The Julianna peg ma tite vein sys tem at the Pi³awa Górna Mine, Góry Sowie Block, SW Po land – pre lim i nary data on ge ol ogy and de scrip tive min er al ogy
Adam SZUSZKIEWICZ1, *, Eligiusz SZE£ÊG2, Adam PIECZKA3, S³awomir ILNICKI4, Krzysztof NEJBERT4, Krzysztof TURNIAK1, Magdalena BANACH5, Marek £ODZIÑSKI6,
Ro man RÓ¯NIAK5 and Piotr MICHA£OWSKI5
1 In sti tute of Geo log i cal Sci ences, Uni ver sity of Wroc³aw, M. Borna 9, 50-204 Wroc³aw, Po land
2 De part ment of Geo chem is try, Min er al ogy and Pe trol ogy, Fac ulty of Earth Sci ences, Uni ver sity of Silesia, Bêdziñska 60, 41-200 Sosnowiec, Po land
3 De part ment of Min er al ogy, Pe trog ra phy and Geo chem is try, AGH Uni ver sity of Sci ence and Tech nol ogy, Al. Mickiewicza 30, 30-059 Kraków, Po land
4 In sti tute of Geo chem is try, Min er al ogy and Pe trol ogy, Uni ver sity of War saw, ¯wirki i Wigury 93, 02-089 Warszawa, Po land
5 DSS Com pany, Pi³awa Górna Mine, Sienkiewicza 96, 58-240 Pi³awa Górna, Po land
6 De part ment of Gen eral Ge ol ogy and Geotourism, AGH Uni ver sity of Sci ence and Tech nol ogy, Al. Mickiewicza 30, 30-059 Kraków, Po land
Szuszkiewicz A., Sze³êg E., Pieczka A., Ilnicki S., Nejbert K., Turniak K., Banach M., £odziñski M, Ró¿niak R. and Micha³owski P. (2013) The Julianna peg ma tite vein sys tem at the Pi³awa Górna Mine, Góry Sowie Block, SW Po land – pre - lim i nary data on ge ol ogy and de scrip tive min er al ogy. Geo log i cal Quar terly, 57 (3): 467–484, doi: 10.7306/gq.1097 The newly dis cov ered Julianna peg ma titic sys tem from the Pi³awa Górna Quarry (the Góry Sowie Block, Sudetes, NE mar gin of the Bo he mian Mas sif) is de scribed in terms of geo log i cal set ting, pe trog ra phy and de scrip tive min er al ogy. The sys tem rep - re sents the larg est peg ma titic oc cur rence in the Pol ish Sudetes and con sists of a com plex net work of cogenetic rare-el e ment gra nitic pegmatites that in truded into tectonized am phi bo lite as dis cor dant dikes. The pegmatites range from bar ren and weakly zoned to tex tur ally well-dif fer en ti ated ones that are com posed of a fine-grained bor der zone, coarse-grained wall zone, graphic and blocky feld spar in ter me di ate zones and a quartz core. Uni di rec tional and skel e tal so lid i fi ca tion tex tures are well-de vel oped. The Julianna pegmatites con sist of rock-form ing plagioclase (£An39), microcline, quartz and bi o tite ac - com pa nied mostly by ac ces sory to mi nor mus co vite, tour ma line, gar net and beryl. They crys tal lised from anatectic melt of hy brid NYF (ni o bium-yt trium-flu o rine) + LCT (lith ium-ce sium-tan ta lum) geo chem i cal char ac ter is tics. Pegmatites with a low to mod er ate de gree of frac tion ation, that dom i nate in the Julianna sys tem, bear NYF-sig na ture ac ces sory min er als, such as al la nite-(Ce), colum bite-, euxenite- and samarskite-group min er als, fergusonite-(Y) and gadolinite-(Y). How ever, rare dikes that at tained a very high de gree of frac tion ation con tain typ i cal min er als of LCT-sig na ture in clud ing tour ma lines of the elbaite-olenite-rossmanite se ries, le pido lite, lithiophilite, spodumene, Cs-rich beryl and pollucite.
Key words: rare-el e ment peg ma tite, mixed (NYF + LCT) sig na ture, gra nitic pegmatites, Pi³awa Górna, Góry Sowie Block, Sudetes.
