Journal of the Czech Geological Society 51/12(2006)

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The Krásno Sn-W ore district near Horní Slavkov: mining history,geological and mineralogical characteristics
Sn-W rudní revír Krásno u Horního Slavkova  historie tìby, geologickáa mineralogická charakteristika(47 figs, 1 tab)
PAVEL BERAN1  JIØÍ SEJKORA2
1
2

Regional Museum Sokolov, Zámecká 1, Sokolov, CZ-356 00, Czech Republic
Department of Mineralogy and Petrology, National Museum, Václavské nám. 68, Prague 1, CZ-115 79, Czech Republic

The tin-tungsten Krásno ore district near Horní Slavkov (Slavkovský les area, western Bohemia) belongs to the most important areas ofancient mining in the Czech Republic. The exceptionally rich and variable mineral associations, and the high number of mineral species,
make this area one of the most remarkable mineralogical localities on a worldwide scale. The present paper reviews the data on geologicalsetting of the ore district, individual ore deposits and mining history. Horní Slavkov and Krásno were known as a rich source of exquisite
quality mineral specimens stored in numerous museum collections throughout Europe. The old museum specimens are often known under
the German locality names of Schlaggenwald (= Horní Slavkov) and Schönfeld (=Krásno). The megascopic properties and paragenetic
position of selected mineral classics are reviewed which include arsenopyrite, fluorapatite, fluorite, hübnerite, chalcopyrite, carpholite,
cassiterite, quartz, molybdenite, rhodochrosite, sphalerite, topaz and scheelite.
Key words: Sn-W ores; tin-tungsten mineralization; mining history; ore geology; mineralogy; Slavkovský les; Krásno, Horní Slavkov ore
district; Czech Republic.

Introduction
In the mining history of Central Europe, Bohemia andMoravia are known as important source of gold, silver,tin, and iron. Later on, uranium and other metals were
exploited. The medieval mining activities gave rise to
several mining centres in the Kingdom of Bohemia suchas Kutná Hora, Jílové near Praha (Prague), Jáchymov,
Pøíbram and also the Horní Slavkov  Krásno mining district (Fig. 1).
The Krásno district is located near Horní Slavkov in
the Slavkovský les renowned in the past by rich depositsof tin, silver, bismuth, and uranium. The district is represented by mineralization in several granite cupolas ofthe large Kruné hory (Erzgebirge) granite batholith, underlying metamorphic rocks of the Slavkov gneissblock. The Krásno district comprises several deposits,
such as the Huber stock (Hub stock in some publications),
Schnöd stock, Gellnauer elevation and the Gellnauer setof veins (Gellnau in some publications). It represents themost important concentrations of Sn-W ores in the Slavkovský les area.

valleys dissected parts of the area. In the ore district area,
the detailed surface morphology is modified by large depressions caused by the collapse of old undergroundworkings and by extensive dumps. The average altitude
around the deposit is 620 m. A single natural drainage in
the area, the Slavkov brook, was modified in the Middle
Ages to a channel for the transport of wood to the mines.
In the postwar period the Krásno mining area of
240.9 ha in total, has been claimed for exploitation of tin

Topography
The Krásno ore district is located at a distance of about
1 km of Krásno nad Teplou (old name Schönfeld) and 2
km of Horní Slavkov (old name Schlaggenwald) (Fig. 2).
The ore district is located in the Slavkovský les elevatedupland area. The undulating leveled surface attains anaverage altitude of 800 m. At the west, it nearly borders
the Bohemian Forest hills and at the east it joins the Teplá
Upland. The highest elevations in the Slavkovský les areLesný (981 m) and Lysina (978 m) hills. Deeply incised

Fig. 1 Sketch map displaying the geographical localization of the
Krásno ore district (black square).

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Journal of the Czech Geological Society 51/12(2006)

History of ore mining before the 17th century

Fig. 2 A map showing the Sn-W deposits and occurrences in the Krásno
 Horní Slavkov area

and tungsten ores, by ruling of February 11, 1961, with
cassiterite, wolframite and chalcopyrite as ore minerals.
The mining of tin and tungsten ores was terminated in
January 1991. The Rudné doly Pøíbram n.p. enterprise(incorporated later on into DIAMO s.p.) was appointed
to administer the Krásno deposit. The mining of uranium ores was active throughout 1948 to 1962 in proximity of the Krásno Sn-W deposit. The exploitation of uranium ores terminated in 1963. In 1992, a mining area offeldspar, of 16.9 ha in extent, was defined being administered by the KMK Granit s.r.o. Company. Since 1991
the area Horní Slavkov  Krásno  Èistá was claimed
as a protected ore deposit area with Sn-W ores and feldspar raw material, 3155 ha in extent and it is administered by DIAMO s.p. (sine 1995).
History of mining in the Slavkovský les area
The mining history of tin deposits in the Slavkovský lesarea can be described in three main periods: before 17th
century, 18th to 20th century, and the period after 1945.

The first reliable written record of tin export from the
Krásno area to western Europe and eastern markets is by
an Arab merchant Ibrahim ibn Jakub, dated 965966.
Prior to underground tin mining in the area of Slavkovský
les, cassiterite was exploited from alluvial deposits as early as the middle part of the second millenium before
Christ (Majer  Jangl 1995). Since the 13th century, tin
production existed due to the exploitation of primary deposits. The mining was centred at Krásno and Horní
Slavkov, the towns obtained mining town status in 1355
1356. A major extension of tin mining occurred earlyin the 16th century, particularly as the Huber stock was
discovered in 1516. At that time, silver ore was minedin several ore veins near Horní Slavkov, which resulted
in establishing a coin-minting office in Horní Slavkov
during 15261527. In support of mining activities, themine owner Jan Pluh of Rabtejn issued mining rules forsilver mines in 1507 and for tin mines in 1509. During15171541 the regulations were supplemented by several additional rules. In 1548 these regulations were declared as Kings regulation obligatory for all mines in the
Slavkovský les area.
The regulations specified methods of granting concessions, supervision of mining methods, specification ofdimensions of underground workings and duties of mining administration. In addition to the Horní Slavkov 
Krásno deposits, tin mining proceeded at some othernearby locations including Èistá and Prameny. The mining kept intensifying during the 40s and 50s of the 16th
century, with an average annual production of 400500
tons of tin. The mining was concentrated at the Huber
stock in some vein zones, and main tin-bearing veins.
Since 1548 the exploitation of the Schnöd stock started.
The regular mining was supported by steady demand fortin, especially in Germany, as testified that major tin traders from southern Germany used to pay supplies in advance. Owing to quality and favourable pricing, tin fromthe Horní Slavkov district dominated in the markets ofwestern Europe and in the first half of the 16th century
its export nearly replaced tin produced in Devon and
Cornwall of England.
The permanent increase of tin mining in the Horní
Slavkov district was adversely affected by war conflictsin 1546 1547 and introduction by King of tin monopoly during the years 15501555. These developments disrupted established export ties and resulted in the declineof mines. To boost the mine production, Krásno andHorní Slavkov were granted in 1547 the status of freemining towns. The same status was granted to Èistá in1551. The discovery of the Schnöd stock in 1548 resulted in increased ore production. However, several events
during the 60s of the 16th century caused mining decline
such as civil war in France in 1562 and liberation war in
the Netherlands against Spanish occupation in 1567. In
the same year, an extensive fire demaged 200 houses in-Journal of the Czech Geological Society 51/12(2006)

cluding some public buildings in Horní Slavkov. In 1568
a major collapse of underground workings in the Huber
stock occurred, followed shortly by a similar disaster in
the Schnöd stock (Beran et al. 2001). Increase of living
costs and expenses of mining characterized the following decades. Several mining ventures, both at the Huber
and Schnöd stocks, had to apply for the financial support at the Kings Czech Chamber  the highest economic
institution in the country. The support was urgently needed for continued work on the major drainage adits.
During the following period from 1603 to 1620 decline
in mining continued. Only 55 miners and 9 supervising
personell were employed. The mining at Èistá wasstopped in 1630 for a long time. Only during 60s of 17th
century, the state (Kings) administration supported renewal of mining in the district. The support was directed at sinking a water-drainage shaft. Realization of thisproject permitted to exploitate deeper mineralized partsof the Huber stock. Late in the 17th century, mining was
also renewed at Èistá and some other locations in the
Slavkovský les area (sine 1995).
All major veins and disseminated tin deposits werediscovered during the period from 12th to the middle of
16th century. Early exploitation focused on cassiterite ores
containing 8.510 wt. % Sn. Later on, metal content
dropped to an average of 1.52 % Sn and around 1700
tin content of the ore decreased to 0.20.5 %. Silver-bearing veins in proximity of Horní Slavkov were discoveredand exploited early in 16th century. Tin deposits weremined by shafts and inclines with galleries. Early workings especially at the Huber and Schnöd stocks were rather chaotic, without properly designed plan. Since about
1550 a tendency prevailed to a unified concept of mining.
Four or five shafts served for ore exploitation while one
shaft was used for ventilation. Two water-drainage shafts
have been sunken beyond the periphery of the deposit. Thissystem was in operation for a long time, but another drainage shaft was sunken in 1669 (Majer  Jangl 1995).
Adits provided access to some parts of deposits depending mainly on the terrain morphology. Such adits
were made during the late 14th century at Horní Slavkov
and Krásno and also later at other places like Vysoký
Kámen, Klinge, and Vlèí hills, Huber, Kladská (11 km
southwest of Krásno), Èistá, and Prameny. Some prominent workings around Krásno include Stará tola, Jiøská,Tìaøská, Pluhova, and Schnöd adits. The Pluhova adit
(Fig. 3) was important for the whole ore district, as it wasconnected to numerous older workings and was used till
uranium mining period in the 20th century (Fig. 4). In a
total length of 5.92 km, it is functional even at the present
time (Majer  Jangl 1995).
Mining methods used at tin deposits were comparable to those used at other vein-type ore deposits. However, a different system of narrow adits and chambers(Fig. 5) was used in exploitation of dispersed tin mineralization. The chambers were usually 1015 m high andwide. Some chambers at the Huber stock and at Èistá

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were 3040 m long, 1020 m wide and 1520 m inheight. Miners used fire at tunnel faces and chambers to
disintegrate rocks. Hammers, wedges and crowbars wereused to cut the rock. A single miner produced 2530
metric cents of rock per week, or 4045 cents underfavourable conditions. In narrow adits of a profile ofFig. 3 The Pluhova adit in the area of Schnöd stock, VIIth level of Vilém
mine (photo P. Beran, 1984).

Fig. 4 Memorial plate at the entrance of the Pluhova adit, about 1539
(photo P. Uhlík).

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Fig. 5 Large chamber from 16th century above level 500 m a.s.l. (photo K. Mlynaøík 1975).

170×50 cm, a single miner progressed by 30 cm per week
(Majer  Jangl 1995).
Mine corridors used to be ventilated by spontaneous
drought as some shafts served for ventilation. Adits wereventilated using chimneys and galleries interconnecting
adits at various levels. The Kophan shaft and the Pluhadit served for ventilation from 1602 till the end of the
17th century. A series of water-drainage adits and two or
three shafts serving for water pumping, located outside
the Huber stock, were used for draining the mines. The
pumps were powered by water. The Huber stock was
drained to a level of 200 m and the Schnöd stock, Èistá
and Prameny deposits to a depth of 100 m. At mine workings, where gravitational drainage via adits was impossible, pumping by horse-gear or pumps powered by water were used. Water wheels 3 to 14.5 m in diameter
served to power pumps with efficiency of up to 1 000 m3
per week (sine 1995).
Sufficient and regular water supply was important formine operations. By the end of the 14th century, a channel from Rota River was constructed and a new channel called Dlouhá stoka was put in operation in 1531
1536. Later on, the channel was connected to five large
ponds and 13 smaller reservoirs with a total capacity of
630 000 m3 (Majer 1970).
There was a high demand for wood used for mine timbering, constructions in pumping shafts etc. Large forest
areas around Beèov were selected for free wood supply
for mines. Uncontrolled wood usage resulted in removalof forests for a long distance from Horní Slavkov. The

Journal of the Czech Geological Society 51/12(2006)

wood supplies during early stage of extensive tin mining are estimated to equivalent of 300 hectars of forest
per year. By the end of the 16th century, wood was transported to Horní Slavkov from distances of 30 km. Large
quantities of wood were used in tin smelting.
In order to obtain high-grade concentrate, ore used tobe crushed manually by hammers and ground on manual
mills. Since the 15th century, crushers powered by water
were introduced. Crushing in water was practicised tominimize the metal loss in fine powder fraction. Whenneeded, ore was roasted and washed using sluices. Laterin the 16 th century, 96 ore processing sites operated
around Krásno and Horní Slavkov. Annual production ofa stamper in the 16th and 17th century is estimated at 6501000 tons of ore (Majer  Jangl 1995).
The intensity of mining in the Slavkovský les area
during the 14th to 17th centuries was influenced by a variety of operational, economic, and political factors. Nevertheless, mining areas mainly around Krásno and Horní
Slavkov (Fig. 6) produced about 60 000 tons of metal for
respective period. The accuracy of the estimate is affected by the absence of reliable data for the period from1300 to 1500. About 77 % of the total quantity was produced in the Krásno district. The tin price depended on
the foreign competition and demand, and on various political factors. The prolonged mining activities in the
Slavkovský les area contributed to legislature and innovations in technologies.
Mining history in 18th20th century
This period represents an important era in tin mining in
the Slavkovský les area (Figs 710). Private investors
operated mines in the Krásno district. During early stages of this period, tin production was sufficient to cover
operation costs. In middle of 18th century, the extent ofunderground workings surpassed the proportion of economic feasibility. Although the Huber and Schnöd stocks
and dispersed mineralization contained sufficient ore reserves, mining became uneconomic. Unlike some major
silver mining districts in Bohemia (Kutná Hora, Jáchymov, Pøíbram), important for the state as the sources forsilver coin minting, tin mining did not enjoy permanentstate support. Interests in tin and later in tungsten production proved to be episodic and depended mainly onarmament production.
Five-times during this period, state intervened by significant investments to increase production: in 70s of the
18th century, in early and middle parts of the 19th century
and during the World Wars One and Two. During these
periods, the previous investments and technical innovations financed by state proved insufficient to continue
economic production. Private operators continued mining but activity was often limited to cheeper picking ofore leftovers at upper levels, exploitation of small veinsand even ore collecting at old dumps. State often continued in financing the most urgent operations such asJournal of the Czech Geological Society 51/12(2006)

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Fig. 6 Historical mapof mines between Krásno and Horní Slavkov,
1699 (District Archive
Jindøichovice, photo
L. Vondráek).

Fig. 7 Mine map of the Krásno ore district, 1756 (Central State Archive, Praha, photo L. Vondráek).

Fig. 8 Mine map of the Krásno ore district, 1768 (Central State Archive, Praha, photo L. Vondráek).

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Ore mining after 1945

Fig. 9 Huber stock, Krásno, 1820 (District Archive Jindøichovice, photo
L. Vondráek).

Fig. 10 Kreuz-zech mine, Krásno, 1906 (Archive of the Sokolov
Regional Museum, photo P. Beran).

maintenance of major adits, water-pumping installations
etc. (Beran et al. 2001).
A limited extent of manufacture and industrial enterprizing in the 18th century was a factor in tin price and mining economy. Tin consumption in the production of tin
kitchenware and white metal sheets was relatively low.
Production from some other mines in the Bohemian partof the Kruné hory/Erzgebirge, e.g. Krupka, Høebeèná andHorní Blatná mines, and imports (or smuggling) of cheap
tin from Saxony competed for the limited market. During
the 19th century industrial production increased but thisdevelopment was accompanied by expansion of road andrailway network for the transportation of goods. At thesame time, these factors improved transport conditions forimports of cheap tin from South-eastern Asia and Bolivia. Local tin mining could not resist competion and mining ceased in middle 19th century. The continued tin production at Krupka was based on processing of old tin
products and benefication of raw tin from overseas. It became clear that tin mining in the Horní Slavkov district
could continue only in absence of competion or under thecondition that tin price would not be compared with theprices on the world market (Majer  Jangl 1995).

