. Claudetite also occurs together with kaatialaite and scorodite on specimens fromthe Geschieber vein.
Lattice par.
[Å, °]

a = 7.834(8) b =15.70(2) c = 6.70(1)Coffinite U(SiO4)1-x . (OH)x
Coffinite occurs as minute grape-shaped brittle aggregates of a cinnamon brown colour. The surface material
is of a lighter colour compared to the interior parts. The
aggregates are matte on surface and on fractures. It occurs in crevices up to 3 mm long in a uraninite specimen
with pyrite. Coffinite is overgrown by acicular crystalsof milky white calcite. The specimen was collected in
the mine Eliáš.

a =5.336(2) b =12.981(1) c =4.5393(6)E =94.242(2)EDX, WDX

major elements:
U, Si
150

Referencesminor elements:
Mg

Compreignacite K2(UO2)6O4(OH)6 . 8 H2OCompreignacite carries striking and massive red brown
to orange glassy crystalline crusts, which are very friable, soft and have a yellow colour of powder. X-ray
analysis shows that the crusts correspond to mixture ofseveral phases, with vandendriesscheite predominatingover compreignacite.
Needle-like claudetite crystal in vug with crystals of arsenolite. Magnification 500
X-ray powder diffraction pattern of compreignacite from Jáchymov
Irel

dobs

dcalc

h

k

l

1)

Irel

5
7.898
4
76
7.397
7.433
0
0
2
6
100
7.214
*
7
3
4.791
*
18
5
4.434
*
3
6
3.943
5
25
3.711
3.716
0
0
4
2
60
3.607
3.581
2
0
0 *
2
29
3.546
3.531
1
3
0 *
4
22
3.508
6
20
3.235
3.226
2
0
2
14
79
3.183
3.189
1
3
2 *
16
24
3.149
8
4
2.985
8
3
2.914
2
1) - diffractions of vandendriesscheite (signed " * ")

dobs
2.766
2.582
2.557
2.528
2.47822.40902.30802.26592.19842.04942.0323
1.98981.9762
1.95501.8786

dcalc

h

k

l

2.579
2.560

2
1

0
3

4
4

2.4776

0

0

6

1)

Irel

dobs

dcalc

h

k

l

*

2
5
3
6
4
4
2
2
2
3
4
3
1
2

1.85871.79881.77991.77051.74991.72211.70301.67571.65001.63611.60691.59291.57881.52071.8582

0

0

8

*
*
*

2.05782.02891.9832

3
0
3

3
6
3

0
0 *
2 *

1.9589

1

5

4

18

Journal of the Czech Geological Society, 42/4 (1997)

Kasolite and uranophane are associated with theseminerals in the form of buff powdery coating. All thesesecondary minerals are deposited on weathered uraninite.
Compreignacite forms also glassy spheres up to 0.5
mm in diameter. They have an uneven surface, glassy
lustre and light yellow or brown yellow colour. It occurs
on fractures penetrating the vein or the country rockclose to the vein. Compreignacite forms coating on cuprosklodowskite or becquerelite.
The specimens originate in the Geschieber vein.
Compreignacite was also identified as glassy spheres
up to 0.5 mm in diameter with uneven surface and glassy
lustre. The colour is light yellow or brown yellow. The
spheres are coating fractures in vein material or in proximity of the vein, deposited on cuprosklodowskite or
becquerelite. The specimen with compreignacite wascollected in the Geschieber vein.
Lattice par. [Å]EDX, WDX
Referencesa = 7.16(1) b = 12.17(2) c = 14.87(2)major elements:
minor elements:
UK
205

pieces, e.g., rails. The absence of carbonates is characteristic for copper formation as a cementation mineral.
Coquimbite Fe2(SO4)3 . 9 H2OCoquimbite (mixed with other sulphates) occurs inearthy to powdery yellow brown aggregates. They are
cemented with fragments of quartz and gypsum as adeposit on fractures of wall rock near weathered pyritearsenopyrite veins. Only a single sample with coquimbite was analysed in a mixture with natrojarosite andgypsum.
Corkite PbFe3(PO4)(SO4)(OH)6Corkite has been found as minute spheres only several
tens of microns in diameter, sitting on brown tabular
pseudomorphs composed of amorphous iron hydroxides,
probably after autunite. The pseudomorphs used to be
designated by an incorrect name bassetite. The corkite
spheres have a glassy lustre and yellow brown colour.
EDX, WDX

major elements:
Pb, Fe, P

minor elements:
S

Copiapite Fe2+Fe43+(SO4)6(OH)2 . 20 H2O
Copiapite forms compact flow films and crusts up to 5
mm thick composed mainly of very fine crystals of sulphur-yellow colour. Some parts show light yellow togrey brown yellow colour. The crusts rim strongly
weathered parts of the Geschieber vein composed ofquartz, proustite and pyrite. Copiapite occurs in paragenesis with whitish epsomite, gypsum, light pink andacicular apjohnite, and pink compact chvaleticeite.
Copiapite was also identified in mixture with metavoltine. The mixture forms small, fine-grained, earthy
aggregates up to 0.5 mm long which are olive yellow incolour. It is typically deposited on radiating halotrichite
aggregates, in other cases on pyrite, in cavities of porous
quartz gangue with pyrite and proustite in paragenesis
with halotrichite, alunogen and melanterite. The specimens were collected in the Geschieber vein.
Copiapite, in analogy to jarosite, is a common product of decomposition of Fe sulphides (± arsenides).
However, the two minerals never occur together in
Jáchymov. This situation is caused by different conditions of their crystallisation. Copiapite is more soluble
and mobile than jarosite, especially in an acidic environment. For this reason, it tends to accumulate at alonger distance from primary sulphides.
EDX, WDX

major elements:
S, Fe

minor elements:
Mn, MgCorkite spheres deposited on amorphous pseudomorphs of Fe-oxihydroxides after meta-autunite. Magnification 600

Cornwallite Cu5(AsO4)(OH)4 . H2O
It was identified in a single specimen from the Geistervein. Cornwallite forms minor isolated spheres and botryoidal crusts coating the wallrock as a single secondary
mineral. Its colour is strong green, the lustre is glassy.
Coronadite Pb(Mn4+, Mn2+)8O16
In several samples examined, coronadite was identified
in a mixture with pyrolusite or cryptomelane, i.e., either
in crystalline pyrolusite aggregates or in compact crusts
with cryptomelane. It occurs on porous quartz gangue atthe Mariánská locality.

Copper Cu
Cryptomelane
Native copper forms arborescent groups associated withparasymplesite and gypsum on wallrock fractures next to
the Geister vein [40] and also up to 4 mm long aggregates in vugs of vein quartz in the Geschieber vein. Local precipitation of copper was also observed on old ironK(Mn4+, Mn2+)8O16

Cryptomelane forms grape-shaped to botryoidal crusts ofgrey black colour, with a brown shade. The crusts arematte and show relatively high to moderate hardness.
They are compact to fine-grained on fracture surface.
Cryptomelane is intergrown with coronadite and it isJournal of the Czech Geological Society, 42/4 (1997)

younger than pyrolusite. It occurs on porous quartz
gangue at the Mariánská locality.
Cuprite Cu2O
Cuprite was found in the rim of a cake 5 cm in diameterof cementation copper, deposited on wall rock, probably
under a (man-made) iron object. The rim, brown black incolour, is powdery, composed of a mixture of cuprite andnative copper. It formed by oxidation of cementationcopper.

19

yellow brown colour, showing a waxy lustre and yellow
streak, are rare.
Curienite was identified in paragenesis with mottramite, metatorbernite and zeunerite in vanadium-enrichedparts of the Geister vein.
Lattice par. [Å]EDX, WDX
Referencesa = 10.41(1) b = 8.464(8) c = 16.25(2)major elements:
minor elements:
U, Pb, VSi
256

Cuprosklodowskite (H3O)2Cu(UO2)2(SiO4)2 . 2 H2ODevilline CaCu4(SO4)2(OH)6 . 3 H2O

Although this mineral was defined and named in 1933
by Vaes [198] on specimens from the Shaba Province,
Zaire, mineral corresponding to cuprosklodowskite wasmentioned and partly analysed by John [199] in 1845,
using specimens from Jáchymov. John designated thismineral Kieselkupfer-Uranoxyd.
Nováþek [35] described cuprosklodowskite as very
minute acicular crystals in radiating groups with a silky
lustre, forming light green crusts and thin coatings onlimonitized and brittle vein material. The green colour inthe centres of aggregates changes to green yellow towards terminations. Slightly flattened crystals are 5 to 10
Pm wide and up to 50 Pm long. Nováþek gave two
chemical analyses, the first one designated as uranochalcite, the second as voglianite: CuO 8.99 (9.07), PbO
trace (0.18), UO3 64.96 (64.65), SiO2 13.40 (13.90)? H2O
11.72 (11.88), Total 99.07 (99.68) wt. %.

Devilline forms aggregates of randomly oriented, flatacicular crystals with a characteristic silky lustre on
cleavage planes. The colour is light blue. Devilline isaccompanied by brochantite, langite, and posnjakite
coating tennantite with pyrite in vein quartz.

Lattice par.
[Å, °]

a = 9.21
b = 6.63
c = 7.06
1 D = 90.0
E = 110.0
J 108.5
EDX, WDX
major elements:
minor elements:
U, Si, Cu
Therm. analysis 2 20-145 8.09 (4.05 H2O), 145-228 2.31
(1.13 H2O), 228-844 5.20 (1.80 H2O),[°C, wt. %]844-1000 (0.5 O2)
Density [g.cm-3] 1 Dm = 3.50, Dx=3.83 for Z=1
References35, 158, 159, 198, 199
1 - Cuprosklodowskite, Jáchymov. Bariand [158]
2 - Cuprosklodowskite, Jáchymov. ýejka et al. [7] (NM 26534)

Nováþek gave the following values of the indices ofrefraction: nD = 1.654, nE = 1.664, nJ = 1.664, 2V = 15q.
Cuprosklodowskite is pleochroic, X = a (nearly colourless), Y = c and Z = b (yellow green) [36].
According to Kašpar [106], secondary uranium silicates form only in the stage of sulphates, i.e., after decomposition of sulphides. Sufficient time, necessary fordecomposition of sulphides, was represented in Jáchymov by the pause between silver mining (since the 16th
century) and uranium mining (since about 1850). This is
the reason why this mineral was encountered only in thepast and in shallow workings.
Curienite Pb(UO2)2V2O8. 5H2O
The typical mode of occurrence is in abundant coatings
and as fill of strongly silicified and hematitized gangue.
It is yellow to yellow brown. Compact soft aggregates ofRadiating aggregates of lath-shaped crystals of devilline. Magnification 80

Lattice par.
[Å, °]
EDX, WDX
Referencesa = 20.82(1) b= 6.113(6) c = 22.18(2)E=102.55(1)major elements:
minor elements:
Cu, Ca, S
233

Dewindtite Pb3(UO2)6H2(PO4)4O4 . 12H2O
Dewindtite occurs as compact coatings of yellow to yellow orange colour. It is usually mixed with other minerals of the paragenesis, i.e., uranophane, tyuyamunite,meta-autunite, torbernite, and sklodowskite ?, on weathered material of uraninite vein in the Eliáš mine.
In a rare occurrence in the Geister vein, dewindtite
forms minute, indistinct tabular yellow crystals deposited on fine-grained yellow core in paragenesis with anorange mixture of zippeite and "pseudo-zippeite (Mg)".
Lattice par. [Å] 1 a= 15.817(8) b=17.286(6) c= 13.667(5)2 a= 15.79(3) b= 17.32(1) c= 13.62(1)EDX, WDX
major elements:
minor elements:
U, Pb, P
References276
1 - sample: 25Jb, Albrecht vein, Rovnost I. mine2 - sample: BM-5865a, Eliáš mine

Diadochite Fe2(PO4)(SO4)(OH) . 5 H2O

20

Journal of the Czech Geological Society, 42/4 (1997)

Diadochite was described from old adits on the Geistervein as brown red translucent coating on skutterudite,gypsum, pateraite, and pyrite [118]. This mineral was notconfirmed by the present study.
Duftite PbCu(AsO4)(OH)
Duftite forms minor spheres on limonite-coated open
fractures in vein quartz. The spheres tend to cluster into
continuous crust up to 0.5 mm thick, eventually passing
in minute three-dimensional curtains. The colour is variable from light yellow green to black green. In crosssection, the crusts are homogeneous, with a uniform
composition. No compositional difference was found forvariously coloured portions.
Duftite from Jáchymov is a solid solution transitional
between mottramite and duftite. In view of difference inthe crystal structure of duftite and mottramite, indexingof the powder diffraction pattern is not equivocal, seemottramite [156, 157]. It is also noted that some published diffraction data and newly measured patterns for
the Jáchymov duftite show inconsistencies for somediffraction.
EDX, WDX
References

major elements:
Pb, Cu, As
156, 157

minor elements:
V, P, Ca

Epsomite MgSO4 . 7 H2O
No pure end-member epsomite has been found and thesamples studied correspond to solid solutions of Mg, Fe,
Ni heptahydrate sulphate, showing prevalence of Mg
relative the other cations. The composition of such solid
solutions changes from place to place.
The variation in composition can be also estimatedvisually from colour variation. Highly magnesian members are light coloured to transparent, relatively intermediate members are pale yellow to dark grey greenishblue. In case of increased Fe the colour depends on thecontent of other complex hydro-sulphates and grades to
red brown. Epsomite with other sulphates forms massive
crystalline crusts and hollow stalactites, which are internally coated by minute imperfectly shaped crystals.
In addition to the assemblage with other Mg. Fe, andNi sulphates, i.e., hexahydrite, melanterite, rozenite,
szomolnokite, rhomboclase, morenosite, and nickelhexahydrite, epsomite was found with arsenolite, gypsum, and further unidentified phases with the following
qualitative composition: Mg-AsO4-SO4, Mn-SO4-AsO4,
and Mg-Ni-SO4.
Epsomite forms in places where mining encounteredpyrite-marcasite or arsenopyrite veins. Owing to actionof acid water in the mine, catalytic reactions take place
resulting in decomposition of the sulphide vein in relatively short time; sulphuric acid is the catalyzer. Besides
Mg sulphates, iron sulphates, dominantly melanterite,
are also formed. However, introduction of Mg derived
from carbonates of weathered veins is an important con-dition. The role of mineral waters (encountered in themines) in introduction of Mg is at present uncertain.
Epsomite stability exceeds that of melanterite; it isdependent not only on concentration and composition of
supplied solutions and pH (lower values are stabilising),
but mainly on other local conditions in the mine, i.e.,
temperature, humidity, and air circulation. In case thatthe latter conditions are unfavourable (relatively hightemperatures, intense air circulation, dry air), thesephases undergo dehydration and recrystallisation.
Erythrite Co3(AsO4)2 . 8 H2O
It occurs in radiating aggregates up to 3 mm long. They
are dark violet red. In one of few erythrite specimens
verified it formed as crust coating radiating spherical Feerythrite, which is reddish orange in colour. Erythrite ismainly coating weathered skutterudite.
In numerous papers, erythrite is erroneously mentioned as a common mineral in Jáchymov. Köttigite coloured pink by Co substitution was often taken for erythrite. Cobalt-bearing phases of the erythrite group areyounger, as indicated by the increasing intensity of pinkcolour in outer parts of radiating aggregates, and byother aggregates which are dark green in the centre,
grading to pink towards periphery. The pink arsenates
are increasing in abundance in specimens containing
native bismuth. The material studied comes from the
Geschieber vein.
EDX, WDX
References

major elements:
Co, As59

minor elements:
Ni, FeEulytite Bi4(SiO4)3
Eulytite forms dominantly half-spheroidal to spheroidal
radiating aggregates up to 1 cm large, translucent toopaque, or small spheres and individual dodecahedral
crystals up to 2 mm long. It is usually yellow grading tobrown yellow or grey yellow. Brown and nearly black
colour was also recorded. It has a conchoidal fracture
and adamantine lustre.
The quantitative chemical analyses done by P. ýerný,GPUP, (using Microscan M-5, Cambridge, 1975): Bi2O3
83.16, SiO2 16.48, PbO 1.39, ZnO 0.13, FeO 0:08, CuO
0.06, Total 101.30 wt. % results in the following formulabased on 12 oxygen atoms:(Bi4.00Pb0.07Zn0.02Cu0.01Fe0.01)Si3.01O12
Another analysis (average of four analyses) done by
V. Šrein using JEOL JXA-50 analyser was published by
Sejkora [193]. It results in the following formula:
Bi4.00[(SiO4)2.96(AsO4)0.03]2.99
Eulytite was also studied as a 2 cm thick vein, partly
altered to a massive grey to grey brown mixture of bismutite and kettnerite. These massive aggregates, as wellas eulytite, are coated by powdery, strong yellow bismutite. The associated minerals include native bismuth,beyerite, bismutite, kettnerite, namibite, and pucherite.

Journal of the Czech Geological Society, 42/4 (1997)

21

Lattice par.
[Å, °]
EDX, WDX

a = 10.298(4)1 a = 10.3146(6)major elements:
minor elements:
Bi, Si, Pb
Zn, Cu, Fe-1IR [cm ]495,545,920 and 1050
Density [g.cm-3]
Dm = 6.523 (determined by pycnometer),
Dx = 6.757
References27, 68, 50, 101, 102, 193
1 - eulytite, Jáchymov. Sejkora [193]Ferrohexahydrite FeSO4 . 6 H2O
It was identified in isostructural mixtures of Fe-Mg
sulphates of the hexahydrite group. Ferrohexahydrite
forms coatings and crusts with very fine crystalline texture and glassy, transparent to translucent crusts of lightgreen colour. The mineral paragenesis includes hexahydrite, epsomite, gypsum and unidentified Fe (Mg) sulphates, sampled in the Geschieber vein.
EDX, WDX

major elements:
Fe, S

MgO 19.48, FeO 2.94, MnO 1.42, CO2 45.35, insoluble
residue 0.99 wt. %. This shows that the reaction of theweathering products of native arsenic with the dolomitic
carbonate results in separation of manganese, which
enters the calcium and manganese arsenate - fluckite.
Geminite Cu2(HAsO4)2 . 2 H2OGeminite ranks among very rare secondary copper minerals in Jáchymov. Groups of tabular crystals are coating
arsenolite, which covers native arsenic. Geminite is grey
green with a glassy lustre. It occurs as a single mineral in
the respective paragenetic stage.
Geminite was synthesised via the reaction of As2O3
with malachite [137]. In Jáchymov, geminite probably
formed through reactions of weathered arsenic or arsenolite with Cu-bearing solutions.

minor elements:
Mg, NiFluckite CaMn(HAsO4)2 . 2 H2O
The mineral forms isolated spheres up to 3 mm in diameter with a characteristic rugged surface, corresponding tohigh pyramidal terminations of radiating crystals.
Fluckite is always pale pink with a violet shade. It occurs
on vein carbonates strongly corroded by products released during weathering of native arsenic. Arsenic isrimmed by an amorphous yellow green fractured material, passing towards arsenic to weakly coherent porous
aggregates of pink carbonate with fluckite spheres. It is
accompanied by additional arsenates of Ca, Mg, and Mn,i.e., picropharmacolite, rösslerite, sainfeldite and sometimes villyaellenite.
Lattice par.
[Å, °]
EDX, WDX

a = 8.48(3) b = 7.61(1)c = 6.940(9)D = 82.05(2) E = 98.70(3) J 96.21(2)major elements:
minor elements:
As, Ca, Mn

Aggregate of tabular crystals of geminite. Magnification 300

Lattice par.
[Å, °]
EDX, WDX
Referencesa = 6.402(7) b = 8.113(9) c = 15.78(2)D = 92.23(2) E = 94.13(2) J 95.13(1)major elements:
minor elements:
Cu, As137

Goethite FeO(OH)
Goethite forms up to 2 mm thick coating in open fractures and vugs. It formed by crystallisation from amorphous oxides-hydroxides of iron resulting from weathering of pyrite and marcasite. Goethite is not as abundant
as could be expected, mainly owing to very low pH of
solutions, which favours iron leaching and removal.
Goslarite ZnSO4 . 7 H2OGoslarite was listed by Kratochvíl [118] without any
specific information. It was not confirmed by the present
study.
Goyazite SrAl3(PO4)2(OH)5 . H2O

A detail of terminated crystal of fluckite. Magnification 150

Carbonate gangue of buff pink colour in a place carrying fluckite has the following composition: CaO 29.29,

Goyazite was identified as an intermediate member ofthe goyazite-florencite-(Nd) series. It forms minuteequant crystals 0.1 mm in diameter. The crystals are nontransparent, brown red in colour, with a weak glassy
lustre. Goyazite was found on fracture of altered wallrock with arsenopyrite. It occurs as overgrowth on black22

Journal of the Czech Geological Society, 42/4 (1997)

equant anatase crystals. Specimens of goyazite originate
from the vein No. 3.

Gypsum is pure white, yellowish, yellow brown andrarely pink.

Guerinite Ca5(AsO4)2(AsO3OH)2 . 9 H2OHaidingerite Ca2(HAsO4)2 . 2H2O

Guerinite is a rare secondary mineral in Jáchymov. It
occurs in isolated radiating groups of tabular crystals
with a glassy lustre and grey white colour. They formed
in proximity of or directly on a glassy coating of bluishwhite aragonite. Carbonate specimens with minor skutterudite carrying guerinite originate from the Kryštof
vein.

The mineral was first studied by Haidinger [225], who
described its crystal morphology in 1825, as one of a
new mineral from Jáchymov. In the same year, Turner[226] provided a chemical analysis and in 1827 suggested the name haidingerite for this mineral, to honour
the outstanding Austrian mineralogist Wilhelm Haidinger.
Lattice par. [Å]a = 6.946(3) b = 16.16(2) c = 7.955(4)Density [g.cm-3] 1 2.848
Hardness
1 2 - 2.5
EDX, WDX
major elements:
minor elements:
Ca, AsReferences
27, 70, 107, 130
1 - haidingerite, Jáchymov. Haidinger [225]Aggregate of very thin tabular crystals of guerinite. Magnification
150

Lattice par.
[Å, °]
EDX, WDX
Referencesa = 17.71(4) b = 6.72(1)c = 23.53(4)E = 90.38(3)major elements:
minor elements:
Ca, As107, 129, 130
A fan-shaped aggregate of haidingerite crystals. Magnification 25

Gunningite-Szomolnokite(Zn,Mn)SO4 . H2O, FeSO4 . H2O
A member of this solid solution series was identified in asingle specimen (No. NM 17259) from the collection of
the National Museum in Prague. The original designation is morenosite.
It forms grey white powdery efflorescence and coatings on weathered pyrite-marcasite vein material. The
analyses of separated material indicate a mixture ofrhomboclase and an intermediate member of the gunningite-szomolnikite group.
Szomolnokite forms as a final member of a series ofgradual dehydration products derived from melanterite
and rozenite. The reaction of rozenite to szomolnokite isreversible, though at a slower rate compared to the alteration of melanterite to rozenite. The presence of szomolnokite indicates that the original melanterite was freeof copper, since siderotile would form from a Cu-bearing
melanterite [292].
Gypsum CaSO4 . 2 H2OGypsum is the most common secondary mineral in
Jáchymov. The typical mode of occurrence is in small
crystals to 5 mm and fine-grained crystalline crusts.

A single orthorhombic crystal of haidingerite. Magnification 70

Turner [226] obtained the following composition:
CaO 28.4, As2O5 58.1, H2O 14.3, Total 100.8 wt. %. The
crystal morphology of haidingerite was later studied byTschermak [224].
Haidingerite forms radiating spherical aggregates up
to 5 mm long composed of shortly prismatic crystals.
The surface of the spheres shows a distinct faceting. It
also forms flat radiating aggregates with a small central
sphere of the same species. Isolated single crystals to 1
mm long are relatively rare. It is colourless, transparent

Journal of the Czech Geological Society, 42/4 (1997)

with a rather high glassy lustre, which makes it distinct
from some similar arsenates. Haidingerite occurs withother Ca-Mg arsenates such as rösslerite, pharmacolite,
and picropharmacolite.
The mineral is optically positive, nD= 1.590, nE =1.602, nJ = 1.638, 2Vmeas.= 58q [162].
Halotrichite FeAl2(SO4)4 . 22 H2O

23

Hidalgoite PbAl3(AsO4)(SO4)(OH)6
Hidalgoite was found on a single specimen as minor
irregular aggregates greenish yellow brown in colour,with a waxy matte surface. They are deposited on coarse,
thick tabular crystals of zeunerite-metazeunerite. Mimetite, pyromorphite, and parsonsite accompany hidalgoite. The specimen consisting mainly of vuggy veinquartz was collected on the Geister vein.

Halotrichite forms clusters of thin acicular crystals of a
glassy lustre. The crystals are white, greenish (coloured
by melanterite) or bluish (coloured by a Mo-phase). The
intensity of blue colour tends to vary depending on
variation in temperature and humidity of the environment. This behaviour is typical of some Mo-phases.
Halotrichite occurs in mixture with alunogen in porous
quartz gangue as deposited on pyrite and minuteproustite crystals. It is associated with other secondary
minerals showing the following succession: gypsum,
halotrichite + alunogen - melanterite + Mo-phase - metavoltine + copiapite. The specimens were collected in the
Geschieber vein.
Hematite Fe2O3

Aggregate of hidalgoite crystals. Magnification 600

Finely disseminated hematite is common as intergranularmaterial imparting a characteristic colour mainly to
dolomite veins. Because these veins are often carrying
primary uraninite, it is possible that iron for hematite
was released from the primary minerals by radiolysis.
However, a correlation between uranium abundance andhematite coloration is not supporting this mode of hematite formation. Uraninite may occasionally contact hematite-free carbonates.
At least some part of hematite probably formed byoxidation of Fe2+ ions during reduction of the uranyl ion(UO2)2+ to insoluble UO2 as uraninite was deposited in
the veins [106].
Hemimorphite Zn4Si2O7(OH)2 . H2OHemimorphite was described as crystals groups, smalltransparent hemi-spherical or fan-shaped aggregates, andas fibrous/prismatic textured pieces. It occurred on theGeister vein, the Eliáš mine, in a vug coated withsphalerite crystals [118].
EDX, WDX
References

major elements:
Zn, Si118

minor elements:
S

Lattice par. [Å]EDX, WDX

a = 7.099(9)major elements:
Pb,Al,Asc = 17.00(2)minor elements:
Fe, (Cu,S,P)

Hörnesite Mg3(AsO4)2 . 8 H2O
Hörnesite occurs in radiating spherical aggregates or
crystalline crusts composed of acicular crystals up to 1
mm long. Individual crystals are colourless, transparent
or white, with a glassy lustre. It also forms white efflorescence or powdery coating. Chemical composition
frequently corresponds to solid solutions of Mg, Zn, Ni,
Co, and Fe arsenates of the erythrite group, rather than topure Mg end member.
Larsen [162] measured the following optical properties on hörnesite from Jáchymov: nD = 1.563, nE = 1.571,
nJ = 1.596, 2V = 60°, extinction angle between Z and the
direction of elongation = 31°, the mineral is optically
positive.
It occurs with other arsenates of Ca and Mg on carbonate vein containing arsenides, which on weatheringgave rise to the secondary minerals.
EDX, WDX

major elements:
Mg, Ni, As
98, 117minor elements:
Co

Hexahydrite MgSO4 . 6 H2OReferences

It was identified in isostructural mixtures of hexa- andhepta-sulphates of Mg, Ni, (and Fe). These minerals
constitute coatings and crusts with a very fine-grained
texture, which are transparent or translucent, glassy
crusts, and aggregates of acicular crystals. Hexahydrite
was identified in association with nickelhexahydrite,
annabergite, gypsum, and closer unidentified Fearsenates on the Geschieber vein. See also information
on nickelhexahydrite and epsomite.

Hydronium jarosite (H3O)Fe3(SO4)2(OH)6
Hydronium jarosite occurs as relatively common powdery to earthy fill of a strong yellow colour in porousparts of the Geschieber vein composed of quartz,
proustite and pyrite. It was observed in paragenesis withparasymplesite, annabergite and gypsum.
Hydronium jarosite is a common decomposition
product of Fe sulphides (± arsenides). In Jáchymov, it24

Journal of the Czech Geological Society, 42/4 (1997)

often occurs in proximity of decomposed primary sulphides. This probably reflects instability of rather acidic
solutions of Fe sulpho-complexes (in absence or nearabsence of alkalis); the complexes were buffered over ashort distance by surrounding solutions and precipitated(or recrystallized) as hydronium jarosite.
Lattice par. [Å]EDX, WDX
Referencesa = 7.323(5)major elements:
S, Fe
259

c = 16.94(3)minor elements:
Ca, NaHydrozincite Zn5(CO3)2(OH)6
It is coating walls in old mine workings as a white crustwith a smooth and lustrous surface. The crusts up to 3
mm thick consist of numerous thin layers, which may
show a texture of perpendicular fibres. Hydrozincite may
form minor stalactites, up to 2 cm long, which arelargely composed of an amorphous material. Owing tolocal presence of znucalite, some parts of hydrozincite
coatings show an intense yellow colour. The mineralformed by decomposition of sphalerite which, althoughinconspicuous, is relatively abundant in Jáchymov veins.
Hydrozincite-znucalite accumulations formed only inthose parts, where marcasite-pyrite or arsenic-arsenide,
as well as low pH solutions were absent. Some connections also exist to abundance and composition of carbonates in veins or in wall rocks. Ca-rich carbonates buffer
solutions with relatively mobile Zn2+ and UO22+ cations
and result in formation of carbonate and hydrogencarbonate hydro-complexes of Zn and Zn-U, which are
unstable at low pH values. The mobility of the complexes is thus diminished and owing to release of CO2,hydrozincite and znucalite precipitated.
Irhtemite Ca4Mg[(AsO4)2(AsO3OH)2] . 4 H2O
Irhtemite occurs in very fine acicular white crystals,
typically in radiating aggregates. It is coating carbonate

gangue in aggregates extremely similar to those of
picropharmacolite. This probably contributed to its laterecognition and, in some cases, to possible misidentification for picropharmacolite.
Stability of picropharmacolite is not known andtherefore it is difficult to exclude the possibility ofirhtemite formation by dehydration of some picropharmacolite specimens in a special condition.
The X-ray powder diffraction pattern of irhtemite(15J) indicates a mixture of irhtemite and an unidentified
Ca-Mg arsenate. The table below lists all diffractions
observed. We record indexing of some irhtemite diffractions which were not reported in the original description[265].
Lattice par.
[Å, °]

a = 16.56(1) b = 9.539(4) c= 10.873(5)E=97.239(7)major elements:
minor elements:
Ca, As, Mg
265

EDX, WDX
References

Isoclasite Ca2(PO4)(OH) . 2 H2OThis mineral was described by Sandberger [212] in 1875
on a specimen from Jáchymov kept in the Würzburg
collection. It was described as transparent prismatic crystals up to 4 cm long, with a pearly lustre on cleavage
planes. Its hardness is 1, density 2.92 gcm-3. The analysis
given by Sandberger [212] is: CaO 49.51, P2O5 29.90,
H2O (to 100 qC) 2.06, H2O (above 100 qC) 18.53, Total
100.00 wt. %. Larsen [162] characterised isoclasite as
biaxial, optically positive, with indices of refraction nD =1.565, nE = 1.568, nJ = 1.580; crystal morphology indicates the monoclinic symmetry.
The direction X//b, the angle Z/c is not large, 2V ismoderate. Isoclasite crystals were described by Sanberger [212] as orthorhombic, the angle between prismatic
faces measured by contact goniometer was 136q50' andthe angle between prism and basal faces 110q.