INTRODUCTION
Un til the be gin ning of the 1900s, pegmatites of the Góry Sowie Block (GSB) were lo cally mined for feld spar and quartz for use in the ce ram ics and glass in dus try. The min ing ac tiv ity in cluded un der ground ex ploi ta tion and was es pe cially in ten sive in the area be tween Pi³awa, Ró¿ana, Owiesno and Bielawa (Meister, 1932 fide Lis and Sylwestrzak, 1986). Since the end of
the ex ploi ta tion, no new large-scale oc cur rences have been un - cov ered. Thus, con tem po rary stud ies of GSB pegmatites have been lim ited to old quar ries, mine dumps, and small nat u ral ex - po sures along the shore line of Lake Bystrzyckie and road and rail road cuts. As a con se quence, the amount of avail able re - search ma te rial was in suf fi cient for study ing rare min er als and the lack of in situ ex po sures of larger peg ma titic bod ies pre - cluded sys tem atic re search on their tex tural and geo chem i cal in ter nal zon ing.
In 2001 the Dolnoœl¹skie Surowce Skalne min ing com pany ini ti ated a pro ject to open a quarry for am phi bo lite and migmatite at Pi³awa Górna. At the end of 2007, the pre pa ra tory work un cov ered the first por tion of a sys tem of peg ma titic veins, which was later named “Julianna” (Sze³êg et al., 2010). Var i ous sec tions of Julianna were ex posed be tween 2008 and 2010. The whole peg -
* Corresponding author, e-mail: adam.szuszkiewicz@ing.uni.wroc.pl Received: December 14, 2012; accepted: April 16, 2013; first published online: May 13, 2013
ma titic sys tem con sisted of nu mer ous anastomosing and lo cally cross-cut ting veins hosted by tectonized am phi bo lites. In 2009, when the most com plete ex po sure was achieved, the sys tem ex - tended over 60–80 metres in plan view and was de fined by three main dikes ori ented NNE–SSW and dip ping WNW at mod er - ate-to-steep an gles. Some peg ma titic dikes could be traced for up to 50 metres in ver ti cal sec tion. The di men sions of this ex po sure, un prec e dented on the scale of the whole GSB mas sif, and the pos si bil ity of sam pling var i ous sec tions of the veins sys tem at i cally un cov ered dur ing the on go ing ex ploi ta tion of fered a unique op por - tu nity for com pre hen sive pet ro log i cal and min er al og i cal stud ies.
This pa per aims at pro vid ing the first co her ent re port on the re sults of field stud ies of the Julianna sys tem, sup ported by iden ti fi ca tion of se lected min er als by means of X-ray pow der dif frac tion, semi-quan ti ta tive SEM-EDS or quan ti ta tive WDS elec tron microprobe anal y ses. The pres ent study fo cused on the low- to mod er ately-evolved pegmatites which largely dom i - nate in the Julianna sys tem. How ever, sec tions of pegmatites that dis play a very high de gree of geo chem i cal frac tion ation, as shown by the pres ence of Cs- and Li-rich min er als, were also found (Pieczka et al., 2010c).
GEOLOGICAL SETTING
The Sudetes form the NE mar gin of the Bo he mian Mas sif and rep re sent the NE ter mi na tion of the Eu ro pean Variscan orogenic belt. The re gion ex tends be tween the WNW–ESE trending re gional tec tonic zones of the Up per Elbe and the Mid - dle Odra. Sudetic rocks subcrop un der Permo-Me so zoic and Mio cene strata in the NE and SE, re spec tively, and merge with the Neoproterozoic Lusatian Mas sif to wards the NW (Mazur et al., 2007 and ref er ences therein). The Sudetes are gen er ally built of: (1) base ment units that in clude frag ments of Cadomian crust with Lower Pa leo zoic metasedimentary and metaigneous rocks, in jected by Variscan granitoids and (2) a late- to post-Variscan cover of Lower Car bon if er ous–Ce no zoic age.
Based on ma jor dif fer ences in li thol ogy, struc tural char ac ter is - tics and geo log i cal evo lu tion, the Sudetes are di vided into west - ern, cen tral and east ern parts, each con sist ing of a num ber of smaller, mostly tec toni cally bounded, units (Mazur et al., 2007).