The mining history after 1945 is closely tied with thechange of political situation in former Czechoslovakia.
By paragraph § 12 of the decree by the President of the
Republic of October 24, 1945, No. 100 Sb., nationalization of mines and some industrial enterprises was declared, and following the agreement of the Minister offinance and Minister of industry according to § 1 of theGovernment ruling of January 15, 1946, No. 6 Sb., thePøíbramské rudné doly, national enterprise, was established. Also, by § 12 and § 13 of the Presidents decree
No. 100/1945 Sb. and § 1 to § 17 of government ruling
No. 6/1946, the Czechoslovak state as of January 1, 1946
tranfered property from the nationalized enterprises andstate enterprises to the Pøíbram rudné doly, národní podnik national enterprise (sine 1995). The properties of enumerated national enterprises included mines and processing plants for Sn-W ore, including Krásno and Horní
Slavkov. Thus, after 1945, exploitation in the Slavkovský
les area, including the Krásno ore district, was conductedby the Pøíbram rudné doly enterprise, which was in 2001
incorporated into DIAMO s. p. enterprise.
Shortly after 1945, mining of Sn-W ores proceeded ona small scale at the Schnöd stock, opened by the Vilém
shaft. An extensive prospecting program for uranium ores
started as early as 1946. Uranium minerals occurred in
the hydrothermal veins, which intersect metamorphic
rocks around granite intrusions. In 1948, extensive uranium exploitation started at the Horní Slavkov ore district. During a short time, 26 shafts were sunken, 135 kmof connecting galleries and 228 km of galleries following the ore veins were constructed in relatively small
area. After extraction of 2 668 tons of uranium, the mining in the Slavkov uranium district gradually ceased during 19611963. The uranium district did not extend into
Sn-W mines and thus after termination of uranium mining, galleries reaching into the Sn-W mines were sealed.
A systematic opening of the Huber stock in 1957
marked the beginnings of mining of Sn-W ores on a larger scale. Opening workings started from the 4th level ofthe shaft No. 9 of the former uranium mines. In the courseof a tunnel excavation in November 1959, the flood bywaters from the old mine working, estimated to a total of
100 000 m3 occurred. This event resulted in draining of
the water from the Huber stock. After removing damages
resulting from the flood, mine opening workings, preparations, and exploration continued till 1965.
Calculation of ore reserves at the Huber stock wascompleted and presented in 1966 and at the same timethe mining of ore started.
In 1968 the investment venture Opening of the Huber stock was proposed and approved in 1970 by the decision of the Goverment of Czechoslovakia and the Directors Board of Ore Mines and Magnesite Enterprises
in Bratislava. In the frame of the first stage (19711973)

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Fig. 11 The Huber shaft of Stannum mine (photo P. Beran, 1988).

new main Huber exploitation shaft (Fig. 11) was constructed, till 1982 (second and third stage) the originalore dressing plant with a capacity of 100 000 tons wasreconstructed and a new dressing plant with a capacityof 200 000 tons was built (sine 1995). These investments,
together with underground workings and preparation ofore blocks for exploitation, were planned to the mining
and processing of 300 000 tons of Sn-W ore per year.
The new Huber (Stannum) exploitation shaft at an altitude of 620 m a.s.l. opened the deposit by levels at 50 m
intervals. The 4th level (475 m a.s.l.), the 5th level (425
m a.s.l.), and two additional levels at 500 and 455 m a.s.l.
served as the main exploitation horizons. Besides the newlevels Nos. 4 and 5 in the new Huber shaft, old levels(with intervals of 15 m) were utilized from the Vilém
shaft for the mining of the Schnöd stock. Owing to thissituation, the Xth level of the Vilém shaft was approximately at 485 m a.s.l., i.e. above the 4th level newly constructed from the Huber shaft.
At this time, unified names for the ore deposits in the
district were proposed. The whole area is named Horní
Slavkov  Krásno  Èistá ore district. It includes the main
deposits as well as smaller showings of Sn-W ores. By
administrative decision, the Huber stock and Schnöd
stock deposits, together with adjacent area, were named

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Krásno ore district. It includes Krásno and Horní Slavkov ore districts, except the Vysoký Kámen (greisen) and
Vysoký Kámen (feldspar) deposits.
In the last period of mining in the Krásno ore district(19841989) large investments aimed to production of
300 000 tons of crude ore per year were done. This included mainly new construction of ventilation shaft,large-diameter ventilation drillholes and introduction ofmining machines without rails. Although by the end of
80s of the 20th century the mining of some large and rich
deposit parts was possible, the planned goal of 300 kt wasnever achieved and in 1989 and 1990 the amount of mined
ore was 200 kt per year. Better results were hampered
mainly by irregular ore distribution and collapsed domains
resulting from old mining but containing rich ore. Below
the 4th level of the mine, the ore blocks were mainly at the
granite endocontact and were of smaller sizes.
The exploited ore after crushing and milling was gravity-separated and passed through flotation to remove Cu
and Zn sulfides. The Cu-Zn concentrate was treated in
the base-metal plant at Krompachy (Slovakia). Sn-W concentrate was separated electromagnetically. Metalimex
state enterprise exported the concentrates for metal extraction to Great Britain and later to Freiberg in Germany.
The mining in the Krásno ore district terminated for
economic reasons in January 1991. For the production of
one ton of tin metal, with the retail price of 157 000
Czechoslovak crowns, a support of additional 357 000
crowns was provided from the state budget (sine 1995).
Within the project of the mine closure, a (12 m2) drainage adit, 1050 m long, was made (Fig. 12), collecting thewater both from tin and uranium underground workings.
The water is treated in the processing plant at Nadlesí toremove radioactive components and particularly iron,
before release into the surface drainage system. According to the mine closure plan, surface constructions of themines were in part removed and in part transfered to otherorganizations for alternative use. In the area of the Vilém
mine (Figs 1314), a Mining Museum shows history ofmining in a wider area (Fig. 15), including the nearby
Sokolov region. The mine was flooded and the surface
marks of mining were removed. The Krásno ore district
and nearby places host considerable quantities of tin, estimated at 60 thousand tons of tin metal in geologic reserves, including nearly 14 million tons of ore reserves.
Geology of the ore district
The Krásno ore district belongs to the Kruné hory Thuringia area of the Saxothuringian Zone of the
Variscan orogenic belt. The Kruné hory (Erzgebirge)
granite batholith, represented in the northern part of the
Slavkovský les by the Karlovy Vary Massif, together with
its envelope of metamorphic rocks, belongs to the above
given unit. Granitoids of the Karlovy Vary massif areclassified into an older igneous complex (OIC) mainlyof biotite calc-alkali monzogranite and a younger igneous complex (YIC) (Kruné hory granite) of alkali-feld-

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Fig. 12 Entrance of new drainage Barbora adit (photo P. Beran, 1997).

Fig. 13 The Vilém shaft in the area of Krásno mining museum (photo P. Beran, 1999).

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Fig. 14 The shaft bottom of
the Vilém shaft, Krásno (photo J. Sejkora, 2005).

spar syenogranite, enriched in Li. In the Krásno ore district, highly evolved albite granite (Èistá  Krásno type,
Fiala 1962) and Milíøe type two-mica granite (YIC) predominate (Fig. 16).
A significant part of Sn-W mineralization is associated with small massifs of the YIC granites, which intruded along transversal NWSE fault zones. Tin ore is concentrated in the apical parts of granite stocks or inelongated endocontacts of elevation zones. The Huber
stock is the largest granite intrusion of this type. The envelope of the granite intrusions consists from intensively folded Proterozoic rocks, including biotite orthogneisses, paragneisses and migmatites.
The main geological units

Fig. 15 Horní Slavkov museum (photo J. Sejkora, 2005).

The Slavkovský les area (called in the past as the Císaøský
les or Kaiserwald) represents an uplifted block bound by
several fault-zones, including the Kruné hory fault at the
NW, Mariánské láznì fault at the SW and the Litomìøice
lineament zone at the SE. A fault zone in the Teplá rivervalley marks the limits at the East.
Together with the Kruné hory (Erzgebirge), theSlavkovský les area belongs to the southeastern part of
the Saxothuringian Zone. This relationship is underlinedby the presence of granites of the Kruné hory batholithand the associated Sn  W  Li, U, and Ag  Bi  Co 
Ni  As mineralizations and by the similarities in granite magmatism in both areas, as emphasized by Fiala(1962).

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Journal of the Czech Geological Society 51/12(2006)

Fig. 16 Geological map of the Horní
Slavkov  Krásno area. Simplified
from 1:50 000 geological map, sheet
11-23 Sokolov, published by the
Czech Geological Survey, Prague.

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Metamorphic rocks of the Slavkovský les area
The core part of the metamorphic complex in the Slavkovský les area of a probable Proterozoic age consists ofbiotite paragneisses and two-mica gneisses, in part accompanied by migmatites. It is crosscut by aplitic orthogneiss, migmatitic granite gneiss and biotite orthogneiss.
Metamorphosed mafic rocks (amphibolites) are of limited occurrence. Vondrová (1962) studied the eastern partof the metamorphic complex in proximity of the Krásno
ore district.
Metamorphic rocks of the eastern part are deformed
into folds with steeply dipping axial planes and amplitudes on the order of hundred metres. Orthogneisses occur preferentially in the cores of antiforms. Three E-W
trending belts of paragneisses with a variable degree ofmigmatization are separated by granite gneiss or biotite
orthogneiss. The western part of the complex is relatively monotonous, including alternation of biotite paragneiss
with orthogneiss. The crest of the structure contains smallintercalations of pyroxene calc-silicate gneiss and amphibolite near Lobzy (Fiala 1962). The gneiss complex
is cross cut by the dykes of aplite and aplitic granite abundant especially in the central part. The dyke swarms may
contain somewhat older dykes related to the OIC Variscan
granite pluton.
Metamorphic rocks in the NW part of the Slavkovský
les area are probably younger than the rocks in the central part. A quartzite horizon at the base is overlain by auniform sequence of mica-rich sillimanite paragneiss withlayers of sillimanite-cordierite hornfels (Neuilová  Vajner 1963 and Fiala 1962). Numerous conformable bodies of Variscan biotite granite belong to the OIC type.
Metamorphic rocks south of the Rabùvka fault zone
characterized by variation in lithology probably belong
to the Upper Proterozoic. The unit, designated as Rabùvka Group (Pleinerová  Hladká 1960, Fiala 1962), includes biotite-cordierite-sillimanite, garnet, biotite-anthophyllite, biotite-amphibole, and amphibole hornfelsic
gneisses and hornfelses. The rocks were affected by contact metamorphism and possibly by metasomatism by intrusion of OIC biotite granite.
At the south, the Rabùvka unit borders along a fault
zone the Mariánské Láznì metabasite complex (MLMC)
composed of amphibolites, gabbroamphibolites, eclogitic amphibolites, eclogites, and less widespread metasedimentary schists and gneisses. Geology, petrology andgeochemistry of MLCM were studied by Fiala (1958),
Kastl  Tonika (1984), Timmermann et al. (2004), tìdrá
(1996), tìdrá et al. (2002), and tìdrá (2003). A serpertinite belt at the northwestern edge of MLMC marks
the boundary against structurally lower Kladská Unit,
classified with the Lower Palaeozoic of the Saxothuringian Zone (Kachlík 1997).
The Kladská Unit, considered to be the stratigraphically youngest member among the metamorphic rocks of
the Slavkovský les, includes phyllitic schist (± andalusite), quartzites, graphitic schists enriched in apatite,

13

carbonate intercalations, and amphibolites. The sequencestudied by Fiala (1962) hosts the uranium veins.
Granitoids of the Slavkovský lesA large part of the Slavkovský les area is underlain by
Variscan granitoids, belonging to the southern part of theKruné hory (Erzgebirge) batholith. Owing to the obvious association of younger granites with the Sn-W-Li
mineralization, the rocks attracted attention and were repeatedly studied during the 20th century. The older geological, petrographical and petrochemical data were presented by Fiala (1962, 1968), new data were publishedby Jarchovský  temprok (1979), temprok (1986), andBreiter et al. (1991).
Three main granite groups are recognized: a) OIC
granitoids, including biotite granite, minor masses of gabbrodiorite and quartz diorite, b) transitional group of twomica granite, c) muscovite albite YIC granite with anenrichment in Li and F.
Granitoids of the OIC group crop out at large continuous bodies north of Horní Slavkov (Loket  Vítkov), in
the central area (around Nová Ves) and at the southwestof the area. Aplites, at places containing tourmaline, closethe magmatic sequence. A prominent granite type is the
Loket porphyritic granite with euhedral phenocrysts of alkali feldspar several cm long, exhibiting typical Carlsbad
twinning. Plagioclase in the groundmass is oligoclase to
sodic andesine. Some varieties contain minor amphibole.
Granites of the transitional group show geochemical
features between those of OIC and YIC granites. They
include two-mica granite and biotite granite with subordinate muscovite and accessory andalusite or tourmaline(Fiala 1968).
The YIC granites crop out at small massifs localized
often at intersection of fault zones. These are represented by the Krudum massif at the northeast (among Krásno, Èistá, Rovná, and Nadlesí) and the Lesný-Lysina
massif at the southwest (among Kladská and Kynvart).
Petrochemical variation has been noted mainly in thevariable content of Li, Rb and F, while the bulk compositions remain uniform. Maximum enrichment in Li andF characterizes the so-called Li-F granites (Kovalenko etal. 1977). Characteristic petrographic features include
enrichment in albite, replacement of feldspars by muscovite, replacement of biotite by Li-bearing micas, andthe presence of accessory topaz.
The Krudum massif, 50 km2 in outcrop, shows a sequence of granite intrusions. Fine-grained porphyritic biotite granite with muscovite forms the central part and contains transitions to a coarse-grained facies (Svárov-Polom)
or to the types similar to granite porphyry. These rocktypes do not show typical autometamorphism, contain low
concentrations of volatile elements and are classified bysome authors (ovíèková in Polanský et al. 1973, Jarchovský  temprok 1979) with transitional granites.
The northwestern part of the Krudum massif consistsof the Milíøe type of two-mica granite, which is porphy-

14

ritic at places and carries signs of autometamorphism. At
some localities, e.g., the Sklenný vrch elevation, it shows
weak greisenization, structurally lower positioned feldspar-enriched derivates and a marginal pegmatite at thecontact with hanging wall biotite-sillimanite-cordierite
hornfelsic gneiss (S-2 borehole, Jarchovský  Pavlù
1980). Novák (1988) recorded similar features including
greisenization, sericitization, kaolinization and formationof accessory topaz and cassiterite in this granite.
Highly evolved Li-F granites afftected by autometasomatism belong to the YIC granites. Compared to the
Milíøe type, these granites contain increased amounts ofalbite, Li-mica, and topaz, in addition to perthitic orthoclase and quartz. Of the trace elements the granites areenriched mainly in F, Li, Rb, Cs and depleted in Ba, Sr,Ti, and Zr. The main representative of Li-F granites in
the Slavkovský les is fine-grained to medium-grainedÈistá granite (Fiala 1968). It occurs in northern, southern, and southeastern parts of the Krudum massif andcontinues below the Slavkov gneiss roof pendant towards
the Vysoký Kámen locality. It represents the main rocktype in the Krásno district, where it contains important
greisen-type accumulations of Sn-W ores. Fine-grained
porphyritic granite occurs as a variety of this granite. It
forms relatively small bodies with sharp contacts to themedium-grained granite. It is documented from deeper
levels of the Huber and Schnöd stocks and in the Lánský dvùr elevation.
Albite-topaz microgranite cements fragments of biotite
gneiss roof above the apical part of the Huber stock andrepresents thus intrusive breccia pre-dating metasomatismand greisenization (Jarchovský  Pavlù 1991). This microgranite is comparable with ongonites described from
Mongolia (Kovalenko et al. 1971) or to extrusive rhyolites described from the USA (Christiansen 1983).
Aplitic leucocratic albite granite containing only negligible amount of mica, carrying topaz, apatite, andsometimes beryl (Polák et al. 1969) belongs probably
to the youngest differentiates of YIC granites. Alkali
metasomatism resulted in the formation of Na-K feldspathites (Fiala 1968, Pácal  Pavlù 1972, 1979), giving
rise to ceramic feldspar deposit at Vysoký Kámen near
Krásno. A marginal pegmatite, the so-called stockscheider, frequently occurs at the top of Li-F granites.
Where the contact is nearly horizontal (dip of 030°),
the pegmatite is up to several metres thick, but it becomes much thinner (few centimetres to zero), where
the contact is steep.
Neovolcanics
Tertiary volcanics occur at few places in the Slavkovský
les area. Nefeline basanite forms the top of the Lysina
hill southeast of Láznì Kynvart (Fiala 1962) and olivine basalt occurs at the Buková hill NW of Boíøany
(Vondrová 1962). The neovolcanics indicate that somepre-existing faults served as magma conduits during thisevent.