X-ray powder diffraction pattern of mixture of irhtemite and unnamed Ca-Mg-arsenate.
Irel

dobs

6
32
9
10
16
100
32
12
1
16
6
<1
23
2
13
<1
30
9
7
40

12.953
9.485
8.788
7.973
6.873
6.715
6.466
6.122
5.361
5.137
5.043
4.822
4.693
4.392
4.326
4.115
4.115
3.993
3.804
3.689

dcalc

h

k

l

6.762

1

1

-1

5.393

0

0

2

4.794

2

0

-2

4.389
4.362
4.125
4.108

1
0
2
4

1
2
2
0

2
1
0
0

3.775

3

1

-2

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

15
6
18
49
45
7
5
5
17
3
22
18
10
5
3
1
10
4
3
5

3.594
3.447
3.362
3.246
3.220
3.098
3.060
3.018
2.983
2.893
2.857
2.812
2.770
2.711
2.659
2.617
2.589
2.47772.40382.3465

3.573
3.486
3.375

0
4
1

2
0
1

2
-2
-3

3.222
3.107
3.069
3.018
2.980
2.895
2.871
2.815

1
5
4
1
1
5
0
4

1
1
2
3
3
1
2
2

3
0
-1
-1
1
1
3
-2

3
2
0
1
6
7
5
8

1
4
4
1
2
1
3
2

4
1
2
-5
-3
-3
-3
-1

3
2
1
4
4
4
0

3
0
1
2
2
0
2

-1
-4
-4
2
-3
-4
4

2.24022.21872.1835
2.11762.08502.04092.01101.8981
1.89811.80561.75541.73071.71291.61131.59081.5581
1.5371
1.52471.47102.24212.22442.18102.12022.08932.04122.00991.8930

2.706
2.663
2.612
2.591
2.47292.39712.3474

8
5
3
4
4
5
4
7
<1
5
3
6
8
12
2
4
3
2
2

1.80531.75611.73051.71171.61111.5916
1.55771.53691.52501.4713

9
8
3
2
2
9
6
5
0
9

1
2
5
0
2
3
4
5
6
1

-1
-3
-2
6
6
-1
3
-3
2
-5

Journal of the Czech Geological Society, 42/4 (1997)

25

Admitting that the measurement was rather inaccurate, the crystals could be hexagonal, probably of apatite,which is possible with the analysis given above.
However, the indices of refraction are by 0.1 lower
than for apatite. Doubts concerning validity of data on
isoclasite are supported by absence of any additionaldescription or find of isoclasite anywhere.
Sandberger [212] noted that some isoclasite crystals
are partly altered to a white matte phase with the composition CaO 1.00, MgO 17.30, Na2O 9.80, P2O5 34.00,
Fe2O3 (+ Al2O3) 0.36, insoluble residue 0.18, H2O (to100 qC) 24.26, H2O (above 100 qC) 9.22, Total 96.12 wt.
%.
Larsen described isoclasite as white, cotton-like fibres composed of minute prisms. This description isdifferent from that given by Sandberger.
Isoclasite was described [212] in paragenesis with areddish dolomite vein in hornfels.

X-ray powder data of jáchymovite result in a monoclinic cell with the space group P21/a; unit cell dimensions are given in the table above. The mineral is biaxial,
optically negative, with the following indices of refraction: nD = 1.715(2), nE = 1.718(2), nJ = 1.720(2), 2Vcalc. =78q. The quantitative chemical analysis gave: UO3 84.20,
SO3 2.79, H2O 13.32, Total 100.31 wt. %, corresponding
to the formula:

Jáchymovite (UO2)(SO4)(OH)14 . 13 H2OJohannite was found in Jáchymov for the first time in1819 on the vein Geister and in 1850 on the veins Fluther and Fiedler. In both cases, the occurrence was in old
re-opened adits. Johannite occurred on pieces of weathered uraninite ore with gypsum, uranopilite, and zippeite.
Johannite was first described as a new mineral from
Jáchymov in 1828 by John [165] under the name Uranvitriol. In the year 1830 Haidinger named this mineraljohannite [26] to honour the Austrian archduke andfounder of the museum in Styria in Graz - Johann Baptist
Josef Fabian Sebastian (1782-1859) [161].

The mineral name jáchymovite was used in 1935 byNováþek [35] for cuprosklodowskite. In the publication[35] Nováþek pointed this synonymity and the namejáchymovite was abandoned.
A new mineral identified in 1979 [175] on a single
specimen from Jáchymov and later described by ýejka etal. [18] was named jáchymovite. The type specimen is in
the collection of the National Museum in Prague, No.
NM 68905.
All the data on jáchymovite are given following ýejka et al. [18]. Jáchymovite forms rich, up to 5 mm thickmicrocrystalline aggregates and earthy crusts 3 by 5 cm
in size, accompanied by small prismatic gypsum crystals, on weathered vein material. The individual jáchymovite crystal are up to 0.1 mm long, translucent; they
have a yellowish colour, glassy lustre, and light yellow
colour of powder. Cleavage on (010) is very good. Luminescence is moderate, with yellow colour. Jáchymovite occurs with gypsum, uranopilite, and uraninite.
Similar to other sulphates of uranium, jáchymovite
forms in small amounts in oxidation zone in presence ofsulphides of heavy metals and uraninite. Sulphuric acidforms in the course of the hydration-oxidation process,which results in complex ions with uranyl cations. Although these ions are not as stable as the uranylcarbonate ions [173], they significantly increase solubility of uranium and support its migration. Jáchymovite
and other uranyl-sulphates form by a quick evaporationof such solutions, which carried only small amounts ofother cations.
Lattice par.
[Å, °]
Density [g.cm-3]
IR[cm-1]
Therm. analysis[qC, wt. %]References

a= 18.553(8) b= 9.276(2) c= 13.532(2)E=125.56(2)Dx = 4.79 for Z = 2
582,622,860,880,902,932,1071,1120,
1145,1175,1590,1620,1670,3200,3445
20-97 3.26 (5 H2O), 97-145 3.53 (5H2O), 145-576 6.53 (10 H2O), 576-884
4.05 (1 SO3 + 1.32 O2 )all data after [18] 18, 35, 58, 173, 175(UO2)(SO4)(OH)14 . 13 H2OJarosite KFe3(SO4)2(OH)6
Jarosite was described by Ulrich [194] as coating onmine walls with pyrite affected by weathering. Jarosite
was considered without additional data for natrojarosite
and hydronium - jarosite.
Johannite Cu[(UO2)2(SO4)2(OH)2] . 8 H2O

Lattice par.
[Å, °]

1 a=16.509(4) b=17.871(4) c = 6.812(2)D = 91.14(1) E = 90.48(1) J 110.66(1)4 a = 8.908(2) b= 9.502(2) c = 6.814(2)IR
2[cm-1]
Therm. analysis 2[°C, wt. %]D=109.89(1) E=112.01(1) J 100.39(1)250,384,426,619,790,821,912,935,1035,
1093,1137,1628,1657,3220,3525,3598

60-100 7.34 (H2O), 100-145 7.02 (H2O),
145-235 2.76 (H2O), 235-390 2.69
(H2O), 390-550 0.05 (H2O), 550-750
13.79 (SO3), 750-810 0.86 (SO3),
further partial disintegration of the uranates formed and oxygen release.
endothermic reaction: 135,165,215,760,
exothermic reaction: 370, 495
Density [g.cm-3] 3 Dm = 3.32 (average of 5 measurements,
Berman's method)
5 Dx = 3.27
References11, 26, 28, 41, 59, 161, 164, 165, 166,
167, 168, 169, 189, 201
1 - johannite, Jáchymov - Mereiter, [166]2 - johannite, Jáchymov - ýejka et al., [11]3 - johannite, Jáchymov - Hurlbut, [168]4 - johannite, Jáchymov - ýejka et al., [201]
5 - johannite, Jáchymov - [164]

Following Haidinger [26], johannite has hardness 2
to 2.5 and a weak sour, rather than astringent, taste on
tongue. It is weakly soluble in cold water. Ježek [189]described its crystal morphology as monoclinic but the
optics is of a triclinic mineral.

26

Journal of the Czech Geological Society, 42/4 (1997)

Johannite occurs most frequently on vein fractures in
exploited parts of the Eliáš mine. It forms as a recent to
sub-recent mineral, in less than 15 years. Johannite crystallised from acid sulphate solutions enriched in Cu andU in oxidation zone of uranium-bearing vein material
with pyrite, chalcopyrite and rarely bornite, in absence ofarsenides and carbonates.
Johannite crystals with acicular habit are up to 2 mmlong and are grouped in radiating aggregates. Its colour
is bright apple green to emerald green. It has a strong
glassy lustre, it is translucent to transparent, brittle, witha pale green colour of powder. Johannite does not fluoresce in ultraviolet light. New optical data for johannite[169]: nD = 1.572, nE = 1.595, nJ = 1.614, 2V = 90q, withstrong pleochroism and dispersion. The extinction angle
between Y and the direction of elongation is 5-8q [41].
Nováþek considered the original analysis by Lindacker [59] as erroneous and he performed a new analysis: CuO 8.07, UO3 61.34, SO3 16.59, H2O 13.84, Total
99.84 wt. %, corresponding to formula:Kaatialaite aggregates are composed of acicular crystals from several Pm up to 100 Pm long. Fine-grained
aggregates have a silky lustre, coarser aggregates a
glassy lustre. It is often accompanied by scorodite, arsenolite, and claudetite. Kaatialaite aggregates containsome sulphuric acid, which was instrumental in its formation and stabilisation. The specimens are from the
Geschieber vein.
Kaatialaite from Jáchymov has nD = 1.579(2), nE |nD, nJ = 1.638. The chemical analysis gave H2O 24.8 wt.
%.

Cu[(UO2)2(SO4)2(OH)2] . 6 H2O
On the basis of single crystal X-ray measurement ofjohannite from Jáchymov [166], thermogravimetricstudy [167], and calculation of compatibility using the
Gladstone-Dale relationship [166], the following formula
was proposed [166]:
Cu[(UO2)2(SO4)2(OH)2] . 8 H2O
Hurlbut [168] suggested from single crystal X-ray
study a multiple face-centered unit cells. Mereiter [166]proposed a primitive cell (see table above). The paper[11] gives thermogravimetric analysis and infra-red spectra (concise information in table above), and accurate Xray powder diffraction data.
Johannite was recorded in assemblage with gypsum,
uranopilite, zippeite, and exceptionally with schröckingerite. Several cases of intergrowth with a new phase“pseudo-johannite” were observed.
Kaatialaite Fe[AsO2(OH)2]3 . 5.25 H2O
It was found as abundant white or greenish weakly
coherent or powdery fill of vugs in native arsenic and as
relatively compact aggregates of greenish colour.
Lattice par.
[Å, °]
EDX, WDX
IR[cm-1]
Therm. analysis[°C, wt. %]Density [g.cm-3]
References

a=15.3377(8) b=19.8051(8) c =4.7520(3)E=91.898(3)major elements:
minor elements:
Fe, AsCa, K
236,318,419,475,600,665,748,781,855,
1150,11981342,1632,2318,2420,2970,
3390, 3500
20-145 17.89 %, 145-370 8.13 %, 370610 3.25%
endothermic reaction: 159, 201, 252,
783, 884,
exothermic reaction: 612, 675, 816
Dm = 3.32 (average of 5 measurements,
Berman's method), Dx = 3.27 [164]44, 64, 177, 214, 261

Aggregate of a little elongated crystals of kaatialaite. Magnification
400

Kahlerite Fe(UO2)2(AsO4)2 . 10-12 H2OKahlerite occurs as soft coating composed of light yellow platy crystals, locally with a green shade. It shows agreasy lustre and does not fluoresce in UV light.
Kahlerite is a component of symmetrically zoned polymineral coatings with the following full sequence(from centre outwards): kahlerite - zeunerite - tyuyamunite - phase “Ca-(VO)-AsO4”, with pink köttigite,
agardite, lavendulan and strashimirite further on sides.
The coatings are deposited on quartz vein with pyrite,uraninite and tennantite. The source of vanadium is unknown. The specimen studied was collected in the Geister vein.
Kamotoite-(Y) Y2(UO2)4(CO3)3O4 . 14.5 H2OKamotoite-(Y) is identified as minute, flat radiating aggregates composed of flattened needles. The strong yellow aggregates are 0.5 mm in maximum diameter.

Radiating aggregate of kamotoite-(Y) crystals. Magnification 500

Journal of the Czech Geological Society, 42/4 (1997)

27

References

Kamotoite-(Y) has a glassy lustre and it does not fluoresce in UV light. It occurs in a minor fracture cutting
thin quartz veinlet in muscovite pegmatite. No otherradioactive mineral occurs in the veinlet.
KaĖkite FeAsO4 . 3.5 H2O
Two types of kaĖkite were identified. It forms minutespheres with a matte surface, occurring in cavities ofporous quartz. It also accompanies or covers small crystals of pyrite or proustite. The material was collected in
the Geschieber vein.
The second type is identical in appearance with thetype locality at KaĖk near Kutná Hora. It occurs as
grape-like aggregates of a bright light green colour on
specimens with altered arsenopyrite, in association withgreen grey scorodite. The original arsenopyrite is replaced in part by grey powdery sulphur.
Lattice par.
[Å, °]
EDX, WDX
References

a=18.795(7) b=17.487(4) c = 7.635(2)E=92.749(3)major elements:
minor elements:
Fe, As261

Kasolite Pb(UO2)SiO4 . H2O
Kasolite occurs in earthy microcrystalline aggregates up
to 5 mm long, which may represent pseudomorphs or fillof vugs in vein quartz. Colour of the aggregates is yellow, grading to brown towards margins. It does not fluoresce in ultraviolet light. The specimen identified is fromthe Geister vein.
Lattice par.
[Å, °]
EDX, WDX
References

a=13.307(9) b=7.022(7)c =6.730(6)E=104.90(1)major elements:
minor elements:
U,Pb,SiCa
7, 83

Kasolite was also identified in the course of revisionof old specimens in the collection of the National Museum in Prague. Specimen No. NM 17365 (donated by
V. Wraný in 1902) was designated as bismutosferit. It
consists of weathered uraninite with orange crusts, representing mixture of vandendriesscheite with compreignacite, with powdery coatings of beige kasoliteuranophane mixture.
Kermesite Sb2S2O



Kettnerite CaBi(CO3)OFKettnerite was identified in a mixture with eulytite,
bismutite, and beyerite, constituting a massive 2 cm
thick fill in quartz veinlet. The mixture has brown tobrown-grey colour. It is probable that the threecarbonates of bismuth form a pseudomorph after originalveinlet composed of black eulytite with minute grains of
native bismuth.
Lattice par. [Å]Referencesa = 3.806(3)236

c = 13.54(2)Koritnigite Zn[(H2O)AsO3(OH)]
Koritnigite forms spheroidal radiating aggregates ofminute crystals, which are up to 1 mm long. In the aggregates, the crystals are only 1 to 10 Pm long. Due to a
low Co content, the colour is mainly red violet to strawberry pink and violet red in the coarser aggregates.
Schmetzer [43] published a partial analysis: As2O5
53.66 (54.67), CoO 3.88, (4.54), NiO 0.52 (2.44), CuO
0.08 (0.08), ZnO 29.06 (25.83), FeO 0.03 (0.05) wt. %.
Koritnigite forms by reaction of weathering arsenides
with sphalerite and it is not confined exclusively onveins with carbonates. The specimens are from the
Geschieber vein.
Lattice par.
[Å, °]
Referencesa = 7.948

b = 15.829

c = 6.668

D = 90.86
43

E = 96.56

J 90.05

Köttigite Zn3(AsO4)2 . 8 H2OAt least three genetic types of köttigite occur in Jáchymov. The youngest, recent to sub-recent type, forms
powdery coatings and crusts on vein material, whitish,pink to red in colour. The older, second type occurs aslight pink radiating groups of crystals. The oldest köttigite is in the form of crystals, dark red wine in colour,
composing spheroidal aggregates or crystalline crusts.
Lattice par.
[Å, °]

IR[cm-1]
EDX, WDX

1 a=10.109(2) b=13.421(1) c= 4.7653(8)E=101.77(1)2 a=10.124(5) b=13.434(6) c = 4.765(3)E=101.86(1)430, 480, 530, 795, 860, 1045, 1110,
1450, 1635, 3100, 3175 a 3455
major elements:
As, Zn27, 91, 127

minor elements:

Kermesite was described as fan-shaped aggregates ofacicular crystals, cherry-red or brown red in colour. It
occurred in a vug with sphalerite, quartz, and antimonyochre on the Geister vein, at contact of porphyry withschist of blue colour [59]. Kermesite was mentioned
without further data already by Glückselig [247].

1 - this study, köttigite, crystals (second type)
2 - this study, köttigite, red powder (youngest type)

Lattice par.
[Å, °]

It occurs in irregular aggregates of microscopic, randomly oriented crystals. Its colour ranges from pink buff

a= 8.158(2) b=10.718(2) c= 5.7889(9)D=102.800(3) E=110.547(3) J (3)References

Ca, Mg, (Ni, Co, Mn)

Krautite Mn[(H2O)AsO3(OH)]28

Journal of the Czech Geological Society, 42/4 (1997)

to dark pink. Wet aggregates on freshly collected specimens are soft and harden after drying.
As in koritnigite, the intensity of pink colour depends
on the content of cobalt, which substitutes Mn. Krautite
occurs on crusts consisting of gypsum crystals of variable size or as powdery coating on mine walls together
with annabergite or nickelhexahydrite. It was identifiedin specimens from the Geschieber vein.
Lattice par.
[Å, °]

a=7.963(3) b=15.813(7) c =6.709(4)E=96.498(7)major elements:
minor elements:
Zn, Co, Ni
Mn, As237

EDX, WDX
References

Krautite in minute crystals with acute termination. Magnification 700

chalcopyrite. It occurs with brochantite, devilline, andgypsum.
Lavendulan NaCaCu5(AsO4)4Cl . 5 H2OLavendulan is a typical species for the assemblage of
secondary minerals in Jáchymov and at the same time it
is rare in this ore district. It was described in 1853 byVogl from the Eliáš mine [60] on the Geister and ýervená veins as an alteration product in old adits [125].
However, the type locality for this mineral is Annaberg,
where lavendulan was described in 1837 by Breithaupt[200]. The most typical form of lavendulan are sky blue,
glassy botryoidal crusts and coatings on vein material
carrying tennantite and chalcopyrite. The coatings arecomposed of microscopic spheroidal radiating aggregates of platy crystals. Crystalline aggregates are rare.
Lavendulan formation is dependent on acidity, influenced by the primary Cu-sulphides. It is accompanied byseveral younger minerals such as lindackerite, köttigite,
picropharmacolite, strashimirite, and olivenite.
Scanning electron photographs show that lavendulan
crystals are several tens of Pm long and only fractions of
1Pm thick. This corresponds to interpretation of X-ray
powder diffraction patterns (the Bragg-Brentano method), indicating a prominent preferred orientation of
microcrystals. As the X-ray patterns of various samplesof this mineral from Jáchymov show differences and also
differ from lavendulan data given by Guillemin [25], fulllisting of diffractions is presented in table below.

Langite Cu4(SO4)(OH)6 . 2 H2OLangite was observed always in mixture with posnjakite
as small blue crystalline coating.
Lattice par.
[Å, °]

a=11.253(2) b = 6.059(8) c = 7.089(3)E = 89.86(1)major elements:
minor elements:
Cu, S
242

EDX, WDX
References

Lattice par. [Å] 1 a=9.817(4) b=40.39(1) c=9.997(6)2 a=9.821(9) b=40.43(5) c=9.97(1)EDX, WDX
1 major elements:
minor elements:
Cu,As,CaSi, Na, Cl
2 major elements:
minor elements:
Cu,As,SiCa
References25, 60, 200
1 - lavendulan, Jáchymov. This study (J-263)
2 - lavendulan, Jáchymov. This study (NM4892)

The minute crystals are imperfect, grown on open
fractures of vein quartz, in a proximity of tennantite and
X-ray powder diffraction patterns of two lavendulan samples
NM4892Irel

dobs

26 10.370
100 9.898
4 7.879
3 7.374
6 7.165
3 5.962
4 5.763
6 4.950

dcalc h k

J-263

NM4892

l

Irel

dobs

dcalc h k

9.821 1 0 0
7.936 1 3 0

100
0.3

9.859
7.668

9.817 1 0 0
7.933 1 3 0

7.098 0 4 1

0.6

7.123

7.105 0 4 1

1.6
3.2
0.5
0.2

4.928
4.896
4.481
4.170

4.909 2 0 04.480 0 4 2
4.188 2 3 1

0.1
0.4

3.529
3.354

3.526 1 7 2
3.366 0 12 05.773 0 7 04.949 0 1 2

3

4.512

4.506 0 8 1

2
2
3
14
3

3.798
3.508
3.374
3.355
3.347

3.780 1 9 1
3.502 2 7 1
3.368 0 12 0
3.338 1 8 2

l

J-263

Irel

dobs

dcalc

h k

l

3
3
2
7
2

3.024
2.978
2.918
2.872
2.778

3.031
2.978
2.903
2.876
2.777

3 3
2 10
3 5
2 8
0 8

1
1
1
2
3

2
2
2
3

2.680
2.656
2.622
2.536

2.682
2.656
2.627
2.535

3 3
2 4
2 13
3 6

2
3
0
2

1 2.4702 2.4700 3 7 2
3 2.2428 2.2414 3 5 3

dobs

dcalc

h k

0.9 2.980

2.978

2 10 1

1.1 2.749
0.8 2.721

2.751
2.713

2 1 3
3 2 2

Irel

l

0.4 2.560 2.556 3 9 1
0.3 2.509 2.5137 1 15 1
0.7 2.4428 2.4432 3 11 0
0.1 1.9609 1.9612 5 1 0
0.3 1.9172 1.9180 5 2 1
0.3 1.8213 1.8215 2 4 5

Journal of the Czech Geological Society, 42/4 (1997)

5
2

3.180
3.065

3.181 3 3 0
3.066 1 3 3

2.9
0.5
2.2

3.259
3.185
3.102

29

3.262 3 1 0
3.184 1 12 0
3.101 3 1 1

0.3 1.7669 1.7660 1 21 2
0.5 1.6265 1.6262 2 22 2
0.3 1.5511

mineral is biaxial, positive, with indices of refraction nD= 1.497, nE = 1.502, nJ = 1.539, 2V = 40°.
Thermogravimetric analysis of liebigite is discussedby ýejka et al. [4] (see table below). Mereiter [29] presented structure analysis using liebigite single crystal
from Jáchymov.
Several published liebigite chemical analyses are included in table below:
1

Lavendulan aggregate of thin tabular orthorhombic crystals. Magnification 300

Libethenite Cu2(PO4)(OH)
It forms rare thin coatings of small needle crystals ofgreen colour. Libethenite occurs on fractures of the Geister vein.
EDX, WDX

major elements:
Cu, P

minor elements:

Liebigite Ca2[(UO2)(CO3)3] . 11 H2O
It was first found in Jáchymov in 1853 and described by
Vogl [60]. The specimens originated from the Fluthervein, the Eliáš mine at a depth of 150 to 170 m undersurface. Liebigite was accompanied by voglite, uraniumores, fluorite, dolomite, clay, and a decomposed schist.
However, the first mention of this mineral is in 1848 by
J. L. Smith [218], who also introduced the name liebigite.
The mineral forms thin crystalline crusts or equant toshort prismatic crystals, usually tenths of a mm long,rarely up to 5 mm long. The colour is green yellow, yellow green to apple green, always bright to fluorescent (inday-light). The crusts are clouded but crystals are translucent, with a glassy lustre. In ultraviolet light, it shines
an intense grey green.
Liebigite is typically coating uraninite set in carbonate gangue with minor pyrite and chalcopyrite, together
with schröckingerite and zellerite. Occasionally, liebigite
impregnates schröckingerite aggregates, which are thendevoid of the characteristic silky lustre and the aggregates are similar to andersonite. The continuos coating ofliebigite on uraninite is absent over sulphides (mainly
pyrite), where limonite occurs instead of liebigite. The
sulphuric acid released by decomposition of sulphides
prevents formation of uranyl-carbonates.
Copper can substitute for a part of Ca owing to similarity of the ion radii. Members of the continuous substitution series between Ca and Cu end-members weresynthesised [106]. According to Kašpar [106] liebigite in
Jáchymov is unstable and transforms to schröckingerite.
No support for this statement was found in the present
study.
Frondel et al. [23] gave X-ray powder pattern ofJáchymov liebigite. Following Evans et al. [160], the

2

3

4

CaO
15.56
16.42
16.28
15.40
FeO
2.48
37.11
36.29
35.45
39.27
UO3
23.87
22.95
23.13
18.13
CO2
23.35
23.72
22.44
27.21
H2O
Sum
99.89
99.38
99.78
100.001 - liebigite, Jáchymov. Vogl [59]2 - liebigite, Jáchymov. Schrauf [208]3 - liebigite, Jáchymov. von Foullon in Brezina [55]
4 - liebigite, theoretical values

Liebigite was also recorded in old uranium workings,
including the Hieronymus vein [60] and in Dürrnberger
and Johann Bock adits [55].
Lattice par. [Å] 1 a = 16.71
b = 17.55
c = 13.79
3 a=16.699(3) b=17.557(3) c=13.697(3)EDX, WDX
major elements:
minor elements:
U, Ca, C as (CO3)2Cu, Sr, FeIR
5 520, 685, 738, 841, 888, 902, 932, 1020,
1069, 1110, 1378, 1538, 1590, 1630,[cm-1]
3450, 3570
Therm. analysis 2 50-150 22.75 (9.2 H2O), 150-300 2.22
(0.9 H2O), 300-510 14.28 (2.3 CO2),[°C, wt. %]510-650 3.07 (0.5 CO2), 650-720 2.43
(0.5 CO2), 720-900 0.27
endothermic reaction: 105, 480
Hardness
4 2.5 - 3
-3
Density [g.cm ] 1 Dm = 2.41, Dx = 2.43
3 Dx = 2.41
References
4, 14, 27, 29, 55, 56, 59, 60, 106, 160,
208, 218
1 - liebigite, Jáchymov. Evans et al. [160]
2 - liebigite, Jáchymov. ýejka et al. [4]3 - liebigite, Jáchymov. Mereiter [29]4 - liebigite, Jáchymov. Vogel [60], Schrauf [208]5 - liebigite, Jáchymov. ýejka et al. [14]Lindackerite (Cu, Co)5(AsO4)2(AsO3OH)2 . 10 H2OThis rare mineral was described in 1853 for the first timeby Vogl [60] in specimens from old workings on theGeister and Eliáš veins, mine Eliáš. Lindackerite witherythrite, annabergite, pitticite, and ganomatit coated Ni,
Co, Bi, Pb, and Cu complex ores. It was named by Haidinger [118] to honour the pharmacist Josef Lindacker,
who did the first analysis of this species [161].
The chemical analyses given in [60] and results ofthe present study suggest that the older descriptions of30

Journal of the Czech Geological Society, 42/4 (1997)

lindackerite ([60], [25]) are based on mixture of two
mineral phases: lindackerite proper and another phase,
which we provisionally denote "pseudo-lindackerite"
Lindackerite occurs as inconspicuous crystalline
crusts or aggregates composed of fine, lustrous crystals.
The crystals are up to 2 mm long, lath-shaped, showing
an orthorhombic habit and a single set of perfect cleavage. Radiating aggregates of the crystals are common. A
typical feature of the crusts is their similarity in appearance to those of gypsum. Unlike other associated Cu
arsenates, lindackerite is always transparent.
Formation of lindackerite is strongly dependent on
acidity, influenced by the primary minerals (tennantite,chalcopyrite, bornite, and others) and their chemical
stability. At very low pH values, lindackerite withoutlavendulan forms on grains of primary minerals. Moreoften, it forms an aggregate deposited centrally on older
lavendulan. Lindackerite occurs in crystalline or glassy
crusts and no powdery aggregates were observed.
Lindackerite occurs in assemblage with light apple
green "pseudo-lindackerite", geminite, lavendulan,strashimirite, olivenite, and pink köttigite. It appears
among the early decomposition products of tennantite or
chalcopyrite in the environment of strongly acid, mobileions [AsO3OH]2-. This mineral was found on the Geister
and Geschieber veins.
Until present, definition of lindackerite was subjected
to major modifications because of both rarity of thismineral (including Jáchymov) and its intergrowths with“pseudo-lindackerite”. Vogl [60] published the following
analysis: CuO 36.34, NiO 16.15, As2O5 25.58, FeO 2.90,
SO3 6.44, H2O 9.32, Total 99.73 wt. %, resulting in theformula:Cu6Ni3(AsO4)4(SO4)(OH)4 . 5 H2O
Guillemin [25] presented analyses of lindackerite
from 8 specimens from Jáchymov. Lindackerite is given
as monoclinic (table below), Z = 1, non-pleochroic, biaxial, optically positive, 2V = 68q, indices of refraction nD= 1.627, nE = 1.659, nJ = 1.729.
According to Larsen [162], the optical character ofthe mineral is the same, nD = 1.629, nE = 1.662, nJ =1.727, Y=b, extinction angle between X and the directionof elongation = 26°.
Guillemin [25] also stated that the mineral contains
also Ni, minor Co, while SO3 is always absent. Two fullquantitative analyses were given by Guillemin [25]. For
the first one (original specimen number: nq5): CuO 34.5,
CoO 2.3, NiO 1.5, As2O3 44.4, Fe2O3 0.2, H2O 16.9,

Total 99.8 wt. %, was calculated to: 2(As2O3), 5.04(CuO,
CoO, NiO), 9.74 H2O, simplified to:(Cu,Co,Ni)5H2(AsO4)4 . 9 H2O
On the basis of the present study, the following recalculation of the analysis is proposed:(Cu,Co,Ni)5.04(AsO4)2.08(AsO3OH)1.92 . 9 H2O.
The second complete analysis by Guillemin [25](specimen nq7): CuO 39.0, CaO 0.5, Fe2O3 0.3, As2O5
43.7, H2O 16.2, Total 99.7 wt. %, corresponds to material
free of Co and Ni. The following simplified formula wasproposed:
Cu5H2(AsO4)4 . 8 H2OHowever, the second analysis can be alternatively
calculated (based on 16 O):
Cu5.17(AsO4)2.34(AsO3OH)1.60 . 8.67 H2O
In conclusion of his study, Guillemin gives the following formula for lindackerite:
Cu5H2(AsO4)4 . 8 - 9 H2O
As a result of the present study, the following formula is preferred:
Cu5(AsO4)2(AsO3OH)2 . 9 H2O
The monoclinic cell suggested by Guillemin [25] appears as unrealistic, because it is not compatible with thestrongest reflections measured in the powder patterns.
Compatibility coefficients [153], [154] were calculated
from the analyses given by Guillemin. For the specimen
nq5 Compat. = 0.050 (good), for the specimen nq7 Compat. = 0.080 (fair poor), which shows that some measurements are not sufficiently accurate. It is suggested
that for the specimen nq7, density value is inaccurate.
The X-ray powder diffraction patterns obtained inthis study show some differences from data of Guillemin[25], including absence of some reflections or differences in reflection intensity. It is noted that in 1956 only
the Debye-Scherrer camera was available. In view of theexcellent cleavage of the mineral, resulting in preferredorientation of sample used in powder diffractometermeasurement, it is concluded that the measurements
were done on the same species.