Thus the whole re gion rep re sents a com plex mo saic of dis tinct tectono-strati graphic units, whose mu tual re la tions are blurred by block tec ton ics re lated to the Al pine orog eny. The Sudetic Bound ary Fault, a NE–SW trending Late Variscan struc ture re - ju ve nated dur ing the Al pine orog eny (Aleksandrowski et al., 1997; Badura et al., 2003), sep a rates the Sudetes into a top o - graph i cally dis tinc tive moun tain ous part in the SW and strongly peneplained low lands of the Fore-Sudetic Block in the NE, now mostly un der thick Ce no zoic cover.
The tri an gu lar Góry Sowie Block (GSB) is one of the main geo log i cal units of the Cen tral Sudetes (Fig. 1). It ex tends over
~600 km2 be tween Szczawno Zdrój, Srebrna Góra and Oleszna, SW of Wroc³aw (SW Po land). The GSB is crossed by the Sudetic Bound ary Fault and about two-thirds of the area is lo cated in the Fore-Sudetic Block, whilst the re main ing one-third is in the el e vated moun tain ous part of the Góry Sowie Mts. The fore land do main is con sid ered to rep re sent an in ter - sec tion level about 5 km deeper than the moun tain ous part (¯elaŸniewicz, 1995).
The GSB (Fig. 1) is com posed pre dom i nantly of metase - dimentary and fel sic metaigneous gneiss es and migmatites, with mi nor in ter ca la tions of am phi bo lite, granulite, re cently dis - cov ered eclogite (Ilnicki et al., 2010, 2011), hyperite, highly serpentinised man tle rocks, mar ble and calc-sil i cate rocks
(e.g., Polañski, 1955; Grocholski, 1967; Morawski, 1973; Kryza, 1981; ¯elaŸniewicz, 1985, 1987; Gunia 1997). The meta mor - phic suite is cut by gran ites, aplites, pegmatites, rhyolitic and lamprophyric dikes as well as by bar ite and quartz hy dro ther mal veins. The late Pro tero zoic–Early Cam brian protolith (Gunia, 1985; Kröner and Hegner, 1998; Kryza and Fan ning, 2007) has un der gone polymetamorphic evo lu tion (Kryza, 1981; ¯elaŸ - niewicz, 1987, 1990). An early high-pres sure/high-tem per a ture (HP–HT) ep i sode at ~400 Ma was over printed by a high am phi - bo lite fa cies event at ca. 385–370 Ma (Breemen et al., 1988;
Brueckner et al., 1996; O’Brien et al., 1997; Bröcker et al., 1998;
Aftalion and Bowes, 2002; Gordon et al., 2005; Kryza and Fan - ning, 2007). De com pres sion led to lo cal par tial melt ing and for - ma tion of anatectic granodiorites and pegmatites (Kryza, 1981;
Timmermann et al., 2000).
Pi³awa Górna is lo cated in the east of the GSB fore land, about 10 km SE of Dzier¿oniów and over 50 km SW of Wroc³aw (Lower Silesia, SW Po land). The “Pi³awa Górna” open quarry, sit u ated on Rybak Hill 1.5 km north of the town (Fig. 2), ex ploits the migmatite-am phi bo lite rock de posit with over 323 mil lion tons of es ti mated re sources. Migmatite ac counts for about 72%
of the raw rock and the rest is mainly am phi bo lite, with mi nor bod ies of gra nitic peg ma tite. Rock pro cess ing takes place in a plant lo cated nearby (Fig. 3). The fi nal prod ucts are used as con struc tion and con crete rock ag gre gates.
THE GÓRY SOWIE PEGMATITES
In the GSB, pegmatites oc cur as pods, lenses and dikes in am phi bo lites, migmatites, gneiss es and granu lites, rarely in other rock types (Smulikowski, 1952; Polañski, 1955;
Grocholski, 1964, 1967; Kryza, 1977; ¯elaŸniewicz, 1987). At most oc cur rences the pegmatites are from centi metres to 1 m thick, reach ing sev eral metres only ex cep tion ally. Tex tural and min eral zonation is well-pro nounced only in the thick est peg ma - titic bod ies. Field re la tion ships al low the dis tinc tion of an older gen er a tion of pegmatites, con cor dant with the host rocks, mainly migmatites, and a youn ger gen er a tion cross cut ting the sur round ing rocks dis cor dantly. Syntectonic older pegmatites are clearly re lated to the Late De vo nian migmatitisation event.