Journal of the Czech Geological Society 51/12(2006)

Ore deposits in the Slavkovský les area
Important Sn-W ore deposits occur in the Krudum granite massif  the Krásno ore district at the southeastern
margin and the Èistá deposit at the southern contact. Mineralization in the southern part of the area is rare, except
for a small granite stock west of Prameny.
There are two main morphological types of tin-tungsten mineralization. Greisen bodies in the apical parts andalong flanks of Li-F granite stocks carry disseminated
Sn-W ores. This type represents the dominant part of theore and was the main exploration target. Morphology ofgreisen bodies is rather complicated but tabular or hoofshaped bodies up to several tens of metres thick prevail.
Greisens may occur at some distance (about up to 30 m)from the granite contact but they are often tied directly
to the contact with the country gneiss. The vertical rangeof the endocontact greisens does not exceed 200 m but
the richest parts are limited to the distance of 50 m fromthe contact. The apical parts of stocks carry light coloured
quartz-topaz greisen and intermediate or deeper zones
contain a darker quartz-topaz-zinnwaldite greisen. Sulfides often accompany cassiterite and wolframite in theupper parts but they are absent at deeper levels.
Quartz veins with the wall rock greisenization represent the second type of Sn-W mineralization. They occur in the exocontact of mineralized granite cupolas. The
best examples offer the Gellnauer and Hán veins and theMarie and Vlèí Dvùr veins. These veins were extensively exploited in the past but their importance declined with
the introduction of mechanized mining. They also served
as an indication of mineralized granite stock at depth.
Dark greisens accompanying quartz veins in gneiss were
designated as zwitter. On transition to neighbouring
granite, such quartz veins became thinner and the associated greisenization in surrounding granite was more extensive, indicating thus transition to endocontact greisens.
Hydrothermal veins with uranium and Ag-As-Bi-Co-Ni
minerals represent another type of vein mineralizations.
The veins were extensively exploited after the World War
Second around Horní Slavkov (the Horní Slavkov uranium ore district). Insignificant are Pb-Zn veins nearKynvart (16 km southwest of Krásno), and Fe-Mn andfluorite-barite mineralization near Novina. Among industrial non-metallic raw materials, the Vysoký Kámen deposit of Na-K feldspar is the most important.
General characteristics of deposits in the Krásno ore
district
In the area of the Stannum company activities aroundKrásno and Horní Slavkov, several deposits and someminor localities of tin-tungsten ores were prospected andconsidered for mining with the aim to utilize the dressing plant. There were some variations in mining methods, contents of economic minerals, and ore dressing requirements among individual deposits. As a rule, tin,tungsten, exceptionally copper and lithium, were the sub-

Journal of the Czech Geological Society 51/12(2006)

ject of interest. In view of proximity of the dressing plant
and the possibility to exploit some deposits by open pit
mines, even some relatively low-grade primary ores wereconsidered for mining.
Although the geology of deposits in the Slavkovský
les area shows many common features, the actual geological situation at individual deposits is variable. Beran Beranová (1995) classified the deposits in six groups:
 the Jeroným deposit at Èistá and showings in theneighbourhood, group of deposits and showings around Krásno(Vysoký Kámen, Koník, Vysoký Kámen-granite,
Klinge, and ibeník), the northern zone near Horní Slavkov (Smrèiny and
Hán elevations, pièák, veins in the Slavkov gneissroof pendant),
 small showings of mineralization and low-grade Sn-W
ores in northern and southern parts of the Slavkovský
les area, the Krásno ore district (including deposits Huber and
Schnöd stocks, area southwest of the Gellnauer andLánský Dvùr elevations, area to the South and Southeast of the latter, the Gellnauer set of veins etc.),
 alluvial deposits along the Stoka stream.
Geological situation of the Krásno ore district
The Krásno deposit comprises several elevations (cupolas) of a large body of the autometamorphosed YIC granites and its dyke suite. The largest elevation is the Huber stock with its apical part exposed at the surface. In
the course of mining during the past centuries, the upper
part of the cupola was mined out. Extensive refuse dumps
later on covered the resulting funnel-shaped open pit. The
Schnöd stock had its apical part covered by the 70 m
thick Slavkov gneiss roof pendant. The extensive mining in the past also resulted in collapse reaching up to
the surface. Both the stocks have a shape of a blunt conewith an elliptical base, widening with depth. At a levelof c. 485 m a.s.l. the stocks join to a single body, withprojected centres of the two stocks trending NW-SE andlocated 700 m apart. The width of the stocks at this lev-

Fig. 17 A section of Huber
and Schnöd granite stocks,
view in direction SWNE[P. Ondru according to Beran(1999)].
1  YIC granites;
2  greisenized granites;
3  paragneisses;
4  cave-in parts of greisen
stocks and their envelope.

15

el is c. 400 m. In the area northwest of the two stocks,
there is a flat granite elevation, which joins the northwestern side of the stocks.
The granite of elevations has a discordant intrusive contact with the gneiss envelope. The contact plane is uneven,with local steps of several metres. The dip of the contact
plane varies from 50° to 70° along the slopes of cupola butat the 4th level (475 m a.s.l.) it becomes flat with a dip of20°. The contact is rimmed by a marginal pegmatite (stockscheider), which is from several cm to nearly 4 m thick.
In the deeper parts with flat-lying contact, the marginal
pegmatite is only several cm to several dm thick.
Several marginal tin-bearing localities explored by the
Geoindustria Company (Najman 1990) belong spatially to
the Krásno deposit. They include the Lánský Dvùr elevation, NW, SE and S surroundings of the Huber stock andthe so-called K-5 elevation. In addition, the Gellnauer setof veins and veins in the area to the south, and SE of the
Huber stock are also classified with the Krásno deposit.
Tectonic situation in the Krásno ore district
Predominant tectonic structures are fractures striking
NW-SE and NE-SW. The N-S and W-E structures are oflesser importance. The fractures are mostly less than
0.5 cm wide but some fractures are 25 cm (exceptionally 10 cm) wide and often open. Some fractures werefilled in by quartz but may contain the water. Clay minerals, iron or manganese oxides, sericite or fluorite coatsome fracture walls while the coatings of pyrite, molybdenite or graphite are rare. Any wider dislocation zones
in the granite stock are very rare. Some significant faults
observed in the Slavkov gneiss roof pendant do not continue into the granite stock.
Deposits of the Krásno ore district
The Huber stock deposit
The granite of the Huber stock probably contains the largest quantities of tin in the whole region. The stock is bellshaped in section or similar to a blunt cone (Fig. 17). At

16

the 3rd level, the size is 200 m × 100 m. At the 4th level
the stock extends 400 m NE-SW and it is about 250 m
wide.
The Huber stock consists basically of autometamorphosed Li-mica-topaz granite with a variable degree of
secondary alterations. These alterations include greisenization. It is assumed that the whole apical part of thecupola (now collapsed) was formed by greisen andquartz. Greisen also contours the endocontact of thestock. Zoning is not clearly defined and greisen passes
gradually into the granite. Continuous greisen bodies may
split into several lenses giving way to greinized granite
and at deeper levels to unaltered Li-mica-topaz granite.
Three genetically distinct greisen types are recognized:
 greisen bodies in endocontact formed probably alonga network of fine fractures, free of infillings or a zoning, which pass to the granite; greisen bodies formed along thin, isolated fracturesand sets of parallel fractures, accompanied by a distinct greisen zoning. Greisen is in places symmetrically zoned along the fluid conduits, with the strongest alteration next to the conduit. This type ofgreisen is typical for the central parts of the stock; greisens along the quartz veins are usually symmetric to the strike of the vein.
Towards deeper levels, the number of quartz veins with
Sn-W mineralization and accompanying greisen declines.
At a depth of 200300 m, there are 2040 m thick lenses with fine-grained cassiterite. The data indicate that in
the near-contact zone of the Huber stock Sn-W ores continue several hundred m below the 4th level of the Huber
shaft but in the central part of the stock such ores do notextend below this level. Dispersed cassiterite and wolframite in all rock types represent the ore minerals. As,
Cu and Zn mineralization joins the Sn-W minerals in theapical parts of the stock. The contents of tin and tungsten vary from traces to tens of wt. %. During mining theore grade could not be determined by macroscopic criteria and all samples had to be analysed chemically.
Mineralization in some parts of the stock (generally
above the 5th level) occurs closely near the contact. Elsewhere, it is separated from the contact by a barren zone
up to 30 m wide. It is assumed that the width of the barren zone increases with depth (Kozubek et al. 1985). The
vertical asymmetry in position of mineralized endocontact zones is interpreted as resulting from the channels
supplying the metals. The deepest extension of mineralization was at the NE (Kozubek et al. 1985).
Exploration indicates that the mineralization in the
Huber stock continues to deeper levels. The morphology of granite contact with the roof rocks is decisive inthe control of ore zones. This deep level mineralization occurs at the SW, N and NE margins of the stock.
In addition to various types of Li-mica-topaz granite,
below the 5th level occur several types of two-mica granite. The contacts between individual granite types are irregular and modified by superimposed alterations. Mineralization is represented by dispersed cassiterite andJournal of the Czech Geological Society 51/12(2006)

wolframite in all granite types, and exceptionally also in
exocontact metamorphic rocks. A preferential association
with a single granite type has not been documented.
A specific feature of the Huber stock is the existenceof so-called cave-in reserves, resulting from ancientmining and a collapse of the chambers in the upper partsof the stock.
The cave-in fill is a heterogenous mixture of all rocks
types including some metamorphic country rocks andcrushed remains of the support pillars. Circulating water
brought sand and clay material from weathered rocks into
its free spaces. This compacted material was difficult tobe penetrated during excavation of mine galleries or by
drilling.
Numerous quartz veins intersect the Huber stock andare accompanied by 1 to 4 m wide wall rock greisens(Drozen 1965). Archive data indicate the four types of
Sn-bearing quartz veins: the oldest quartz veins with wall rock greisen, which
do not show mutual displacement at intersections, but
are displaced at the intersection with younger veins(examples: Frantiek, Karel, Hubská, Pinková, Panská, Messer, and Tscherper veins);
 quartz veins containing clay infilling usually free ofa greisen border and displacing the older veins. Examples include the Starohubská and Èervená veins; quartz veins with imperfect greisen borders, of no
economic significance. The Kophan vein and a number of unnamed veins belong to this group; tectonic fractures filled by clay, but rarely showing
mineralization. They had minimal importance in mining. Examples include the Èervená fracture and Èervená offshoot.
The Schnöd stock deposit
The mineralization in this stock does not reach the 4th level in the Huber shaft. The lowest limit of mineralizationis slightly above the lowest exploitation Xth level of the
Vilém shaft. The Schnöd stock was explored in a moredetail during the last decades, as the upper levels wereless affected by ancient mining. Even so, there are notsufficient data on apical part of the stock, 70 m below
the present surface (Fig. 17).
The envelope of this stock is built by fine- to medium-grained migmatized biotite paragneisses. The complex contains aplites and tourmaline pegmatites in proximity of the stock. The endocontact pegmatite(stockscheider) is thickest in the apical part. It contains
large crystals of pink orthoclase oriented perpendicular
to contact plane. At the contact with paragneiss, the orthoclase crystals are smaller and are accompanied bymicas. The boundary with granite is gradational.
Medium-grained and pink granite, which builds thestock, is often affected by secondary alterations. Albite
granite is widespread in the upper parts of the elongatedgranite elevation and in the lower part of the Schnöd
stock at transition of greisen to granite. Greisens in theJournal of the Czech Geological Society 51/12(2006)

Schnöd stock are usually fine-grained or medium-grained
and rich in quartz. At places, the stock contains partly
greisenized and kaolinized granite with the Sn contents
lower than those in typical greisen. This type of granite
is developed at the upper levels only in the eastern partof the stock, but at the VIIIth level it is rather widespreadthroughout.
Deposit to the northwest of the Huber and Schnöd
stocksJaneèka (1973) explored a flat granite elevation trending
NE-SW, with economic tin mineralization. The long axisof the elevation is nearly 500 m long and the transversal
axis at an altitude of the 4th level of the Huber shaft is
170 m long. The elevation consists of albite-Li-mica-topaz granite and greisenized granite with a considerable proportion of greisen. The greisens are either composed ofquartz-mica-topaz or of nearly pure quartz or quartz-topaz.
The mineralized lenses are from 5 to 30 m thick andthey continue below the 4th level. At the southwest, exploration documented the presence of flat mineralized
lenses only 3 to 7 m thick at an altitude of 500 m a.s.l.
In the upper parts, usually above the greisen horizons,fine-grained mineralized granite shows a typical banded
structure and it is usually kaolinized and sericitized orsilicified at places.
In the area NW of the Krásno deposit, two-mica granite occurs directly above albite granite (Kozubek et al.
1989). Marginal pegmatite (stockscheider) is composed
mainly of feldspar with lesser quartz and is developed
direcly at the top of this granite as a prominent 4 m thickbody. Biotite in stockscheider forms characteristic rims
at contact with the country rocks. The contact plane of
the intrusion is flat, from 1525° to nearly horizontal.
Gellnauer vein
The set of tin-bearing veins includes the Gellnauer vein,
succeeded upwards by the Marie vein and the Puklinová(Kluftgang) vein. The veins are parallel and follow thetrend joining the stocks but they dip toward the stocks,
i.e., to the NW. The veins are accompanied at the SW by
the perpedicular Antonín vein. Additional veins include
the Trojièná, Ondøejská, and Nepomuckého veins. The
veins carried high Sn contents in their upper parts but themetal content quickly declined with increasing depth. At
the VIII th level of the Vilém shaft (509 m a.s.l.), theGellnauer vein is thin and weakly mineralized. The quartz
veins with Sn and W are known to continue along strike
for a distance of 800 m. The Gellnauer and Marie veinshave a moderate dip of 2535° at the upper levels but
they steepen down (below the sixth level) to 3555° dips.
The Gellnauer vein splits at the upper levels to several
offshoots, which unite at the VIth level to a single vein.
It is slightly offset by transversal dislocations but rare
parallel dislocations are also present. The width of thevein is reduced in granite: at the upper level the vein is173040 cm wide but in granite at the VIIIth level it is decreased to 520 cm. At lower levels, granite and also
marginal pegmatite are greisenized along the vein margin but greisen border becomes narrow in gneiss.
The Gellnauer vein is characterized by massive mineral infilling and comb structure of quartz. Parallel-banded structures are absent. The ore minerals occur at themargins in the broader parts of the vein and rich mineralization correlates with a strong alteration of wall rock.
The greisenization zones, or zwitter bands in gneiss, retain a regular width even along narrow veinlets and often coalesce into a single, wide band of greisenization(Janeèka 1964). Greisenization in the footwall is usuallywider than that in the hanging wall. Recent exploration
followed the continuation of the veins from the historical area to the SE. The exploration revealed six structures
corresponding to a direct continuation of veins from thehistorical district.
Gellnauer elevation (area southeast of the Schnöd
stock)
A flat elevation of Li-mica-topaz granite with disseminated mineralization and greisenization in the area southeast of the root zone of the Gellnauer vein system.
According to the geological position, this elevation issimilar to the main stocks at Krásno. The contact of Limica-topaz granite with the gneiss dips steeply below the
4th level of the Huber shaft, at places the contact is partly overhanging but it turns to a moderate dip at this smallelevation. This cusp has its axis orientated parallel withthe direction of the Huber and Schnöd stocks. The granite is medium-grained, kaolinized, hematitized, and silicified. Lenses of medium-grained mica-bearing greisen ora rare quartz-rich greisen occur at the SE. These rocks
are petrographically comparable with those from the
Huber stock. Endocontact greisen is absent at the SW
margin, which shows a steep dip. In the endocontact of
the Huber stock the Gellnauer vein system wedges-out
over a short distance from the granite contact.
Lánský dvùr elevation
A small, elongated granite elevation east of the Huber
stock is trending SW-NE and slightly plunging to the NE.
The ore mineralization occurs at the southwestern flankbut it is absent in the apical part. Ore minerals are in Limica-topaz granite, its greisenized portions and in greisen (Najman 1990). At this deposit, contacts appear to belargely tectonic. Marginal pegmatite was not observed.
Area to the South and southeast of the Huber stock
The geological situation is similar to the neighbouring
areas. Contact beetween the granite and the envelope isusually rimmed by a marginal pegmatite (stockscheider)and less commonly it is a tectonic or a sharp intrusive
contact. Typical granite above the mineralized lenses is18

a medium-grained Li-mica-topaz granite of the Èistá 
Krásno-type, less commonly occur fine-grained or porphyritic varieties. The Milíøe granite is very rare. Mineralization associates with the granites, topaz-mica-quartz
and mica-quartz greisens. The area to the SE of the Huber stock has the granite structure unfavourable for Sn
mineralization (Najman 1990). The northern part contains
mineralized horizons to a depth of 450 a.s.l. The ore isassociated with greisens and Li-mica-topaz granite affected by greisenization of a variable intensity. The ore bodyis 3 to 70 m thick and follows conformably the relief ofgranite contact. The ore horizon shows local blows andnotable increases in Sn and W contents.
Genesis of Sn-W deposits
Drozen (1969) studied genesis of greisens and veins at
Krásno. According to the classification by Smirnov(1983), the Krásno deposit belongs to endogenic and hydrothermal greisen deposits. In a modified classification
by Havelka (1985) the deposit is classified as magmatogenic hydrothermal metasomatic deposit of greisen type.
Greisen alteration was accompanied by precipitation of
the ore minerals along open fractures of variable dimensions. The components were transported via hydrothermal solutions carrying fluorine, lithium, ore elements andsome components released from country rocks. The mineralization process was characterized by gradual decreaseof temperature and pressure and by the change in the concentration of components in ore-bearing solutions. This
resulted in a series of mineral assemblages corresponding to certain stages in the deposit formation. All authors
who studied genesis of these deposits (e.g., Jarchovský
1962, Drozen 1965, 1969), agree on a multi-staged process of mineralization with some overlap of individual
stages in various parts of the deposit.
There is a diversity of views about the sequence ofmineralization stages and relations between mineralization and greisenization. Under favourable lithological andtectonic conditions, precipitation of ore minerals was accompanied by greisenization. In most cases, there is goodcorrelation in associations of vein filling and greisens,
which point to their close relations in the process of deposition from the same batch of solutions. Mineralized
greisens show irregular distribution of ore minerals andsome greisen bodies or their parts are barren. Ore minerals are sometimes accumulated along certain preferential lines indicating tectonic controls, however, the control of mineralization by tectonic factors cannot be
evidenced in most cases. The import of ore elements is
not a single event as the ore minerals, especially cassiterite, precipited also later together with sulfides (Kunír 
Jarchovský 1967). Probably, the youngest episodes of tin
import are not accompanied by greisenization and cassiterite occurs also in altered granite. However, this does
not prove an independence from the greisenization process (Kozubek et al. 1985).