X-ray powder diffraction pattern of lindackerite from Jáchymov (sample J-268).
Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

100
7
1
2
4
2
2
1
1
2
3
7
3

10.139
7.954
6.727
6.097
5.131
5.071
4.951
4.476
4.413
4.268
4.171
3.984
3.794

10.174
8.019
6.456
6.152
5.158
5.087
4.967
4.522
4.395
4.305
4.172
3.990
3.795

0
1
1
-1
1
0
1
-1
1
1
1
1
2

1
0
1
1
0
2
1
1
2
-1
1
2
1

0
0
0
0
1
0
1
1
0
1
-1
1
0

10
2
2
7
4
1
1
11
1
4
1
4
1

3.237
3.156
3.088
3.052
2.910
2.860
2.790
2.666
2.640
2.609
2.569
2.535
2.507

3.236
3.162
3.095
3.056
2.915
2.869
2.790
2.664
2.642
2.612
2.579
2.532
2.500

0
0
1
1
-1
-1
0
1
1
2
2
3
1

3
0
3
1
3
0
-3
1
3
1
0
0
3

1
2
1
2
1
2
1
-2
-1
2
2
1
2

1
2
2
1
<1
1
1
2
1
1
2
1
1

2.29982.26422.21002.16582.13962.12562.05562.03232.00151.98001.9464
1.9213
1.89822.2986
2 .2608
2 .2132
2.16692.13692.1216
2 .05402.03482 .0020
1 .9792
1 .9474
1 .9230
1.8982

2
-2
2
3
1
3
-1
0
-1
-3
-1
3
2

3
2
4
-2
-4
0
4
5
0
3
5
-3
-3

-1
2
1
1
1
2
2
0
3
1
1
1
2

Journal of the Czech Geological Society, 42/4 (1997)

11
1
7
3

3.637
3.492
3.387
3.341

3.661
3.508
3.391
3.340

0
2
0
1

-2
0
3
-2

1
1
0
1

31

2
1
1
2

2.48362.47102.41882.3794

2 .4833
2.45992.41882.3809Sharp at al. [279] re-defined lindackerite as an analogue of geigerite (Mn-member) and chudobaite (Mg,
Zn), with the following composition: CoO 1.24, CuO
36.47, NiO 0.50, As2O5 43.71, H2O (18.08), Total 100.00
wt. %, corresponding to:

2
4
3
2

2
0
1
1

1
1
1
1

1.8434
1.77991.7644
1.5497

1 .8428
1.78001.76481.5483

-2
-2
-3
3

4
2
4
-2

2
3
1
3

c = 6.277

Magnesium-zippeite often occurs in powdery coatings or
as earthy aggregates, in mixture with other uranium sulphates, which include several types of zippeite (Na, K,
Fe, Ni, Mn) with various cations, "pseudo-zippeite(Mg)", uranopilite, jáchymovite, and other phases. Magnesium-zippeite aggregates show variety of habits, including earthy, granular/crystalline, and soft or hardened
intense yellow to orange to red brownish yellow.
The specimens were collected in the Evangelistavein.

E = 100.30
2 a = 8.14(3) b = 10.40(3) c = 6.45(2)a = 8.649(1) b= 14.241(2) c =17.696(2)(Cu4.90Co0.18 Ni0.07)(AsO4)2.02 [(AsO3)2.03(OH)2.21] . 9.6 H2Oideally:(Cu,Co)5(AsO4)2(AsO3OH)2 . 10 H2O
Lattice par.
[Å, °]

2
1-2
3

1 a = 3.95

b = 8.02

D = 80.35(4) E = 84.25(5) J 88.36(4)3 a = 8.103(7) b=10.394(8) c = 6.474(8)EDX, WDX

D = 79.60(1) E = 85.35(2) J 86.07(1)4 a = 8.056(8) b=10.357(9) c = 6.454(5)References

E=104.111(5)major elements:
minor elements:
U, S, Mg, Fe(K)
132, 152, 161, 165, 170, 252, 260

D=79.568(7) E=85.042(7) J 86.327(7)5 a = 8.035(2) b=10.368(4) c = 6.453(5)D = 79.60(3) E = 84.83(3) J 86.17(3)major elements:
minor elements:
Cu, As(Mg)-3
Density [g.cm ] 1 Dm = 3.27(2), 3.20(3)Dm = 3.39 for Z = 1
5 Dm = 3.35(2), Dx = 3.37(1) for Z = 1
References25, 60, 118, 154, 155, 161, 163
EDX, WDX

1 - lindackerite, Jáchymov. Guillemin [25]
2 - newly calculated values from original Guillemin’s data (samplen°7) [25]
3 - newly calculated values from original Guillemin’s data (samplen°5) [25]4 - lindackerite, Jáchymov. This study (J-268)
5 - lindackerite, Jáchymov. Sarp et al. [279]Tabular crystals of lindackerite. Magnification 250

The single crystal X-ray study [279] indicated triclinic symmetry (unit cell parameters are given in tablebelow), Z = 1, P1 or P 1 , transparent, glassy, biaxial (+),
2Vmeas = 74°, 2Vcalc = 72q, indices of refraction nD =1.632(2), nE = 1.662(2), nJ = 1.725(5), r < v strong,weak pleochroism from green (J) to colorless (D = E), E/a = 21.3q on {010}, and 34.4q on {001}.
Magnesium-zippeite [Mg(UO2)2(SO4)(OH)4]2 . 3 H2O

Detail of sandwich-like aggregate of minute magnesium-zippeite
crystals. Magnification 600

Mixture of short, acute and doubly-terminated crystals of the"pseudo-zippeite (Mg)" and of magnesium-zippeite in sandwich-likeaggregates. Magnification 900

Occasionally, it forms isolated crystals and their radiating aggregates, probably favoured by lower-concentration solutions and a moderate pH gradient.
Magnesium-zippeite was described as associatedwith gypsum, uranopilite, zippeite, sodium-zippeite,
nickel-zippeite, "ferro-zippeite", "pseudo-zippeite (Mg)",

32

Journal of the Czech Geological Society, 42/4 (1997)

johannite, exceptionally jáchymovite, sklodowskite,metaschoepite.
In present study, mixtures of "pseudo-zippeite (Mg)"always with zippeites (all types) were regularly observed.
On a basis of a structure of a synthetic zinc-zippeite[152] and a chemical analogy of isostructural zippeites(Ni, Mg, Co, Zn, Mn, Cd) [132], it is possible to proposed a chemical formula for magnesium-zippeite as
follows:

sufficiently abundant carbonate (mainly dolomite) toneutralise the solutions. Calcite veins are relatively rare.
This situation results in common occurrence of arsenates, hydrogen-arsenates, or sulphates in place of carbonates.
Masuyite Pb3U8O27 . 10 H2O
Masuyite was identified as crystalline aggregates up to 1
cm2 in size, composed of yellow-orange to orange brown
minute acicular crystals. It also occurs as a substantial
component of orange-red crystalline aggregates withpoorly defined radiating pattern.
Masuyite occurs usually with other minerals of the
PbO-UO3-H2O group in a paragenesis with uranophaneand gypsum, next to partly weathered uraninite.
X-ray powder diffraction data of masuyite given in
the table below include indexing of some diffraction
missing in the original description [266]. The diffraction
data for Jáchymov masuyite are based on the sample BM
6106.

[Mg(UO2)2(SO4)(OH)4]2 . 3 H2O
See also other minerals of the zippeite group (sodium-zippeite, zippeite, nickel-zippeite, "ferro-zippeite","pseudo-zippeite (Mg)").
Malachite Cu2(CO3)(OH)2
It was found only once as small spheres composed ofmalachite and brochantite mixture, deposited on fractures of vein quartz with thin veinlets of a white carbonate. The spheres are accompanied by small brochantite
crystals and by picropharmacolite.
The rarity of malachite can be explained by composition and migration of solutions responsible for mineralization. Copper-bearing veins always contain sulphides
and sulpho-arsenides, which give rise to rather acid solutions. Vein or country rock carbonates do not contain

Lattice par.[Å]EDX, WDX
References

a= 13.847(6) b= 12.211(6) c= 14.128(8)major elements:
minor elements:
U, Pb
Si
266

X-ray powder diffraction pattern of magnesium-zippeite from Jáchymov.
Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

17
5
8
100
5
17
13
13
13
4
1
15
3
6
10
10
58
38
38
11
2
1
4
40
40
3
5

8.567
7.590
7.481
7.112
6.212
5.477
4.288
4.191
4.191
4.130
4.078
3.911
3.747
3.674
3.613
3.613
3.559
3.449
3.449
3.288
3.244
3.225
3.181
3.104
3.104
3.041
2.950

8.581

0

0

2

7.121
6.211
5.480
4.290
4.194
4.193
4.131
4.085
3.911

0
1
0
0
2
2
1
1
1

2
1
2
0
0
0
3
1
3

0
1
2
4
0
-2
-1
-4
1

19
4
3
6
6
6
22
13
6
21

2.859
2.809
2.738
2.714
2.714
2.691
2.653
2.632
2.515
2.4774

3.614
3.613
3.558
3.451
3.449
3.289

2
2
1
2
2
0

2
2
3
0
0
4

0
-2
-3
2
-4
2

2.40752.37312.28732.22932.20392.16142.14442.13172.09682.06862.05202.0432

0
1
0
2
1
2
0
1
2
2
2
3
0
0
0
3
4
0
2
4
4
0
2
2

0
3
4
4
2
0
2
5
2
4
4
3
6
6
4
3
0
0
0
0
2
2
2
2

6
-5
4
-2
-6
4
6
1
4
2
-4
-3
0
2
6
-5
-2
8
-8
-4
-2
8
6
-8

1
1
5
5
7
22
22
5
4
5
8
4
12
4
10
9
2
2
13

2.00271.99191.97591.9575
1.9546
1.9518

3
16
10
12
3
9
4
7
5
12
3
8

2.860
2.811
2.740
2.714
2.713
2.689
2.654
2.633
2.516
2.47792.47712.40872.37362.28772.22982.2013
2.16222.14522.13222.09642.06902.05402.04362.0426

1.93101.9022
1.84771.82681.78851.77981.7572
1.74391.7243
1.71631.7144
1.69452.00211.99501.9771
1.9556
1.9552
1.9522
1.95141.93041.90281.84811.8266
1.78961.7802
1.75751.74441.7253
1.7162

4
3
1
2
2
0
1
4
1
4
0
3
0
1
2
4
0

1
5
7
6
6
6
7
0
7
4
6
5
8
7
0
0
0

-5
-3
-1
2
-4
5
1
-6
-3
-2
6
3
0
-5
-10
4
10

9

1.67601
52.02782.01162.01162.0111

4
4

2
2

0
-4

<1
<1
4
2

1.66691.6592
1.6441
1.63751.69501.6943
1.67681.67591.6684
1.65791.64491.6374

2
2
4
4
0
0
3
2

2
2
2
2
2
7
7
3

8
-10
4
-8
10
6
-3
-10

3.183
3.105
3.104

0
2
2

3
2
2

4
2
-4

X-ray powder diffraction pattern of masuyite from Jáchymov (sample BM 6106).
Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

3
100
5
4
6
5

7.603
7.067
6.023
4.564
4.382
3.598

7.685
7.064
6.023
4.579
4.382
3.601

1
0
2
2
1
1

1
0
1
2
2
2

1
2
0
0
2
3

14
11
10
12
3
8

3.109
2.989
2.919
2.734
2.699
2.632

3.109
2.984
2.917
2.734
2.700
2.637

4
0
1
3
1
4

0
4
4
1
1
3

2
1
1
4
5
0

6
4
10
8
6
7

2.2592
1.98381.94791.90991.8813
1.76842.2602
1.98381.94701.9083
1.8816
1.7686

5
3
4
6
5
6

3
2
0
1
2
1

1
6
6
4
5
5

Journal of the Czech Geological Society, 42/4 (1997)

75
50
8
<1

3.530
3.440
3.256
3.140

3.532
3.462
3.265
3.146

0
4
3
2

0
0
2
0

4
0
2
4

33

<1
5
<1
10

2.35782.35782.34882.29122.36432.35472.34292.2916

3
0
5
4

1
0
1
2

5
6
3
4

5
4
7

1.71801.58031.5702

1.71801.58021.5700

1
6
8

7
5
2

dcalc

h

k

l

Irel

dobs

7
9
7
11
16
7
17
9
5
5
8
10
14
8
13
9
13
8
14
15
5
5
14
6
9
9
2
12
11
10

2.45792.43712.41342.40162.37612.29902.2706
2.25212.24072.19222.17392.14892.12982.04702.03782.02291.99671.96581.96181.95031.9304
1.9124
1.9071
1.8913
1.8832
1.82301.81351.8095
1.78661.76252.37372.30002.26852.25062.2403
2.19182.17262.15082.13012.04852.03642.02351.9953
1.9651
1.9593
1.94951.93051.91281.9066
1.89151.88291.82291.8142
1.80991.78851.7602

1
3
3

dcalc

h

k

l

2.45862.43662.4158

-5
1
1

4
-4
3

1
2
2

-3
-1
-3
1
-2
3
-6
-4
-5
5
-3
2
-2
-2
2
3
2
5
3
1
4
-3
7
7
0
2

6
1
6
-1
6
3
3
5
4
-2
7
1
7
6
4
4
-6
-5
3
5
-6
5
-4
-3
-6
3

0
3
1
3
1
1
1
2
2
2
0
3
0
2
-2
-1
2
2
2
-2
2
3
1
1
2
3

X-ray powder diffraction pattern of mcnearite from Jáchymov.
Irel

dobs

42
87
100
26
4
4
9
6
33
39
4
15
35
12
11
43
6
34
10
19
12
5
31
14
10
8
32
6
17
42

14.08912.412
12.203
11.690
7.776
7.585
7.160
7.144
7.061
6.953
6.713
6.652
6.559
6.276
6.242
6.193
6.087
5.710
5.685
5.662
5.437
5.266
5.214
5.176
5.042
4.897
4.831
4.746
4.690
4.587

dcalc

h

k

l

12.4770

1011.742

1

0

0

7.121
7.020
6.953
6.710

6.239
6.160
6.086

-1
1
0
-2

0
-1
0

2
1
0
1

2
1
-1

0
0
1
0

0
1
1

5.041
4.898
4.845

1
1
1

1
-2
1

-1
1
1

4.702
4.606

-1
-2

3
3

0
0

Irel

dobs

5
76
18
8
11
28
11
38
59
51
23
12
9
4
14
23
29
31
11
18
4
36
27
14
5
27
8
6
13
4

4.495
4.438
4.376
4.273
4.161
4.141
4.028
3.912
3.895
3.812
3.762
3.693
3.614
3.569
3.536
2.930
2.895
2.867
2.850
2.819
2.815
2.807
2.747
2.724
2.704
2.635
2.590
2.576
2.551
2.537

Mcnearite NaCa5H4(AsO4)5 . 4 H2O
It occurs as thin and soft powdery crust covering
about 1 cm thick zoned crust of gypsum and arsenate,deposited on wall rock. The full sequence of the crust is
as follows: at the base a thin, milky amorphous zone
deposited on wall rock, followed by radiating aggregatesof white picropharmacolite, zone of crystalline gypsum,
followed by milky rösslerite zone, and the topmost zoneof mcnearite - thenardite mixture. The specimens werecollected in the Geschieber vein.
The matrix to the crust studied is a partly greisenizedgranite (with kassiterite grains) collected at a site near tothe subsurface discharge of radioactive water used in the
Jáchymov spa. Sodium bound in mcnearite was possibly
supplied by the spring, while the ultimate source of Na isprobably plagioclase in the granite (Na released due toactivity of sulphuric acid).
Lattice par.
[Å, °]
EDX, WDX

References

a= 13.450(6) b=14.258(6) c = 6.963(7)D = 88.38(1) E=93.828(8) J 119.01(1)major elements:
minor elements:
As, Ca, Mg
Na
Dm = 3.35(2), Dx = 3.37(1) for Z = 1
273

Melanterite FeSO4 . 7 H2O

4.391

-3

1

0

4.159

0

3

0

3.914
3.886
3.818
3.766

3
2
1
2

0
1
2
-3

0
-1
1
1

3.621
3.577
3.534
2.929

3
0
-3
2

-2
3
3
-2

1
-1
1
2

2.851
2.820
2.812
2.810
2.748
2.724
2.707
2.637
2.591
2.577
2.553
2.538

0
-3
2
-3
1
-1
1
2
4
2
-5
1

4
1
3
5
2
5
4
3
1
3
3
4

-1
2
0
0
2
0
0
-1
0
1
1
-1

Melanterite accompanied by other sulphates forms massive crystalline crusts and hollow stalactites with imperfect skeletal crystals coating the internal free surfaces.
The colour varies from light yellow to dark greenish blue
with variation in the Fe/Mg ratio and the content ofcomplex hydroxyl-sulphates of ferric iron. The lattermay result in a red-brown colour.
It occurs often in solid solutions with other heptahydrates of Fe, Mg, and Ni in places with pyritemarcasite veins. Owing to action of acid mine waters,
containing sulphuric acid as a catalyzer, the vein fill canbe decomposed in a rather short time. Stability of melanterite (with a general formula Me2+SO4.7 H2O) is affected not only by composition of solutions and by their
pH value, because other conditions in the mine including
temperature and circulation of dry air are important.
Elevated temperatures and circulation of dry air result in
gradual dehydration of melanterite and its alteration to
powdery material.
In the sulphate heptahydrate solid solutions melanterite was identified as a marginal member associated withnickelhexahydrite, morenosite, gypsum, rozenite, epsomite, and as yet unidentified Fe-arsenates. Kratochvíl[118] described melanterite as coatings of imperfect
crystals accompanied by chalcanthite. The mineral also
occurs on mine dumps.
EDX, WDX
References

major elements:
Fe, S
118

minor elements:
Mg, Ni

34

Journal of the Czech Geological Society, 42/4 (1997)

Meta-autunite Ca(UO2)2(PO4)2 . 2-6 H2OThis mineral occurs in Jáchymov in two different associations. In the first one, it forms light yellow-green
tabular crystals with a light yellowish colour or darkgreen tabular crystals dominated by the (001) faces. It is
associated with walpurgite. Light green meta-autunite
fluoresces in ultraviolet light intense yellow green, thedark type shows only a weak fluorescence.
In the associations of the second type, meta-autunite
is often replaced by amorphous iron oxides and hydroxides. It occurs on small quartz crystals as tabular crystals
up to 1 cm long in vugs of the Geister vein.
X-ray study confirmed the mineral as U-mica related
to meta-autunite. Spectral analyses done in the past confirmed elevated iron content and absence of Ca which
led to the suggestion that the mineral is bassetite. Recent
microscopic and microprobe study of polished sections
resulted in identification of the supposed bassetite as a
mixture of meta-autunite and amorphous Fe-hydroxides,
which replaced the original U-mica. The pseudomorphs
fluoresce mottled yellow in ultraviolet light. Glassy yellow-brown spherules tens of microns in diameter, coating the pseudomorphs, correspond to corkite in composition. The second association includes churchite-(Y),fresh meta-autunite, and parsonsite.
Lattice par. [Å]EDX, WDX
Water content[wt. %]
Density [g.cm-3]
Referencesa = 6.991(3)c = 8.438(2)major elements:
minor elements:
U, P, CaFe, Sr, Ba
14.37 (dark green), 11.86 (yellow)
Dm = 3.68 (dark green), 3.45 (yellow).
(determined by pycnometer)
27

Metalodevite Zn(UO2)2(AsO4)2 . 10 H2OMetalodevite forms isolated think tabular crystals up to 7
mm in size. It has bright yellow colour and vitreous lustre. Metalodevite was found in a small vugs in quartz
vein containing bismuthinite and native bismuth. It isvery rare. It originates in the Eliáš mine.
EDX, WDX

major elements:
Zn, U, Asminor elements:
Mg

Metanováþekite Mg(UO2)2(AsO4)2 . 4-8 H2O
It was always identified in a mixture with nováþekite. It
occurs in two paragenesis. In the first one it forms small
light yellow coating on carbonate gangue carrying disseminated chalcopyrite and tennantite. Metanováþekite
formed here probably by neutralisation of acid solutions
containing uranyl-arsenate ions, while Mg was released
from carbonate. The specimens were collected in the
Evangelista vein.
The second type forms 3 mm long crystals accompanied by bismutite in vugs of quartz vein. On fresh exposure it has a strong yellow green colour and is nearlytransparent. During one day, the mineral becomes turbidand non-transparent. The specimens were collected on
dump of the Eliáš mine.
Lattice par. [Å]EDX, WDX

a= 7.166(5)major elements:
Mg, U, As

c= 8.598(8)minor elements:

Metaschoepite UO3 . n H2O, n < 2
Metaschoepite occurs as yellow soft earthy aggregates.
Similar to other hydrated uranyl-oxide-hydroxides, it
is rather unstable [6], which results in limited data on its
properties. The new X-ray powder diffraction data formetaschoepite from Jáchymov (see table bellow) correspond to the phase Na2(UO2)6(OH)14 . 4 H2O describedby Brindley et al. [205].

X-ray powder diffraction patterns of metaschoepite from Jáchymov.
Jáchymov
Irel

dobs

18
4
4
100
4
8

9.561
8.827
2
8.388
1
7.367 100
7.142
6.495
1
2
1
5.388 <1
5.058
2
4.982
4.879
1
4.790
4.750
4.460
5
4.341 <1
<1
4.199
1
1
1

3
6
4
5
3
4
10
3
3

Irel

1)

Jáchymov

dobs

Irel

8.644
8.325
7.327
6.440
6.060
5.510
5.360
5.040

2
11
5
68
42
3
7
3
6
7

dobs
3.440
3.350
3.317
3.231
3.172
3.050
2.974
2.889
2.833
2.756

4.870

4.450
4.330
4.290
4.174
4.010
3.830

30
6
16

2.569
2.553
2.539

12
3
8

2.44672.42322.32041)

Jáchymov

1)

Jáchymov

1)

Irel

dobs

Irel

dobs

Irel

dobs

Irel

dobs

Irel

dobs

10

3.480

1.70881.6750

2.960
2.890
2.830
2.730
2.670
2.630
2.590
2.560

2.17712.15282.11842.08632.06612.03422.01952.00722.0038

8
5

1
4
3
2
<1
1
1
15

<1
3
1
2
3
7
5
2
4

1.7456

3.330
3.310
3.220
3.160

2.16102.13792.12372.09232.05762.04422.02232.01152.0074
1.99451.9865
1.9692
1.9534

16

2
1
50
25

10
4
3
17
5
26
15
18
9
4
6
25
3

1

1.9888103
111.6333
1.62701.613991.95991.90301.91941.90301.8951
1.8775
1.8496
1.83481.81401.5863
1.5682
1.5625

4

1
1
1
1
<1
2
2

8
4
1
4
2

1.52271.5128

2
3
1
1
2
1
1
1
2
2
2
3
1
2
2
1
1
1
1
<1
<1

1.74741.7412
1.72631.72081.69981.68191.66811.65591.63261.62501.61371.60981.58691.57741.5644
1.54141.53071.51851.51091.49511.4837

8
1
2
1
1

2.530
2.46002.45002.42002.38329

1.8168

Journal of the Czech Geological Society, 42/4 (1997)45
3.674 253.670
623.598 40
3.580
7
3.560
5
3.560
38
3.518 20
3.490
1 - metaschoepite. Debets et al. [87]

3
5
5
6

2.27102.26292.23312.2132

35

2
2
2
1

2.30682.26742.22592.2010The mineral does not fluoresce in ultraviolet light.
Metaschoepite was observed with gypsum, uranopilite, zippeite, sodium-zippeite, magnesium-zippeite,"ferro-zippeite", sklodowskite and, "pseudo-zippeite(Mg)" on specimens from the Evangelista vein.
EDX, WDX
References

major elements:
U, S
6, 87, 205

minor elements:

Detailed image of metaschoepite earthy aggregate. Magnification 700

Metatorbernite Cu(UO2)2(PO4)2 . 8 H2OMetatorbernite crystals up to 5 mm long or fine-grained
scaly aggregates occur as coatings. The light green crystals are tabular on (001) and often compose radiating
aggregates. The mineral with glassy lustre is translucent
to transparent and very brittle.
It is a common secondary mineral in Jáchymov.
Powdered torbernite kept in a dry place dehydrates tometatorbernite. A single crystal of uranium mica, 5 mm
long, was identified as a mixture of torbernite and minor
metatorbernite 20 years after collecting. Only metatorbernite was present in a subsample studied three weeks
after it was powdered. However, some metatorbernite
formed as a primary phase.
It is relatively common on all veins carrying uranium
minerals. Metatorbernite is accompanied by torbernite,
zeunerite, metazeunerite, tyuyamunite, churchite-(Y),and parsonsite on specimens from the Geister vein.
Lattice par. [Å] 1 a = 6.978(3)c = 17.37(1)2 a = 6.982(1)c= 17.356(5)EDX, WDX
major elements:
minor elements:
U, P, CuIR
3 258,295,405,465,550,615,680,800,845,
910,930,990,1100,1645,2930,3350[cm-1]
References

15, 27, 75, 84

1, 2 - metatorbernite, Jáchymov. This study
3 - metatorbernite, Jáchymov. ýejka et al. [15] (NM 26719)

Metatyuyamunite Ca(UO2)2(VO4)2 . 3 H2O

12
16
7

1.7974
1.78541.756612
7
11.80891.7925
1.77891.75664

1.4486<1<1<1
11.47881.47281.45691.4466

Metatyuyamunite occurs as a strong yellow powdery
coating on fractures in the vein or in wall rock close to
the vein. It does not fluoresce in UV light. It is associated with green zeunerite, gypsum and pink köttigite.
The primary minerals in this vein are tennantite, pyrite
and uraninite. Specimens studied were collected in theGeister vein.
Meta-uranopilite (UO2)6(SO4)(OH)10 . 5 H2O
Meta-uranopilite was first described on specimens from
Jáchymov in 1935 by Nováþek [35] under the name uranopilite; the name meta-uranopilite was introduced byNováþek in 1941 [35].
Kašpar [106] described meta-uranopilite as a grey
green to brownish mineral, which contrasts with brightyellow uranopilite. Meta-uranopilite was described on asingle specimen No. NM 17365 from the National Museum in Prague [35]. Though a specimen with this number was located during the present revision study, it isdesignated bismutosferit and notably differs from thedescription given by Nováþek. Vandendriesscheite, compreignacite, uranophane, and kasolite were identified by
X-ray and chemical analysis of this specimen i.e., nophase containing sulphur was observed. A re-numberingof specimens is considered as a probable reason of thisdisagreement. Another specimen No. NM 24272, designated as E-uranopilite, carries yellow acicular crystals
containing U, Si, and Ca and corresponding to a mixtureof uranophane and minor schoepite, determined by X-ray
analysis. Negative results from search for type material
in the collection were also reported by ýejka et al. [6].
The type specimen of meta-uranopilite was never studied
by X-ray methods and Nováþek [196] stated that there
was insufficient material for additional work.
Based on a thermogravimetric analysis of uranopilite,Nováþek [196] assumed that meta-uranopilite forms bydehydration of uranopilite at 60 to 70 °C. In the courseof the present study, uranopilite was heated to 60, 80,
100, 150, and 200 qC, and kept in each step for 30 minutes under respective temperature. The dehydrated samples were studied by X-ray (figure below) with the resultthat uranopilite transforms to an amorphous phase during
quick dehydration.