Ac cord ing to ¯elaŸniewicz (1990), sub-ver ti cal peg ma titic veins of the youn ger gen er a tion were emplaced along gen er ally N-trending extensional frac tures in the D4 tectonometamorphic event. Crystallisation ages of the GSB pegmatites were es tab - lished at 370 ± 4 Ma us ing mus co vite from Lutomia (Breemen et al., 1988; Rb-Sr method) and 383–370 Ma us ing xeno time from Zagórze Œl¹skie (Timmermann et al., 2000; U-Pb method).
Pegmatites of the GSB have been well-known for large, well-de vel oped crys tals of K-feld spar, beryl, gar net and tour ma - line since at least the early 1800s (Sachanbiñski, 1972, 1973;
Lis and Sylwestrzak, 1986 and ref er ences therein). The most spec tac u lar spec i mens were en coun tered dur ing min ing of the peg ma titic bod ies near Pi³awa Górna, Kamionki, Bielawa, Ró¿ana, Owiesno and Grodziszcze in the Fore-Sudetic Block.
Most of the peg ma titic bod ies have a sim ple min eral com po si - tion, lim ited to rock-form ing quartz, al bite-oligoclase, K-feld spar and micas. Com mon ac ces sory min er als in clude tour ma line, gar net and ap a tite and lo cally also beryl whilst hornblende, an - da lu site, sillimanite, kyan ite, cor di er ite, zir con, ti tan ite and oth - ers are rare (Sachanbiñski, 1972; Kryza, 1977). Hy brid iza tion of peg ma titic melt emplaced in metabasites re sulted in en rich - ment in bi o tite, epidote, hornblende, ap a tite and tour ma line at the ex pense of quartz, plagioclase and mus co vite and some - times led to the for ma tion of cor di er ite-bear ing bod ies (Kryza,
1977). The gar net be longs to the almandine-spessartine se ries and the tour ma line is mostly Al- and Mg-en riched schorl grad - ing to wards Li-en riched schorl and Fe-bear ing elbaite only lo - cally (Pieczka, 1996; Pieczka et al., 1997, 2004). Beryl com - monly dis plays low con tents of al kali el e ments, mainly Na (Sachanbiñski, 1973; £odziñski, 2007). Nb-Ta ox ides, up to 0.5 cm in size, have oc ca sion ally been found near Pi³awa Górna (Pilati, 1863 fide Traube, 1888; Römer, 1864; Roth, 1867) and in the area of Owiesno–Kietlice (£odziñski, 2008; £odziñski and Pieczka, 2008). Lo cally the en rich ment in P of peg ma titic melt re sulted in the crystallisation of phos phates, such as sarcopside (with the type lo cal ity at Micha³kowa), huréaulite, vivi an ite, triplite, ferrisicklerite, graftonite, Ca-rich beusite, stanìkite and alluaudite de scribed from Micha³kowa, Lutomia and Pi³awa Górna (Sadebeck, 1855 fide Fiedler, 1863;
Websky, 1868; Dathe and Finckh, 1924; Hintze, 1933; Pieczka et al., 2003).
Geo chem i cal stud ies of the GSB crys tal line rocks (Sachanbiñski, 1971; Mikuszewski et al., 1976) have not re -
vealed sig nif i cant con cen tra tions of Li, Be, Nb and REEs al - though Sachanbiñski (1971) noted slightly el e vated con cen tra - tions of Be in some of the gneiss es. Mikuszewski et al. (1976) con cluded that the meta mor phic con di tions were not high enough to gen er ate zoned pegmatites with el e vated con cen tra - tions of in com pat i ble el e ments.
Avail able data on the con cen tra tions of trace el e ments in some min er als such as micas (Zawidzki, 1971; Dumañska- S³owik, 2004), gar net (Pieczka et al., 1997), beryl (£odziñski, 2007) and tour ma line (Pieczka, 1996; Pieczka et al., 2010b), in - di cate a rel a tively prim i tive geo chem i cal char ac ter of the ma jor - ity of the GSB pegmatites. How ever, frag ments of pegmatites with signs of ad vanced geo chem i cal frac tion ation and sig nif i - cant Li-en rich ment have also been ob served (Pieczka et al., 2003, 2004, 2010c, 2012; Nejbert et al., 2010). This sug gests that, at least lo cally, the peg ma titic melts at tained high con cen - tra tions of rare el e ments.