Journal of the Czech Geological Society 51/12(2006)

According to some authors (temprok 1985, Drozen
1965, 1969, Ïuriová 1984 a.o.), it is more probable thatan independent tin import period occurred, overlappingwith greisenization, but some cassiterite was deposited after the complete evolution of greisens. Thus, greisens remained barren at some parts. The gap between greisenization and cassiterite deposition is relatively small, as
indicated by the existence of rare barren greisens. However, cassiterite deposition separately from the greisen formation is relatively significant as indicated by tin ore bodies in granites showing various stages of deuteric alteration.
Jarchovský (1962) presented a model of deposit formation. Magma of the YIC granite was relatively rich involatile components. In the course of crystallization, plagioclase (albite-oligoclase) and later orthoclase, crystallized after precipitation of quartz. The remaining albite
components with silica and fluorine concentrated in a
residual liquid, which resulted in the formation of albite
granite with topaz. With decreasing temperature and increasing concentration of volatile components the alreadyprecipitated minerals became unstable and underwent
metasomatic replacement resulting in greisenization. In
addition to these secondary greisens, some primarygreisens were possibly formed via crystalization fromsupercritical fluids including the so-called primary rocks
in the apical parts of stocks. A vertical differentiation
occurred in the stocks. Primary greisen formed in theapical and marginal parts of the granite elevation. The
central parts contain more or less greisenized granite or
granite with other types of alteration (sericitization andkaolinization). The ore veins were deposited along fractures, which also served as channels for the release ofvolatile components.
Mineralogy of the Krásno ore district
The Slavkovský les area, and particularly the Krásno ore
district belong to the oldest mining districts in Europe.
There are several hundred published papers dealing withmineralogy, however, a complete and complex mineralogical study of this district is missing untill the present
time.
History of mineralogical and petrological studies
The ore deposits have been studied by a number of notable mineralogists. The first important specialist wasprobably Georgius Agricola (1556). Preserved papers
dated before 1850 are oriented mainly to montanistic andgeological aspects (Ferber 1774, Peithner 1780, Born
1790 in Drozen 1969, Peschel 1805, Günther 1820, Zippe1847). Specialized mineralogical studies include those of
Lindacker (1791), Haidinger (1830), and Presl (1837 inDrozen 1969) dedicated to topaz and pseudomorphs after wolframite.
Kenngott (1851) described carpholite as a new mineral using the specimens from Krásno. Besides mineral

Journal of the Czech Geological Society 51/12(2006)

description, the paper presents results of a goniometricstudy and a chemical formula based on analyses by Steinmann and Stromeyer. The publication by Krejèí (1855)
contains a detailed list of minerals known then from the
Horní Slavkov  Krásno area. An important paper by
Nowicky (1857) brings information on petrology, mining geology, and information on minerals of quartz veins
and mineralized granite stocks. A detailed topographic
mineralogy of the Cheb region by Glückselig (1862) presents data on local tin deposits. Rücker (1864a) publisheda widely based geological and petrographic descriptionof Horní Slavkov tin deposits. In addition to petrographic,ore mineralization, and minerogenetic characteristics (inpart valid till present), the paper gives extensive information on minerals of the quartz veins and greisen stocks.
Erben (1884) studied crystal morphology of cassiterite
crystals. Klvaòa (1886) presented detailed descriptions of
numerous minerals.
Additional papers published before 1900 include studies by Krejèí (1851), Jantsch (1853, 1854, 1858), Reuss(1854, 1863), Hochstetter (1856), Jokély (1857),
Zepharovich (1857, 1864), Gehlièka (1858), Rücker
(1864a), Sadebeck (1869), Reyer (1880, 1881), Döll
(1883), and Katzer (1892). In addition to mineralogy
data, these publications bring mainly petrographic andmining geology information.
In a very interesting work, Krusch (1916) assumes
mineralization in two periods and gives information onore grades of that time (0.2 to 0.4 wt. % Sn). Two classical mineralogical papers deal with topaz (Rosický 1916)
and cassiterite (Heilmaier 1930). Additional informations
are in papers by Gareiss (1901), Barvíø (1903), Hoffmann(1903, 1904), Slavík (1903), Cornu (1905, 1906),
Woldøich (1905), Jeek (1914), Frieser (1916), Groth(1916), Kettner (1917), and Kudielka (1919).
Historical studies by Bílek (1957, 1958) present a deep
analysis of available information and via reconstructionof missing data give an integrated evaluation of the Krásno area. These data significantly contributed to renewalof mining at the Huber stock. Fiala et al. (1960) describedgeology and petrology of the Horní Slavkov and Krásno
region based on detailed geological maps at the scale of
1 : 5000. Publications by Jarchovský (1959, 1962, 1969)
Jarchovský  temprok (1979), and Jarchovský  Pavlù
(1980, 1991) present important data on mineralogy,
geochemistry, and petrography. Drozen (1959, 1962,1969) presented the first complex study of mineralogy
and petrology of the Krásno ore district.
The publications by Fiala (1948, 1950, 1952), Vtìlenský (1955), Fiala et al. (1956, 1957); Fiala  kvor(1956), Halar (1956), Strunz (1957), Konta (1957),
Obdrálek (1958), Kratochvíl (1960), Zemánek  Gregorová (1959), Bernardová  Poubová (1961), Tacl  Blüml(1961, 1974), and others, provide additional informationon the Krásno ore district.
Relatively extensive new studies by Z. Mrázek,P. Korbel, Z. Mach, M. Fikar, T. Øídkoil, P. Beran,19

V. rein, P. Ondru, F. Veselovský, J. Sejkora etc., stilllargely await publication. Nevertheless, several papers
have been published (Korbel 1983, 1991; MachKorbel
1990; Mach 1979; Mrázek 1981). Some of these new data
have been included in the unpublished studies by Beranet al. (1989), Beran  Beranová (1995) and information
without analytic data has been included in the book by
Beran (1999).
Mineralogy of the Krásno ore district
Mineralization at the Krásno ore district is notably richin mineral species present. The unpublished final reportby Beran  Beranová (1995) lists 191 valid minerals. The
list gives 245 names, if some old descriptions and mineral varieties are considered. After the inclusion of new
data presented in this volume and revision of some older mineral descriptions, the number of described minerals in the Krásno ore district is 228 valid mineral species. Eleven probable new minerals, awaiting in part a
detailed study and publication (review presented in Table 1), expand the list of minerals. Some more species
will likely result from a future detailed study of incompletely known Nb-Ta minerals and from study of primary sulfides in quartz veins and greisens, which received
little attention till present.
The following text gives brief information on some
mineral classics, which are widely known from the
Krásno ore district and represented in numerous mineralcollections throughout world. Mineralogists of the 18thand 19th century used specimens of several minerals, collected in the Krásno tin mines, as ideal study material indetermination of physical and compositional properties.
Arsenopyrite
Zepharovich (1857), Jantsch (1854, 1858), Nowicki(1857), Glückselig (1862) and some other authors described arsenopyrite as an abundant mineral in the district.
It was common mainly in upper levels of the deposits
and arsenopyrite content steeply declined with depth. The
presence of arsenopyrite was closely monitored during
the modern mining, as it was a harmful component incassiterite concentrate. Only trace amounts have been evidenced at the level of 500 m a.s.l. In this respect, it isinteresting that a rich local arsenopyrite accumulation
occured in the form of clusters several cm to dm across,over a distance of 6 m at the 5th level. Arsenic contents
due to arsenopyrite reached up to several wt. % in the orefrom the open pit at the Huber stock. Control analyses fromthis site document the highest (exceptional) content of
10 wt. % As and an average content of 1 wt. % As in ore.
Arsenopyrite occurrences in the district are variable,
including irregular aggregates and grains bound by somecrystal faces, in part striated. It is associated mainly withsphalerite and cassiterite and at other places with molybdenite, chalcopyrite, covellite and luzonite. Microscopic

20

Journal of the Czech Geological Society 51/12(2006)

T a b l e 1 List of mineral species occurring in the Krásno Sn-W ore district and Horní Slavkov uranium ore district.
mineral1 2 3 4

acanthite* **adamitealbite* * *mineral1 2 3 4mineral1 2 3 4florencite-(Ce)*pitticite*

fluellite*

posnjakite

fluorapatite*

powellite

allophane*

fluorite* * * *

almandine* *frondelite*

proustitealunite*galena* *pseudomalachite

andalusite*

preisingerite

goethite* * *psilomelane

anglesite*

gorceixite*

pyrargyrite

ankerite* *goyazite*pyriteannabergite* *graphite* *pyrrhotite

antlerite*

greenockite*

quartzapatite

* *

*

*
*

grossular*rammelsbergite

*
*
*
* * *
*
* *
* *
* * * **

aragonite*

gypsum* * *rockbridgeite*

arsenic* *halloysite*

rodochrosite*

arseniosiderite*

hematite* * * *

rooseveltite*

arsenolite*

hentschelite*russelite*

arsenopyrite* *hübnerite*

rutherfordine

aurichalcite*

chalcanthite*rutile* **autunite* *chalcocite* *scoroditeazurite* *chalcophyllite*

serpierite

barite* *chalcopyrite* * * *

scheelite
schultenite

bavenite

*

*

*

*
*

*

chalcosiderite* *benyacarite*

chenevixite*

siderite* *beraunite*

chrysocolla*sillimanite**

silverbertrandite*

illiteberyl*

ilmenite

*

*

* *

skutterudite*

betpakdalite*

ilsemannite*

soddyite*bindheimite*

isokite*sodiumuranospinite** * * *

jarositebiotitebismite*sphalerite* *kaatialaite* *kaòkite*bismuthinite* *kaolinite

bismutite*kësterite

bismutoferrite*

koechlinite

bornite* *kolbeckite*

bismuth*brochantite
brookite*cacoxenite* **stannite* *stannoidite** * * *

stibnite* **stolzite***strengite

* *

*

*

talc

kyanite* *tennantite* *langite*tenorite*tetrahedrite* *leucophosphite* *calcite* *libethenite

cannonite*liebigite*

limonite* * * *

torbernite*

tremolite

carnotite*

carpholite*

linaritecassiterite* * * *

löllingite

clinoclase*

cobaltite**** * * *
* **triplite*

triploidite**

tungstite*

turquoise* *tyrolite**magnetite*malachite

* * *

*

manganite* *mansfieldite*

cordierite

* *

topaz

*

*
*

titaniteluzonitecompreignacite
copper*magnesitecoffinite
cookeite

* *

*

*

uraninite*uranophane

marcasite* *uranospinite

cornwallite*

mawsonite*

variscite

covellite* *melanterite*

varlamoffite

*
* *
*
*
*

Journal of the Czech Geological Society 51/12(2006)

21

T a b l e 1 (continued)
mineral1 2 3 4mineral1 2 3 4mineral1 2 3 4

crandallite*

metaautunite* **vermiculite*

cryptomelane*

metanováèekite*

vesuvianite*

cubanite*

metatorbernite* *vivianite* *cuprite*metazeunerite* *wavellite* **waylandite*

cuprosklodowskite*

millerite

cyanotrichite*

mixite*whitmoreite*

devillite*

mohrite* *wittichenite*

dickite* * *molybdenite* * *wolframite* * * *

digenite*molybdite*wollastonite

diopside*monazite-Ce)*

wulfenite**

dioptase*montmorillonite*

xenotime-(Y)djurleite*

morinite*zavaritskite

dolomite* *muscovite* * * *

zeunerite

dufrénite*

nacrite* *zinnwaldite

dumortierite*

natrodufrénite

*zippeitedussertite*

natrojarosite*

zirconearlshannonite*

nickeline

emplectite*

nickel-skutterudite

epidote* *nováèekite

erythrite* *oliveniteeuchroite*

opal

eulytite
euxenite-(Y)

*
*

*
*

*

UNK2

*

UNK3

*

*

UNK4

*

orthoclase* * * *

UNK5

petitjeanite

*

UNK6

*

* *

UNK7

*

*

UNK8

*

UNK9

*

* *

UNK10

*

*

UNK11

*

*

pharmacosiderite

ferritungstite*

phenakite

ferrocarpholite*

phlogopite*

phosphosiderite

*

* *
*

UNK1

ferrimolybdite

ferrotapiolite

* *
* *

* *

pharmacolite

*

*

*

*

ferrocolumbite*

zwieselite

ferberite

phosphuranylite

*

* *

*

*

*

*

1 – Vysoký Kámen (feldspar) deposit (Sejkora et al. 2006a); 2 – Vysoký Kámen (greisen) locality (Sejkora et al. 2006a); 3 – Huber and Schnöd
stock, Gellnauer vein system, Krásno (Sejkora et al. 2006b, c, d); 4 – Horní Slavkov uranium ore district (Plášil et al. 2006, Sejkora et al. 2006c).
Minerals studied during the present project are shown by bold print (Sejkora et al. 2006a–d; Plášil et al. 2006).

intergrowths of arsenopyrite with the enumerated minerals also occur. Cavities with arsenopyrite contain younger
clay minerals and fluorite. Arsenopyrite is usually leadgrey with bluish iridiscent colour and silver grey withmetallic lustre on fresh fractures. It has been commonly
found in grains of about 1 cm in size, often partly affectedby supergene alteration. Exceptionally well-formed crystals (Fig. 18), up to 5 cm long, occurred in the cavitiesof quartz veins in the outcrops of the Huber stock. Arsenopyrite from these localities is associated with quartz
grading to rock crystal and sulfides.
Carpholite
Carpholite (Figs 19 and 20) is a relatively rare mineralat these deposits. Specimens from Krásno served as a typematerial on which Kenngott (1851) described this species as a new mineral. Gehlièka (1858), Glückselig(1862) and Klvaòa (1886) also described carpholite

occurrences in the district. Documented finds include
VIIIth to Xth level in the central part of the Schnöd stockand the area of inclined tunnel between the 4th level anda site at the level of 500 m a.s.l. Besides these places,
carpholite also occurred in the Huber open pit and at the
4th level in association with hübnerite.
At the VIIIth level of the Schnöd stock, there was acluster of carpholite veins up to 10 cm wide. The mineral is associated with siderite, fluorite, and rare Fe-richcarpholite. The marginal parts of veins carried hübnerite. The largest occurrence of carpholite is between the IXthand Xth level of the Schnöd stock. The veins intersect bothlevels. The widest veins measured 15 cm while the common width was 1 cm. Carpholite from these occurrences
has a bright yellow-golden colour and is associated withrhodochrosite, fluorite, apatite, hübnerite and cassiterite.
In the so-called Dovrchní area, carpholite occurredin a vein with hübnerite and clay minerals in an adit at
the 4th level. The largest carpholite vein occurred at a site

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Journal of the Czech Geological Society 51/12(2006)

Fig. 18 Crystal of arsenopyrite in quartz
gangue, Krásno near
Horní Slavkov. Widthof photo 3 cm; Nicon
SMZ1500 microphotography (J. & E. Sejkora).