36

Journal of the Czech Geological Society, 42/4 (1997)

Results of this experiment correspond to a spontaneous re-hydration under room temperature of uranopilite
dried at 150 °C, described by Frondel [174]. The single
chemical analysis reported by Nováþek [35] yielded:
UO3 82.40, Fe2O3 2.03, (CaO not determined), SO3 4.17,
H2O 9.40, Total 98.00 wt. %, which he interpreted to theformula:6UO3 . SO3 . 10 H2O
The indices of refraction nD = 1.72, nE = 1.76, nJ =1.76 given by Nováþek [35] are significantly higher than
indices for uranopilite. The mineral is weakly pleochroic,
optically negative, it has extinction parallel with elongation (// Y) and the obtuse bisectrice (Y) coincides withthe large faces of lath-shaped crystals - (010).
The colour is grey-yellow with a brownish shade; itshows a very weak fluorescence in ultraviolet light.
References

6, 35, 106, 196

Meta-uranospinite Ca(UO2)2(AsO4)2 . 8H2O
Meta-uranospinite (17Å) forms a thin, firm and finely
crystalline crust with distinct crystal faces on its surface.
It also tends to occur as indistinct botryoidal aggregates.
It is whitish grey to light yellow and shows a glassy lustre. Meta-uranospinite is associated with yellow coatingsof zellerite and minor liebigite and schröckingerite. It
was identified in specimen collected in 1869 or 1870 anddeposited in the Landesmuseum Joaneum in Graz, Austria.
Meta-uranospinite (18Å) occurs as distinctly crystalline crust composed of flat crystals constituting an isolated convex rib. It is light yellow in colour. The associated schröckingerite crystallised in exceptionally coarse
flakes. The minerals are deposited on uraninite-carbonate
vein.
Meta-uranospinite (17Å) fluoresces a low-intensity
yellowish white in UV light, while meta-uranospinite(18Å) fluoresces a greenish yellow white of a moderateintensity.
The calculated unit cell parameters and the X-ray
powder diffraction pattern of meta-uranospinite (18Å)
from Jáchymov (specimen VS-12698a) show a very
good agreement with abernathyite (ICDD PDF2-[275])(unlike meta-uranospinite [275]), but the chemical composition excludes this possibility. The mineral studied
probably represents a member of the meta-uranospinite trögerite series.
Lattice par. [Å] 1 a = 7.180(2)2 a = 7.155(4)EDX, WDX
major elements:
U, As, Ca
References
263, 264, 275

c= 18.116(5)c = 17.27(7)minor elements:
Mg, Si1 - sample VS-12698a (white-yellowish crust like schröckingerite,with nováþekite)2 - sample JG-13142 (white-grey-yellowish crust on uraninite, withuranospinite)

Metavoltine K2Na6Fe2+Fe63+(SO4)12O2 . 18 H2OMetavoltine always occurs in a mixture with copiapite as
olive yellow, small, fine-grained earthy aggregates up to
0.5 mm long. They are deposited on radiating aggregatesof halotrichite or sometimes directly on pyrite. The aggregates occur in porous vein quartz with pyrite andproustite, in paragenesis with halotrichite, alunogen andmelanterite. The specimens were collected in the
Geschieber vein.

Journal of the Czech Geological Society, 42/4 (1997)

Metazellerite Ca[(UO2)(CO3)2(H2O)2] . H2OMetazellerite ranks among rare minerals in Jáchymov.
Hloušek [27] gave the first description of its occurrence.
The mineral forms buff yellow botryoidal aggregates andearthy coatings, which fluoresce intense yellow in ultraviolet light. Its appearance is similar to that of uranium
sulphates, in particular zippeite. Metazellerite is associated with zellerite, schröckingerite, liebigite and rabbitite.
Lattice par. [Å] 1 a = 9.65(5) b=18.40(10) c = 5.03(3)2 a = 9.73(2) b= 18.25(3) c = 4.90(3)EDX, WDX
major elements:
minor elements:
U, Ca, C
Mg, FeReferences
27, 96
1 - Metazellerite. This study, sample J-384 (Bratrství mine)
2 - Metazellerite. This study, sample 26J (Svornost mine, Daniel level,
Evangelista vein)37

It was always observed as intergrown with zellerite.
Zeunerite, torbernite, metatorbernite, tyuyamunite, andhidalgoite are associated with metazeunerite. It is a relatively abundant mineral observed in all mines with veinsof uranium minerals. The majority of specimens in collections come from the Rovnost mine where it was lesscommon than zeunerite.
Lattice par. [Å]EDX, WDX
Referencesa = 7.113(1)major elements:
U, As, Cu
238

c= 17.433(3)minor elements:

Mimetite Pb5(AsO4)3Cl
The single occurrence of mimetite was in the form ofyellow-white powdery aggregates filling vugs in porous
quartz gangue in the Geister vein. It was associated withzeunerite, metazeunerite, and bayldonite.

Metazeunerite Cu(UO2)2(AsO4)2 . 8 H2O
It occurs as coatings of thick tabular to equant crystals
on fractures of the vein fill. The crystals up to 3 mm long
are transparent, of a strong green or grey-green colour,
and a strong lustre.
Metazeunerite forms by a slow dehydration of zeunerite at the room temperature and normal humidity. The
alteration can take place in mine if appropriate conditions prevailed.

Lattice par. [Å]EDX, WDX
IR[cm-1]
References

a =10.233(4)c = 7.432(5)major elements:
minor elements:
As, Pb, P
430,475,550,575,790,825,980,1025
27, 9038

Mixite BiCu6(AsO4)3(OH)6 . 3 H2OJáchymov is the type locality for this mineral. It was firstfound on the sixth level of the Geister vein by Anton
Mixa in 1880 and described by Schrauf [136], who
named the mineral after its discoverer.
Schrauf [136] described mixite as bluish or emerald
green coating and aggregates composed of fine acicular
crystals, which are showing six faces in the prismaticzone and extinction under an angle of up to 6-9q. Sejkora[193] described several morphological types of mixite.
The first type is dark green coating up to 1 mm thick andwith botryoidal surface, similar to cornubite, on quartznative bismuth veins. The second type represents isolated light green acicular crystals associated with bismutoferrite, bismutite, walpurgite, and eulytite. The third
type includes aggregates up to 1 cm across, composed ofvery fine acicular crystals, accompanied by bismutoferrite on vein quartz. Mixite of the fourth type is in pearly
lustrous aggregates of microscopic acicular crystals. All
the types described in [193] are from the sixth level ofthe Geister vein in the Rovnost mine.
Sejkora [193] gave two quantitative mixite analyses:
Bi2O3 20.76 (20.78), SiO2 0.55 (0.55), As2O3 23.54(25.03), P2O5 4.36 (3.60), CuO 42.11 (43.05), CaO 0.79
(0.75), H2O 8.56 (8.71), Total 100.67 (102.47) wt. %.
Recalculation of the first analysis on the basis of 18 oxygen atoms gives the following formula:

Journal of the Czech Geological Society, 42/4 (1997)

koritnigite and is accompanied by pink köttigite andpicropharmacolite. The secondary minerals crystallisedon fractured quartz-carbonate gangue.
Moorhouseite formed by spontaneous dehydration ofbieberite.
It was identified on samples from the Geschieber andEvangelista veins.
Lattice par.
[Å, °]

a =10.034(1) b = 7.226(1) c=24.277(4)E=98.356(2)major elements:
minor elements:
Co, S
Ni
275

EDX, WDX
References

Morenosite NiSO4 . 7 H2OMorenosite was described by Ulrich [195] as efflorescence composed of light blue-green fibrous aggregates
and acicular crystals coating ore minerals. Indices ofrefraction are according to Ulrich [195] nearly identicalto those given for natural morenosite by Topsoe andChristiansen [in 195]: nD = 1.4669, nE= 1.4888, nJ =1.4921. The mineral has a stringent taste [195].
EDX, WDX

major elements:
Ni, S
195

Referencesminor elements:
Fe

Bi0.99(Cu5.88Ca0.16)6.04[(AsO4)2.28(PO4)0.68(SiO4)0.10]3.05(OH)5.76 . 2.4 H2O

The deficiency in molecular H2O is possibly due toinaccuracy of the analysis.
In the present restudy, mixite was observed in association with bayldonite, zeunerite, metazeunerite, torbernite, metatorbernite, and parsonsite.
Lattice par. [Å] 1 a =13.608(5)c = 5.904(6)EDX, WDX
major elements:
minor elements:
Bi, Cu, AsP
Hardness
2 3-4
Density [g.cm-3] 2 Dm = 2.66
IR284,384,428,473,535,802,842,1001,
1082,1624,3340,3490[cm-1]
References
118, 121, 136, 143, 193
1 - mixite, Jáchymov, Sejkora [193]2 - mixite, Jáchymov, Schrauf [137]Monohydrocalcite CaCO3 . H2O
It forms minute spheres with smooth surface, grey-whitein colour. The mineral occurred exclusively with talmessite, also accompanied by picropharmacolite, köttigite,
annabergite, and gypsum. It was identified only on several specimens of coarse-grained carbonate vein withisolated skutterudite grains from the Josef vein.
Moorhouseite (Co,Ni, Mn)SO4 . 6 H2O
Moorhouseite forms pseudomorphs after minute skeletaland orthorhombic tabular crystals of bieberite. It has abuff pink colour and a weak glassy lustre. It overgrows

Mottramite PbCu(VO4)(OH)
Mottramite forms small spheres deposited on limonitecoated fractures in vein quartz. The spheres tend to coalesce to continuous crusts up to 0.5 mm thick or curtainlike aggregates. Its colour varies from light yellow-green
to black-green.
Lattice par. [Å] 1
2
3
EDX, WDX
1

Referencesa = 7.65(1) b = 9.25(1) c = 6.03(1)a = 7.545(4) b = 9.550(8) c = 5.927(6)a = 7.50(1) b = 9.66(4) c = 5.91(2)major elements:
minor elements:
Pb, Cu, V
Ca, As2
Pb, Cu, As
V, Ca, P
3
Pb, Cu, V
Ca, As156, 157

1 - mottramite, Jáchymov. This study, (black-green)
2 - mottramite, Jáchymov. This study, (light yellow-green sample)
3 - mottramite, Jáchymov. This study, (dark-green)

Mottramite from Jáchymov represents a member of ahypothetical mottramite-duftite compositional series. Differences in crystal structure between mottramite andduftite indicate that additional study is needed.
The lattice parameters for the specimen 1 (table
above) are similar to those of mottramite [157]. The
specimens 2 and 3 correspond to Ca-mottramite [156].
The X-ray powder diffraction data for mottramite from
Jáchymov show some significant differences for somediffractions, compared to published data for mottramite.

Journal of the Czech Geological Society, 42/4 (1997)

39

X-ray powder diffraction patterns of mottramite from Jáchymov.
1
h

k

l

0

1

1

0
1
1
2

2
1
2
0

0
1
0
0

2
1

1
2

0
1

2

0

1

2

2

0

1
2
1

3
2
1

0
1
2

Irel

dobs

31

8.773

40
6

2

3

dcalc

Irel

dobs

5.044
4.785

5.042

21
8
51

8.716
6.730
5.009

5.044

38

4.206

4.193

5
6
15
14
23
42
66

3.792
3.567
3.518
3.341
3.253
3.202
3.188

3.776

6
44
10
5

4.650
4.191
3.971
3.834

4.620
4.214
3.957
3.834

3.511
3.336

16
22

3.541
3.343

3.186

37
53
15
100
34
15
19

2.964
2.934
2.871
2.651
2.627
2.588
2.515

2.969
2.931

100
21
54

3.224
3.182
2.969

48
88

2.870
2.651

2.858
2.649

35
20
5

2.586
2.505
2.46382.522
2.463329

2.27922.279811
72.25252.21582.2363
2.2116916

2.09292.06762.072616
51.8715
1.78781.8695
1.77812328
7
8

1.7654
1.6412
1.61081.5426

2.650
2.654

0 2 2
2.521
3 1 0
2 3 0
6 2.4389 2.4325
3 0 1
3 1 1
2 1 2
34 2.2654 2.2672
3 2 0
1 4 0
5 2.2260
1 4 1
7 2.1221 2.1240
3 2 1
21 2.0824 2.0847
1 3 2
3 1 2
5 1.8882 1.8824
3 3 1
27 1.8725 1.8731
2 0 3
3 2 2
4 1 1
14 1.7652 1.7681
1 3 3
32 1.6404
4 0 2
11 1.5901
0 6 0
1 - mottramite, Jáchymov. This study, (black-green)
2 - mottramite, Jáchymov. This study, (light yellow-green sample)
3 - mottramite, Jáchymov. This study, (dark green)

dcalc

Irel

dobs

100

8.782

31
9

5.046
4.807

5.038

25

4.209

4.181

8

3.707

3.747

3.541

10
44
25

3.526
3.360
3.232

3.489
3.334

3.234

51

3.189

3.167

2.950

21
29
10
52
10
8
8

2.973
2.940
2.878
2.654
2.628
2.594
2.518

2.962
2.936

5

2.28592.301816

2.26482.258292.08402.074412

1.87591.866875121.77011.75251.64241.77371.75601.6424
1.61691.5398

dcalc

2.641
2.647
2.519

in porous vein quartz. Mrázekite is younger than pyromorphite as it is implanted on pyromorphite needles andolder than pseudomalachite, which covers mrázekite.
Small spheres of eulytite tend to be associated withmrázekite and they show a similar size.

Botryoidal crust of the light-coloured type of mottramite. Magnification 700

Mrázekite Bi2Cu3(PO4)2O2(OH)2 . 2 H2OMrázekite forms thin coating on fractures or small isolated spheres up to 0.1 mm in diameter, deposited incavities. The coatings are light blue, spheres are strong
blue. It occurs with native Bi and secondary Bi minerals

Crystalline aggregates of mrázekite. Magnification 250

40

Journal of the Czech Geological Society, 42/4 (1997)

Mrázekite is also associated with torbernite which isdeposited on pseudomalachite, and preisingerite, bismutite and petitjeanite, constituting pseudomorphs after
native Bi. The specimen studied was collected in theGeister vein.
EDX, WDX
References

major elements:
Bi, Cu, P
176

minor elements:
Fe, Si, Ca

Namibite Cu(BiO)2(VO4)(OH)
It is a light to dark green mineral forming coatings andminute acicular crystals enclosed in beyerite or overgrowing beyerite. Spheroidal aggregates of acicular crystals, 0.3 mm long in maximum, are deposited on quartz.
Rarely, namibite accompanies spheroidal aggregates orindividual crystals of eulytite. It occurs in vuggy, fractured, fine-grained quartz with disseminated native bismuth. Also associated with namibite are beyerite, eulytite, bismutite, and rare tabular crystals of pucherite.
Namibite was found on dumps of the Eliáš mine, inveinlets along gneiss-quartz porphyry contacts. All analytical data in table below are from Mrázek et al. [32].
Namibite is biaxial, with extremely high indices of refraction (n > 2.2); the median refraction index calculated
following [153, 154] is 2.7. Chemical analysis: CuO
12.03, Bi2O3 72.24, V2O5 13.77, H2O 1.51 Total 99.55
wt. %, can be recalculated on the basis of 7 (O,OH) to
the following formula:
Cu0.98(BiO)2.01(VO4)0.98(OH)1.03 . 0.03 H2O
Lattice par.
[Å, °]
EDX, WDX
IR[cm-1]
Therm. analysis[°C], [wt. %]Density [g.cm-3]
References

a= 11.877(2) b = 3.702(1) c = 7.497(1)E=109.76(1)major elements:
minor elements:
U, Ca
Cu, Sr, Fe
230,330,360,430,480,510,552,630,736,
850,1030,1630,3400
430 - 490, 1.5 (dehydoxylation), 810 880, 0.6 (release of oxygen)endothermic reaction: 463, 796
Dx = 6.91 for Z=2
all data after Mrázek et al. [32], 153, 154

It occurs as transparent to white, compact or fine-grained
crusts up to 2 mm thick in patches 15 by 5 mm in maximum size. The crusts are deposited on altered rock together with dusty aggregates of bright-yellow sodiumzippeite. It fluoresces in intense yellow green to green in
short-wave ultraviolet light. Neshquehonite, identified
by Sejkora [203], was very rare on several specimensfrom the Geschieber vein at the fifth level of the Svornost mine.
Lattice par.
[Å, °]

1 a = 12.12(1) b = 5.365(4) c = 7.701(4)E = 90.58(1)EDX, WDX
1 major elements:
minor elements:
Mg
Ca, Si, Pb a S
Density [g.cm-3] 1 Dm = 2.686 (determined by pycnometer)
References203
1 - Neshquehonite, Jáchymov. Sejkora [203]

Nickel-zippeite Ni2(UO2)6(SO4)3(OH)10 . 16 H2O
The mineral was first described in 1976 by Frondel [24]on type specimens from Happy Jack mine, Utah andfrom Jáchymov. For the specimen from Jáchymov, Frondel [24] gives Ni/Co ratio near to 10/3 and minor Fe andZn. According to Frondel the Ni/Co ratio corresponds torelative contents in primary ores in the uraninite vein(smaltite-chloanthite and nickeline).
Nickel-zippeite aggregates are earthy or granular, softor somewhat hardened, brown-yellow to orange yellow
in colour. Nickel-zippeite, in analogy to zippeite, forms
by relatively quick precipitation of free uranyl-sulphateions, which are mobile and stable in highly acid solutions.
Nickel-zippeite was observed with gypsum, zippeite,
sodium-zippeite, and johannite, exceptionally with jáchymovite, sklodowskite, and "pseudo-zippeite (Mg)".
See also other minerals of the zippeite group (sodium-zippeite, zippeite, magnesium-zippeite, "ferro-zippeite", "pseudo-zippeite (Mg)").
EDX, WDX
References

1 major elements:
U, S, Ni6, 24

minor elements:
Co

1 - nickel-zippeite, Jáchymov. Frondel [24]Natrojarosite NaFe3(SO4)2(OH)6

Nickelhexahydrite NiSO4 . 6 H2ONatrojarosite occurs as yellow dusty fill and coatings inweathered ore veins. It was formed by decomposition of
pyrite and marcasite in a relatively dry environment.
Natrojarosite is always accompanied by gypsum andoften by limonite. It is common on all sulphide-bearingveins in Jáchymov. Older reports on jarosite occurrencein this ore district probably relate to natrojarosite.
The mineral was also described by Ulrich [194] ascoating of walls with weathered pyrite in old workings.
Lattice par. [Å]References

a= 7.331(3)194

c =16.76(2)Neshquehonite Mg[(CO2OH)(OH)] . 2 H2O

It forms coatings and crusts with very fine crystalline
texture, acicular crystals and glassy crusts. The crystals
and glassy crusts are transparent to translucent, with aglassy lustre. Although the crystals are very brittle, one
crystal 1 cm long and 1 mm wide at its base was observed.
Nickelhexahydrite occurs in Jáchymov at a depth ofapproximately 500 m, where it forms by oxidation of
marcasite and nickel arsenides. Its coatings cover altered
granite portions rich in clay minerals and vuggy quartz
next to granite. The mineral is accompanied by annabergite, gypsum, a mineral similar to jarosite, and a probable lavendulan.

Journal of the Czech Geological Society, 42/4 (1997)

41

It is interesting that nickelhexahydrite was foundonly in the deepest level of the mine, near contact of
granite with metamorphic rocks. Probably, granite buffers pH of solutions at values necessary for crystallisationof this mineral. The same vein some 50 m higher, positioned in metamorphic rocks, is free of nickelhexahydrite.
The quantitative chemical analysis by M. Waldman(1974) is NiO 22.69, MgO 4.07, CoO 0.21, SO3 30.67,
H2O 41.96, Total 99.60 wt. %. Recalculation based on 10
oxygen atoms gives the formula:(Ni0.78Mg0.26Co0.01)(SO4)0.99 . 5.99 H2O
Lattice par.
[Å, °]
EDX, WDX
IR[cm-1]
Density [g.cm-3]
Referencesa = 9.93(2) b = 7.21(2)c = 24.01(4)E = 98.03(2)major elements:
minor elements:
Ni, S
Mg, Co, Ca
485,635,670,790,1120,1645,2370,3300
and 3470
Dx = 2.01
27, 114, 139

Opal forms transparent coating on fractures and vugs ofvein quartz. It also fills free spaces as massive material
coloured yellow-brown by disseminated limonite. Opal
is associated with secondary Pb minerals in the Geister
vein.
Orpiment As2S3
It occurs as thin cleavable grains of bright yellow colour
along cleavages of a carbonate in specimens with arsenic
and proustite. Proustite forms minute crystals and powdery pseudomorphs after skeletal crystals of silver originally intergrown in arsenic.
The specimens are from the Geschieber vein.
Pararealgar AsS
Pararealgar occurs as thin powdery or fine-grained coating of brown-orange colour on specimens of arsenicintergrown with carbonate and on realgar crystals grownon native arsenic. Pharmacolite and rösslerite occur onpararealgar.
The specimens originate in the Geschieber vein.

Nováþekite Mg(UO2)2(AsO4)2 . 12 H2OParascorodite FeAsO4 . 2 H2ONováþekite was always identified in a mixture withmetanováþekite. It occurs in two paragenesis. In the first
type it forms small and thin light yellow coating on veincarbonates with disseminated chalcopyrite and tennantite. Nováþekite probably formed by neutralisation ofacid solutions containing uranyl-arsenate ions and Mg
released from carbonates. The specimens were collectedin the Evangelista vein.
The second type is represented by crystals up to 3
mm long with bismuthinite in vugs of vein quartz.
Freshly exposed crystals are transparent to translucent
and intense yellow. During 24 hours the crystals turnmilky and gradually change to opaque. Specimens of thistype come from vein fragments on the dump of the Eliáš
mine.
EDX, WDX

major elements:U, Mg, Asminor elements:
Ca

Olivenite Cu2(AsO4)(OH)
It occurs as minor spheres to 0.2 mm in diameter, composed of dark olive radiating crystals. The aggregates aredeposited on botryoidal aggregates of strashimirite. Olivenite is associated with lavendulan and lindackerite on
fractures of vein quartz carrying minor tennantite andpyrite.
Lattice par.
[Å, °]
EDX, WDX
References

Jáchymov is the second locality for parascorodite, after
the type locality Kutná Hora, Czech Republic [290].
The mineral occurs in very rare earthy aggregateswith a conchoidal fracture. The aggregates are depositedin small cavities of quartz gangue with pyrite andproustite, accompanied by small spheres of kaĖkite. The
specimens analysed appear to be always a mixture ofscorodite and parascorodite. The specimens were collected in the Geschieber vein.
References67, 290

Parasymplesite Fe3(AsO4)2 . 8 H2O
In Jáchymov, this mineral occurs always in a mixture
with symplesite. Both the minerals form flat radiating
aggregates up to 5 mm in diameter, composed of minor
acicular crystals. It is green, light green to black-green,
often with a blue shade.
Lattice par.
[Å, °]
EDX, WDX

a = 10.41(4) b = 13.44(5) c = 4.83(2)E=105.46(6)1 major elements:
minor elements:
Fe,As
Mn<Co
2
Fe,As
Mn~Co
3
Fe,As
Mn>Co
27, 91, 112

a = 8.230(5) b = 8.627(4) c = 5.934(3)References

E=90.119(6)major elements:
minor elements:
Cu, As240

1 - parasymplesite, Jáchymov. This work (needle end)
2 - parasymplesite, Jáchymov. This work (needle centre)
3 - parasymplesite, Jáchymov. This work (aggregate centre)

Opal SiO2 . n H2O

42Journal of the Czech Geological Society, 42/4 (1997)

Parasymplesite often accompanies glassy greenbrown amorphous Fe, Ni - arsenates, which form in thefirst stage of decomposition of Fe, Co, Ni - sulphoarsenides (arsenopyrite, löllingite, skutterudite, marcasite, a. o.). It also occurs with köttigite and arsenates ofMg and Ca, as well as on specimens with native arsenic.
Parnauite Cu9(AsO4)2(SO4)(OH)10 . 7 H2OParnauite was identified in association with chalcophyllite in coating of light green spheroidal aggregates, withindividual spheres to 2 mm. The diffuse and weak diffractions suggest that parnauite formed by rather rapid
precipitation from weakly acid to neutral solutions. The
specimens from the Svornost mine, carrying parnauitewith chalcophyllite represent the single confirmed occurrence.
EDX, WDX

major elements:
Cu, Asminor elements:
Al

Parsonsite Pb2(UO2)(PO4)2 . 2 H2OParsonsite forms yellow to brown-yellow acicular crystals, exceptionally to 4 mm long, with a waxy-glassy
lustre. The crystals occur sometimes in radiating groups.
It is deposited on pyromorphite which covers limonite(or Mn-oxide) coated quartz. Alternatively, parsonsite
crystallised on transparent torbernite-metatorbernite. It is
associated also with mottramite. Another type of parsonsite forms minute radiating spheres of acicular crystals,
accompanied by churchite-(Y), meta-autunite, ferruginous pseudomorphs after meta-autunite, and by corkite.
Lattice par.
[Å, °]
EDX, WDX
Referencesa = 6.873(6) b=10.416(5) c = 6.684(3)D=101.41(6) E=98.358(7) J 86.39(1)major elements:
minor elements:
Pb, P, U
241, 268

Petitjeanite Bi3O(OH)(PO4)2
It was identified most often in a mixture with bismutite
as powdery to earthy fill in cavities after leached native
Bi in vein quartz. Powdery petitjeanite is light grey buff,
the earthy type is somewhat darker and more brownish.
Exceptionally, it was identified in compact pseudomorphs after native Bi, which are composed dominantlyof bismutite and preisingerite. Petitjeanite belongs to theyoungest secondary Bi minerals. Though it occurs in thesame vein as mrázekite, the succession relation could not
be determined, since the two minerals have not beenfound together.

Pharmacolite Ca[(H2O)2AsO3(OH)]
Acicular crystals elongated parallel the c axis are mostcommon. They are typically 3 to 5 mm long, but crystals
up to 15 mm long have been found. Radiating aggregatesand crystalline crusts are very common. It is colourless,grey or yellowish, transparent to translucent with aglassy lustre and a perfect (010) cleavage.
Chemical analysis was done by M. Waldmann in
1975: As2O5 52.74, CaO 26.12, MgO 0.21, H2O 21.16,
insoluble residue 0.31, Total 100.54 wt. %, corresponds
to the following formula (recalculation based on 6 oxygen atoms):
Ca1.00Mg0.02(HAsO4)0.91(AsO4)0.07 . 2.06 H2O
It occurs with picropharmacolite on primary ores
containing As or native As in carbonate gangue. The
other associated minerals include rösslerite, minerals of
the erythrite group, haidingerite, and sometimes gypsum.
Lattice par.
[Å, °]

a = 5.948(1) b = 15.41(1) c = 6.267(1)E=114.42(2)major elements:
minor elements:
As, CaSi, Bi, Fe, Mg
IR
1 425, 435, 460, 540, 620, 670, 708, 875,
915, 1120, 1190, 1390, 1640, 1700,[cm-1]
2380, 2870, 2930, 3230, 3465, 3555
2 420, 435, 460, 545, 625,675, 715, 880,
915, 1130, 1195, 1405, 1655, 1705,
2380, 2945, 3225, 3470, 3540
3 435, 460, 540, 620, 665, 707, 875, 910,
1025, 1125, 1185, 1395, 1455, 1640,
1700, 2380, 2860, 2945, 3220, 3465,
3535
Therm. analysis
0.5 (20-110), 6.75 (110-200), 10.75(200-285), 3.0 (285-495), 1.0 (495-1000)[wt. %, °C]
at 250 °C endothermic dehydratation anddehydoxylation, at 460 °C endothermic
recrystalization of anhydrous arsenate
Density [g.cm-3]
Dm = 2.686, Dx = 2.732
References27, 68, 105, 107, 115, 130, 135
EDX, WDX

1, 2, 3 - different type of pharmacolite, Jáchymov. This work

Pharmacosiderite KFe4(AsO4)3(OH)4 . 6-7 H2O
It was identified only in a single specimen as yellowbrown to brown-black indistinct crystalline aggregates. It
shows no cleavage and it has a glassy lustre on fracturesurface. Pharmacosiderite was observed in paragenesis
with erythrite in sample PF20851 collected in 1853 andoriginally listed as ganomatit.
Lattice par. [Å]EDX, WDX
References

a= 15.993(3)major elements:
Fe, As, Si, K, Al
269

minor elements:
Co, Ni, Zn, Ca, S

Journal of the Czech Geological Society, 42/4 (1997)

43

Phosphuranylite KCa(H3O)3(UO2)7(PO4)4O4 . 8 H2O
Plumbojarosite PbFe6(SO4)4(OH)12This mineral occurs, together with unidentified phases,
only in several specimens as crystalline coating andcrusts composed of fine, yellow accicular crystals.
The mineral probably corresponds to intermediate
members of the series phosphuranylite - yingjiangite,with predominance of Ca above K.
The X-ray powder pattern does not show good correspondence with the pattern in the original description[227].
Lattice par. [Å]EDX, WDX
Referencesa = 15.48(2) b =17.41(4) c = 13.82(2)major elements:
minor elements:
U, P, CaK
277

Picropharmacolite Ca4Mg(AsO4)2(AsO3OH)2 . 11 H2OPicropharmacolite is a common secondary mineral in
Jáchymov. It occurs in white acicular to hair-thin crystals
grouped in radiating aggregates and spheres.
Lattice par.
[Å, °]
EDX, WDX
IR[cm-1]
Therm. analysis[wt. %] [°C]
Density [g.cm-3]
References

Plumbojarosite occurs as very fine-grained, soft earthy
aggregates up to 2 mm long. The colour is light brown. It
is deposited on the surface of samples carrying gypsum,
uranopilite and minerals of the zippeite and jarosite
group. The specimens originate from the Evangelista
vein.
Lattice par. [Å]EDX, WDX
Referencesa = 7.318(1)major elements:
Pb, S, Fe98

c = 33.73(1)minor elements:

Posnjakite Cu4(SO4)(OH)6 . H2O
It is always mixed with langite in small, strong blue
crystalline patches. The aggregates consist of imperfectly
shaped crystals, deposited on fractures of vein quartz
close to tennantite or chalcopyrite, which served as asource of Cu and S. Posnjakite is associated with brochantite, devilline, and gypsum.

a= 13.546(5) b=13.528(5) c = 6.728(3)D=99.823(5) E=96.511(5) J 91.576(4)major elements:
minor elements:
Ca, As, Mg(Sr)420, 435, 460, 625, 730, 810, 870, 900,
1030, 1120, 1260, 1400, 1535, 2300,
2380, 2540, and 5425
13.6 (20-245), 9.2 (245-575)
endothermic reaction: 180, 385
exothermic reaction: 690
Dm = 2.605, Dx = 2.630 (determined bypycnometer)
27, 68, 107, 130, 131

The aggregates are either compact or carry a compact
core from which radiate thin, up to 1 cm long crystals. It
also forms botryoidal or compact crusts. Picropharmacolite tends to accompany nearly all secondary arsenates. A
pale pink variety is probably coloured by a minor cobalt
admixture.
The quantitative chemical analysis As2O5 49.11, MgO
4.46, CaO 23.66, H2O 22.69, insoluble residue 0.40,
Total 100.32 wt. %, analyst P. Povondra 1976 (Geological Institute, Czechoslovak Academy of Science).
Recalculation of the analysis on 16 oxygen atoms
gives the following formula:
Ca3.95Mg1.04(AsO4)1.97(AsO3OH)2.03 . 10.77 H2OPitticite (amorphous hydrated Fe-arsenates-sulphates)
Pitticite was described as a secondary red-brown mineral, which forms compact masses with a botryoidal
surface; it is yellow when powdered. Pitticite can beovergrown by gypsum and pharmacolite. It also forms
dropstone and fills vugs. Occurrences in the Anna,
Himmel Krone, Geister, and Geschieber veins were recorded by [118].