Fig. 19 Carpholite vein
formed by radiating fibrous crystals, Schnöd
stock, Krásno near
Horní Slavkov. Widthof photo 5 cm; CanonDS1 macrophotography (J. & E. Sejkora).

Journal of the Czech Geological Society 51/12(2006)

23

Fig. 20 Carpholite veinlets in altered greisenrock, Schnöd stock,
Krásno near Horní
Slavkov. Width of photo
8 cm; Canon DS1 macrophotography (J. & E.
Sejkora).

500 m. a.s.l. Carpholite with apatite formed 6 cm wideveins and radiating aggregates along country rock fractures. An exceptional find in the Kaiser shaft area at the
500 m level was a cavity with crystals of quartz, fluorite
and apatite, which supported individual acicular carpholite crystals reaching the size up to 4 cm.
Cassiterite
As a matter of course, all authors dealing with these deposits mention cassiterite. Detailed information on cassiterite present for example Erben (1884), Klvaòa (1886)
and Heilmaier (1930). In rocks of the Huber stock, cassiterite occurs in grains from a fraction of mm to 2 cm
(Drozen 1965). The mineral has a honey brown to black
colour and it is transparent in thin fracture splinters withbrown to red shade. It is common to see colour variationin single grains in thin section under the microscope. The
crystals are highly lustrous with a vitreous to adamantine lustre. Cassiterite shows a strong tendency to euhedral crystallization in all paragenetic settings. However,the crystals are often unevenly developed. The best specimens come from quartz vein cavities and local bonanzas where cassiterite crystallized in clay matrix. Thereis hardly any record of single crystals, since cassiterite
has a strong tendency to twinning (Figs 21 and 22). It
forms twins in simple cases but octuplets are not rare(Figs 23 and 24). As the first genetic setting, cassiterite
occurs in greisens and some altered granites in grains to
1 mm and often strongly fractured. The grains show locally colour zoning and lamellar deformation twinning.
Macroscopic cassiterite occurs in greisens at the Huber
open pit and in some coarse-grained quartz-topaz greis-ens. It is accompanied by sulfides. At other places, it represents usually a single ore component.
In the second genetic type, cassiterite occurs in quartzcassiterite and quartz-cassiterite-sulfide veins. Cassiterite forms anhedral, equant grains several cm in diameter. This cassiterite is usually younger than some part ofthe vein quartz. A special type of this mineralization is
the so-called quartz body at position of the 3rd level,

Fig. 21 Idealized drawing of
crystal twin of cassiterite from
Krásno near Horní Slavkov(according to Jeek 1932).

Fig. 22 Idealized drawing of
cassiterite crystals showing
multiple twinning from Krásno
near Horní Slavkov (according
to Jeek 1932).

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Journal of the Czech Geological Society 51/12(2006)

Fig. 23 Crystals of cassiterite, Krásno near
Horní Slavkov. Widthof photo 5 cm; CanonDS1 macrophotography (J. & E. Sejkora).

Fig. 24 Cassiterite twin
crystal, Krásno near
Horní Slavkov. Widthof photo 5 cm; CanonDS1 macrophotography (J. & E. Sejkora).

Journal of the Czech Geological Society 51/12(2006)

carrying dominantly quartz-wolframite mineralization. At
this place, cassiterite is clearly the youngest mineral, deposited on quartz crystals in cavities.
The third type of cassiterite occurrence is in ore pocketin the so-called bonanzas. These nests of a lenticular or
loaf-like shape are about 50 cm long and 2030 cm thick,or exceptionally larger. They occur in greisens and rarely in greisenized granite. The open spaces are filled by a
mixture of clay minerals, most frequently greenish yellow flaky dickite and cassiterite, sometimes accompaniedby perfectly crystallized topaz. The mechanism of formation of these pockets is not clarified, as there are no fluid conduits observed in their vicinity.
Probably the largest cassiterite crystals occur in quartz
veins, in cavities and in bonanzas in top parts of thestocks. Historical collections contain multiple crystal
twins up to 20 cm in size. Loose cassiterite crystals to
5 cm sizes have been found during mining in numerous
pockets in the last decades. Small-sized crystals (usually smaller than 2 cm) were abundant in the open pit at
the Huber stock. Perfect twins to 7 cm were rare. Also
notable is find of brown cassiterite crystals to 5 cm in aquartz vein at the 4th level of the Huber stock. Exceptional
are specimens of light brown 1 cm crystals, which aretransparent with some translucent areas, from quartz veinwith sulfides at an extraordinary level at 500 m a.s.l.
Chalcopyrite
Jantsch (1854, 1858), Krejèí (1855), Glückselig (1862),Klvaòa (1886), Katzer (1892) and other authors describedchalcopyrite occurrences in the district. It is widely distributed in several generations (Drozen 1965). Only some
important documented finds can be mentioned here. Chal-

Fig. 25 Group of chalcopyrite crystals from
Krásno near Horní
Slavkov. Width of photo
12 cm; Canon DS1 macrophotography (J. & E.
Sejkora).

25

copyrite typically occurs as impregnation with other sulfides in apical parts of the stocks. During some periodsof mining chalcopyrite was dressed to chalcopyrite concentrate. With increasing depth chalcopyrite content
sharply declined and no occurrence was recorded below
the 4th level of the Huber shaft.
At the Schnöd stock chalcopyrite together withsphalerite impregnated the uppermost part composed ofgreisen. In a similar way, chalcopyrite with arsenopyrite,
sphalerite, and some other sulfides occurs in greisen at
the Huber stock. The largest aggregates of compact chalcopyrite are several cm long, e.g. at the Xth and VIIIth levels of the Schnöd stock, at a site near 500 m a.s.l. of the
shaft Kaiser. Quartz, sphalerite, bornite, tetrahedrite, andother minerals accompany chalcopyrite.
Crystallized chalcopyrite (Figs 25 and 26) was common in quartz veins inside the stocks as well as in thegneiss envelope. This is documented by specimens in old
mineral collections, finds at old dumps behind the ventilation shaft No. 2, the dumps around the Huber stock orat the outcrop of the Gellnauer vein system. Tunnelingworkings on new ventilation shaft exposed veins withmassive aggregates of chalcopyrite having dm sizes, withsphalerite and cassiterite. This find probably belongs to
the Ondøejská vein. Chalcopyrite crystals from quartz
veins are 0.5 to 1 cm in size and associate with fluorite,
sphalerite, cassiterite, apatite, chalcedony, wolframite,and others. During modern mining of cassiterite, crystallized chalcopyrite was very rare. Crystals often carrycomplete coating of blue or blue-violet covellite andreach only 5 mm at maximum. At the Xth level of the
Schnöd stock, chalcopyrite crystallized to 3 mm is associated with triplite, siderite, apatite, fluorite, cassiterite,
topaz, and quartz.

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Journal of the Czech Geological Society 51/12(2006)

Fig. 26 Chalcopyrite
crystals overgrown byviolet fluorite, Krásno
near Horní Slavkov.
Width of photo 1.1 cm;
Nicon SMZ1500 microphotography (J. &E. Sejkora).

Fluorapatite
It belongs to minerals widely known from the district. It
is mentioned already by Zippe (1847), Jantsch (1853,
1854), and Glückselig (1862). Several types of fluorapatite occur in various mineral associations.
Rock-forming fluorapatite is a primary accessory
mineral in tin-bearing granite. It occurs in subhedral

crystals enclosed in mica or some other minerals. A hydrothermal fluorapatite is anhedral and it occurs in relatively larger grains in greisens or altered mineralized
granite. Fluorapatite in cavities of greisen forms macroscopic compact and irregular infillings of red-brown
to brown colour. On microscopic scale, granular aggregate or an aggregate of well-formed small crystals areobserved, which are often associated with fluorite. In

Fig. 27 Fluorapatite
crystals in cavity ofquartz gangue, Krásno
near Horní Slavkov.
Width of photo 7 cm;
Canon DS1 macrophotography (J. & E. Sejkora).

Journal of the Czech Geological Society 51/12(2006)

places, the masses are porous and coated by small macroscopic crystals.
Of mineralogical interest are nearly perfectly formed
crystals up to 2 cm large in cavities of quartz veins (Figs

Fig. 28 Group of fluorapatite crystals on partly weathered quartz
gangue, Krásno near
Horní Slavkov. Widthof photo 12 cm; CanonDS1 macrophotography(J. & E. Sejkora).

Fig. 29 Fluorapatite
crystals on quartz
gangue, Krásno near
Horní Slavkov. Widthof photo 1.1 cm; Nicon
SMZ1500 microphotography (J. & E. Sejkora).

27

2731). They are often associated with cassiterite andsulfides. Their colour ranges from green and yellow,
through pink, violet, blue and brown to colourless. Crystal habitus is prismatic to lenticular, with a large number

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Journal of the Czech Geological Society 51/12(2006)

Fig. 30 White columnar
crystals of fluorapatite
in cavity of quartz
gangue, Krásno near
Horní Slavkov. Widthof photo 9 mm; Nicon
SMZ1500 microphotography (J. & E. Sejkora).

Fig. 31 Fluorapatite
crystal, Krásno near
Horní Slavkov. Widthof photo 1.8 cm; Nicon
SMZ1500 microphotography (J. & E. Sejkora).

Journal of the Czech Geological Society 51/12(2006)of crystal faces. Rare examples of multicoloured, zoned
prismatic crystals were noted. Fluorapatite occured especially in surface outcrops of the Huber stock in quartz
veins inside as well as outside the stock. This material
was moved to a secondary location to dumps between the
Huber quarry and ventilation shaft No. 2. Exceptionallyesthetic specimens, carrying pink and violet fluorapatite
crystals of 5 mm size on 10 cm smoky quartz crystals andaccompanied by cassiterite and sulfides, were found in acavity in the NW forefield area.
Druses of fluorapatite carrying clusters of small crystals cover the cavities in granite, greisen or in marginal
pegmatite. A similar type of occurrence in gneisses has
a green colour of fluorapatite. This type comes especially from a site at 500 m a.s.l., in the section of cave-in
reserves. Nice specimens of this type occured at the Xthlevel of the Schnöd stock or in marginal pegmatite in the
NW forefield.
Fluorapatite forms perfectly shaped crystals up to 5 cmlong in mylonitic clay and alteration material of somedislocation zones. The crystals are usually green, grey
blue or violet. Cavities and negative imprints after dissolved crystals occurred, sometimes with skeletal fluorapatite remains. The preserved crystals are rather rare
and they were collected mainly at upper levels of all exploited stocks or in the Gellnauer quartz veins.
Compact or massive fluorapatite occurs with otherphosphate minerals in phosphate-rich accumulations (Sejkora et al. 2006d).

Fig. 32 Zoned fluorite
crystals in cavity ofquartz gangue, Krásno
near Horní Slavkov.
Width of photo 1.8 cm;
Nicon SMZ1500 microphotography (J. & E.
Sejkora).

29

Very young fluorapatite generation (probably supergene) forms finely acicular to fibrous aggregates similar
to cotton wool and finely crystalline coatings of white,yellowish, grey, reddish or brown colour on other minerals. This type is known from nearly whole district but
it is particularly abundant in the cave-in reserves of the
Huber stock. Especially fine, colourless or light pink acicular crystals with silky lustre or earthy coatings andinfill in coroded older fluorapatite or triplite are characteristic.
FluoriteKrejèí (1855), Nowicki (1857), Jantsch (1858), Glückselig (1862), Klvaòa (1886), and numerous other authors
reported fluorite occurrence. Fluorite is one of widelydistributed minerals at the deposits. It occurs as impregnation in various rocks, it forms veinlets up to several
cm wide, either monomineralic or in association with other minerals. Fluorite colours are varied, but dark violet
colour is the most typical (Figs 3236).
In the Gellnauer vein cluster, fluorite occurs as 4 cm
long octahedra consisting of tiny hexahedral crystals.
Similar fluorite (usually light violet and partly transparent) comes from the open pit in the Huber stock and fromsome quartz veins at the level 500 m a.s.l., often in association with fluorapatite and other minerals. Quartz
veins usually carry violet fluorite hexahedra and yellow
crystals are rare. Green fluorite is known from rare oc-30

Journal of the Czech Geological Society 51/12(2006)

Fig. 33 Group of dark
violet fluorite crystals,
Krásno near Horní
Slavkov. Width of photo
1.8 cm; Nicon SMZ1500
microphotography (J. &E. Sejkora).

Fig. 34 Dark violet toblack fluorite crystals,
Krásno near Horní
Slavkov. Width of photo
2 cm; Nicon SMZ1500
microphotography (J. &E. Sejkora).

Journal of the Czech Geological Society 51/12(2006)

31

Fig. 35 Rare yellow,
partly zoned crystalsof fluorite on quartz
crystals, Krásno near
Horní Slavkov. Widthof photo 1.2 cm;
Nicon SMZ1500 microphotography (J. &E. Sejkora).

currence in cavities in quartz at old dumps behind theventilation shaft No. 2.
Fluorite hexahedra are exceptionally large to several
cm, while crystals up to 1 cm in size are common. Some
cavities in quartz vein at the level of 500 m a.s.l. carried
crystals to 3 cm sizes. Interesting is the association of
black-violet fluorite with zinnwaldite and fluorapatite. A
unique sample with individualized acicular carpholite
crystals was collected. Also unusual are compact violet
fluorite masses with enclosed or intergrown thin needles
or radiating aggregates of carpholite (or clay mineral
pseudomorphs after carpholite) from the VIIIth level ofthe Schnöd stock. Specimens with perfect octahedral
crystals of violet fluorite about 1 cm size occurred in
vuggy quartz vein from the level of 455 m a.s.l. Anotherinteresting example from milky white quartz mass at the
5th level of the Huber stock is a fluorite in 1 cm colourless crystals enclosing 5 mm hexahedra of dark violet fluorite. At the NW forefield fluorite crystals to 5 mm, associated with clay minerals, show corroded crystal faces.
Hübnerite

Fig. 36 Fluorite crystal overgrowing white columnar crystals of fluorapatite, Krásno near Horní Slavkov. Width of photo 4 mm; Nicon
SMZ1500 microphotography (J. & E. Sejkora).

Several old-time mineralogists described this mineral
under the obsolate name of megabasite, for the first timein 1869 (Kratochvíl 19571964). Hübnerite was very
abundant in quartz veins of the Gellnauer cluster as acicular crystals up to 4 cm long and 4 mm wide (Figs 37

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Journal of the Czech Geological Society 51/12(2006)

Fig. 37 Group of columnar hübnerite crystals, Krásno near Horní
Slavkov. Width of photo
1 cm; Nicon SMZ1500
microphotography (J. &E. Sejkora).

Fig. 38 Group of lathlike hübnerite crystals,
Krásno near Horní
Slavkov. Width of photo
1.5 cm; Nicon SMZ1500
microphotography (J. &E. Sejkora).

Journal of the Czech Geological Society 51/12(2006)

33

Fig. 39 Group of tinylath-like hübnerite
crystals, Krásno near
Horní Slavkov. Widthof photo 2.5 mm;
Nicon SMZ1500 microphotography (J. &E. Sejkora).