EDX, WDX
References

major elements:
Cu, S
242

minor elements:

Preisingerite Bi3O(AsO4)2(OH)Preisingerite associated with atelestite occurs as compact
aggregates or irregular veinlets with surface of up to
several cm2 in vein quartz. The yellow to dark grey aggregates show a pitch-like lustre (similar to that of mimetite) and a moderate hardness.
Preisingerite associated with bismutite constitutepseudomorphs after native Bi. The pseudomorphs arerather similar to quartz but show a stronger lustre. Relicsof native bismuth were observed in cores of some pseudomorphs.
Preisingerite occurs in two paragenesis:
1. paragenesis with atelestite: atelestite, native bismuth,beyerite and walpurgite; it was identified in specimens from the Rovnost I shaft.
2. paragenesis with bismutite: bismutite, bismutoferrite,
walpurgite, torbernite, and metatorbernite; it was
identified on the Geister vein.
Lattice par.
[Å, °]
EDX, WDX
References

1 a = 9.986(7) b = 7.401(8) c = 6.943(7)D= 87.77(1) E=115.14(1) J 111.03(1)1 major elements:
minor elements:
Bi, AsP
92

1 - Preisingerite from paragenesis with atelestite

Proustite Ag3AsS3Secondary proustite forms powdery fill of minor cavities
after leached skeletal crystals of silver, originally intergrown in arsenic in a carbonate veinlet. The secondary
proustite is red-brown.

44

Journal of the Czech Geological Society, 42/4 (1997)

The specimen was collected in the Geschieber vein.

acicular crystals. It is associated with wulfenite, parsonsite, mottramite, and other minerals in the Geister vein.

Pseudomalachite Cu5(PO4)2(OH)4
It was found on a single specimen as a botryoidal cruston altered wallrock, free of additional minerals. The
individual small aggregates are up to 2 mm across, blue-green in colour, with a matte glassy lustre. The specimen is from the Geister vein.
Psilomelane (amorphous Mn-oxides)
It occurs as black powdery or earthy coating on fractures
and as thin depositions between layers of secondary
minerals. Psilomelane also occurs on radiating aggregates of talmessite.
Pucherite BiVO4
Pucherite forms rare brown tabular crystals with an adamantine lustre, exceptionally up to 1.5 mm long. The
crystals occur in widely disseminated small clusters deposited on powdery bismutite, which fills places among
eulytite spheres. It is accompanied by beyerite and namibite. Pucherite was found on dump of the Eliáš mine.
Sejkora [193] gave two quantitative analyses ofpucherite: Bi2O3 72.82 (72.62), V2O5 24.74 (24.97),
As2O5 0.50 (1.55), P2O5 1.68 (0.69), Total 99.74 (99.83)
wt. %, which were calculated on the basis of four oxygen
atoms to the formula:
Bi1.03(V0.90As0.03P0.05)O4
Lattice par. [Å] 1 a = 5.08(1) b = 12.04(3) c = 5.27(1)References
121

Minute crystals of the youngest generation of pyromorphite grown on
needles of Ca-pyromorphite. Magnification 400

Rabbittite Ca3Mg3(UO2)2(CO3)6(OH)4 . 18 H2O
Rabbittite occurs in radiating aggregates of freely grownacicular crystals, which are often malformed, including
bent and conical crystals. It does not fluoresce in ultraviolet light.
Lattice par.
[Å, °]
EDX, WDX

References

a= 32.492(2) b=23.654(8) c = 9.410(3)E=89.838(5)V = 7232.3(5)major elements:
minor elements:
U, Ca, F
S, Mg(C not analysed)
12, 54

1 - pucherite, Jáchymov. Sejkora [193]Pyrolusite MnO2
It occurs as black lenticular crystals, as steel grey, shortprismatic crystals with longitudinal striation, or as granular aggregates showing locally radiating structure, deposited on fractures of a porous vein quartz. Pyrolusite is theoldest mineral in the succession pyrolusite - coronadite cryptomelane. It occurs in the Mariánská locality.
Pyromorphite Pb5(PO4)3Cl
Pyromorphite forms compact light yellow mass with ahigh waxy lustre, filling small vugs in quartz veins.
Lattice par. [Å] 1 a = 9.926(3)c = 7.292(5)2 a = 9.875(3)c = 7.218(6)EDX, WDX
1 major elements:
minor elements:
Pb, P
Ca
2
Pb, P, CaAs
IR [cm-1]
400,440,480,550,580,795,810,1030
References
27, 901 - pyromorphite, Jáchymov. This study
2 - pyromorphite, Jáchymov. This study

It represents one of the youngest secondary Pb minerals. Pyromorphite was also found in minute white
X-ray powder diffraction patterns of rabbittite from Jáchymov.

Aggregates of imperfect acicular crystals of rabbittite. Magnification700

It is often associated with zellerite, schröckingerite,
liebigite, and gypsum, which constitute coating of
weathered uraninite-bearing vein.
The qualitative chemical analysis of rabbittite from
Jáchymov confirmed an elevated content of fluorine,
which probably substitutes for the (OH) group in theabove formula. X-ray powder diffraction pattern corresponds to the original rabbittite data [54].

Journal of the Czech Geological Society, 42/4 (1997)

45

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

29
21
43
23
12
15
23
100
39
22
82

19.096
13.39011.099
9.834
9.543
9.165
8.997
8.135
7.733
7.362
7.090

19.12313.392
11.114
9.847
9.562
9.046
9.032
8.133
7.691
7.364
7.093

1
2
1
3
2
1
1
2
2
0
2

1
1
2
1
2
0
0
0
1
2
3

0
0
0
0
0
1
-1
-1
-1
1
0

9
18
11
30
32
18
30
34
9
5
23

6.754
6.442
5.902
5.807
5.660
4.473
4.375
4.331
4.268
4.180
4.065

6.812
6.498
5.913
5.818
5.658
4.464
4.374
4.334
4.259
4.191
4.062

3
5
0
1
4
6
5
1
4
1
8

1
0
4
4
3
3
4
2
4
5
0

1
0
0
0
0
0
0
2
-1
-1
0

15
15
21
13
23
25
17
5
13
8

4.018
4.018
3.871
3.818
3.548
3.340
3.308
2.854
2.800
2.691

4.030
4.008
3.854
3.816
3.547
3.340
3.308
2.852
2.801
2.690

6
4
4
5
4
9
2
3
11
12

3
1
2
0
6
1
7
8
1
1

-1
-2
2
2
0
1
0
0
1
0

X-ray powder diffraction pattern of rabejacite from Jáchymov.
Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

13
28
100
2
3
3
1
30
46
4
43
16
7
17
8
9
9
6

8.585
8.347
7.924
7.606
7.169
5.226
4.347
4.154
3.960
3.622
3.479
3.409
3.381
3.346
3.245
3.174
3.132
2.956

8.592
8.347
7.926
7.640
7.160
5.251
4.346
4.161
3.962
3.599
3.500
3.401
3.393
3.339
3.228
3.170
3.125
2.964

1
0
0
1
0
0
1
2
1
1
1
2
1
0
0
0
2
0

0
2
0
1
1
3
1
1
2
0
3
3
4
5
3
0
3
2

0
0
2
0
2
1
3
0
3
4
3
0
2
0
4
5
2
5

23
14
12
4
3
8
7
3
2
<1
5
1
1
5
10
12
8
4

2.857
2.824
2.778
2.691
2.680
2.640
2.604
2.550
2.507
2.47542.43442.39092.28482.21582.15892.13542.12452.1062

2.860
2.823
2.779
2.694
2.682
2.642
2.605
2.551
2.511
2.46202.43962.38872.28382.22092.16062.13612.1253
2.1074

2
0
3
3
1
0
2
2
1
0
2
2
0
1
1
2
3
1

3
5
1
0
5
0
4
0
6
6
2
4
7
5
4
6
0
7

3
3
1
2
3
6
3
5
2
3
5
4
2
5
6
3
5
3

6
2
5
5
2
5
3
3
4
2
3
5
11
6
5
5
4

2.07502.05682.04782.01301.99671.9806
1.93601.89991.8837
1.84751.79541.75511.7414
1.7283
1.71941.70171.67692.07332.05742.04352.01411.99571.98091.93571.8962
1.88491.84651.7962
1.75641.7422
1.72541.72051.70301.6771

4
4
0
1
3
2
4
4
2
0
4
0
2
1
4
2
3

0
1
7
5
6
4
2
4
3
8
4
6
7
0
4
9
8

2
2
4
6
0
6
3
1
7
4
3
7
5
9
4
0
1

The unit cell parameters given in the table above represent an improvement in precision by two or three orders, compared to values presented in [54]. Newly measured X-ray powder diffractions and their indices areincluded above

Rabejacite occurs in paragenesis with johannite deposited on strongly weathered uraninite breccia.
Lattice par. [Å]Referencesa = 8.592(4) b=16.695(7) c= 15.852(8)19Rabejacite Ca(UO2)4(SO4)2(OH)6 . 6 H2O
Rauenthalite Ca3(AsO4)2 . 10 H2ORabejacite was identified in a single specimen collectedin 1887. It forms soft earthy aggregates up to 1 mm long,across an area of several cm2. The aggregates are finegrained, strong yellow with a green grey shade. The
mineral fluoresces yellow-white of a moderate intensity
in UV light.

It was found by Fontan [237] on a brassite specimen in a
mixture with weilite, haidingerite and pharmacolite. No
detailed description is available. The specimen is deposited in the collections of École nationale supérieure desmines in Paris.
Retgersite NiSO4 . 6 H2ORetgersite from Jáchymov was described by Sejkora anděídkošil [47] as crusts deposited on gersdorffite andveinlets penetrating this mineral. It forms apple green
granular mass or blue-green fibrous aggregates. Retgersite is accompanied by gypsum, aragonite, and finegrained annabergite. It is easily soluble in water. A quantitative wet chemical analysis: NiO 28.31, SO3 29.77,
MgO 0.63, CaO 0.33, FeO 0.09, CoO 0.12, H2O 40.35,
Total 99.60 wt. %, gives on recalculation to four oxygen
atoms the formula:(Ni1.01Mg0.04Ca0.02)(S0.99O4) . 5.96 H2OAggregate of small rabejacite crystals showing acute double termination. Magnification 900

The indices of refraction are no = 1.511(3) and
ne=1.483(3). The authors [47] suggested that retgersite
formed directly in its primary occurrence, not by dehy-

46

Journal of the Czech Geological Society, 42/4 (1997)

dration of heptahydrate (i.e., morenosite). This is indicated by the fact that no morenosite was found in thespecimen rich in retgersite. It was also noted that temperatures of crystallisation of morenosite, retgersite, andnickelhexahydrite are 31.5, 31.5 to 53.5, and 53.5qC
respectively. The crystallisation temperature can be lowered by surplus acid by as much as 15qC. Surplus acidcan be expected in the environment of Jáchymov veins.

Prague. This specimen was originally designated as morenosite.
It forms grey-white powdery efflorescence and coating on weathered gangue material with pyrite and marcasite. The analyses correspond to a mixture of rhomboclase with a member of the series gunningiteszomolnokite.
EDX, WDX

Lattice par. [Å]IR[cm-1]
Therm. analysis[°C]
References

1 a = 6.772(1)c=18.249(5)1 467,631,797,1100,1306,1635,1689,
1755,2364, 3418

major elements:
Fe, S

minor elements:
ZnRichetite PbU4O13 . 4H2O

1 Endothermic reaction: 130 (2 H2O), 170(3 H2O), 405 (H2O), 910 (disintegration
NiSO4 to NiO a SO3)
47, 103, 179, 180

1 - retgersite, Jáchymov. Sejkora et al. [47]Sejkora and ěídkošil [47] indicated location of retgersite-bearing specimens as the fifth level of the Svornost mine, the Geschieber vein, because this locality was
given in the description of krutovite as a new mineral[180]. The circumstances of collecting of these specimens are somewhat complicated. Kašpar and PadČra
[179], in their first description of krutovite as gersdorffite with unusually large unit cell, indicated PotĤþky
as the locality, where the material was collected in 1963
at a secondary storage place. This results in some uncertainty concerning the original locality of krutovite andretgersite specimens.

The mineral was identified in a single specimen as
brown yellow powdery aggregates about 2 cm2 in size.
Richetite formed as an immediate weathering product ofuraninite or gummite. It is accompanied by an unidentified orange-brown oxide, listed in this study as “UO3H2O(1)”, green aggregates of antlerite, zeunerite andlangite mixture, and light yellow aggregates of tabular
crystals representing a mixture mainly of metazeuneriteand nováþekite.
The unit cell dimensions of Jáchymov richetite show
clearly shifts in comparison with the original data [258],
but the unit cell volume is comparable. The indices ofdiffractions presented in [258] correspond very well tothe measured pattern.
Lattice par.
[Å, °]

a=20.352(7) b=12.232(7) c=16.252(5)D=103.86(1) E=114.92(1) J 89.47(1)major elements:
minor elements:
U, Pb
Si,Cu,V21, 258

EDX, WDX

Rhomboclase HFe(SO4)2 . 4 H2O
Rhomboclase was identified in a single specimen (No.
NM 17259) in the collection of the National Museum in

References

X-ray powder diffraction pattern of richetite from Jáchymov (sample J-361).
Irel

dobs

15
4
10
27
3
11
48
64
48
9
5
10
18
18
23
8
16
10
5
4
9
5
1
10
21

16.28515.65615.20110.437
9.696
8.382
7.779
7.693
7.141
6.769
6.414
6.047
5.945
5.945
5.676
5.211
5.049
4.980
4.546
4.458
4.314
4.177
4.062
3.976
3.925

dcalc

h

k

l

10.440

-1

1

0

8.355

1

-1

1

7.117
6.784

0
-3

0
0

2
1

6.038
5.924
5.905
5.680
5.216
5.051

0
-1
0
-3
3
-4

2
1
2
1
1
0

-1
2
0
0
0
1

4.565
4.459
4.294
4.178
4.056
3.966
3.934

1
-4
1
3
0
1
-1

2
1
-1
2
2
-3
3

1
2
3
-3
2
1
0

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

3
22
17
32
44
21
15
7
100
21
10
13
19
15
3
13
6
9
8
11
1
10
11
7

3.849
3.787
3.710
3.576
3.551
3.485
3.375
3.305
3.216
3.174
3.103
3.052
2.922
2.904
2.824
2.765
2.637
2.625
2.572
2.518
2.505
2.44792.37152.3073

3.833
3.795
3.716
3.575
3.558
3.480
3.374
3.303
3.220
3.178
3.107
3.053
2.920
2.900
2.818
2.766
2.633
2.627
2.574
2.516
2.506
2.44832.37222.3069

-5
-5
1
-2
0
-3
-5
0
-6
1
3
0
2
-7
6
-7
0
-3
4
-2
0
-6
0
-8

1
1
-3
3
0
3
2
2
1
3
-3
-4
0
0
2
1
-4
0
3
2
4
3
0
2

1
2
2
1
4
0
1
3
1
-4
2
1
4
2
-1
1
4
6
1
5
2
3
6
1

8
13
5
5
10
5
4
4
19
6
34
6
9
21
12
2
6
6
1
14
8
3
11
5

2.28622.25492.20572.1784
2.1597
2.10742.08962.06662.03532.0204
1.9776
1.96691.9311
1.8952
1.85631.81471.79671.77391.75431.72961.72001.67011.64251.59632.28572.25462.20692.17842.1603
2.10792.08942.06742.0350

2
2
8
6
7
2
-9
8
0

5
2
1
0
-2
-5
1
2
3

-4
-7
-6
3
2
4
5
0
-7

Journal of the Czech Geological Society, 42/4 (1997)

Römerite Fe2+Fe23+ (SO4)4 . 14 H2O

which remain transparent, are more striking than brassite
in old specimens.

It was analysed in a mixture with an unidentified sulphate. The mixture forms a light pink efflorescencecomposed of very fine rhombohedral crystals adhering topyrite. Römerite formed by a slow decomposition of
pyrite, probably in a low-humidity environment.
EDX, WDX

major elements:
Fe, S

47

minor elements:
SiIR[cm-1]
Density [g.cm-3]
Water content[wt. %]
References

475,740,860,885,1055,1120,(1465),
1655,2440,2945 a 3430
Dm = 1.911, Dx = 1.945
46.25
27, 68, 107, 135, 145

Rösslerite MgHAsO4 . 7 H2ORozenite FeSO4 . 4 H2ORösslerite usually forms colourless or milky white single
crystals 1 to 40 mm in size. The crystals are typicallytabular on (010) and contact matrix by this face. Crystalsof prismatic habit parallel the vertical zone show parallel
growth on (010). On rare occasions, rösslerite occurs as
acicular crystals in radiant groups. This type of rösslerite
is similar to picropharmacolite, except for a rather weak
vitreous lustre of the former species. Rösslerite also
forms coatings and crystalline crusts. Skeletal or bent
crystals, reminiscent of some quickly growing soluble
sulphates, were also observed. Some rösslerite crystals
are matte. A weak blue green shade in some specimens iscaused by Ni and Cu admixture.
Rösslerite is often intergrown with pharmacolite or
encloses acicular crystals of picropharmacolite. Rarely it
is overgrown by sainfeldite. Köttigite, parasymplesite,and symplesite accompany rösslerite in few cases. All
these minerals are deposited on vein carbonates intergrown with partly altered primary ore minerals including
skutterudite, native arsenic, bismuth, and sphalerite.
Rösslerite and associated secondary minerals form byalteration of arsenic-bearing ores.
It occurs in long time abandoned mine workings,
typically at a depth near 160 m. The tabular crystals arerecorded mainly from levels between -120 and -240 m.
At deeper levels, it attains a different habit and becomesscarce. At the levels -350 to -400 m it forms small acicular aggregates similar to picropharmacolite.
The quantitative chemical analysis: As2O5 39.45,
MgO 14.08, H2O 46.26, insoluble residue 0.36, Total
100.15 wt. %; analyst P. Povondra, ýSAV, 1976. Recalculation on the basis of 11 oxygen atoms results in theformula:Rozenite forms brittle clusters of irregular skeletal crystals, in part fibrous or striated parallel to elongation,
which are in part bent. It is grey-green, with milky
clouding, translucent. Rozenite occurs in the same paragenesis as melanterite, because it forms by dehydrationof melanterite. Dehydration depends on environment of aparticular specimen. Separated, powdered pure melanterite dehydrates in less than one hour. Melanterite next topartly weathered pyrite matrix, i.e., with hygroscopic
sulphuric acid, may persist unaltered.
The alteration of melanterite to rozenite is reversible.
Additional hydration of rozenite results in its alteration
to szomolnokite [292].

Mg1.02H0.96AsO4. 7.00 H2O
Larsen presented optical data for rösslerite under theheading of wapplerite. Optical character of the mineral is
positive, nD = 1.525, nE = 1.53, nJ = 1.550, 2V is small ormoderate.
In a dry environment rösslerite turns white during
several weeks and alters to brassite. The alteration starts
from randomly positioned sites, including positions inside crystals. In other instances, rösslerite remains unaltered in collections for time longer than 20 years. Possibly, presence of free sulphuric or arsenic acid supports
water retention in rösslerite. X-ray diffraction examination of some whitened rösslerite crystals shows no newly
formed crystalline phase.
The paragenesis of rösslerite is similar to that ofbrassite. However, haidingerite and other minerals,

Sainfeldite Ca5(AsO4)2(AsO3OH)2 . 4 H2O
Sainfeldite occurs in Jáchymov in small spheres, lessthan 1 mm in diameter, in part clustered in grape-likeaggregates. Some spheres are hollow, others are composed of radiating acicular crystals. The spheres aremilky white to vitreous transparent; occasional pinkviolet sainfeldite contains up to 1 wt. % MnO.
Lattice par.
[Å, °]
IR[cm-1]

EDX, WDX
References

a=18.656 (4) b= 9.489(2) c= 10.015(3)E=96.932(3)440, 480, 640, 755,(860), 885, (900),
1055, 1110 1290, 1640, 1460, 1640,
2315, 2485, 2890, 2950, 3240 a 3475
(data identical with villyallenite from
Jáchymov)major elements:
minor elements:
Ca, AsMn,Mg,Cu,Zn,Co27, 68, 69, 71, 107, 130, 151

Surface of spheroidal aggregates of sainfeldite. Magnification 300

48

Journal of the Czech Geological Society, 42/4 (1997)

X-ray diffraction pattern of Jáchymov sainfeldite
does not compare closely enough to published data on
this mineral [130]. It corresponds better to Cavillyaellenite [69]. Because these minerals are isostructural, variation in diffraction pattern may depend largelyon the Mn/Ca ratio.
Sainfeldite occurs with Ca-Mg arsenates and withminerals of the erythrite group.
Scorodite FeAsO4 . 2 H2OScorodite is a relatively common mineral forming radiating aggregates of acicular crystals, or compact spheres.
The mineral has a vitreous lustre and white, greenish
grey or brown-yellow colour. It occurs on vein quartz orintergrown with dickite next to weathered native arsenic,
löllingite or arsenopyrite. Scorodite with a metallic lustre
and white streak forms sometimes compact pseudomorphs after decomposed löllingite or arsenopyrite.
Lattice par.
[Å, °]
References

a= 8.9530(7) b=0.3264(6) c=10.0456(8)66, 257

Schoepite [(UO2)8O2(OH)12] . 12 H2O
It was identified as a minority component in long yellow
acicular crystals is specimen No. NM 24272, designatedas E-uranopilite, in collection of the National Museum,
Prague. Uranophane is the main species besides schoepite.
References

280

Schröckingerite NaCa3[(UO2)(CO3)3](SO4)F . 10 H2OThis mineral was found in 1873 by Schröckinger, who
named it Uranoxyd-Karbonat [159]. In the same year,
Schrauf [183] published description of this mineral andnamed it schröckingerite. The type specimen was collected in the Evangelista vein.
The original description by Schrauf [183] gives only
a qualitative determination of U, CO2, H2O, minor CaO
and traces of SO3. Loss on ignition was 36.7 wt. %.
Nováþek [211] reported the following analysis: CaO
19.1, UO3 32.4, SO3 9.1, H2O 20.2, insoluble residue 0.4,
loss on ignition 36.04, Total 100.12 wt. %. Na2O and
CaO were not determined for lack of material.
Schrauf [183] gave the angle of 58.5q between edgesof the hexagonal plates; following Nováþek [211] theangle is 60q and the mineral with perfect basal cleavage
is hexagonal. It is pleochroic: X- colourless to light yellow, Y and Z - light green-yellow, optically negative,
with 2V 0 to 25q, exceptionally 40q. The indices of refraction are nD = 1.496, nE = nJ = 1.539 to 1.545.
Minute scales and hexagonal platy crystals, somewhat similar to uranium micas, make soft, earthy aggregates. The aggregates are transparent, with a high vitreous to pearly lustre, yellow to greenish yellow. It fluoresces bright yellow-green in ultra-violet light.
Schröckingerite is fairly soluble, especially at pH<4
(Kašpar [106]). Its occurrence thus indicates a lower

acidity, in agreement with association with uraninitecarbonate. It is deposited on uraninite or in its proximity.
Schröckingerite is accompanied and penetrated by liebigite. The aggregates of these two minerals are unlike
schröckingerite and they are rather similar to andersonite. Coating of uranyl-carbonates avoids pyrite or marcasite grains, which are covered by limonite.
Mereiter [202] studied structure and crystallographyof schröckingerite. The following optical properties are
given: nD=1.4892(3), nE= 1.5388(3), nJ = 1.5412(3), and2Vcalc = 24.6(3) q.
Lattice par.
[Å, °]

1 a = 9.634(1) b = 9.635(1) c= 14.391(2)D = 91.41(1) E = 92.33(1) J 120.26(1)2 525, 608, 665, 705, 739, 750, 790, 816,
842, 903, 932, 1015, 1078, 1093, 1182,
1367, 1572, 1638, 2640, 3260, 3455,
3620
Density [g.cm-3] 1 Dx = 2.563
3 Dm = 2.515
EDX, WDX
major elements:
minor elements:
U, Ca, C as (CO3)2Mg, Na
References
10, 12, 27, 56, 106, 159, 202, 211
IR[cm-1]

1 - schröckingerite, Jáchymov. Mereiter [202]
2 - schröckingerite, Jáchymov. ýejka et al. [10]3 - schröckingerite, Jáchymov. Nováþek. [211]

Schultenite PbHAsO4
Very fine schultenite needles constitute cotton-like aggregates with a silky lustre. It occurs with yellow uranium ochres, light yellow uranium mica and glassy anglesite crystals on fracture in uraninite veinlet with pyriteand sphalerite. Schultenite is identified on specimens
collected in the Eliáš mine.

Aggregates of small randomly oriented crystals of schultenite. Magnification 100

Silver Ag
It was described, besides other forms, as wire silver;some types of silver formed by cementation process.
Small leaves of silver are marginally altered to argentite.
In other specimens, argentite crystals are sometimes
corroded and covered by minor scales of silver [118].
Secondary silver was also found along fractures ofvein quartz as sheet-like aggregates intergrown in ten-Journal of the Czech Geological Society, 42/4 (1997)

49

nantite and pyrite. These specimens come from the
Geschieber vein.

Sodium-zippeite forms by relatively quick precipitation of free sulphate and uranyl ions, which are mobile
and stable only in an acid environment. It typically occurs as efflorescence, powdery coating, or in earthy mixtures with other uranium sulphates. Aggregates of themineral tend to be soft or hardened, strong yellow, orange to red, brownish yellow.
Somewhat larger isolated crystals or radiating aggregates probably formed from relatively diluted solutions
or in places with a moderate pH gradient. Due to variety
of appearance and habit of various types of zippeite, it is
impossible to identify sodium-zippeite from several unknown phases (see "pseudo-zippeite (Mg)"). The mineral
fluoresces a weak yellow-brown in ultra-violet light.
Powder X-ray diffraction pattern was indexed using
orthorhombic model proposed by Frondel [24]. Sodiumzippeite was observed in association with gypsum, uranopilite, zippeite, nickel-zippeite, johannite, and exceptionally with jáchymovite, metaschoepite and "pseudozippeite (Mg)".
See also other minerals of the zippeite group (magnesium-zippeite, zippeite, nickel-zippeite, "ferro-zippeite","pseudo-zippeite (Mg)").

Sklodowskite (H3O)2Mg(UO2)2(SiO4)2 . 2 H2OSklodowskite occurs as soft, earthy and buff coloured
nodules up to 2 mm long. It was rare on some specimens
with gypsum, sodium-zippeite, uranopilite, and "pseudozippeite (Mg)". It does not fluoresce in ultra-violet light.
Specimens were collected in the Evangelista vein.
Lattice par.
[Å, °]
EDX, WDX
Referencesa = 17.39(1) b = 7.07(1)c = 6.624(6)E=105.60(1)major elements:
minor elements:U, Mg, Si
S53, 249

Smrkovecite Bi2O(PO4)(OH)
Smrkovecite [48] was identified by Sejkora [193] byquantitative analysis as very minor aggregates among
mixite acicular crystals. In view of the small size of theaggregates, the mineral could not be examined by X-ray
diffraction.

Lattice par. [Å] 1 a = 8.816(9) b = 17.16(2) c = 7.323(8)2 a = 8.82
b = 17.12
c = 7.32
EDX, WDX
major elements:
minor elements:
U, S
Na
References
6, 24, 132, 152, 191, 252

Soddyite (UO2)2SiO4 . 2 H2O
Soddyite from Jáchymov was listed by Kašpar [106] as arare, compact light brown to brown mineral. It was considered to be younger than cuprosklodowskite; no additional data on soddyite was presented.

1 - sodium-zippeite, Jáchymov. This study, sample J-331
2 - orthorhombic model proposed by Frondel[24]Sodium-zippeite Na4(UO2)6(SO4)3(OH)10 . 4 H2O
Sodium-zippeite belongs to some of the least studied
uranium minerals with a layered structure. It appears tobelong to relatively unstable or meta-stable minerals
which alter readily under natural conditions [6]. An additional problem is analytical-instrumental and resultsfrom difficulties of analysis of relatively low concentrations of alkalis, in particular potassium, in presence ofuranium (see: new chemical re-definition of the zippeite
group [24]).
Aggregate of minute doubly terminated crystals of sodium-zippeite.
Magnification 600
X-ray powder diffraction pattern of sodium-zippeite from Jáchymov (sample J-331).
Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

2
100
1
4
3
2
4
5
16
7
45

8.618
7.353
5.859
5.587
4.707
4.364
4.291
4.251
4.120
4.010
3.667

8.582
7.323

0
0

2
0

0
1

4.014
3.661

1
0

3
0

1
2

1
3
4
2
5
3
4
1
6
1
0

2
0
1
2
0
1
0
0
0
2
1

3
<1
1
6
2
1
1
1
1
1
1
<1

2.700
2.663
2.592
2.576
2.562
2.510
2.46992.41172.39802.34882.29092.2747

0
1
1

1
1
0
0
0

0
2
1
0
1
2
2
3
0
2
3

5
6
2

2
2
0
4
1

3.581
3.492
3.413
3.368
3.199
3.152
3.075
2.896
2.861
2.779
2.727

2
0
3

0
1
2
0
2

3.580
3.501
3.409
3.369
3.224
3.159
3.067
2.891
2.863
2.752
2.740

2.708
2.665
2.599

5.571
4.709
4.408
4.291
4.269

<1
40
1
1
8
52
1
2
21
1
1

2.551
2.504
2.46182.41662.39972.34782.29182.2803

1
0
3
0
2
0
3
2

6
5
3
1
6
2
0
6

1
2
1
3
0
3
2
1

50

Journal of the Czech Geological Society, 42/4 (1997)

Strashimirite Cu8(AsO4)4(OH)4 . 4 H2O
It forms minor bright green spheres or botryoidal coatings, fractions of mm thick, and developed as small
patches several mm2 in size. The aggregates show a radiating structure and silky lustre. It is accompanied bylindackerite, lavendulan, and olivenite on fractures ofquartz vein with tennantite.
Lattice par.
[Å, °]
EDX, WDX
Referencesa = 9.71(3)b = 18.93(7) c = 8.91(8)E = 97.7(1)major elements:
minor elements:
Cu, AsS, Si
243

Sulphur S
Kratochvíl [118] described small sulphur crystals on
native arsenic accompanied by calcite.
Sulphur occurs as small light yellow equant crystals
with a high adamantine lustre. It crystallised on corroded
specimens with sulpho-arsenides and arsenides, fromwhich it was released. Sulphur is associated with köttigite and picropharmacolite. This type is documented
from the Geschieber and Evangelista veins.
Sulphur also forms pseudomorphs after barrel-shaped
grey crystal up to 2 mm long, striated parallel to elongation, grown scattered in porous vein quartz. Probably,
marcasite or argentopyrite was the original mineral of
the pseudomorphs. The specimens come from the
Geschieber vein.
Greyish white powdery sulphur constitutes pseudomorphs after altered arsenopyrite or chalcopyrite. This
type occurs in the Schweizer vein as a product of partial
oxidation of sulphides and sulpho-arsenides, a processslower (and characterised by less acidic conditions) thandecomposition of pyrite or marcasite. The latter sulphides feature a spontaneous decomposition characterised by the catalytic role of H2SO4. During slow decomposition of arsenopyrite, the surplus arsenate acid isgradually removed or neutralised and the process may
locally result in neutral pH conditions.
For this reason, "less acidic" or neutral iron arsenates- scorodite and kaĖkite formed by decomposition ofarsenopyrite.
Symplesite Fe3(AsO4)2 . 8 H2O
Symplesite forms radiating aggregates of accicular crystals. It is light green-grey, sometimes with a yellow
shade. Mixture with parasymplesite is common and pure
symplesite is rather rare. Symplesite is accompanied byannebergite and köttigite in porous vein quartz in the
Geschieber vein.
Symplesite often accompanies green-brown amorphous arsenates of Fe and Ni, which form in the firststage of alteration of sulphides and sulpho-arsenides of
Fe, Co, and Ni (arsenopyrite, löllingite, skutterudite,marcasite a.o.). It also associates with köttigite and arsenates of Mg and Ca. It was observed on specimens withnative arsenic.

Lattice par.
[Å, °]
EDX, WDX

Referencesa = 7.88(1) b = 9.476(4) c = 4.713(5)D=100.61(1) E= 96.68(1) J 105.41(1)1 major elements:
minor elements:
Fe,As
Mn<Co
2
Fe,As
Mn~Co
3
Fe,As
Mn>Co
27, 65, 91

1 - symplesite, Jáchymov. This study (needle end)
2 - symplesite, Jáchymov. This study (needle centre)
3 - symplesite, Jáchymov. This study (aggregate centre)

Synchisite Ca(Ce,La)(CO3)2F
Synchisite was identified on a single specimen from thedump of the Eliáš mine. It forms mixture with beyerite
pseudomorphs after acicular crystals of bismuthinite in a
vug of vein quartz. The pseudomorphs consist of whitish
yellow spheres; dusty coating of the mixture also developed on walls of the vug. It was identified only by X-ray
diffraction.
Talc Mg3Si4O10(OH)2
It forms coating on wall rock fractures and occurs insome veins. Talc has a variable colour including white togreen, yellow, and red. Coloration is caused by incorporated admixtures [118].
It is probable that the talc mentioned in older reports
corresponds to compact aggregates of dickite, which are
relatively common in the veins [3].
Talmessite Ca2Mg(AsO4)2 . 2 H2OTalmessite occurs in fan-shaped and spheroidal radiating
aggregates of buff yellow colour. Central parts of theaggregates are compact. Its higher hardness makes it
distinct from otherwise similar picropharmacolite. It has
a matte lustre.
One particular specimen carries talmessite overgrownby radiating acicular crystals of gypsum, mimeticallyarranged in the same growth pattern as the radiating
talmessite. On other specimens, talmessite is the oldest
secondary mineral, on which Mn-oxide, annabergiteköttigite, and picropharmacolite deposited. Monohydrocalcite is also associated with talmessite. It is rare secondary mineral in Jáchymov, which was identified on several specimens of coarse-grained carbonate vein withskutterudite from the Josef vein. The carbonate vein is
only 2 cm wide.
The powder X-ray pattern was indexed following
Rios [178].
Lattice par.
[Å, °]
EDX, WDX
Referencesa = 5.912(5) b = 6.97(1)c = 5.567(7)D = 97.11(2) E=109.06(2) J 108.03(2)major elements:
minor elements:
Mg, Ca, As
107, 130, 178

Journal of the Czech Geological Society, 42/4 (1997)

Tenorite CuO
Tenorite was described by Kratochvíl as coating andvinlets. It forms from chalcocite and occasionally it isaccompanied by native copper. It was found in the Eliáš
mine and the ýervená vein.
Thenardite Na2SO4
Thenardite was identified as accompanying the assemblage of Mg-arsenates. The specimens represent several
cm thick fragile crust, consisting of perpendicular vitreous prismatic/skeletal crystal aggregates, with powdery
thenardite on surface. Milky white, radiating acicular
crystals of picropharmacolite deposited directly on matrix rock, constitute the base on which thenardite crystallised. Middle part of the crust consists of glassy acicular
crystals of an unknown arsenate, mixed with gypsum
and thenardite. These arsenate-sulphate crusts originate
from the Geschieber vein.
Formation of the thick crusts was associated withtransport of significant amounts of material. As primaryarsenides-sulphides are the source of As and S, it could
be expected that Fe is also a significant element. In fact,
no Fe was detected. It is probable that several cations inthese crusts derive from mineral waters percolating
through fractured granite. The arsenate-sulphate crusts
were observed at three sites, always associated with
granite. Springs of mineral water occur only several tensof metres of these occurrences. It is assumed that the
carbonate mineral water was first neutralised by acidsulphates and arsenates of Fe and Fe was removed as
neutral and insoluble carbonates. The arsenates/sulphatesof Na, Ca, and Mg probably recrystallized through actionof additional batches of mineral water.
Thenardite was observed in association with a new
Mg-arsenate, picropharmacolite, and gypsum.
Lattice par. [Å]EDX, WDX
References

a= 9.826(2) b= 12.317(3) c = 5.867(2)major elements:
minor elements:
Na, S
244

Torbernite Cu(UO2)2(PO4)2 . 8-12 H2OTorbernite was first described from Jáchymov by Werner[192] as early as 1793. Compared to metatorbernite,
torbernite is less common in Jáchymov. Its fractured or
powdered aggregates are unstable and easily dehydrate
to metatorbernite. Under natural conditions of humidity,
low temperature, suitable pH and composition of solutions, torbernite is relatively stable. A transparent torbernite crystal, collected more than 20 years ago and associated only with minor metatorbernite, changed to metatorbernite during three days after powdering.
According to Kašpar [106], water in uranium micas
is comparable to zeolite water and escapes rather continuously. According to Frondel [164], the loss of waterin torbernite is irreversible.
Torbernite occurs mainly on fractures of veins, which
are covered by tabular crystals with perfect (001) cleavage and minor scales. The crystals are 1 mm long on

51

average, rarely up to 5 mm long. Crystals of equant,dipyramidal habit was also observed. Parallel growth ofcrystals is relatively common and it may involve otheruranium mica minerals. Torbernite shows various shadesof green, from apple green to yellow-green, and darkemerald green. It is transparent to translucent, with avitreous lustre. Opaque torbernite with a matte surface
also occurs.
Torbernite was observed with metatorbernite, zeunerite, metazeunerite, tyuyamunite, churchite-(Y), parsonsite, etc. It was relatively common mineral in all mines
with uranium veins. The Werner mine supplied majorityof specimens.
EDX, WDX
References

major elements:
minor elements:
U, P, Cu27, 75, 84, 93, 133, 192

Trögerite (UO2)3(AsO4)2 . 12 H2O
The occurrence of trögerite was mentioned by Ježek
[189] as questionable. New studies did not confirm its
occurrence.
The indices of refraction measured by Mrose [8]: nD= 1.584, nE = 1.620, nJ = 1.623, correspond to values
given by Larsen [162] but they are lower than those for
specimens from Schneeberg, which are described aströgerite. A comparison of X-ray data also shows differences between samples from these two localities. The
mineral from Jáchymov corresponds to values fornováþekite but contains no Ca and Mg. It contains As >P [8].
Quantitative chemical analysis could not be obtained
due to the small quantity of material. Trögerite is pleochroic: X - nearly colourless, Y and Z - light lemon yellow, sign-, 2V | 20q, X = c [8].
Tyuyamunite Ca(UO2)2V2O8 . 5-8 H2OTyuyamunite was identified in several specimens as
powdery coating light yellow in colour, passing to lightgreen-yellow. It was always closely associated with thinveinlets of primary bornite and chalcocite. Transport ofvanadium, contained in these sulphides, took place overa minimal distance. Vanadate ions, formed during oxidation, were quickly bound in tyuyamunite. This is indicated by widened and lower-intensity diffractions, whichindicate poor crystallinity of the material.
The specimens originated in the Geister vein, theWerner mine.
EDX, WDX

major elements:
U, V, Caminor elements:
Fe, CuUrancalcarite Ca(UO2)3(CO3)(OH)6 . 3 H2O
It was identified or indicated by X-ray powder diffraction of mixture with zellerite and metazellerite, whichconstitute soft powdery coating or fine-grained crusts,
light yellow or light buff in colour. The coatings formedon surface of partly weathered uraninite. The material

52

Journal of the Czech Geological Society, 42/4 (1997)

does not fluoresce in UV light. The paragenesis includes
zellerite, metazellerite, liebigite and schröckingerite.
In view of poor crystallinity of urancalcarite, theidentification is not quite safe.
Uranocircite Ba(UO2)2(PO4)2 . 12 H2OUranocircite from Jáchymov is mentioned by Ježek, who
considered its presence as questionable [189]. It was notconfirmed by new studies.

The mineral has positive elongation, 2Vm = 71.5q
perfect cleavage on (010). In distinction to other localities, uranophane-beta from Jáchymov has a notable zoning, most prominent on fragments lying on (010) and at
termination of crystals. The early (most internal) zoneshows lower indices of refraction and a larger extinction
angle, compared to the outer zone. The cause of the zoning is unknown. Zoning-free uranophane-beta from otherlocalities has indices of refraction corresponding to thoseof the outer zone in Jáchymov specimens [319].

Uranophane Ca(UO2)2[SiO3(OH)]2 . 5 H2O
It is a common uranium mineral in Jáchymov. Uranophane forms powdery fill of vugs in uraninite or inweathered uraninite-bearing veins and coating on thesematerials. Its colour is variable, powdery aggregates are
beige yellow to brown. Minute acicular crystals are lesscommon. It is associated with a variety of secondary
uranium minerals, regular associated phase is uranophane-beta.
Nováþek [35] gave indices of refraction for two
specimens from Jáchymov:a) minute yellow acicular crystals: nD=1.648, nE=1.666,
nJ=1.675b) thin acicular crystals from a vug in uraninite:
nD=1.647, nE=1.661, nJ=1.668.
Pjatnitzky [39] gave the extinction angle of 2°, according to Frondel [164] the extinction is parallel.
Lattice par.
[Å, °]
EDX, WDX
References

a= 15.909(6) b = 7.007(4) c = 6.669(2)E=97.447(5)major elements:
minor elements:
U, Si, Ca
7,53, 78,80,85

Uranophane-beta Ca(UO2)2[SiO3(OH)]2 . 5 H2O
It was first described from Jáchymov in 1935 byNováþek [35, 36] under the name E-uranotile. The lattername was abandoned in recognition of priority of thename uranophane [206, 207] before uranotile [124],
though the description by Websky was incomplete, inaccurate, based on a qualitative chemical analysis, density
and hardness, obtained on a mixture. Uranophane-beta
usually forms coatings on uraninite and in vugs.
Nováþek in his description [35] gave the following
chemical analysis: UO3 66.29, SiO2 13.11, CaO 7.32,
H2O 12.87, Total 99.59 wt. %, and the formula:
CaO . 2SiO2 . 2UO3 . 6H2O
The following data are also given: an oblique extinction on the face (010), c/Z = 41q, c/Y = 49q, in the plane(100) the extinction is parallel. The acicular crystals areyellow-green; the crystals are much thicker compared touranophane and nearly always twinned, and show astrong pleochroism X - colourless, Y and Z - dark yellow. The indices of refraction are distinctly higher compared to uranophane, nD=1.665, nE=1.686, nJ=1.696.
Very strong dispersion is characteristic.
This mineral usually forms coating on uraninite but
occurs also as small crystals grown freely into cavities.

J:c [°]

biref.

2Vcalc [°]Min. 1.661 1.682 1.689

52-57

0.028

66

Max. 1.671 1.694 1.702

44-48

0.031

60

nD

nE

nJ

According to the authors [319], uranophane-beta isless stable than uranophane under normal pressure androom temperature. It can transform to uranophane during
powdering of a sample.
X-ray diffraction data of uranophane-beta from
Jáchymov are given by Frondel et al. [23].
It is relatively rare mineral in Jáchymov, which was
identified in several specimens only, including those incollections of the Mineralogical Institute, Charles University and National Museum, both in Prague. The
maximum crystal size observed was 3 mm. The specimen No. NM 26537 contains relatively thick acicular
crystals on matrix of brown silicified vein material. It
provided the single subsample of pure uranophane-beta.
Lattice par.
[Å, °]

a = 6.636(8) b = 15.46(2) c = 14.07(2)E=91.355(9)1 450,550,(615),710,779,(792),850,882,
939,990,1418,1635,(1668),(3200)3445
Density [g.cm-3] 2 Dm = 3.953
References
7, 23, 35, 36, 53, 124, 206, 207
IR [cm-1]

1 - uranophane-beta, Jáchymov (NM 27465) [7]
2 - uranophane-beta, Jáchymov. Nováþek [35]Uranopilite (UO2)6(SO4)(OH)10 . 12 H2OUranopilite was first described from Jáchymov in 1854
by Dauber [171] under the name basisches Uransulfat.
The name uranopilite was introduced by Weisbach [172].
As other uranium sulphates, uranopilite forms in oxidation zone enriched in heavy metals and uraninite. Sulphuric acid, resulting from the hydration-oxidation process, results in formation of complex uranyl-sulphateions. According to ýejka et al. [173], these ions are morestable in acid conditions than uranyl carbonates, and theuranyl sulphate ions have better migration capability. A
quick evaporation of such solutions with low concentration of other cations results in precipitation of uranopilitein the form of coating and crusts, or as an efflorescenceon walls of mine workings.
Uranopilite occurs as crystalline aggregates of randomly oriented minute, short acicular crystals. The aggregates are strong yellow to greenish yellow, with avitreous to silky lustre. Unlike zippeite, uranopilite fluoresces strong yellow-green in ultra-violet light. The crys-Journal of the Czech Geological Society, 42/4 (1997)

tals are pleochroic, exhibit good cleavage parallel toflattening, and oblique extinction Y/c = 18q (Nováþek
[35]).
Larsen [162] presented indices of refraction by 0.002
lower, positive optical character and extreme dispersionof optical axes (increasing from red to violet). The extinction angle Y/elongation = 15q.
Uranopilite is associated with gypsum, zippeite, sodium-zippeite, metaschoepite, johannite, uraninite, andas yet closer unidentified phases "pseudo-johannite" and"pseudo-zippeite (Mg)". Uranopilite is relatively abundant in the Eliáš mine.
The first reliable compositional data on uranopilite
were provided by Nováþek [35]. He presented threequantitative analyses of which the following he considered as representative: UO3 81.20, CaO 0.93, SO3 4.04,
H2O 14.03, Total 100.20 wt. % and suggested the formula:
6UO3 . SO3 . x H2O
where x = 16 or 17. The following indices of refraction
were measured: nD = 1.6228, nE = 1.6248, nJ = 1.6336.
The X-ray powder diffraction data and unit-cell parameters (table below) are given in [18].
Lattice par.
[Å, °]

1 a = 14.03(1) b = 14.60(1) c = 9.184(6)E = 96.87(6)2 248,257,280,423,465,545,585,624,843,
895,955,1082,1106,1145,1169,1622,
3200,3430, 3610
1 530,581,620,845,900,936,1073,1108,
1140,1165,1625,1650,3180,3440,3590
Therm. analysis 1 20-104 6.59 (8 H2O),104-128 2.11 (2H2O), 128-575 6.72 (8 H2O), 575-884[°C, wt. %]5.01 (1 SO3 + 1 O2)References18, 35, 171, 172, 173
IR[cm-1]

1- uranopilite, Jáchymov - ýejka et al. [18], sample A
2 - uranopilite, Jáchymov - ýejka et al. [18], sample B

Uranospathite HAl(UO2)4(PO4)4 . 40 H2O53

weathered uraninite or on unidentified, very thin strong
yellow coating. It was observed in paragenesis with arsenuranospathite, whitish to transparent anglesite,nováþekite and white-green metatorbernite.
EDX, WDX
References

major elements:
U, Al, P
289

minor elements:

The semiquantitative chemical analyses suggest thatin the specimens studied there are members of a continuous series uranospathite-arsenuranospathite. The
specimens were collected on dumps of the Eliáš mine.
Uranosphaerite Bi2U2O9 . 3 H2O
The specimen No. NM 17365 in the collection of the
National Museum in Prague, donated by V. Wraný in
1902, is designated "uranosphaerite". The following
minerals were identified in the specimen during the present re-study: vandendriesscheite, compreignacite, kasolite, and uranophane.
According to Ježek [189] the mineral from Jáchymov, marked as uranosphaerite, is identical with uranopilite (as well as the mineral designated uraconite). This
strengthens the view that uranosphaerite was listed as
occurring in Jáchymov by error. The present re-study ofmany specimens did not confirm presence of uranosphaerite. Ježek [189] suggested that the names uranosphaerite (and uraconite) can be considered as synonymous to Vogl's term Uranoker (uranium ochres), as
far as specimens from Jáchymov are concerned.
Uranospinite Ca(UO2)2(AsO4)2 . 10 H2OJežek [189] considered its occurrence in Jáchymov asquestionable. But it was identified in a mixture withmeta-uranospinite (see description) on a sample (No.
13142) from Joaneum, Graz.
Valentinite Sb2O3
Kratochvíl [118] listed valentinite from Jáchymov as okt.
Arseniksäure, which suggests that valentinite was mentioned by error. The presence of this mineral was notrecently confirmed.
Vandendriesscheite PbU7O22 . 12 H2OAggregates of thin tabular crystals of uranospathite. Magnification
300

Uranospathite occurs as inconspicuous planar to spheroidal aggregates of light green to light yellow-green
colour, composed of rose-shaped clusters of tabular
tetragonal crystals.
The crystals show a strong pearly lustre. Uranospathite aggregates are deposited directly on partly

The mineral was identified in a single specimen, in thecourse of revision of old specimens in the collection of
the National Museum in Prague. The specimen No.
17365 (donated by V. Wraný in 1902) was designateduranosphaerite. The specimen contains massive glassy
red-brown to orange crusts with a yellow streak, which
are soft and very friable. The present study shows thatthe crusts are composed of several phases, with vandendriesscheite predominating over compreignacite. Also
associated are kasolite and uranophane in beige powdery
coatings. The matrix of the specimen is a weathered
piece of uraninite, covered by crusts and penetrated byveinlets of the above secondary minerals.

54

Lattice par. [Å]EDX, WDX
References

Journal of the Czech Geological Society, 42/4 (1997)

a = 14.18(1) b=39.43(13) c = 43.25(3)major elements:
minor elements:
U,Pb,SiK
21

fractures in the vein material or in the country rock next
to the vein. The specimen identified was collected in theGeister vein.
EDX, WDX

Villyaellenite (Mn,Ca,Zn)5(AsO4)2[AsO3(OH)]2 . 4 H2OVillyaellenite occurs in small tabular crystals with vitreous lustre, which are either isolated or grouped in grapelike or radiating aggregates. The colour is light pink buff.
No example of the extreme Mn-rich member was recorded and the samples examined represent Cavillyaellenite.
EDX, WDX
IR[cm-1]

Density [g.cm-3]
References

major elements:
minor elements:
As, Mn, Ca
440, 480, 645, 755, (855), 875, 900,
1055, 1100, 1290, 1450, 1640, 2515,
2475, 2885, 2935, 3190, a 3475.
(data identical with sainfeldite from
Jáchymov)
Dm = 2.686 (determined by pycnometer)
69, 71, 151, 130

Aggregate of villyaellenite crystals. Magnification 500

It is noted that some specimens show chemical composition similar to sainfeldite [130], but lattice parameters and the diffraction patterns, including intensities,
compares much better with villyaellenite. The two species are isostructural and the diffraction patterns can be
expected to reflect merely variation in the Mn/Ca ratio.
Villyaellenite is associated with rösslerite, pharmacolite, picropharmacolite, and fluckite.

major elements:
Fe, P

minor elements:

Voglite Ca2Cu(UO2)2(CO3)2O3
The mineral was first found in Jáchymov and describedin 1853 by Vogl [60] under the name Uran-Kalk-KupferCarbonat. The name voglite was introduced by the Austrian mineralogist and geologist Haidinger, to honour the
discoverer Josef Florian Vogl, who published studies ofminerals from the Jáchymov mines [16]A quantitative chemical analysis of voglite was donein 1853 by J. Lindacker [60], a pharmacist and chemistin Abertamy. No additional analysis appears to be donein later times.
Voglite is described as rhomboidal scales similar inshape to gypsum, constituting thin coatings and also
scaly twins of emerald green to grass green colour, witha green streak and pearly lustre [60]. It is compared by
its appearance to zeunerite or metatorbernite.
It was found by Vogl in the Fluther vein (whichyielded also eliasite), Eliáš mine, at a depth of 150-170
m. It was associated with liebigite, uranium ores, fluorite, dolomite, clay, and disintegrated schist [60]ýejka et al. [16] presented three infrared spectra ofvoglite and noted absence of fluorescence in ultra-violet
light.
Piret et al. [42] published powder X-ray pattern ofvoglite from Jáchymov and proposed a monoclinic unitcell (table below) for Z = 16.
Voglite is pleochroic: X - dark blue-green, Y - dark
blue-green, Z - light yellowish. Directions Y and Z lie inthe plane of cleavage [162].
In the present study we attempted to index (table below). The X-ray powder data by Piret et al. [42] with aunit-cell (table below) approximately three times small
compared to that of Piret et al. ýejka et al. [16] gave
powder X-ray data, obtained with Debye-Scherrer camera, for four specimens. However, diffraction values andintensities vary substantially and it is uncertain if theresults are reflecting extremely small amounts of sample,
properties of the mineral, or a polyphase nature of thesample.
Optical properties of voglite were published by several authors as follows:

Vivianite Fe3(PO4)2 . 8 H2OVogl [59] mentioned vivianite as earthy aggregates inpeatbog near Jáchymov and as indigo blue dusty coatingin vugs of corroded limonite.
Vochtenite Fe2+Fe3+[(UO2)(PO4)](OH) . 12-13 H2OVochtenite occurs as minute foliated aggregates similar
to mica. The colour is light beige to brown. It does not
fluoresce in UV light. Vochtenite occurs with limonite,occasionally with autunite and torbernite as coating ofnD
Larsen [162]Berman 1954
Piret, Deliens [42]nEnJ

1.541 1.547 1.564
1.513 1.525 1.542
1.544
1.558

2V [°]

note60--in [164]white light

Optical character is positive [162]. Schrauf [138]measured under the microscope angle of edges 78 to 80q
seen on the platy crystals.

Journal of the Czech Geological Society, 42/4 (1997)

55

X-ray powder diffraction pattern of two types of voglite from Jáchymov compared to data from [42]voglite (the first type), this study

Piret et al. [42] (Debye-Scherrer)

voglite (the second type), this study

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

100 13.284
16 12.854

12.8512

0

0

92 12.908
53 12.304
16 10.176
17 9.608

12.742

2

0

0

100
10

12.6
11.2

12.59911.204

2
2

0
1

0
0

9.648

1

1

-1

80

9.65

9.67

1

1

-1

9.507

0

1

1
48

8.586

8.599

2

1

-1

100

8.7

8.782

2

1

-1

8.709
8.349
7.547
7.181
6.727

2
1
1
3
2

2
1
3
1
3

0
1
0
-1
0

3
2

1
3

-1
0

60

7.1

7.136

3

1

-1

3

2

-1

7.150
6.858
6.587
6.405
6.184
6.107
6.000

7.183
6.847

6.358

43
15
45
100
27
31
15

6.397
6.163
6.089
5.986

3
4
0
1

2
1
4
3

-1
0
0
1

40

6.13

6.124

0

4

0

12
26

5.170
5.093

5.169
5.097

0
5

0
0

2
0

10

5.19

5.19

0

0

2

24
8

4.869
4.758

4.871
4.758

0
0

5
2

0
2

20

4.83

4.835

2

2

-2

30

4.65

4.653

2

4

1

20
11
15
12

4.551
4.499
4.404
4.300

4.550
4.500
4.407
4.300

2
1
0
4

5
2
5
2

0
2
1
-2

50

4.32

4.32

4

2

-2

11
10
15
16

4.206
4.105
4.077
3.939

4.206
4.109
4.088
3.941

4
5
3
0

3
1
5
4

1
-2
-1
2

10

4.1

4.095

5

1

-2

30

3.94

3.939

0

4

2

18

3.502

3.502

3

0

-3

10

3.55

3.553

1

0

-3

6
3
6
10
5
10
6

3.431
3.370
3.277
3.242
3.176
3.135
3.028

3.434
3.366
3.278
3.242
3.175
3.134
3.026

1
3
2
5
5
2
4

5
2
5
0
5
7
7

2
-3
2
-3
1
1
-1

20

3.42

3.420

2

2

-3

6
6
12
8
3
7
11
5

2.717
2.643
2.604
2.40542.11112.07872.0427
1.951961.7405

Irel

13
4
19
18
5
1
20
52
42
17

9.831
9.452
8.839
8.711
8.323
7.553
7.220
6.735
6.629
6.383

2
11

5.666
5.182

5.648
5.190

4
0

2
0

0
2

10
5

4.968
4.897

4.965
4.883

4
3

0
1

1
-2

17
24

4.674
4.607

4.658
4.602

1
4

5
0

0
-2

1

4.421

4.421

1

3

-2

9

4.275

4.284

6

0

0

2
12
13
41
7
2
4
8

4.009
3.965
3.836
3.551
3.454
3.421
3.349
3.311

4.010
3.964
3.821
3.558
3.460
3.424
3.355
3.306

3
1
3
2
0
0
1
4

5
4
2
0
0
1
7
3

-1
-2
2
-3
3
3
0
2

3
7
8
2
2

3.154
3.149
3.042
2.970
2.719

3.154
3.147
3.042
2.970
2.719

5
3
8
6
7

5
7
3
2
6

1
0
-1
-3
-1

4
5
4

2.43072.09512.06152.43092.09522.0613

10
2
6

3
7
1

-2
-4
-5

3
6
12
4

1.95381.93011.90811.86071.95381.93031.90791.8606

5
10
6
4

8
5
8
9

3
2
-4
-4

20
18

1.64431.59291.6443
1.5931

2
10

8
11

5
1

The analysis by Lindacker (in 1853) gave the following results: CaO 14.09, CuO 8.40, UO2 37.0, CO2 26.41,
H2O 13.9, Total 99.8 wt. % and the proposed formula:
Ca2CuU4+(CO3)5 . 6 H2O,
which, recalculated by Berman [cited in 164] gave:
Ca2Cu(UO2)(CO3)4 . 6 H2OThis formula does not correspond well with theanalysis, which would show a surplus of carbonate anions. Presence of anions (CO2OH)1- appears improbable.
Authors of the present work assume, that the original
analysis may be in error. For this reason, the compatibility factor, calculated density, and Z number were notcomputed.

56

Journal of the Czech Geological Society, 42/4 (1997)

Lattice par.
[Å, °]

EDX, WDX
IR[cm-1]

Density[g.cm-3]

References1

a = 25.97

b = 24.50

2a=26.416 (8)E= 104b=23.702(8) c=10.680(5)c = 10.70

3a=26.27 (2)E=103.63(1)b=24.36(1) c=10.655(5)E=104.02(1)major elements:
minor elements:
U, Ca, Cu,CO324a 610,741,796,841,875,903,1030,1053,
1073,1105,1151,1410,1465,1540,1618,
3340, 3385
4b 615,675,742,795,836,903,1015,1110,
1410,1535,1560,1620,3400
4c 612,633,741,833,902,1020,1115,1170,
1420,1512,1560,1620,3400
1 Dm = 2.8
Dx = 2.81 for Ca2Cu(UO2)(CO3)3(OH)2 . 4 H2O
Dx = 2.77 for Ca2Cu(UO2)(CO3)4 . 2 H2O
Dx = 3.06 for Ca2Cu(UO2)(CO3)4 . 6 H2O
16, 30, 42, 56, 60, 161, 163, 164

1 - voglite, Jáchymov [42]2 - voglite (the first type), Jáchymov. This study (Joaneum, Graz,
No.1656A)
3 - voglite (the second type), Jáchymov. This study
4 - voglite, Jáchymov [16] (a - M17, b - M19, c - M20)

The second type forms very thin flat crystals withfurrows in one direction. Their max. size is 0.5 mm. It isof bright bluish green colour. Its lustre is vitreous. Crystals are perfectly transparent and extremely brittle. Voglite is associated with small balls of cuprosklodowskite,liebigite, rösslerite, brassite, zellerite, unnamed phase
Ca-Cu-(UO2)-(CO3)-H2O, and amorphous vitreous dark
yellow-green U-Cu-carbonate.
The sample of voglite of the second type originatesfrom the vein No. 3.
Voltaite K2Fe52+Fe43+(SO4)12 . 18 H2O
Voltaite was listed by Kratochvíl [118] clearly by error,as Tschermak [224] described voltaite from Kremnica.
Walpurgite (BiO)4(UO2)(AsO4)2 . 2 H2O
Walpurgite occurs in thin tabular to lath-shaped crystals
up to 3 mm long. Its colour - waxy yellow - is notably
different from other uranium minerals in Jáchymov. The
lustre is vitreous to adamantine. Walpurgite has perfect(001) cleavage. The present study dealt with specimen
No. NM 4877 from the collection of the National Museum in Prague; the specimen designated as waltherite
was identified as walpurgite. Massive crystalline crusts
tens of cm2 are covered by flat, imperfect crystals ofgrey-brown mineral up to 1 cm long, which is accompanied by torbernite.
The mineral is optically negative, nD= 1.90, nE=
2.00, nJ = 1.205, the angle 2V is moderate; the direction
X is nearly normal to the large face of tabular crystals[162].
Lattice par.
[Å, °]

EDX, WDX
Group of voglite crystals showing parallel growth. Magnification 500

Piret et al. [42] recommend the chemical formula:
Ca2Cu(UO2)(CO3)3(OH)2 . 4 H2O
because of similarity between measured and calculated
densities.
Two different types of voglite were studied in thispaper.
Description of the first type, from Joaneum (Graz,
number: 1656A) corresponds with voglite describedabove.
Average result of 5 quantitative chemical analyses ofthis sample is: Ca 10.64, Cu 6.54, U 53.93, O 25.32, C
3.19, total 99.62 wt. %, and the proposed empirical formula (based on 13 O):
Ca2.18Cu0.84(UO2)1.86(CO3)2.18O2.68(OH)0.05
leads to simplified formula:
Ca2Cu(UO2)2(CO3)2O3

Referencesa = 7.111(4) b = 10.38(1) c = 5.495(2)D=101.48(1) E=110.72(1) J 88.044(9)1 a = 7.098(7) b = 10.37(1) c = 5.479(6)D=101.52(9) E=110.81(8) J 88.04(7)major elements:
minor elements:
Bi, U, As
P
2, 23, 27, 75, 104, 108, 122, 144, 193

1 - walpurgite, Jáchymov. Sejkora [193]Walpurgite is associated with torbernite, metatorbernite, bismutite or bismutoferrite in vein material including minor native bismuth.
It is interesting that the arsenate mineral walpurgite isaccompanied by phosphorus-bearing torbernite, which
may reflect preference of P for the particular mineral
structure.
Some specimens of walpurgite originate from theGeister vein.
Weeksite K2(UO2)2Si6O15 . 4 H2O
It was identified only in the specimen No. 4913 in collection of the National Museum in Prague. The specimen
designated as gummite contains part of weathered uraninite vein. Colour of this secondary material, which appears as metamict and amorphous, varies from brownish
to yellow or orange. Weeksite was identified in the part

Journal of the Czech Geological Society, 42/4 (1997)57

of specimen containing sulphur-yellow vitreous lustrous
layers, seemingly of amorphous nature.