39). The crystals show reddish reflections. Even atpresent, it is possible to collect similar hübnerite but insmall size crystals to 1 cm on old dumps behind the ventilation shaft No. 2. The mineral occurs in quartz gangue
with fluorite, quartz, chalcopyrite, and other less common minerals. Small crystals, rarely to 1 cm, occurredin the Huber open pit.
Hübnerite was common at the level of 500 m a.s.l. incavities in quartz in greisen and in quartz veins intersecting the stock. Very interesting and exceptional was a findof perfectly transparent, strong red acicular crystals to
5 mm from a site near the level of 500 m a.s.l., adit CH
4062. Some of the crystals are translucent, of blood-red
colour. These specimens can be considered as the purest
known (end-member) natural hübnerite. Also interestingis hübnerite occurrence in carpholite veins in association
with fluorite, rhodochrosite, apatite, and cassiterite at the
VIIIth and Xth levels of the Schnöd stock.
QuartzAll authors dealing with the district mentioned quartz as
the main mineral in ore. Quartz is especially abundant ingreisens. White massive quartz is present in quartz veinsand quartz bodies (e.g., 3rd and 5th level) up to several mlong. These bodies and some cavities in greisens containcrystals of common milky quatz to 0.5 m. Such cavities
occurred at the 5th level of the Huber stock, at the 4th level, and the extraordinary level at 500 m a.s.l. in the former
Kaiser shaft area. Similar quartz crystals have been foundat oucrops of the Huber stock or at old dumps in sur-roundings. Besides the large crystals, more common aresmall crystals of about 1 cm size (Fig. 40), coating cavities or fractured parts of the rocks. In granite stocks andin gneiss, quartz veins carry abundant quartz crystals to
10 cm sizes.
In addition to common quartz, some coloured varieties occur in the district. Amethyst crystals were observedat the 5th level of the Huber stock and at the Xth level ofthe Schnöd stock. Amethyst has been found also at the
4th level of the SE forefield. Citrine crystals to 3 cm occurred in the open pit at Huber stock. Somewhat moreabundant are finds of smoky quartz, up to 15 cm in size,in particular in the Huber open pit. Best known is a 1.5 mhigh cavity at the 4th level of the NW forefield coated byperfectly transparent smoky quartz crystals to 15 cm sizes. The cavity also yielded perfectly black morion druses with individual crystals reaching 5 cm.
Wax-white chalcedony occurs according to Hoffmann(1903) and Kratochvíl (1963) as one of late depositedminerals. It forms botryoidal aggregates passing sometimes to stalactiform shapes. Colours are usually white,
blue or yellow. Chalcedony coats early crystallized minerals such as quartz, fluorite, apatite, chalcopyrite, wolframite, etc.
Jasper has been mentioned without closer identification by some older authors as a monomineralic infillingin numerous veins striking mainly NW-SE to W-E. Recent mining exposed jasper in two veins. The first one
crossed the gallery at the 4th level in a central part of the
Huber stock. The material is jasper of a bright red colour filling a vein from 15 to 20 cm wide. A second find

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Journal of the Czech Geological Society 51/12(2006)

comes from the 5th level at the same stock, where 10 cm
wide vein of pink jasper was at both sides lined up by
quartz crystals locally grading to amethyst.
Molybdenite

Fig. 40 Quartz crystal overgrown by chalcopyrite and fluorite, Krásno
near Horní Slavkov. Width of photo 2 cm; Nicon SMZ1500 microphotography (J. & E. Sejkora).

The old information on molybdenite occurrence is provided by Zepharovich (1857), Jantsch (1854), Glückselig (1862), Klvaòa (1886), Krejèí (1855), Jantsch (1858),
Katzer (1892), and other authors. Molybdenite is located in pockets of white quartz and in quartz veins. Sometimes, it is dispersed in greisen of the stocks. The largest flakes of molybdenite in the open pit at Huber stock
reached up to 5 cm sizes. Molybdenite crystals (Fig. 41)
occur in vuggy quartz in association with fluorite, apatite, emplectite and bismuth. The largest well-formed
crystals of a bright silvery colour and perfect metallic
lustre reached 1 cm sizes. At some places, it is coveredby a thin oxidation coating and has a mat appearance.
Molybdenite was relatively common at dumps from underground mining of quartz veins in proximity of bothgranite stocks. In underground workings, the largest molybdenite occurrence is known from a level at 455 m a.s.l.
A several m long block of greisen with a high topaz content carried a strong impregnation of small molybdenite
grains. At the NW forefield a tectonic mirror several
m2 in size consisted of a smeared, 1 cm thick molybdenite layer with minor tectonic striations.

Fig. 41 Molybdenite
crystals in cavity ofquartz gangue, Krásno
near Horní Slavkov.
Width of photo 1.3 cm;
Nicon SMZ1500 microphotography (J. &E. Sejkora).

Journal of the Czech Geological Society 51/12(2006)

Rhodochrosite
Rhodochrosite is the single carbonate relatively widespread in the district. It belongs to the youngest manganese stage of mineralization. In analogy to other manganese minerals, the mineral was more frequent at the
Schnöd stock than at the Huber stock. At the latter location, rhodochrosite occurred at the level at 500 m a.s.l.
in the area of cave-in reserves as monomineralic aggregates associated with clay minerals. Well-preserved
rhodochrosite specimens come from the VIIIth and Xthlevel of the Schnöd stock. At the first place it occurred
jointly with carpholite and in monomineralic veins. At
the second location, it is associated in several places withcarpholite, fluorite, clay minerals or it formed monomineralic veins. Rhodochrosite aggregates of bright reddish
colour are up to 10 cm large. In the same area, pink crystals to 1 cm sizes associated with fluorite and pseudomorphs of clay minerals after carpholite occur. Numerous small finds of rhodochrosite were recorded from the
4th level at the Huber stock.
Scheelite
Ferber (1774) published an early record of scheelite, followed by Glückselig (1862) and Klvaòa (1886). The oldest specimens of scheelite from Krásno and Horní Slavkov are deposited in the collections of the National Museum

35

in Prague (Fig. 42). The largest crystals reach 10 cm sizes, but their accurate location is unknown. The specimens
date from the late 18th and 19th century. This time indicates
the Gellnauer set of veins as a probable source. The crystals are usually of white or grey-white colour. Smaller crystals about 1 cm show brown to honey colour shades.
During the period of mining after 1945, scheelite finds
were rather sporadic. A granular scheelite intergrownwith quartz occurs at old dumps in proximity of the pub
Kreuzech. The material comes from mining of theGellnauer veins. Three finds from the late undergroundmining are documented. The best specimen is a groupcomposed of crystals up to 4 cm in size from quartz veinat the 4th level of the Huber stock, where it was associated with wolframite and apatite. This scheelite crystal
cluster has a fine coating of iron oxides. Additional samples from the same spot carry only a few small scheelite
crystals. Most abundant scheelite is recorded at the levelof 500 m a.s.l. in the places of the former Kaiser shaft,where it occurred with sphalerite and chalcopyrite in botryoidal zinnwaldite. New scheelite find comes from ventilation tunnel at the 4th level of the Huber stock. The
quartz vein carried anhedral scheelite grains to 5 cm sizeand small scheelite crystals to 5 mm sizes in cavities withwolframite, apatite, sphalerite, chalcopyrite, clay minerals, and some secondary copper minerals including malachite, pseudomalachite and azurite.
Sphalerite
Glückselig (1862), Sadebeck (1869), Döll (1883), Klvaòa
(1886), and others mentioned sphalerite in the Krásno ore
district. According to old reports, sphalerite formed striated hexahedra with blunt edges, up to 23 cm in size,
in bonanza type of cassiterite accumulations. This typeof specimens is preserved in some mineral collections.
During the modern mining period this type of sphalerite
has not been recorded (Drozen 1965).
Sphalerite is a common mineral in apical parts of bothgranite stocks. Dark brown to black crystals to 5 mm havebeen lately found in the outcrops of the Huber stock inassociation with other sulfides. Greisen exposed in the
cave-in material at the Huber stock shows sphalerite impregnation, which is a feature characteristic also of the
Schnöd stock above the VIII th level. The colours of
sphalerite range from black through a bluish black tobrown.
Topaz

Fig. 42 Scheelite crystal in cavity of quartz gangue, Krásno near Horní
Slavkov. Width of photo 1.5 cm; Nicon SMZ1500 microphotography(J. & E. Sejkora).

Early descriptions of topaz from Horní Slavkov include
those by Lindacker (1791), Presl (1837 in Drozen 1969),
Gehlièka (1858), Groth (1870), and many other mineralogists. Rosický (1916) published a monographic study
comparing crystal morphology of topaz from various localities. In addition to paragenetic series introduced by
Groth (1870), he brings some new ones. Rosický (1916)
documented 27 types of crystal faces plus four addition-

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Journal of the Czech Geological Society 51/12(2006)

Fig. 43 Drawings of topaz crystals from Krásno near Horní Slavkov (according to Rosický 1916)

Fig. 44 Drawing of crystal faces of topaz from Krásno near Horní
Slavkov (according to Rosický 1916)

Another notable topaz accumulation was found at the 5thlevel of the Huber mine. Topaz crystallized in mixtureof clay minerals together with quartz and apatite crystals.
Topaz crystals to 1 cm sizes have imperfect crystal
shapes, are grey, yellowish or yellow green in colour.
There were rare finds of topaz with perfect crystal
shapes in the open pit at the Huber stock. This included
sky blue crystals to 1 cm size, fractured honey yellow
crystals to 1 cm, and transparent crystals to 5 mm sizes
with a strong glassy to adamantine lustre. The largest
crystals found during the recent mining come from aquartz lense at the Xth level of the Schnöd stock in association with quartz, cassiterite, fluorite, phosphates, andchalcopyrite. The light blue crystals were up to 3 cm
long. Relatively common were monomineralic lenses offine-grained topaz (topazite), e.g, at the levels 500 m
a.s.l., 455 m a.s.l., and in the NW forefield of the stocks.
Wolframite

al uncertain planes (Figs 43 and 44) on topaz from this
district.
Topaz is a characteristic mineral (Figs 45 and 46) inthis ore district, associated nearly with all primary minerals at the deposits, from magmatogenic to hydrothermal stages of crystallization. Ever present fluorite indicates abundance of fluorine in the deposit, while thedecomposition of feldspars supplied silica and alumina.
It was subject to decomposition and replacement by other minerals. Replacement by younger quartz, clay minerals in at least two generations, fluorite, and by cassiterite and sulfides was noted.
The largest accumulations of topaz crystals came fromore pockets or from lenses composed of nearly monomineralic topaz, or of quartz and clay minerals. Such topaz-rich lenses are known from the level at 455 m a.s.l.,where imperfectly crystallized topaz with a mixture ofyellow clay minerals forms a body of several m in size.

Haidinger (1830), Krejèí (1851), Klvaòa (1886), and other authors reported wolframite from the ore district. Kratochvíl (1963) published an extensive summary of information from old literature. According to study ofmesoscopic textures and data from ore microscopy wolframite is the oldest ore mineral. It is black brown or
black in colour, has characteristic crystal shapes: tabular, ax-shaped, acicular, and prismatic grains from mm
up to 10 cm (Fig. 47) or simply massive. Wolframite was
replaced by numerous younger minerals including dickite (Drozen 1965). Wolframite was the second economic
component after cassiterite but its contents were approximately 10 times lower.
Wolframite crystals from 2 to 5 cm long in cavities ofquartz veins were often collected in the open pit at the
Huber stock and in old dumps after mining of quartz
veins of the Gellnauer set of veins. The same places
yielded wolframite aggregates of dm dimensions inter-

Journal of the Czech Geological Society 51/12(2006)

Fig. 45 Pale yellow topaz crystals in quartz
grangue, Krásno near
Horní Slavkov. Widthof photo 4.5 mm; Nicon
SMZ1500 microphotography (J. & E. Sejkora).

Fig. 46 White topaz
crystals in quartz
grangue, Krásno near
Horní Slavkov. Widthof photo 1.8 cm; Nicon
SMZ1500 microphotography (J. & E. Sejkora).

37

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Journal of the Czech Geological Society 51/12(2006)

Fig. 47 Prismatic wolframite crystal in quartz
gangue, Krásno near
Horní Slavkov. Widthof photo 10 cm; CanonDS1 macrophotography (J. & E. Sejkora).

grown in milky quartz. Similar specimens, in part withradiating aggregates of wolframite, came from quartz
lenses at the 3rd level of the Huber stock. Wolframite wasrelatively abundant at the 500 m level in area of cavein reserves. Several quartz-wolframite veins carriedwolframite crystals to 20 cm sizes at these places. Unusual topaz-wolframite bonanza accumulations have beenencountered at the 5th level of the Huber stock.
Conclusion
The Krásno ore district carries the largest reserves of tin
and tungsten ores in the Slavkovský les region. The ore
district comprises several deposits with the classic granite related mineralization in greisens in apical parts ofgranite cupolas and in their forefield as well as in theveins in the gneiss envelope. As to the level of knowledge, quality and quantity of reserves, the Huber stockis the most important deposit. Exploitation of this deposit
early in the 16th century resulted in leading role of its tin
in the tin market of Europe, situation, which lasted forsome decades. In these respects, the tin ore district
reached the status of important mining districts, such as
Jáchymov, Pøíbram and Kutná Hora in Bohemia. During
centuries, numerous specialists in mineral deposits, petrology, mineralogy, hydrogeology, ingeneering geology,
geochemistry and other branches of geoscience studied
the deposits. As a result, the extensive literature related
to this ore district has been published.
Exploitation of these deposits has yielded a large number of rare and exceptional mineral specimens. Carpholite has been described as a new mineral from the Krás-

no ore district and numerous mineral species were described as the first occurrence in the Czech Republic. 228
mineral species are known to be present in the district.
In this context, the Krásno ore district represents an exceptional mineralogical locality in the Czech Republic,
known by its specimens worldwide.
It is noteworthy that various exploration projects in
the Krásno ore district brought positive results. However, this qualification relates to practice common in theSoviet block countries during the period of 19601989,
when the value of some important metals was considered separately from the prices prevalent on the world
market. In order to fulfill the expected increase in ore
reserves, new potential ore reserves have been measured. Although tin exploitation during the past centuries and up to 1991 mined out large quantities of metal, the Krásno ore district still contains significant
quantities of tin and tungsten. Unlike the exhausted deposits of Jáchymov and Pøíbram, the Krásno ore district,along with the Cínovec deposit in the Kruné hory, stillcontain significant potential reserves of Sn-W ores in
the Czech Republic. The future use of these reserves
will depend on tin and tungsten prices on the world
market.
Acknowledgements. The present authors gratefuly acknowledge cooperation by Stanislav Vrána, Czech Geological
Survey, Prague, Jiøí Litochleb and Dalibor Velebil, National
Museum, Prague, in preparation of this text. This work
was financialy supported by the Ministry of Culture of
the Czech Republic (Project MK00002327201).
Submitted July 12, 2006

Journal of the Czech Geological Society 51/12(2006)

References
Agricola, G. (1556): De re metallica libri XII.  Basilae
Barvíø, J. L. (1903): Pøehledné zprávy o nìkterých naich místech zlato a
støíbronosných z poslední ètvrti 16. století.  (Brief reports on goldand silver production in the last quarter of the 16th century).  Horn.
hutn. Listy, 4. (in Czech).
Beran, P. (1999): Nerosty cíno-wolframových loisek Slavkovského lesa.
 (Minerals in the tin-tungsten deposits of the Slavkovský les area.) Okresní muzeum a knihovna Sokolov, 287 pp. (in Czech).
Beran, P.  Beranová, V. (1995): Petrologie a mineralogie Sn-W loisek
v oblasti Krásna a Horního Slavkova.  (Petrology and mineralogyof the Sn-W deposits in the Krásno and Horní Slavkov district.)  In:
Závìreèná likvidaèní zpráva závodu Stannum, Rudné doly s.p.
Pøíbram, Geofond Praha FZ6630. (in Czech).
Beran, P.  Fikar, M.  Ondru, P.  Øídkoil, T.  rein, V.  Veselovský, F.
(1989): Sekundární mineralizace z cíno-wolframového loiska Horní
Slavkov.  (Secondary minerals in the Horní Slavkov tin-tungsten
deposit.)  Nepublik. zpr., Rudné doly s.p. Pøíbram, archiv Okr. muz.
a knih. Sokolov. (in Czech).
Beran, P. a kol. (2001): Královské horní mìsto Horní Slavkov.  (Horní
Slavkov and its history of Royal Mining Town.)  Mìsto Horní
Slavkov ve spolupráci s Okresním muzeem Sokolov. (in Czech).
Bernardová, E.  Poubová, M. (1961): Mineralogicko-petrografický
posudek vzorkù achta 8  Horní Slavkov.  (Mineralogical-petrographical report on samples from the shaft No. 8.)  Nepubl. zpráva
Geol. prùzk. Støíbro, In: Blüml, A.  Tacl, A.: Mineralogickogeochemický rozbor rudního materiálu achty è. 8  Horní Slavkov.
Geofond Praha P97418. (in Czech).
Bílek, J. (1957): Dìjiny dolování v oblasti Horní Slavkov  Krásno, I.
Pøedbìná zpráva o montanistických a geologických pomìrech
Hubského pnì.  (History of mining in the Horní Slavkov  Krásno
district, I. Preliminary report on mining and geological situation at
the Huber stock.)  Geofond Praha P9253. (in Czech).
 (1958): Zpráva o báòsko-historickém výzkumu Horní Slavkov II. (Report on research of mining and history in Horní Slavkov, part II.)
 Geofond Praha P9959 (in Czech).
Breiter, K.  Sokolová, M.  Sokol, A. (1991): Geochemical specializationof the tin-bearing granitoid massifs of NW Bohemia.  Mineral. Deposita, 26: 298306.
Cornu, F. (1905): Zur Kenntnis des Schlaggenwalder Mineralvorkommens.
 Tschermaks mineral. petrogr. Mitt., 24, Wien.
 (1906): Versuche über saure und alkalische Reaktion von Mineralien.
 Tschermaks mineral. petrogr. Mitt., 25, Wien.
Döll, E. (1883): Eine neue und einige seltene Pseudomorphosen von neuen
Fundorten.  Verh. Geol. Reichsanst., Wien.
Drozen, J. (1965): Výroèní zpráva o plnìní úkolu Geologické pomìry
loiska Hubský peò za rok 1965.  (Annual report for 1965, projectGeology of the Huber stock deposit.)  Nepublik. zpr., archivRudných dolù s.p. Pøíbram. (in Czech).
 (1967): Geologické pomìry loiska Hubský peò, Výroèní zpráva za
rok 1966.  (Annual report for 1966, project Geology of the Huber
stock deposit.)  Nepublik. zpr., Rudné doly n.p. Pøíbram, Geofond
Praha P22656. (in Czech).
 (1969): Geologické pomìry Sn-W loiska Hubský peò u Krásna nad
Teplou (Slavkovský les).  (Geology of the Huber stock Sn-W deposit near Krásno nad Teplou (Slavkovský les area).)  Kandidátská
dizertaèní práce, Geofond Praha P22651. (in Czech).
Erben, B. (1884): O èeských nerostech.  (On minerals in Bohemia.) 
Vesmír, 13: 20. (in Czech).
Ferber, J. J. (1774): Beiträge zu der Mineral  Geschichte von Böhmen. 
BerlinFiala, F. (1948): Struèné vyjádøení o loisku Sn-W rud v Horním Slavkovì.
 (A brief evaluation of the Horní Slavkov Sn-W deposit.)  Nepubl.
zpr., Geofond Praha. (in Czech).
 (1950): Zpráva o geologickém výzkumu rudonosné oblasti ( Sn-W,Cu)u Horního Slavkova a Krásna n. Teplou provedeném v letech 1946