Lattice par. [Å]EDX, WDX

Lattice par. [Å]EDX, WDX

Referencesa = 14.32(2) b = 35.92(3) c = 14.24(3)major elements:
minor elements:
U, K, Si(Ca)
246

Referencesa = 14.00(1) b=11.908(6) c = 6.884(7)major elements:
minor elements:
U, Ca, Pb
Si270

As a rule, it forms mixtures with other minerals of
the PbO-UO3-H2O group in paragenesis with uranophaneand gypsum next to weathered uraninite.

Weilite CaHAsO4
Wulfenite PbMoO4

Weilite probably forms by dehydration of pharmacolite.
Early stages of this alteration are indicated by change oftransparent prismatic crystals of pharmacolite to milky
white. The alteration tends to affect only certain parts ofa crystal. Weilite was never observed in freshly collectedmaterial but in specimens collected at least several years
ago. However, some specimens collected more than acentury ago still contain fresh pharmacolite. The mechanism controlling alteration of pharmacolite to weilite is
unknown.
Lattice par.
[Å, °]
Referencesa = 7.20(4) b = 7.01(2)Wulfenite was identified in two specimens only. In thefirst specimen, it crystallised on quartz crystals. Up to 2
mm long, pseudo-hexahedral crystals are deposited onquartz crystals in a quartz vein. Wulfenite as well as thequartz matrix are coated by limonite, on which someisolated whitish acicular crystals of pyromorphite occur.
On fresh fracture, wulfenite is grey-white, with adamantine lustre.
In the second specimen, wulfenite forms rare long
dipyramidal crystals and up to 2 mm long crystals ofgrey-brown colour on a matrix of small quartz crystals
and compact grey pyromorphite. All these minerals arecoated by limonite. The second type of wulfenite wascollected in the Geister vein.

c = 7.18(2)D = 94.99(3) E= 101.77(3) J 85.72(5)250

Widenmannite Pb2(UO2)(CO3)3
Lattice par. [Å]EDX, WDX

Widenmannite was identified in a single specimen, in
which it forms relatively abundant yellow to yellow
orange powdery fill of vugs up to 1 cm long in orange to
red Pb-U oxides.
Widenmannite from Jáchymov does not fluoresce inultra-violet light, in agreement with data for the material
from Schwarzwald. All the data in tables below, and thedescription are from [203].

References

a= 5.4310(6)major elements:
Pb, Mo251c= 12.115(1)minor elements:Si

Yingjiangite K2Ca(UO2)7(PO4)4(OH)6 . 6 H2O
The mineral has been found only in several specimens as
crystalline coating and crusts composed of minute accicular crystals of yellow colour. Uranophane accompanies yingjiangite in this paragenesis.
The material probably corresponds to intermediate
members of the series phosphuranylite - yingjiangite,with prevalence of K over Ca.
The X-ray powder diffraction pattern of Jáchymov
yingjiangite does not compare well with data in theoriginal description [278].

Lattice par. [Å] 1 a = 8.975(7) b = 9.367(1) c = 4.951(7)EDX, WDX
1 major elements:
minor elements:
Pb, U
Al (up to 0.5 wt%)
References61, 203
1 - widenmannite, Jáchymov. Sejkora [203]

Wölsendorfite (Pb,Ca)U2O7 . 2 H2OWölsendorfite was identified as a substantial componentof red crystalline aggregates with poorly defined radiating structure or yellow-brown coatings on weathereduraninite.

EDX, WDX

major elements:
U, P, Ca, K
278

Referencesminor elements:
Fe

X-ray powder diffraction pattern of widenmannite from Jáchymov [203]
Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

21
3
9
14
100
11
11
45
64
23

6.505
4.723
4.389
4.340
4.154
4.037
3.950
3.325
3.244
3.188

6.480
4.683
4.378
4.335
4.152
4.047
3.934
3.325
3.240
3.182

1
0
0
1
1
2
1
2
2
1

1
2
1
0
2
1
1
0
2
2

0
0
1
1
0
0
1
1
0
1

6
17
7
9
15
16
17
52
4
12

3.146
2.983
2.950
2.844
2.558
2.517
2.48272.34452.24082.1785

3.134
2.992
2.949
2.850
2.561
2.521
2.47002.34172.24672.1820

2
3
1
3
3
3
3
0
3
4

1
0
3
1
0
2
1
4
2
1

1
0
0
0
1
0
1
0
1
0

6
8
8
7
8
15
7
6
9
5

2.15422.11871.9682
1.92711.90961.8723
1.84461.73571.68161.65752.16012.1264
1.9672
1.93991.9073
1.86901.84401.72801.67611.6608

3
1
2
0
3
3
3
3
5
5

3
2
2
3
0
1
4
4
2
1

0
2
2
2
2
2
0
1
0
1

58

Journal of the Czech Geological Society, 42/4 (1997)

X-ray powder diffraction pattern of zellerite from Jáchymov.
Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

100
7
12
28
36
26
9
23

9.537
7.393
5.558
4.851
4.776
4.334
4.241
3.810

9.528
7.280
5.535
4.855
4.764
4.352
4.219
3.811

0
1
1
2
0
0
2
0

2
2
3
2
4
2
3
5

0
0
0
0
0
1
0
0

10
8
15
10
9
10
20
10

3.713
3.659
3.495
3.461
3.190
3.085
2.924
2.788

3.696
3.666
3.499
3.446
3.176
3.057
2.920
2.791

2
1
3
2
0
1
2
4

0
3
2
2
6
6
4
1

1
1
0
1
0
0
1
0

10
9
7
5
12
8
8

2.678
2.40782.17482.0132
1.95671.93261.90212.677
2.40892.17462.0105
1.95901.93391.9056

3
2
4
3
4
2
0

5
6
4
7
7
5
10

0
1
1
1
0
2
0

Zellerite Ca[(UO2)(CO3)2(H2O)2] . 3 H2OZellerite belongs to very rare minerals in Jáchymov.
Zellerite was found as buff yellow botryoidal aggregatesto earthy coating. It has a similar appearance as uranium
sulphates, which are often designated as zippeite. It does
not fluoresce in ultra-violet light.
It is associated with metazellerite, schröckingerite,
liebigite, and rabbittite
Table above gives powder X-ray diffraction data forzellerite from Jáchymov. The data are indexed following[96], however, some of the diffractions measured areabsent in the original description [96].
Lattice par. [Å]EDX, WDX
Referencesa = 11.29(2) b = 19.06(2) c = 4.892(8)major elements:
minor elements:
U, Ca, C(K)
27, 96

Zeunerit Cu(UO2)2(AsO4)2 . 10-16 H2OZeunerite often occurs along fractures in vein material.
The fracture surface is coated by thick tabular to equantcrystals which are transparent, strong green or milky
grey-green. The transparent crystals are notably lustrous.
The crystals are up to 2 mm long but on average the size
is much smaller.
Zeunerite from Jáchymov is unstable under room
temperature and humidity and through loss of water it
slowly changes to more stable metazeunerite. The alteration is much slower than with torbernite.
Zeunerite was observed in association with metazeunerite, torbernite, metatorbernite, tyuyamunite, churchite(Y), and hidalgoite. It is relatively common mineralfound in all the mines with uraninite veins but most
specimens originate from the Werner mine.
Lattice par.
[Å, °]
EDX, WDX
References

a= 1.3564(2) b=1.3564(2) c= 1.3564(2)D=122.35(2) E=122.35(2) J 122.35(2)major elements:
minor elements:
U, As, Cu
Fe, Si93

Zippeite K(UO2)2(SO4)(OH)3 . H2O
Zippeite was first described from Jáchymov by Zippe[161] and in 1845 Haidinger [170] introduced the namezippeite. Concurrently, John in 1821 [165] described thesame mineral under the name basisches schwefelsäuresUranoxyd. In 1857 Vogl [59] published the first quantita-

tive chemical analyses by Lindacker. Zippeite was redefined by Frondel [24] on a specimen analysed byNováþek [24], in absence of the original type specimen.
Zippeite often occurs in powdery coating or as earthy
aggregates, in mixture with other uranium sulphates,
which include several types of zippeite with various
cations (Na, Mg, Fe, Ni, Mn), "pseudo-zippeite (Mg)",
uranopilite, jáchymovite, and other phases. Zippeite
aggregates show variety of habits, including earthy,
granular/crystalline, and soft or hardened intense yellow
to orange to red brownish yellow. Occasionally, it forms
isolated crystals and their radiating aggregates, probably
favoured by lover-concentration solutions and a moderate pH gradient. It is this variability in appearance,
which decisively contributed to ignorance of additional
associated phases, which can not be recognised and identified without a detailed study. Jáchymovite and "pseudozippeite (Mg)" can serve as example of the latter minerals.
During this study, zippeite containing K only was detected in one sample only. It forms relatively large crystals (up to 0.5 mm), which are flat and a little elongated.
The crystals are mostly grouped in small aggregates infractures of rock. Their colour is yellow, brownish yellow or brownish orange.
Zippeite was described as associated with gypsum,
uranopilite, sodium-zippeite, nickel-zippeite, magnesium-zippeite, "ferro-zippeite", johannite, exceptionally
jáchymovite, sklodowskite, metaschoepite. In present
study were regularly observed mixtures of "pseudozippeite (Mg)" always with zippeite (all types).
Nováþek [35] considered the analyses by Lindacker[59] as erroneous and analysed three specimens (unfortunately, K and Na were not determined), with the following results for the first analysis: UO3 71.98, Fe2O3
1.17, CaO 1.88, SO3 10.02, H2O 13.95, Total 99.00
wt.%. He proposed the following formula:
2UO3 . SO3 . 5-6 H2OIndices of refraction for the three specimens show
significant variation and brought Nováþek [35] to conclusion that water bonding in zippeite is rather unstable.
It is probable that Nováþek studied a mixture of uranium
sulphates, possibly with presence of uranium sulphates
with various additional cations.
Though natural uranyl-sulphates with sheet structure,including zippeite, are known for long time, they belong
to uranium minerals, which were not sufficiently studied
and characterised. Difficulties of their study are aggravated by their instability and tendency to alteration undernatural conditions [6].

Journal of the Czech Geological Society, 42/4 (1997)

59

Frondel [24] gave X-ray powder diffraction patternof zippeite from Jáchymov. On the basis of single crystal
Weissenberg and precession measurements he concluded
that all types of zippeite have identical or very similar
structure with a very large orthorhombic unit-cell (tablebelow); the space group was not determined. Traill [191]derived a monoclinic cell for Z = 1, with parameters
shown in table below. Frondel discussed older analyses
and did new ones, including determination of cation
elements. The following formula was proposed:
K4(UO2)6(SO4)3(OH)10 . 4 H2O
One partial analysis of zippeite gave: K2O 8.06,
Na2O 0.62, loss on ignition at 500 qC 10.7 wt. %. The
corresponding optical data include: optically negative,
biaxial mineral, 2V = 60(15)q, indices of refraction nD =1.655, nE= 1.716, nJ= 1.768.
Vochten et al. [260] gave complete crystal structureof synthetic zippeite. On the basic of crystal structureinterpretation he proposed following formula:K(UO2)2(SO4)(OH)3 . H2O
Larsen [162] presented optical data of Jáchymov zippeite for orange-yellow powder and minute crystals. The
powder has nD = 1.630, nE = 1.70, nJ = 1.720; crystals
gave nD = 1.620, nE = 1.680, nJ = 1.720.
In both cases, zippeite is optically negative with alarge 2V.
Zippeite forms by relatively quick precipitation offree sulphate and uranyl ions with extensive mobility andstability only at a low pH. Frondel [24] supposed thatpotassium in zippeite is derived from the country rock.
According to Kašpar [106], conditions of uranylsulphate formation can be derived by analogy with laboratory experiments, which indicate their formation in
relatively narrow range near pH = 3, in the stage of intense decomposition of sulphides, prior to neutralisationof solutions. It is probable that the variable quantity ofwater in the range 3 to 5 water molecules per formulaunit, indicated by various analyses, is caused, similar toother sulphates, by gradual dehydration and "aging" ofthe mineral, often after the specimen was collected.
Old publications about zippeite contain no information of determination or detection of potassium and othercations. This situation reflects analytical problems of K
determination in the presence of uranium, particularly if
K content is near 5 wt. % or lower.
Lattice par.
[Å, °]

1 a = 8.80
2 a = 8.88

b = 68.43
b = 14.10

c = 14.55
c = 8.83

E = 103.50
3 a = 8.656(2) b= 14.240(4) c =17.706(5)E=104.112(4)4 a = 8.755(3) b= 13.987(7) c =17.730(7)E=104.13(3)-3Density [g.cm ] 4 Dc = 4.696
References
6, 24, 35, 59, 106, 132, 152, 161, 165,
170, 191, 252, 260
1 - zippeite, Jáchymov - Frondel et al., [24]2 - zippeite, Jáchymov - Traill [191]3 - zippeite, Jáchymov. This study
4 - synthetic zippeite - K(UO2)2(SO4)(OH)3 . H2O - Vochten et al.,[260]

Our work shows that many specimens have K content below the detection level, but have significant content of Mg and Fe. It means, pure zippeite (K-member) is
relatively rare in Jáchymov. In opposite, the magnesiumzippeite or "ferro-zippeite" are rather common.
The present work suggests that some Jáchymov
specimens analyzed in the past represented a mixture ofzippeites with the "pseudo-zippeite (Mg)", which effectively diluted zippeite in the polymineral sample.
See also other minerals of the zippeite group (sodium-zippeite, magnesium-zippeite, nickel-zippeite, "ferro-zippeite", "pseudo-zippeite (Mg)").

X-ray powder diffraction pattern of zippeite from Jáchymov.
Irel

dobs

2
2
4
9
6
100
1
8
1
0
1
3
5
3
1
4
1
2
2
38
8

9.955
9.475
9.155
8.571
7.607
7.124
6.223
5.487
4.982
5.074
4.754
4.583
4.286
4.204
4.139
3.916
3.769
3.799
3.677
3.558
3.456

dcalc

h

k

l

8.586

0

0

2

7.120

0

2

0

6.214
5.481

1
0

1
2

1
2

4.293
4.198
4.132
3.912

0
2
1
1

0
0
3
3

4
0
-1
1

3.616
3.559
3.453

2
1
2

2
3
0

0
-3
2

Irel

dobs

2
5
1
2
12
2
10
2
2
5
6
2
6
10
4
2
1
2
4
1
0

3.332
3.289
3.225
3.145
3.109
3.063
2.858
2.716
2.692
2.655
2.635
2.509
2.47992.37132.28822.22922.16402.13422.07062.04652.0106

dcalc

h

k

l

3.288

0

4

2

3.184
3.107
3.106
2.862
2.715
2.691
2.655
2.633
2.517
2.47872.37332.28752.23002.16412.13352.07062.04482.0126

0
2
2
0
2
2
0
1
2
2
0
0
1
4
2
4
2
4

3
2
2
0
4
0
2
5
2
4
6
6
3
0
0
2
2
2

4
2
-4
6
-2
4
6
1
4
2
0
2
-7
-2
-8
-2
6
-4

Irel

dobs

dcalc

h

k

l

1
8
1
1
1
1
2
6
1
3
2
3
1
0
1
2
1
1
4
2
1

1.97371.95371.93461.90091.8657
1.8472
1.8282
1.77991.76961.74401.72701.69571.67751.6463
1.63851.58261.51381.52451.54271.55361.56681.97701.9524
1.93191.9027

1
0
4
1

7
6
0
7

-1
5
-6
-3

1.8492
1.82681.7799

4
0
0

4
6
8

-2
6
0

1.7454
1.7267
1.69601.67801.6452
1.6382
1.5819

2
4
2
4
3
2
2

0
0
2
2
7
3
8

-10
4
8
4
-3
-10
-4

60

Journal of the Czech Geological Society, 42/4 (1997)

the powder pattern collected (mainly of low-angle reflections) on material from Jáchymov using original orthorhombic unit-cell does not provide satisfactory results
and observed and calculated d-spacings are not in good
agreement. This agreement becomes better when angle E
is simultaneously refined with parameters a,b, and ccorresponding to the monoclinic symmetry. Parameter E
is very close to 90°, so authors of the original description
having only the data from the film Guinier de Wolf camera probably cannot find this subtle discrepancy whichbecomes apparent only using most recent diffraction
technique.

Znucalite Zn12Ca(UO2)(CO3)3(OH)22 . 4 H2O
Znucalite forms white to light yellow-green compact
coating and stalactitic accumulations in mine workingsnear carbonate, uranium-bearing veins. Its formation isfavourably affected by weakly acid to neutral solutionsof pH > 4. Znucalite therefore does not form on weathered pyrite or arsenide-bearing veins.
The aggregates of radiating scaly crystals of a microscopic size form crusts up to 1 mm thick. Minute crystals
are closely intergrown with amorphous hydrozincite,
powdery calcite, and transparent gypsum. Znucalite fluoresces yellow-green in ultra-violet light. It can be relatively common in mine adits but its coloration contributes to the characteristics of an inconspicuous mineral. It
was identified on specimens from the Evangelista andOndĜej veins.
Lattice par.
[Å, °]
EDX, WDX
References

a =12.689(8) b = 25.11(2) c= 11.689(7)D=88.974(4) E=91.694(4) J 90.342(5)major elements:
minor elements:
Zn, U, Ca, C
37Zýkaite Fe4(AsO4)3(SO4)(OH) . 15 H2OAggregate of minute randomly oriented crystals of zýkaite. Magnification 800

Zýkaite occurs as soft, wet earthy pieces of weakly
coherent material up to 5 cm across. The mineral has
grey-white colour with a weak green shade and a weaksilky lustre. The surface is locally covered by irregularaggregates of kaĖkite. The mineral formed from arsenopyrite in wet places.
The mineral was identified in samples from the vein
No. 3.
Zýkaite is described to be orthorhombic on the basisof optical data in the original paper [177]. Indexing of

Lattice par.
[Å, °]

a =20.911(5) b = 7.062(2) c= 36.794(7)E=90.99(1)major elements:
minor elements:
Fe, As, S
177

EDX, WDX
Reference

X-ray powder diffraction pattern of zýkaite from Jáchymov.
Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

Irel

dobs

dcalc

h

k

l

5
100
13
3
24
4
3
8
5
23
5
4
10
19
4

13.61610.709
8.460
7.346
6.850
6.547
6.304
6.118
5.911
5.590
5.427
5.190
5.076
5.012
4.573

13.69410.658
8.473
7.358
6.847
6.555
6.299
6.120
5.911
5.592
5.425
5.187
5.076
5.017
4.579

1
1
1
0
2
3
1
0
1
2
1
4
1
3
3

0
0
0
0
0
0
1
1
0
1
1
0
0
0
1

2
-3
-4
5
4
-2
-2
3
-6
-2
-4
-1
7
5
3

8
3
8
5
11
5
5
5
8
3
2
19
5
4

4.285
4.087
4.028
3.787
3.735
3.569
3.510
3.309
3.277
3.244
3.146
3.049
2.997
2.949

4.296
4.088
4.025
3.785
3.738
3.576
3.515
3.311
3.277
3.245
3.144
3.045
2.998
2.949

4
0
1
2
4
5
0
1
6
5
1
3
1
5

0
0
0
0
0
1
2
0
0
0
2
2
1
0

-5
9
-9
9
-7
1
1
-11
-4
7
5
3
-11
-9

4
6
1
5
5
4
4
4
5
4
8
8
4
4

2.903
2.831
2.810
2.779
2.743
2.657
2.638
2.44612.41112.39312.36512.31422.29032.2829

2.904
2.829
2.811
2.780
2.744
2.654
2.638
2.44522.41102.39242.36422.31502.28972.2841

3
2
1
1
2
1
3
3
8
6
4
0
9
3

2
2
0
2
0
2
0
1
1
0
0
2
0
2

-5
-7
-13
-8
-13
-9
-13
13
-3
11
-14
12
-3
11

Journal of the Czech Geological Society, 42/4 (1997)

List of secondary minerals from the Jáchymov ore
district arranged according to chemical composition
Arsenates
Adamite Zn2(AsO4)(OH)
Agardite-(Y) (Y,Ca)Cu6(AsO4)3(OH)6 . 3H2O
Annabergite Ni3(AsO4)2 . 8 H2O
Arsenuranospathite HAl(UO2)4(AsO4)4 . 40 H2OAtelestite Bi8(AsO4)3O5(OH)5
Bayldonite PbCu3(AsO4)2(OH)2 . H2O
Beudantite PbFe3(AsO4)(SO4)(OH)6
Brassite MgHAsO4 . 4 H2O
Chalcophyllite Cu9Al(AsO4)2(SO4)1.5(OH)12 . 18H2O
Chenevixite Cu2Fe2(AsO4)2(OH)4 . H2O
Cobaltkoritnigite (Co, Zn)(AsO3)OH . H2O
Cornwallite Cu5(AsO4)(OH)4 . H2ODuftite PbCu(AsO4)(OH)
Erythrite Co3(AsO4)2 . 8 H2OFluckite CaMn(HAsO4)2 . 2 H2OGeminite Cu2(HAsO4)2 . 2 H2OGuerinite Ca5(AsO4)2(AsO3OH)2 . 9 H2OHaidingerite Ca2(HAsO4)2 . 2H2O
Hidalgoite PbAl3(AsO4)(SO4)(OH)6
Hörnesite Mg3(AsO4)2 . 8 H2O
Irhtemite Ca4Mg[(AsO4)2(AsO3OH)2] . 4 H2OKaatialaite Fe[AsO2(OH)2]3 . 5.25 H2OKahlerite Fe(UO2)2(AsO4)2 . 10-12 H2OKaĔkite FeAsO4 . 3.5 H2O
Koritnigite Zn[(H2O)AsO3(OH)]
Köttigite Zn3(AsO4)2 . 8 H2O
Krautite Mn[(H2O)AsO3(OH)]
Lavendulan NaCaCu5(AsO4)4Cl . 5 H2O
Lindackerite (Cu, Co)5(AsO4)2(AsO3OH)2 . 10 H2OMcnearite NaCa5H4(AsO4)5 . 4 H2OMetalodevite Zn(UO2)2(AsO4)2 . 10 H2OMetanováþekite Mg(UO2)2(AsO4)2 . 4-8 H2O
Meta-uranospinite Ca(UO2)2(AsO4)2 . 8H2O
Metazeunerite Cu(UO2)2(AsO4)2 . 8 H2OMimetite Pb5(AsO4)3Cl
Mixite BiCu6(AsO4)3(OH)6 . 3 H2O
Nováþekite Mg(UO2)2(AsO4)2 . 12 H2OOlivenite Cu2(AsO4)(OH)
Parascorodite FeAsO4 . 2 H2OParasymplesite Fe3(AsO4)2 . 8 H2OParnauite Cu9(AsO4)2(SO4)(OH)10 . 7 H2O
Pharmacolite Ca[(H2O)2AsO3(OH)]
Pharmacosiderite KFe4(AsO4)3(OH)4 . 6-7 H2OPicropharmacolite Ca4Mg(AsO4)2(AsO3OH)2 . 11 H2OPitticite amorphous hydrated Fe-arsenates-sulphates
Preisingerite Bi3O(AsO4)2(OH)
Rauenthalite Ca3(AsO4)2 . 10 H2ORösslerite MgHAsO4 . 7 H2O
Sainfeldite Ca5(AsO4)2(AsO3OH)2 . 4 H2O
Scorodite FeAsO4 . 2 H2OSchultenite PbHAsO4
Strashimirite Cu8(AsO4)4(OH)4 . 4 H2O
Symplesite Fe3(AsO4)2 . 8 H2OTalmessite Ca2Mg(AsO4)2 . 2 H2OTrögerite (UO2)3(AsO4)2 . 12 H2OUranospinite Ca(UO2)2(AsO4)2 . 10 H2OVillyaellenite (Mn,Ca,Zn)5(AsO4)2[AsO3(OH)]2 . 4 H2O
Walpurgite (BiO)4(UO2)(AsO4)2 . 2 H2OWeilite CaHAsO4
Zeunerite Cu(UO2)2(AsO4)2 . 10-16 H2O
Zýkaite Fe4(AsO4)3(SO4)(OH) . 15 H2O

61

Carbonates
Albrechtschraufite MgCa4F2[(UO2)(CO3)3]2 . 17H2O
Andersonite Na2Ca[(UO2)(CO3)3] . 6H2O
Aragonite CaCO3
Beyerite Ca(BiO)2(CO3)2
Bismutite (BiO)2CO3
Calcite CaCO3
Cerussite PbCO3
Hydrozincite Zn5(CO3)2(OH)6
Kamotoite-(Y) Y2(UO2)4(CO3)3O4 . 14.5 H2OKettnerite CaBi(CO3)OFLiebigite Ca2[(UO2)(CO3)3] . 11 H2OMalachite Cu2(CO3)(OH)2
Metazellerite Ca[(UO2)(CO3)2(H2O)2] . H2OMonohydrocalcite CaCO3 . H2O
Neshquehonite Mg[(CO2OH)(OH)] . 2 H2O
Rabbittite Ca3Mg3(UO2)2(CO3)6(OH)4 . 18 H2OSchröckingerite NaCa3[(UO2)(CO3)3](SO4)F . 10 H2OSynchisite Ca(Ce,La)(CO3)2F
Urancalcarite Ca(UO2)3(CO3)(OH)6 . 3 H2OVoglite Ca2Cu(UO2)2(CO3)2O3
Widenmannite Pb2(UO2)(CO3)3
Zellerite Ca[(UO2)(CO3)2(H2O)2] . 3 H2O
Znucalite Zn12Ca(UO2)(CO3)3(OH)22 . 4 H2OElements
Copper Cu
Silver Ag
Sulphur S

Halogenides
Chlorargyrite AgCl

Molybdates
Wulfenite PbMoO4

Oxides, Hydroxides
Allophane (amorphous aluminium silicates)
Arsenolite As2O3
Asbolan (Co,Ni)1-y (Mn4+O2)2-x(OH)2-2y-2x . n H2O
Becquerelite Ca(UO2)6O4(OH)6 . 8 H2OBismite Bi2O3
Cervantite Sb3+Sb5+O4
Claudetite As2O3
Compreignacite K2(UO2)6O4(OH)6 . 8 H2OCoronadite Pb(Mn4+, Mn2+)8O16
Cryptomelane K(Mn4+, Mn2+)8O16
Cuprite Cu2O
Goethite FeO(OH)
Hematite Fe2O3
Kermesite Sb2S2O
Masuyite Pb3U8O27 . 10 H2OMetaschoepite UO3 . n H2O, n < 2
Opal SiO2 . n H2O
Psilomelane (amorphous Mn-oxides)
Pyrolusite MnO2
Richetite PbU4O13 . 4H2O
Schoepite [(UO2)8O2(OH)12] . 12 H2OTenorite CuOUranosphaerite Bi2U2O9 . 3 H2O

62

Valentinite Sb2O3
Vandendriesscheite PbU7O22 . 12 H2OWölsendorfite (Pb,Ca)U2O7 . 2 H2O