39

1950.  (Report on geological research of ore-bearing district (Sn-W,
Cu) near Horní Slavkov and Krásno n. Teplou during the period 1946
1950.)  Nepubl. zpr., Geofond Praha P3310. (in Czech).
 (1952): Zpráva o geologických výzkumech v rudním obvodu
u Horního Slavkova a Krásna nad Lesy provedených v roce 1946. (Report on geological research in the Horní Slavkov and Krásno nad
Lesy ore district in 1946.)  Nepubl. zpr., Geofond Praha. (in Czech).
 (1962): Základní geologický výzkum Císaøského (Slavkovského) lesa.
Závìreèná zpráva o výzkumném úkolu za léta 19551960.  (Geology of the Císaøský (Slavkovský) les area. Final report for the 1955
1960 period.)  Nepubl. zpr., Archiv ÈGÚ. Praha. (in Czech).
 (1958): Hlavní typy hornin v irím okolí Pramenù.  (The main rocktypes in the Prameny area.)  Geol. práce, 50; 370. Bratislava. (inCzech).
 (1968): Granitoids of the Slavkovský Les Mountains.  Sbor. geol.
Vìd, Geol., 14, Praha.
Fiala, F.  Pácal, Z. (1961): Zpráva o výzkumu greisenových tìles záp.
Krásna s výpoètem zásob Sn-Li-Rb rud na loisku Koník.  (Report on study of greisen deposits west of Krásno and calculation of
Sn-Li-Rb ore reserves at the Koník deposit.)  Nepublik. zpr.,
Geofond Praha FZ4274. (in Czech).
 (1962): Loisko albitické aplitické uly záp. Krásna (Císaøský les)jako náhradní ivcová surovina. Výpoèet prognózních zásob.  (Studyof albite aplitic granite deposit west of Krásno (Císaøský les) as substitute material for feldspars. Calculation of prognosis reserves.) Nepublik. zpr., Geofond. Praha P15345. (in Czech).
 (1968): Aplogranit albitowy na tle surowców skaleniowych
Czechoslowacji.  (Albite aplogranite as feldspar raw material in
Czechoslovakia.)  Inst. Geol. Biul., 223: 119154. Varava. (in Polish).
Fiala, F.  kvor, V. (1956): Zpráva o ukonèení orientaèního geologického
mapování dùlních prostorù achet è. 11, 15, 17, a toly è. 13 v Horním
Slavkovì.  (Report on pilot geological mapping of shafts Nos 11,
15, 17 and adit No. 13 in Horní Slavkov.)  Nepublik. zpr., Geofond
Praha P7188. (in Czech).
Fiala, F. et al. (1956): Zpráva o geologických výzkumech v Císaøském
Lese za rok 1955.  (Annual report on geological research in the
Císaøský les area in 1955.)  Nepublik. zpr., Geofond Praha P7751.
(in Czech).
 (1957): Zpráva o geologických výzkumech v Císaøském Lese za rok
1956.  (Annual report on geological research in the Císaøský lesarea in 1956.)  Nepublik. zpr., Geofond Praha P8627. (in Czech).
 (1960): Základní geologický výzkum Císaøského (Slavkovského) Lesa
(19551960).  (Geology of the Císaøský (Slavkovský) les area, report for the 19551960 period.)  Nepublik. zpr., Geofond Praha. (inCzech).
Frieser, A. (1916): Erzvorksmmen im Kaiserwaldgebirge, Separatabdruck.
 Berg  und Hüttenm. Jb., Wien.
Gareiss, A. (1901): Über Pseudomorphosen nach Cordierit.  Tschermaks
mineral. petrogr. Mitt., 20, Wien.
Gehlièka, P. (1858): Die Gebirgsarten in der Umgebung von Eger. Programm Gymnasium, Eger.
Glückseling, A. M. (1862): Das Vorkommen der Mineralien im Egere
Kreise Böhmens.  Versammlung deutscher Naturfor. und Ärzte,
Karlsbad.
Groth, P. (1870): Über den Topaz einiger Zinnerzlagerstätten, besonders
von Altenberg und Schlaggenwalde.  Z. Dtsch. geol. Gesell.,Hannover.
 (1916): Die Lagerstätten  Abteilung der mineralogischen Sammlungdes k. bayer. staates in München.  Z. prakt. Geol., 24.
Günther, I. (1820): Zpráva o slavkovském dùlním obvodu, Archivní zpráva
in Bílek (1959). (Report on the Slavkov mining district), Archival
report in Bílek (1959).
Haidinger, W. (1830): Notiz von einer neuen Pseudomorphose.  N. Jr.
Miner., Geol., Paleont.
Halar, O. (1956): Mineralogický rozbor W-Sn koncentrátu a prùmìrného
technologického vzorku z lokality Krásno n. Teplou.  (Mineralogi-

40

cal analysis of W-Sn concentrate and an average technological sample
from the locality Krásno n. Teplou.)  Nepublik. zpr., Geofond Praha
P14427. (in Czech).
Havelka, J. (1985): Klasifikace loisek nerostných surovin.  (Classification of mineral deposits.)  Geol. Prùzk., 1, Praha. (in Czech).
Heilmaier, J. (1930): Über Zinnerz (Zinnstein) (Formen und Akzessorien).
 N. Jb. Geol. Min. Paläont., Beilage, 61, Stuttgart.
Hladká, N.  Jarchovský, T. (1959): Zpráva o výzkumu paragenetických
a minerogenních pomìrù na slavkovských ilách Sn-W formace as nimi spojených pneumatolyticko-metasomatických pøemìn. Zprávao geol. výzkumech za rok 1957.  (Report on paragenetic andminerogenic relations of Sn-W veins at Horní Slavkov and the associated pneumatolytic-metasomatic alterations. Annual report for 1957.)
 Nepublik. zpr., Geofond Praha. (in Czech).
Hoffmann, J. (1903): Historisch-mineralogische Skizze von Schlaggenwald.
 Programm der k. u k. Staatsrealschule in Elbogen 1903, Loket.
 (1904): Radium in Schlaggenwald.  Zeit. prakt. Geol., 12, Berlin.
Hochstetter, F. (1855): Die geologische Verhältnisse von Karlsbad.  Jb.
geol. Reichsanst., Wien.
 (1856): Allgemeiner Bericht über die geolog. Aufnahme der I. Section der k. k. geol. Reichanst. in Böhmen im Sommer 1855.  Jb. d.
geol. Reichsanst., Wien.
 (1856): Die Verhältnisse des Falkenau  Elbogner Braunkohlenbeckens
in Böhmen.  Jb. d. geol. Reichsanst., Wien.
Holubec, J. (1961): Strukturdiskordanz des variszischen und assyntischen
Baues im Gebirgssystem von Kruné Hory  Smrèiny (Erzgebirge Fichtelgebirge).  Vìst. Ústø. Úst. geol., Praha
Christiansen, E. H. et al. (1983): Petrogenesis of topaz rhyolites from thewestern United States.  Contrib. Min. Petr., 83: 486508. Heidelberg.
Janeèka, J. (1973): Závìreèná zpráva o geologicko-loiskovém výzkumu
Sn-W loisek Èeského masívu.  (Final report on geological-economic geological research of Sn-W deposits in the Bohemian Massif.)  Nepublik. zpr., archiv Ústø. Úst. geol. Praha. (in Czech).
Jantsch, F. (1853): Über das Vorkommen des Zinnes in Böhmen und die
Verhältnisse des Bergbaues von Schlaggenwald.  Jb. d. geol.
Reichanst., Wien.
 (1854): Ueber das Vorkommen des Zinnes in Böhmen.  Österr. Z.
Berg  u. Hüttenwes., Wien.
 (1858): Einiges über das Vorkommen des Zinnes in Böhmen und überdie geognostischen und bergbaulichen Verhältnisse der Zinn 
Industrie von Schlaggenwald.  Z. d. mont. V. im Erzgebirge.
Jarchovský, T. (1959): Zpráva o mineralogicko-geochemickém výzkumu
Sn-W loiska v Krásnì.  (Report on mineralogical-geochemical research of Sn-W deposit at Krásno.)  Nepublik. zpr., Geofond Praha
P10289. (in Czech).
 (1962): Mineralogicko-geochemický výzkum Sn-W loiska v Krásnì
nad Teplou, èást II., Schnödùv peò.  (Mineralogical-geochemical
research of Krásno nad Teplou Sn-W deposit, part II, Schnöd stock.) Nepublik. zpr., archiv Ústø. Úst. geol. Praha. (in Czech).
 (1969): Loiskové pomìry Gelnavské íly v Krásnì  (Montanistic
situation of the Gelnauer vein at Krásno.)  Sbor. geol. Vìd, loisk.
Geol., 10, Praha. (in Czech).
Jarchovský, T.  Pavlù, D. (1980): Geologicko-loiskový výzkum
Slavkovského lesa v letech 19761980.  (Geological and enonomicgeological research in the Slavkovský les area, 19761980 period.) Nepublik. zpr., archiv Ústø. Úst. geol., Praha. (in Czech).
 (1991): Albite-topaz microgranite from Horní Slavkov (Slavkovský
les Mts.), NW Bohemia.  Vìst. Ústø. Úst. geol., 66, 1322. Praha.
Jarchovský, T.  temprok, M. (1979): Geochemistry of granites of the
Slavkovský les Mts.  Sbor. geol. Vìd, loisk. Geol. Mineral., 20, Praha.
Jeek, B. (1914): Drobné zprávy mineralogické.  (Minor mineralogicalreports.)  Èas. Mus. Král. èes., Praha. (in Czech).
 (1932): Mineralogie.  (Mineralogy)  5491368, Ústø. naklad. uèitel.
Èeskoslov., Praha. (in Czech).
Jokély, J. (18561857): Die Erzlagerstätten und Bergbaue im böhmischen
Anteile des Erzgebirges.  Jb. d. geol. Reichsant. 1856, Bergwerksfreund
1857, Wien.
 (1857): Zur Kenntnis der geologischen Beschaffenheit des Egerer
Kreises in Böhmen.  Jb. d. geol. Reichsant., Wien.

Journal of the Czech Geological Society 51/12(2006)

Kachlík, V. (1993): The evidence for Late Variscan nappe thrusting of the
Mariánské Láznì Complex over the Saxothuringian terrane (WestBohemia).  J. Czech. Geol. Soc., 38: 4354. Praha.
Kastl, E.  Tonika, J. (1984): The Mariánské Láznì metaophiolite complex (West Bohemia).  Krystalinikum, 17, 5976. Praha.
Katzer, F. (1892): Geologie von Böhmen.  pp. 305309.
Kenngott, A. (1851): Karpholit von Schlaggenwald.  Berichte über die
Mittheilungen von Freunden der Naturwissenschaften in Wien,
gesammelt und heraragegeben von W. Haidinger, Band VII.
Kettner, R. (1917): Z nejnovìjích výzkumù o rudních nalezitíchv Èechách.  (Information on the present research of ore deposits in
Bohemia.)  Horn. hut. Listy, Praha. (in Czech).
Klvaòa, J. (1886): Nerosty království Èeského.  (Minerals of the Kingdom of Bohemia.)  Uherské Hraditì. (in Czech).
Kolektiv (1995): Likvidaèní zpráva závodu Stannum Horní Slavkov. 
Report on closure of the Stannum enterprise in Horní Slavkov. 
Nepublik. zpr., Geomont s.r.o. Pøíbram, Rudné doly s.p. Pøíbram,archiv Rudných dolù s.p. Pøíbram. (in Czech).
Konta, J. (1957): Jílové minerály Èeskoslovenska.  (Clay minerals ofCzechoslovakia.)  Nakladatelství ÈSAV Praha. (in Czech).
Kopecký, L. jun.  Jake, P. (1985): Petrografický a geochemický výzkum
mariánskolázeòského metabazitového komplexu.  (Petrographicaland geochemical research of the Mariánské Láznì metabasite complex.)  Nepublik. zpr., Archiv ÚÚG. Praha. (in Czech).
Korbel, P. (1983): Sekundární minerály loiska Horní Slavkov.  (Secondary minerals at the Horní Slavkov deposit.)  Diplomová práce,
Katedra mineralogie, geochemie a krystalografie Pøír. Fak. Univ. Karl.,
Praha. (in Czech).
 (1991): Supergene minerals from Horní Slavkov.  Sbor. Nár. Muz.
(Praha); B 47: 124.
Kovalenko, V. I. et al. (1971): Redkometalnye granitoidy Mongolii. (Rare-metal-bearing granitoids of Mongolia.)  Nauka. Moskva.
(in Russian).
Kozubek, P. et al. (1985): Závìreèná zpráva Huberùv peò  5. patro,
2. etapa.  (Final report on Huber stock, 5th level, second stage.) 
Nepublik. zpr., Rudné doly n.p. Pøíbram, Horní Slavkov, Geofond
Praha. (in Czech).
 (1989): Závìreèná zpráva úkolu Krásno sz. pøedpolí.  (Final reporton the project Krásno, northwestern forefront.)  Nepublik. zpr., archivRudných dolù s.p. Pøíbram. (in Czech).
Kratochvíl, F. (1960): Zpráva o geologickém mapování v Slavkovském
Lese.  (Report on geological mapping in the Slavkovský les area.) 
Nepublik. zpr., Geofond Praha P13420. (in Czech).
Kratochvíl, J. (19571964): Topografická mineralogie Èech (A). [Topographic mineralogy of Bohemia (parts A).]  NakladatelstvíÈSAV Praha. (in Czech).
Krejèí, J. (1851): Poèátkové nerostopisu jakoto návod k ustanovovánínerostù dle pøírodopisných znakù, Díl II.  (Introduction to mineralogy aimed at mineral identification based on physical properties, Part
II.)  Praha. (in Czech).
 (1855): O prahorách èeských.  (On ancient rock formations in
Bohemia.)  iva, 3, Praha. (in Czech).
Krusch, P. (1916): Die Wolframit  und Zinnerzlagerstätten bei Schönfeld
 Schlaggenwald, ein Beispiel des Erzgehaltes austelen der Gänge
und alter Halden im Böhmischen Wolframit  Zinnerzgebiet.  Z.
prakt. Geol., Berlin  Halle.
Kudielka, E. (1919): Die Zinn und Wolframbergbaue von Schlaggenwald
in Böhmen.  Montan.-Rsch., Wien
Kunír, I.  Jarchovský, T. (1967): Výpoèet zásob cínových rud a pøedbìná
zpráva o výzkumu na lokalitì Krásno ve Slavkovském lese.  (Calculation of tin ore reserves and a preliminary report on research at
Krásno locality in the Slavkovský les area.)  Nepublik. zpr., Geofond
Praha P19915, V56228. (in Czech).
Laube, G. (1876): Geologie des Böhmischen Erzgebirges, I. Geologie
des westlichen Erzgebirges oder des Gebirges zwischen Maria Kulm  Schönbach und Joachimsthal  Gottesgab.  Archiv fürLandesdurchforschung Bohmens III.
Lindacker, J. T. (1791): Beschreibung einiger Topase, Welche in dem
Schlaggenwald Zinnstocke vorkommen.  Sitz. Gesell. W.

Journal of the Czech Geological Society 51/12(2006)

Mach, Z. (1979): Asociace jílových minerálù spjatých s cíno-wolframovým
zrudnìním v okolí Krásna u Horního Slavkova.  (The association ofclay minerals accompanying tin-tungsten mineralization aroundKrásno near Horní Slavkov.)  Acta Univ. Carol., Geol., 34, Praha.
(in Czech).
 (1979): Chalkosiderit a Ba  farmakosiderit z Krásna u Horního
Slavkova, nálezová zpráva.  (Chalcosiderite and Ba-pharmacosiderite
from Krásno near Horní Slavkov, preliminary report.)  Èas. Mineral. Geol., Praha. (in Czech).
Mach, Z.  Korbel, P. (1990): Sekundární minerály z Huberova pnìu Krásna u Horního Slavkova.  (Secondary minerals from the Huber
stock at Krásno near Horní Slavkov.)  Pøíroda Karlovarska I.,
Karlovarské muzeum v Karlových Varech. (in Czech).
Majer, J. (1970): Tìba cínu ve Slavkovském lese v 16. století.  (Tinmining in the Slavkovský les area in the 16th century.)  Národní
technické muzeum Praha. (in Czech).
Majer, J.  Jangl, L. (1995): Vývoj hornictví cínu ve Slavkovském lese
od 13. do 20. století.  (History of tin mining in the Slavkovský lesarea between the 13th and 20th century.)  In: Závìreèná likvidaèní
zpráva závodu Stannum.  Nepubl. zpráv., Rudné doly s.p. Pøíbram,Geofond Praha FZ6630. (in Czech).
Mrázek, Z. (1981): Crandalit a mixit z Horního Slavkova.  (Crandallite
and mixite from Horní Slavkov.)  Sbor. Vys. k. chem. techn., G 20,
Praha. (in Czech).
Najman, K. (1990): Krásno  Horní Slavkov, è. úkolu 29 79 2107. (Krásno  Horní Slavkov, Report on Project No. 29 79 2107.) Nepubl. zpráva, Geoindustria Praha, Geofond Praha P75709. (inCzech).
Neuilová, M.  Vejnar, Z. (1963): Geologie a petrogeneze krystalických
bøidlic severozápadní èásti Slavkovského lesa.  (Geology and petrogenesis of metamorphic rocks in the nortwestern part of the Slavkovský
les area.)  Sbor. Ústø. Úst. geol., G, 28: 87106. Praha. (in Czech).
Novák, L. (1988): Vertikální opakování intruzívních fází v krudumském
granitovém masívu. Slavkovský les.  (The vertical repetion of intrusion phases in the Krudum granite massif. Slavkovský les area.) 
Sbor. Západoèes. Muz. Pøír., 67: 6873. Plzeò. (in Czech).
Nowicki, C. von (1857): Das Vorkommen des Zinnsteines Schlaggenwald
und Schönfeld, Ein Beitrag zur Kenntnis von diesen Lagerstätten. 
Lotos, 7, Praha.
Pácal, Z.  Pavlù. D. (1972): Nové poznatky o loisku sodnodraselných
ivcù Vysoký kámen u Krásna.  (New data on the deposit of sodium-potassium feldspars at Vysoký Kámen near Krásno.)  Geol.
Prùzk., 14: 357360. Praha. (in Czech).
 (1979): Závìreèná zpráva dílèího úkolu 4/09-4 za léta 19761979 ivcové suroviny Krásno.  (Final report on the project No. 4/09-4
for the period 19761979  feldspar raw material Krásno.)  Nepubl.
zpráva, Geofond. Praha P29587. (in Czech).
Peithner, J. (1780): Versuch über die natürliche und politische Geschichte
der böhmischen und mährischen Bergwerke, Wien.
Peschel, J. (1805): Archivní zpráva.  (Archival report) in J. Bílek (1959).
Pláil, J.  Sejkora, J.  Ondru, P.  Veselovský, F.  Beran, P.  Goliá, V.
(2006): Supergene minerals in the Horní Slavkov uranium ore district, Czech Republic.  Journ. Czech Geol. Soc., 51: 149158
Pleinerová  Hladká, N. (1960): Pøíspìvek k petrogenezi krystalinika
plátì karlovarského masívu v oblasti Císaøského lesa.  (A contribution to petrogenesis of metamorphic mantle of the Karlovy Varypluton in the Císaøský les area.)  Èas. Min. Geol., 5: 2837. Praha.
(in Czech).
Polák, L. et al. (1969): Výpoèet zásob Krásno  ula, ivcová surovina.
Etapa pøedbìná.  (Calculation of reserves at Krásno  granite, feldspar raw material. Preliminary stage.)  Nepubl. zpráva, RD Pøíbram.
(in Czech).
Polanský, J.  Racková, H.  ovíèková, N. (1973): Detailní gravimetrické
mapování 1:25 000 Slavkovský les se zahrnutím èásti chebské asokolovské pánve.  (Detailed gravity mapping 1:25 000 in the
Slavkovský les area and parts of the Cheb and Sokolov basins.) Nepubl. zpráva, Geofond. Praha P24917. (in Czech).
Reuss, A. E. (1854): Kurze Übersicht der geol. Verhältnisse Böhmens,
Praha.

41

 (1863): Geognostische Skizze der Umgebungen von Carlsbad,
Marienbad und Francensbad, Praha.
Reyer, E. (1880): Granit und Schiefer von Schlaggenwald.  Jahrbuch derk. k. geol. Reichsanst.
 (1881): Geologie des Zinnes.  Österrichische Zeitschrift für Berg und Hüttenwesen, Wien
Röhlich, P.  ovíèková, N. (1968): Die Tiefenstörungstektonik und deren
Entwicklung im zentralen Teil der Böhmischen Masse.  Geologie
17: 670694. Berlin.
Rosický, V. (1916): Topaz ze Slavkova v Èechách.  (Topaz from Slavkov
in Bohemia.)  Rozpr. Èes. Akad., Vìdy Sloves. Umìní, Tø. II., 25:
7, Praha. (in Czech).
Rücker, A. (1864a): Zinnerzvorkommen von Schlaggenwald 
Verhandlungen der k. k. geologischen Reichsanstalt, 14: 1.
 (1864b): Beitrag zur Kenntniss des Zinnerzverkommens bei
Schlaggenwald.  Jahrbuch der k. k. geologischen Reichsanstalt, 14,
Wien.
Sadebeck, A. (1869): Über die Krystallformen der Blende.  Zeitschrift
der deutschen geologischen Gesellschaft, 21.
Sejkora, J.  Ondru, P.  Fikar, M.  Veselovský, F.  Mach, Z. 
Gabaová, A. (2006a): New data on mineralogy of the Vysoký Kámen
deposits near Krásno, Slavkovský les area, Czech Republic.  Journ.
Czech Geol. Soc., 51: 4355
Sejkora, J.  Ondru, P.  Fikar, M.  Veselovský, F.  Mach, Z. 
Gabaová, A.  koda, R.  Beran, P. (2006b): Supergene minerals atthe Huber stock and Schnöd stock deposits, Krásno ore district, theSlavkovský les area, Czech Republic.  Journ. Czech Geol. Soc., 51:
57101
Sejkora, J.  koda, R.  Ondru, P.  Beran, P.  Süsser, C. (2006c):
Mineralogy of phosphate accumulations in the Huber stock, Krásno
ore district, Slavkovský les area, Czech Republic.  Journ. Czech Geol.
Soc., 51: 103147
Sejkora, J.  koda, R.  Ondru, P. (2006d): New naturally occurring
mineral phases from the Krásno  Horní Slavkov area, western
Bohemia, Czech Republic.  Journ. Czech Geol. Soc., 51: 159188
Slavík, F. (1903): Nové nálezy minerálù u Slavkova.  (New mineral finds
near Slavkov.)  Rozpr. Èes. Akad., Vìdy Sloves. Umìní, Tø. II., 12:
35, Praha. (in Czech).
Smirnov, V. I. (1983): Geologie loisek nerostných surovin.  (Geology ofmineral deposits.)  SNTL  Nakladatelství technické literatury, Praha.
(in Czech).
Stark, M. (1913): Gebirgsgranit und Erzgebirgsagranit in Kaiserwald nebst
einigen Bemerkungen über ihne Kontaktprodukte.  Mitt. d. naturwiss.
Vereins and. Univ. Wien, 11, Wientìdrá, V. (1996): Retrograde evolution of the Mariánské Láznì Complex
basic rocks  final report of the project 205/94/1455 of the Czech
Grant Agency.  MS Archive Czech Geological Survey Prague, 129 p.
tìdrá, V. (2003): Pre-Carboniferous metamorphic history recorded bymetabasites of the Mariánské Láznì Complex, Western Bohemia. 
Journ. Czech Geol. Soc., 48/12, 117118.
tìdrá, V.  Kachlík, V.  Kryza, R. (2002): Coronitic metagabbros of the
Mariánské Láznì Complex and Teplá Crystalline Unit: inferences forthe tectonometamorphic evolution of the western margin of the TepláBarrandian Unit, Bohemian Massif.  Geol. Soc. Spec. Publ., London, 201, 217236.
Strunz, H. (1957): Ferrokarpholit  Karpholit.  Acta Cryst. 10, Copenhagen.
Svoboda, J. et al. (1964): Regionální geologie ÈSSR, Díl I., sv. I.  (Regional geology of ÈSSR, Part I, vol. I.)  Naklad. ÈSAV, Praha. (inCzech).
temprok, M. (1959): Vznik metasomatických obrub bismutinu kolem
vizmutu z rudní oblasti Horního Slavkova.  (Metasomatic rims ofbismuthinite around native bismuth in the Horní Slavkov ore district.).  Èas. Miner. Geol., 4; 424441. (in Czech).
temprok, M. (1985): Vertical extent of greisen mineralization in the Krunéhory Erzgebirge granite pluton of central Europe.  Sbor. konf. Highheat production granites. St. Austel.
 (1986): Petrology and geochemistry of the Czechoslovak part of theKruné hory Mts. granite pluton.  Sbor geol. Vìd., Loisk. geol.
Mineral., 27, Praha.

42

ovíèková, N. (1971): Hlubinná zlomová tektonika Èeského masívu. (Deep fault tectonics of the Bohemian Massif.)  Pøír. fak. KU. Praha.
(in Czech).
Tacl, A.  Blüml, A. (1961): Mineralogicko  geochemický rozbor rudníhomateriálu achty è. 8  Horní Slavkov.  (Mineralogical-geochemical
analysis of ore samples from the shaft No. 8  Horní Slavkov.) 
Nepubl. zpráva, archiv Rudných dolù s.p. Pøíbram. (in Czech).
 (1974): Mineralogický výzkum sekundárních nerostù loiska Krásno.
 (Mineralogical research of secondary minerals from the Krásno
deposit.)  Nepublik. zpr., archiv Rudných dolù s.p. Pøíbram.
Teuscher, E. O. (1934): Die Stellung des Eibenstocker Granits.  Z. d.
deutsch. geol. Ges., Berlin.
 (1936): Umwandlungserscheinungen an Gesteinen des Granitmassivs
von Eibenstock  Neudeck.  Mitt. Inst. Mineral. Univ. Leipzig, No
361., Mineral. Petrogr. Mitt., 47.
 (1936): Primäre Bildungen des granitischen Magmas und seiner
Restlösungen im Massiv von Eibenstock  Neudeck, Mineral. Petrogr.
Mitt., 47.
Timmermann, H.  tìdrá, V.  Gerdes, A.  Noble, S. R.  Parrish, R. R.
 Dörr, W. (2004): The problem of dating high-pressure metamorphism: a U-Pb isotope and geochemical study on eclogites and related rocks of the Mariánské Láznì Complex, Czech Republic.  Journal of Petrology 45, 13111338.
Vondrová, N. (1962): Závìreèná zpráva o geologickém výzkumu
v severovýchodní èásti Slavkovského lesa.  (Final report on geological research in the northeastern part of the Slavkovský les area.) 
Nepublik. zpr., Geofond Praha P13966. (in Czech).
Vtìlenský, J. (1955): Mineralogický rozbor koncentrátu z Krásnan. Teplou.  (Mineralogical analysis of ore concentrate from

Journal of the Czech Geological Society 51/12(2006)

Krásno n. Teplou.)  Nepublik. zpr., Geofond Praha P14426.
(in Czech).
Woldøich, J. (1905): Geologie se zvlátním zøetelem na zemì koruny èeské,
Díl 3.  (Geology with special emphasy on the countries of the Kingdom of Bohemia.). (in Czech).
Zemánek, V.  Gregorová, M. (1959): Dílèí zpráva o geologických
výzkumech v okolí Horního Slavkova, provedených v roce 1958. (Report on geological research around Horní Slavkov, conducted in
1958.)  Nepublik. zpr., Geofond Praha P10184. (in Czech).
Zepharovich, V. (1857): Mineralogisches Lexikon für das KaiserthumÖsterreich, Wien.
 (1864): Referat in Verhandlungen der k. u. k. geol. Reichsanst, Wien.
Zikmund, J. (1983): Strukturnì-tektonické schéma Slavkovského lesa. (Structural-tectonic scheme of the Slavkovský les area.)  Nepublik.
zpr., Archiv ÈGÚ. Praha. (in Czech).
Zippe, F. X. M. (1847): Allgemeine Übersicht der physikalischen undstatistichen Vehältnisse des Elbogner Kreises, In Sommer C. G. (1847)
Das Königreich Böhmen, sv. XV.  Elbogner Kreis.
Zoubek, V. (1947): Zpráva o geolog. výzkumech a mapování ve støední
èásti jv. svahu Kruných hor.  (Report on geological research andmapping of the central part of the southeastern slope of the Krunéhory Mts.)  Vìst. geol. Úst., 22: 23. (in Czech).
 (1951): Pøedbìná zpráva o geologickém výzkumu a mapování oblasti
karlovarského plutonu.  (Preliminary report on geological research
and mapping in the Karlovy Vary pluton area.)  Vìst. Ústø. Úst.
geol., 26, Praha. (in Czech).
Zoubek, V. et al. (1963): Vysvìtlivky k pøehledné geologické mapì ÈSSR1:200000 M-33-XIII Karlovy Vary.  (Explanation to geological mapof CSSR 1:200 000, sheet M-33-XIII Karlovy Vary.)  Praha. (in Czech).

Sn-W rudní revír Krásno u Horního Slavkova  historie tìby, geologická a mineralogická charakteristika
Sn-W rudní revír Krásno u Horního Slavkova (Slavkovský les, západní Èechy) patøí k nejvýznamnìjím oblastem tìby rud v Èeské republice. Souèasnì
vzhledem k zastoupení jednotlivých minerálních druhù a jejich celkovému poètu je výjimeèným mineralogickým fenoménem a jednou z nejvýznamnìjíchmineralogických lokalit svìta. V práci je podán pøehledný pohled na historii tìby, geologickou situaci revíru, charakteristiku a pøehled jednotlivých
dílèích loisek. Lokality v oblasti Horního Slavkova  Krásna byly známy jako bohatý zdroj kvalitních minerálních vzorkù, které jsou obsaeny v øadìmuzejních kolekcí celé Evropy. Historické muzejní vzorky pocházející z této oblasti jsou obvykle uvádìny pod pùvodními názvy lokalit Schlaggenwald(= Horní Slavkov) a Schönfeld (= Krásno). Souèástí práce je proto i historie geologických a mineralogických výzkumu a pøehled nejvýznamnìjíchvýskytù klasických minerálních druhù tohoto revíru: arsenopyritu, fluorapatitu, fluoritu, hübneritu, chalkopyritu, karfolitu, kasiteritu, køemene,
molybdenitu, rodochrositu, sfaleritu, scheelitu, topazu a wolframitu.