Phosphates
Apatite Ca5(PO4)3(F,Cl,OH)
Autunite Ca(UO2)2(PO4)2 . 10-12 H2OCarbonate-fluorapatite Ca5(PO4, CO3)3F
Churchite-(Y) YPO4.2 H2OCorkite PbFe3(PO4)(SO4)(OH)6
Dewindtite Pb3(UO2)6H2(PO4)4O4 . 12H2O
Diadochite Fe2(PO4)(SO4)(OH) . 5 H2OGoyazite SrAl3(PO4)2(OH)5 . H2O
Isoclasite Ca2(PO4)(OH) . 2 H2OLibethenite Cu2(PO4)(OH)
Meta-autunite Ca(UO2)2(PO4)2 . 2-6 H2OMetatorbernite Cu(UO2)2(PO4)2 . 8 H2OMrázekite Bi2Cu3(PO4)2O2(OH)2 . 2 H2OParsonsite Pb2(UO2)(PO4)2 . 2 H2OPetitjeanite Bi3O(OH)(PO4)2
Phosphuranylite KCa(H3O)3(UO2)7(PO4)4O4 . 8 H2O
Pseudomalachite Cu5(PO4)2(OH)4
Pyromorphite Pb5(PO4)3Cl
Smrkovecite Bi2O(PO4)(OH)
Torbernite Cu(UO2)2(PO4)2 . 8-12 H2OUranocircite Ba(UO2)2(PO4)2 . 12 H2OUranospathite HAl(UO2)4(PO4)4 . 40 H2O
Vivianite Fe3(PO4)2 . 8 H2O
Vochtenite Fe2+Fe3+[(UO2)(PO4)](OH) . 12-13 H2OYingjiangite K2Ca(UO2)7(PO4)4(OH)6 . 6 H2OSilicate:
Bismutoferrite BiFe2(OH)(SiO4)2
Chrysocolla (Cu,Al)2H2Si2O5(OH)4 . n H2O
Coffinite U(SiO4)1-x . (OH)x
Cuprosklodowskite (H3O)2Cu(UO2)2(SiO4)2 . 2 H2OEulytite Bi4(SiO4)3
Hemimorphite Zn4Si2O7(OH)2 . H2O
Kasolite Pb(UO2)SiO4 . H2O
Sklodowskite (H3O)2Mg(UO2)2(SiO4)2 . 2 H2O
Soddyite (UO2)2SiO4 . 2 H2OTalc Mg3Si4O10(OH)2
Uranophane Ca(UO2)2[SiO3(OH)]2 . 5 H2OUranophane-beta Ca(UO2)2[SiO3(OH)]2 . 5 H2OWeeksite K2(UO2)2Si6O15 . 4 H2OSulphates
Alunogen Al2(SO4)3 . 17 H2OAnglesite PbSO4
Antlerite Cu3(SO4)(OH)4
Apjohnite MnAl2(SO4)4 . 22 H2O
Beaverite Pb2(Cu,Fe,Al)6(SO4)4(OH)12
Bieberite CoSO4 . 7 H2OJournal of the Czech Geological Society, 42/4 (1997)

Brochantite Cu4(OH)6SO4
Chalcanthite CuSO4 . 5 H2OChvaleticeite (Mn, Mg)SO4 . 6 H2O
Copiapite Fe2+Fe3+4(SO4)6(OH)2 . 20 H2OCoquimbite Fe2(SO4)3 . 9 H2O
Devilline CaCu4(SO4)2(OH)6 . 3 H2O
Epsomite MgSO4 . 7 H2OFerrohexahydrite FeSO4 . 6 H2OGoslarite ZnSO4 . 7 H2OGunningite-Szomolnikite (Zn,Mn)SO4 . H2O, FeSO4 . H2O
Gypsum CaSO4 . 2 H2OHalotrichite FeAl2(SO4)4 . 22 H2OHexahydrite MgSO4 . 6 H2OHydronium jarosite (H3O)Fe3(SO4)2(OH)6
Jáchymovite (UO2)(SO4)(OH)14 . 13 H2OJarosite KFe3(SO4)2(OH)6
Johannite Cu[(UO2)2(SO4)2(OH)2] . 8 H2O
Langite Cu4(SO4)(OH)6 . 2 H2OMagnesium-zippeite [Mg(UO2)2(SO4)(OH)4]2 . 3 H2OMelanterite FeSO4 . 7 H2O
Meta-uranopilite (UO2)6(SO4)(OH)10 . 5 H2OMetavoltine K2Na6Fe2+Fe63+(SO4)12O2 . 18 H2O
Moorhouseite CoSO4 . 6 H2OMorenosite NiSO4 . 7 H2ONatrojarosite NaFe3(SO4)2(OH)6
Nickel-zippeite Ni2(UO2)6(SO4)3(OH)10 . 16 H2ONickelhexahydrite NiSO4 . 6 H2OPlumbojarosite PbFe6(SO4)4(OH)12
Posnjakite Cu4(SO4)(OH)6 . H2ORabejacite Ca(UO2)4(SO4)2(OH)6 . 6 H2ORetgersite NiSO4 . 6 H2O
Rhomboclase HFe(SO4)2 . 4 H2ORömerite Fe2+Fe3+2(SO4)4 . 14 H2ORozenite FeSO4 . 4 H2O
Sodium-zippeite Na4(UO2)6(SO4)3(OH)10 . 4 H2OThenardite Na2SO4
Uranopilite (UO2)6(SO4)(OH)10 . 12 H2OZippeite K4(UO2)6(SO4)3(OH)10 . 4 H2OSulphides
Acanthite Ag2S
Orpiment As2S3Pararealgar AsS
Proustite Ag3AsS3

Vanadates
Curienite Pb(UO2)2V2O8. 5H2O
Metatyuyamunite Ca(UO2)2(VO4)2 . 3 H2O
Mottramite PbCuVO4(OH)Namibite Cu(BiO)2(VO4)(OH)
Pucherite BiVO4
Tyuyamunite Ca(UO2)2V2O8 . 5-8 H2O

Journal of the Czech Geological Society, 42/4 (1997)

63

List of all “non-secondary” minerals from the Jáchymov ore district
Primary vein minerals
Acanthite
Alloclasite
Ankerite
Antimony
Argentite
Argentopyrite
Arsenic
Arsenopyrite
BariteBismuth
Bismuthinite
BorniteBreithauptite
CalciteCinnabar
Chalcocite
Chalcopyrite
Clinosafflorite
Cobaltite
Coffinite
DickiteDolomite
Fluorite
GalenaGersdorffite
Glaucodot
Gold
Hematite
Kaolinite
Krutovite
Linnaeite
Löllingite
Luzonite
Manganite
Marcasite
Matildite
Maucherite
Millerite
Molybdenite
Nickeline
Nickel-skutterudite
Orpiment
Pararammelsbergite
Pearceite
Polybasite
Proustite
Pyrargyrite
PyritePyrolusite
Pyrostilpnite
Pyrrhotite
QuartzRammelsbergite
RealgarRhodochrosite
Safflorite
Siderite
Siegenite( * - this study)

[221]
*
[118]
[118]
[239]
[118]
[239]
[59]
[118]
[239]
[239]
[228]
[118]
[239]
[118]
[59]
[239]
*
[118]
[150]
[141]
[239]
[239]
[239]
[118]
[141]
[118]
[59]
[118]
[180]
*
[118]
*
[118]
[239]
[215]
[141]
[239]
[118]
[239]
[118]
[118]
*
[118]
[239]
[239]
[239]
[239]
[118]
[118]
[59]
[239]
*
[239]
[59]
[118]
[239]
*

Ag2S
(Co,Fe)AsS
Ca(Fe,Mg,Mn)(CO3)2
Sb
Ag2S
AgFe2S3
As
FeAsS
BaSO4
Bi
Bi2S3
Cu5FeS4
NiSb
CaCO3
HgS
Cu2S
CuFeS2(Co, Fe, Ni)As2
CoAsS
U(SiO4)1-x(OH)4x
Al2Si2O5(OH)4CaMg(CO3)2
CaF2
PbS
NiAsS
(Co,Fe)AsS
Au
Fe2O3
Al2Si2O5(OH)4
NiAs2
Co3S4
FeAs2
Cu3AsS4
MnO(OH)FeS2AgBiS2
Ni11As8
NiS
MoS2
NiAs
(Ni,Co)As2-3
As2S3
NiAs2
Ag16As2S11(Ag,Cu)16Sb2S11
Ag3AsS3Ag3SbS3
FeS2
MnO2
Ag3SbS3
Fe1-xS
SiO2
NiAs2
AsS
MnCO3
CoAs2
FeCO3
NiCo2S4

SilverSkutterudite
Smithsonite
Smythite
Sphalerite
Stephanite
Sternbergite
Stibnite
Stromayerite
Tennantite
Tetradymite
Tetrahedrite
Uraninite
Violarite
Xanthoconite

[239]
[239]
[118]
*
[239]
[239]
[239]
[59]
*
[59]
[118]
[59]
[239]
*
[59]

Ag
CoAs2-3
ZnCO3
Fe13S16(Zn,Fe)SAg5SbS4
AgFe2S3
Sb2S3
AgCuS(Cu,Fe)12As4S13
Bi2Te2S(Cu,Fe)12Sb4S13
UO2
Fe+2Ni2+3S4
Ag3AsS3

Rock-forming minerals
Actinolite
Amphibole
Analcime
AnataseAnniteApatiteAugiteBiotiteCalciteCassiterite
Chlorite
Diopside
EpidoteGarnetGraphite
Grossular
Magnetite
Muscovite
Natrolite
Oligoclase
OlivineOpal
Orthoclase
Palygorskite
Phillipsite
Prehnite
Pyrolusite
QuartzRutileSanidine
Scapolite
Serpentine
Smectite
Titanite
Topaz
Tourmaline
Vesuvianite
Wolframite
Wollastonite
Xenotime-(Y)Ca2(Mg,Fe)5Si8O22(OH)2[118]
NaCa(Mg,Fe)5Si7AlO22(OH)2[59]
NaAlSi2O6 . H2O
[118]
TiO2
*
KFe3AlSi3O10(OH,F)2
*
Ca5(PO4)3(F,OH,Cl)[118](Ca,Na)(Mg,Fe,Al,Ti)(Si,Al)2O6[118][59] K(Mg,Fe+2)3(Al,Fe+3)Si3O10(OH,F)2
CaCO3
[239]
SnO2
[59]
(Mg,Fe)5Al(Si3Al)O10(OH)8[141]
CaMgSi2O6[118]
Ca2(Al,Fe+3)3(SiO4)3(OH)[59](Mg,Ca,Fe)3(Al,Fe)2(SiO4)3
[59]
C
[118]
Ca3Al2(SiO4)3
[118]
Fe3O4
[59]
Kal2(Si3Al)O10(OH,F)2[59]
Na2Al2Si3O10 . 2H2O
[118]
(Na,Ca)Al(Al,Si)Si2O8[118](Mg,Fe)2SiO4[118]
SiO2 . nH2O
[118]
KalSi3O8[59](Mg,Al)2Si4O10(OH) . 4H2O
[118]
(K,Na,Ca)1-2(Si,Al)8O16 . 6H2O
[118]
Ca2Al2Si3O10(OH)2
[59]
MnO2
[141]
SiO2
[239]
TiO2
[59]
(K,Na)AlSi3O8[118][118] (Na,Ca)4(Si,Al)12O24(Cl,CO3,SO4)(Mg,Al,Fe)2-3(Si,Al,Fe)2O5(OH)4[118](Na,Ca)0.3(Al,Mg)2Si4O10(OH)2.nH2O*
CaTiSiO5[118]
Al2SiO4(F,OH)2[118]
NaFe3Al6(BO3)3Si6O18(OH)4*
Ca10Mg2Al4(SiO4)5(Si2O7)2(OH)4[141](Fe, Mn)WO4[215]
CaSiO3
[141]
YPO4
*

64

Journal of the Czech Geological Society, 42/4 (1997)

Origin and deposition of studied samples
The specimens studied originate from numerous private collections, from several institutional collections:- in the Czech Republic: the National Museum in Prague, the Moravian Museum in Brno, the Faculty of
Science, Masaryk University, Brno, the Institute ofChemistry of Solid Phases of the Chemical-Technical
University in Prague, and the Institute of Geochemistry and Mineralogy of the Faculty of Science, Charles
University in Prague.
- in Austria: Naturhistorisches Museum, Vienna, Landesmuseum Joaneum, Graz,- in Germany: Staatliches Museum für Mineralogie
und Geologie, Dresden, Technische Universität Bergakademie Freiberg, Freiberg.

The private collections and donators of specimens are
too numerous to be listed individually; 80 to 90% of
specimens used and studied originated from private collections. Altogether, several thousand specimens were
inspected and studied, but mineral subsamples wereseparated from a smaller part of the specimens.
In the most favourable cases, several samples from a
specific site were available, including at least the nameof the ore vein. Such sample suites, unfortunately notnumerous and contained mostly in private collections,provided valuable paragenetic information. Specimens
collected in mid-nineteenth century are often accompanied by relatively accurate locality information, including name of the mine and vein, sometimes even level inthe mine.

Lists of studied samples from Jáchymov
Moravian Museum, Brno, Czech Republic (BM)sampleoriginal name (locality, year)

determination

***
A271
A440
A852
A973
A1742
A1769
A1840
B114
B1631
B1725
B2186***

bismuthochre
pharmacolite
pharmacolite
liebigite
pharmacolite
pharmacolite
morenosite Svornost shaft 12th lev.
pharmacolite
liebigite
uranochre
annabergite
bismitescorodite, quartz, phlogopite?, bismite
pharmacolite, picropharmacolite, sainfeldite
pharmacolite, brassite, picropharmacolite
metatorbernite, uranophane
picropharmacolite, köttigite
picropharmacolite
retgersite, arsenolite, annabergite“Mg-villyaellenite”, haidingerite, picropharmacolite
cuprosklodowskite
rabbittite, gypsum
annabergite, millerite** bindheimite, dussertite?, vanadinite?,carminite, beudantite, ogdensburgite?, cerussite, As-tsumebite on tetraedrite
pharmacolite
cuprosklodowskite
picropharmacolite
metatorbernite, torbernite, uranophaneuranophane, zippeite
pharmacolite, picropharmacolite
picropharmacolite
uranophane-beta, quartz, calcite, illite, goethite, smectite
brassite, picropharmacolite
kasoliteliebigite
liebigite, schröckingerite, zellerite
liebigite, zellerite** hedyphane, bayldonite, ogdensburgite ?, arsenogoyazite, stolzite
amorphous, arsenolite
uranophane, uranophane-betaamorphousdewindtite
uranophane, tyuyamunite, meta-autunite
dewindtite, (uranophane, torbernite, sklodowskite)
picropharmacolite
picropharmacolite
devilline
cobaltkoritnigite
uranopilite, masuyite, wölsendorfite, uranophane** variscite
mixiteuranophane-betauranophane-beta

B5252
rösslerite
B6430
johannite
B6868
pharmacolite
B6932
cuprosklodowskite
367
zippeite399
liebigite
1889
pharmacolite
2367
uranophane
2400
wapplerite
3725
Eliášit5264
liebigite
5268
liebigite
5270
liebigite
5701
johannite5749
uranosphaerite, Geister vein
5860
gummite with Uranothallit
5861
Eliášit
5862
gummite with uranochre
5864
uranochre, Eliáš mine
5865
uranochre, Eliáš mine
5920
pharmacolite
5923
pharmacolite
5925
lavendulan
5929
lavendulan, Kobaltblüthe
6106
uranopilite, uranochre
6183
mixite6184
mixite9366
uranophane, Werner shaft
9367
uranophane* - this study** - most probably not from Jáchymov*** - Lichtenstein collectionreferences
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
[237]
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*
*

Journal of the Czech Geological Society, 42/4 (1997)65

National museum, Prague, Czech Republic (NM)sampleoriginal name (locality, year)

determination

2006
2009
4877
4879
4880
4881
4882
4888
4889
4890
4891
4892
4902
4905
4910
4913
12913
12914
15693
15695
15697
15698
15699
15700
15701
15702
15703
16892
17259
17270
17351
17353
17354
17357
17358
17359
17365
19216
19223
24272
25017
25907
25913
26325
26534
26535
26536
26537
26538
26719
27147
27465
27961
28212
29581
29641
29922
30357
30481
32295
33949
36542
37167
37633
37634
38310
38370
38403
38405
39060

johannite
zippeite
Waltherit
Uranothallit
vogliteschröckingerite
schröckingerite
johannitejohannite
zippeite
zippeitelindackerite
pharmacolite
Ganomatit
hemimorphite
gummiteVoltzinVoltzin 1902
cuprosklodowskite

johannite
zippeite
walpurgite
liebigite, rabbittite
vogliteschröckingerite
schröckingerite
johannitejohanniteuranopilite
zippeitelavendulan
Ca-Mg-AsO4(1), picropharmacolite
amorphoushemimorphite
weeksite, + ?
sphalerite
sphalerite
cuprosklodowskite
liebigite
cuprosklodowskite, brochantite
cuprosklodowskite
voglitevogliteschröckingerite, uranophane,schröckingerite, metanováþekite, villyaellenite, weilite, pharmacolite
schröckingerite
anglesite
gunningite - szomolnokite, rhomboclase
annabergite, aragonite, (illite)
uranopilite
johanniteuranopilite
uranopilite
uranopilite
uranopilite
vandendriesscheite, compreignacite, uranophane, kasolite
lavendulan, gypsum
amorphousuranophane, schoepite
liebigite
haidingerite, pharmacolite, weilite
uranophane, uranophane-beta, sklodowskite
uranopilite
cuprosklodowskite
cuprosklodowskite
uranophaneuranophane-betauranophane-beta
metatorbernite
johanniteuranophane-beta
schröckingerite
schröckingerite
schröckingerite
villyallenite, picropharmacolite
uranopilite
liebigite
uranopilite
uranopilite
uranophaneliebigite
zippeiteuranopilite
zippeite
zippeiteuranopilite
uranopilite
liebigite
liebigite

Uranothallit
liebigite
voglitevogliteschröckingerite, 1902
schröckingerite, 1872
schröckingerite
Paterait
morenosite
bieberite 1902
uranopilite
zippeiteuranopilite
uranopilite
uranopilite
zippeiteuranosphaerit 1902
lindackerite 1872
Ganomatit 1902
E-uranopilite
liebigite 1927
haidingerite 1932
Uranotilzippeitecuprosklodowskite
cuprosklodowskite
Uranotil
E-uranotil
uranophane-beta
torbernite
johannite
E-uranotil
schröckingerite
schröckingerite
schröckingerite
haidingerite 1939
uranopilite
uranopilite
zippeite
Uranotilzippeiteschröckingeritereferences
[11]
[35]
*
*
[16]
[10]
[10]
[36], [11][36], [11]
[35]
[35]
*
*
*
*
*
*
*
[7]
[57]
*, [7]
[7]
[16]
[16]
*, [10]*, [10]
[10]
*
*
*
[9]
[11]
[9]
[9]
[9]
[9]
*
*
*
*, [7]*, [57]**, [7]
[9]
[7]
[7]
[7]
*
[7]
[15]
[11]
[7]
[10]
[10]
[10]
*
[9]
[57]
[9]
[9]
[7]
[57]
[57]
[9]
[57]
[57]
[9]
[57]
[10]
[57]

To be continued

66

Journal of the Czech Geological Society, 42/4 (1997)Cont.
sample
41443
43410
43865
43866
43867
43872
43873
44797
45149
45157
45158
45159
45160
45161
45162
45163
45164
45165
45168
45170
45171
45172
45173
45180
45181
45182
45183
45208
45225
45562
48847
48975
49191
49298
51527
59707
68905
70241
71021
71624
71668
73554
* - This study

original name (locality, year)

determination

schröckingerite
Uranotilschröckingerite
uranophane-beta
zippeiteuranopilite
zippeiteuranopilite
uranopilite
uranopilite
metatorbernite
schröckingerite
liebigite
liebigite
cuprosklodowskite
liebigite
cuprosklodowskite
cuprosklodowskite
liebigite
liebigite
cuprosklodowskite
voglite ?
johannite
voglitearsenolite, skutterudite, chalcopyrite, moorhouseite
cuprosklodowskite
vogliteschröckingerite
uranophaneuranophane-beta
metatorbernite
cuprosklodowskite
liebigiteschröckingerite
cuprosklodowskite
cuprosklodowskite
cuprosklodowskite
kermesitejáchymovite
uranophaneuranophaneliebigite
zippeiteuranopilite

uranopilite

uranopilite
liebigiteschröckingerite
schröckingerite
schröckingerite
cuprosklodowskite
schröckingerite
cuprosklodowskite
cuprosklodowskite
schröckingerite
schröckingerite
cuprosklodowskite
schröckingerite
johannite
voglitePaterait
cuprosklodowskite
vogliteschröckingerite
sklodowskite
Uranotil
voglitecuprosklodowskite
schröckingerite
cuprosklodowskite
cuprosklodowskite
cuprosklodowskite
kermesitejáchymovite
Uranotil
Uranotilzippeite

Faculty of Science, Masaryk University, Brno, Czech Republic (BU)
sampleoriginal name (locality, year)

determination

1724
4947

pharmacolite 1923
kerargyrite

picropharmacolite
chlorargyrite, acanthite, illite

Institute of Chemical Techonology, Prague, Czech Republic (VS)sample738
829
1819
9294 (3849)
9293
10072
11683
11684
12694
12695
12698
12808
14291
14545
15628
15828
15987
19256
19352
20072
20247
20780

original name (locality, year)

determination

uranopilite (939)
Nasturan with Uranothallit
schröckingerite and Uranothallit
Uranothallit
lindackerite
zippeiteuranopilite
cuprosklodowskite
cuprosklodowskite
schröckingerite
zippeiteuranopilite
pharmacolite
zippeite
Uranothallit
zippeitecuprosklodowskite
liebigite
zippeite 1871
cuprosklodowskite
zippeite with uranopilite

schoepite
weeksite, zippeite
liebigite, schröckingerite
zellerite, liebigite, uranophane
zellerite, liebigite
amorphous
zippeite+UO3-SO3-H2O(1)uranopilite, vandendriesscheite
cuprosklodowskite, zeunerite
cuprosklodowskite
meta-uranospinite, novacekite-20A, schröckingerite
jáchymovite, zippeite
uranopilite
weilite, pharmacolite
zippeite
rabbittite, liebigite, urancalcarite, zellerite, metazellerite
zippeitecuprosklodowskite, compreignacite, UO3. nH2O(2), zeunerite
liebigite
zippeite+UO3-SO3-H2O(1)compreignacite, cuprosklodowskite
zippeite, compreignacite, sklodowskitereferences
[10]
[7]
[57]
[18]
[57]
[57]
[57]
[9]
[16], [57]
[10]
[10]
[10]
[7]
[10]
[7]
[7]
[10]
[10]
[7]
[10]
[11]
[16], [57]*[7][16], [57][10], [57]
[7]
[7]
*
[7]
[57]
[10]
[7]
[7]
[7]
*
[18]
[7]
[7]
[57]
[57]
[9]

Journal of the Czech Geological Society, 42/4 (1997)

67

Faculty of Science, Charles University, Prague, Czech Republic (PF)sampleoriginal name (locality, year)

determination

2859
2882
3884
3912
6058
6470
6968
10068
10137
10415
10774
11541
11542
11729
15622
15623
15869
16237
16249
19825
20851

mixiteuranopilite 1882
uranopilite 1887 (sample 1. and 2.)
Uranothallit 1887
zeunerite 1915
Uranothallit 1915
zippeite 1918
uranopilite 1934
cuprosklodowskite (Uranochalcit)
schröckingerite 1938
Uranothallit
zippeite, Saxony-noble-men adit 1946
zippeite, Saxony-noble-men adit 1946
zippeite, Werner shaft 1957
gummite, Rother vein, Werner shaft 1899
gummite, Rother vein, Werner shaft 1899
voglite, Eliáš mine 1854
mixite, Geister vein, Geister shaft 6th lev. 1883
zeunerite, uranophane
Zippeite
Ganomatit (Kobaltblüthe) 1853

mixite, “phosphate-walpurgite”
yingjiangite or (phospuranylite ?), uranophane
1. rabejacite, 2. uranopilite
liebigite, zellerite
autunite, meta-autunite, metatorbernite, metanováþekite?
"kalium-schröckingerite", liebigite
zippeiteuranopilite
cuprosklodowskite, torbernitenováþekite, metanováþekite
liebigite, zellerite
zippeite
zippeite
zippeitegummitegummitelindackerite
mixite, walpurgite, metazeunerite
uranophane, zeunerite, metatorbernitenováþekite ?, metanováþekite ?
pharmacosiderite

Naturhistorisches Museum, Vienna, Austria (WM)
sampleoriginal name (locality, year)

determination

D3533
4538

voglite, 1886
voglitecuprosklodowskite, compreignacite
vogliteLandesmuseum Joaneum, Graz, Austria (JG)
sampleoriginal name (locality, year)

determination

452
453
1656
1713
3403
9076
9805
13140
13141
13142
13143
13144
13145
13146
14714
14716
35519
38117
38717
38829
39257
75479

Frieseit
Frieseit
voglitePaterait 1939
uranochre, Urangrün, johannite
pitchblende with uranochre 1923
uranochre, uranopilite
johannitejohannitejohannite, 1869/70
johannite
zippeite
zippeite
zippeitejohannite
voglite Eliáš mine, Glüchsgang 1859/60
bismuthinite 1859 - 60
erythrite
erythrite

pyrite, marcasite
hematitevoglitearsenolite, skutterudite, erythrite
cuprosklodowskite, jáchymovite
schröckingerite
torbernite, nováþekite, metanováþekite
schröckingerite, liebigite, uranophane
zellerite, schröckingerite
uranospinite, meta-uranospinite, liebigite, schröckingerite
cuprosklodowskite, uranopilite
uranopilite
uranopilite
uranopilite
cuprosklodowskite
voglite.
"phosphor-walpurgite", torbernite
erythrite
arsenolite, erythriterozenite
zippeite, uranopilite
lindackerite, parasymplesite, lavendulan, erythriteuranopilite
lindackerite

Das mineralogische Museum der Wiener Universität, Viena, Austria
sampleoriginal name (locality, year)

8874
8875

determination
gummit, torbernit, uranofan
uranin, torbernit, uranofan

references
[39]
[39]

TU Bergakademie Freiberg, Freiberg, Germany
sample
10957
16347
16348
20865
* - This study

original name (locality, year)

determination

picropharmacolite
voglite, Fluther vein
voglite, Eliáš mine, 1852
wapplerite, pharmacolite

brassite, pharmacolite
voglitevoglitebrassitereferences
[237]
*
*
[237]

68

Journal of the Czech Geological Society, 42/4 (1997)

Staatliches Museum für Mineralogie und Geologie, Dresden, Germany (DD)sampleoriginal name (locality, year)

determination

2497 Ba2498 Ba
2499 Ba/A
2556 Ba
2557 Ba
6306
7025
7026
7027
7028
7035
7676
13495
14865
15020

zippeite with annabergite
zippeite
zippeiteuranochre with eliasit
uranochrevoglitezippeite, uranopilite
zippeite (medjidit)
zippeite
zippeiteuranochre (zippeite with gypsum)
uranopilite on eliasit
uranochreuranochre with uranothallite
zippeite (Uranblüthe)uranopilite, cuprosklodowskite
sodium-zippeite?,uranophan?, liebigite?
"Mn-zippeite"
massuite, smectite, ?
uranophane, massuite?
vogliteuranopilite
metaschoepite
zippeite
zippeite, uranopilite
uranopilite
uranophane, cuprosklodowskite, vandendriesscheite
cuprosklodowskite, antlerite
liebigite
uranopilite, zippeite, johannite

Harvard University, Cambridge, MA, USA
sampleoriginal name (locality, year)

determination

977
94861

trögerite
uranothallite

trögerite ?
liebigitereferences[8][5]

Department of Mineral Sciences, National Museum of Natural History, Smithsonian Institution, Washington DC, USA
sampleoriginal name (locality, year)

isoklasite
R 2763voglite52057
uranothalite
83971
walpurgite
84651
uranopilite
R - Roebling collection² - missing from the collection (P. Dunn, privat com. )determination
liebigite
liebigite
walpurgite
uranopilite

references[162]²
[34]
[162]
[162]
[162]

Musée Royal de l´Afrique Centrale, Tervuren, Belgium
sampleoriginal name (locality, year)

determination

RGM 13 390

voglitevoglitereferences[42]

Muséum National d´Histoire Naturelle, Paris, France
sampleoriginal name (locality, year)

determinationreferences

61-10
54 391
99 49899 706
99 978104 116106 611
108 660
108 980lavendulan
lindackerite
lavendulan
lindackerite
lindackerite
lindackerite
lindackerite
lavendulan
lavendulan

lavendulan
lindackerite
lavendulan
lindackerite
lindackerite
lindackerite
lindackerite
lavendulan
lavendulan

[152]
[152]
[152]
[152]
[152]
[152]
[152]
[152]
[152]

Laboratoire de Minéralogie de la Sorbonne, Paris, France
sampleoriginal name (locality, year)

determinationreferencesLa, 2
Li. 53 331
LIND. 5305 L
310, P
371
383
53 363lavendulan
lindackerite
lindackerite
lavendulan
lavendulan
lavendulan
lindackerite
lavendulan

lavendulan
lindackerite
lindackerite
lavendulan
lavendulan
lavendulan
lindackerite
lavendulan

[152]
[152]
[152]
[152]
[152]
[152]
[152]
[152]

references

École Nationale Supérieure des Mines, Paris, France
sampleoriginal name (locality, year)

determination

14
20
1963

haidingerite
pharmacolite, haidingerite
pharmacolite

brassite, haidingerite
brassite, weilite, haidingerite, pharmacolite, rauenthalite
brassite (type)

[237]
[237]
[237]

Journal of the Czech Geological Society, 42/4 (1997)

Conclusions
The present publication contains results of four year
project of detailed study of secondary minerals and their
genetic relations in the Jáchymov ore district.
The papers deals with results of new study. The total
number of valid secondary mineral species describedfrom Jáchymov in the literature (70 minerals), was increased by the present study to 207 (plus 30 new secondary phases). For this reason, characteristics of minerals
is given in alphabetic order. Besides new own data, thesystematic part presents also reliable data taken from theliterature. This made it possible to give a complete review of contemporaneous knowledge of secondary minerals in this district.
The extent of data does not permit to mention individually minerals newly identified in this district. In thecourse of the project, approximately 300 specimens wereanalysed using instrumental qualitative chemical analysis and studied by X-ray powder diffraction. Unit-cellparameters were calculated for 90 minerals. This resulted
in proposals of alternative unit-cells for some minerals
and in alternative indexing of diffractions. New quantitative chemical analyses were calculated to emiprical formulae and published analyses were recalculated.
The main emphasy of the project was not primarily
on increasing the number of identified secondary mineral69

to 207 species. Registration of mineral distribution, theirsuccession, and coexistence of secondary minerals in
Jáchymov were considered as important topics. The
present publication brings significant new information inthis respect. The information is used for interpretation of
weathering conditions and processes resulting in crystallisation of secondary minerals. In the context of chemical and mineralogical composition of ore veins, pH conditions, humidity, and temperature, it is possible to predict to some extent formation of some paragenetic
groups of minerals. It is typical for the Jáchymov district
that the secondary minerals form under conditions ofhigh acidity, resulting from the presence of free sulphuric
and arsenic acid, which derive from quick decompositionof sulphides, arsenide-sulphides, arsenides, and native
arsenic. The low content of carbonates in veins is a contributing factor. These conditions are responsible forprevalence of acidic secondary minerals. The variability
in composition of ore veins also contributed to the multitude of secondary minerals.
The data presented in this study and the fact that 308
ore and non-ore minerals were found in Jáchymov showthat this locality ranks with mineralogically most profilic
localities (as far as number of mineral species is concerned), such as Franklin, Langban, or Saint Marie aux
Mines.