Fig. 1. Geo log i cal map of the Góry Sowie Block (af ter Bröcker et al., 1998; mod i fied) BBM – Braszowice–BrzeŸnica Mas sif, JGSM – Jordanów–Gogo³ów Ser pen tin ite Mas sif;
NRM – Nowa Ruda Mas sif, SzM – Szklary Mas sif (all con sti tute the Sudetic Ophiolite)
PETROGRAPHY OF THE JULIANNA PEGMATITE AND OF THE HOST ROCKS
Migmatites and am phi bo lites ex posed in the Pi³awa Górna Quarry show gen er ally gradational con tacts. The migmatites are com posed of quartz, K-feld spar, bi o tite, sub or di nate mus - co vite, gar net and ac ces sory zir con, ap a tite and sillimanite.
Layer-, fold- and net-struc tured migmatite va ri et ies are ob - served. Ophthalmitic augen-like tex tures are also pres ent and in di cate post-anatectic porphyroblastic growth of K-feld spars.
Leucosome segregations cut ting the host rock as dis cor dant veinlets are not un com mon and in places may be con sid ered as synmigmatitic gran ite and peg ma tite. The am phi bo lites are com posed of am phi bole and plagioclase with mi nor gar net and lo cally abun dant bi o tite. Il men ite, rutile, clinozoisite and quartz are ac ces sory min er als. Some of these also con tain relicts of clinopyroxene and spinel. Due to strong but het er o ge neous de - for ma tion and meta mor phism they show a large tex tural di ver - sity from mas sive to well-fo li ated va ri et ies. The fo li a tion strongly var ies due to fold ing and gen er ally dips at 220/70. Mas sive am - phi bo lites that oc cur in weakly strained do mains con tain abun - dant rel ics of eclogitic tex tures. These rel ics are vari ably oblit er - ated by ret ro gres sion un der am phi bo lite fa cies con di tions and are not ob served in the fo li ated am phi bo lites. In places, rel ict do mains of ret ro gressed but not amphibolitised eclogites have been found (Ilnicki et al., 2010), pro vid ing ev i dence of the first in situ oc cur rence of eclogites in the GSB. These rocks doc u ment HP meta mor phism at tem per a tures of 730–840°C and pres - sures of 25–26 kbar prior to nearly iso ther mal de com pres sion to pres sures <5–6 kbar (Ilnicki et al., 2011, 2012). Both the migmatites and am phi bo lites are frac tured; how ever, due to the dif fer ence in their rhe o log i cal prop er ties the frac tur ing is de vel - oped to a greater ex tent in the am phi bo lites. Dom i nant tec tonic frac tures ob served in the quarry trend SW–NE and NW–SE.
Dur ing quar ry ing be tween the end of 2007 and the mid dle of 2010 var i ous sec tions of the Julianna peg ma titic sys tem were ex posed in the SW part of the quarry (Figs. 3 and 4).
Pegmatites oc curred as nu mer ous anastomosing, lo cally cross-cut ting veins that in truded along a tec tonic zone seg - ment ing the am phi bo lite (Sze³êg et al., 2010). The over all ge - om e try of the sys tem was strongly con trolled by rhe o log i cal Fig. 2. Geo log i cal map of the Pi³awa Górna Mine area
(af ter Cymerman and Walczak-Augustyniak, 1988;
Sze³êg and Ga³uskina, 2010; mod i fied)
Fig. 3. The Pi³awa Górna Mine in Sep tem ber 2008
prop er ties of the coun try rocks. Large an gu lar blocks of am phi - bo lite were en vel oped by peg ma tite while smaller ones were also in cor po rated into the thicker peg ma titic veins. The am phi - bo lite xe no liths were in places ro tated with fo li a tion ori ented at an an gle with re spect to the fo li a tion of the am phi bo lite sur - round ing the pegmatites. Gen er ally they re tained an an gu lar shape and were boudinaged or streaked out only ex cep tion ally.
In di vid ual peg ma titic bod ies be came thick est in pres sure shad - ows be tween large am phi bo lite blocks.
In 2009 the whole sys tem ex tended over 60–80 metres in plan view (Fig. 4). Some of the peg ma titic dikes could be traced up to 50 m in ver ti cal sec tion be tween lev els 320 and 360 a.s.l.
They formed a com plex sys tem with a well-de fined frame work that con sisted of three main dikes strik ing NNE and dip ping 30 to 80° WNW (marked as Jul1, Jul2 and Jul4+5 in Fig. 4). They were ac com pa nied by over 20 smaller sub or di nate veins and apophyses that were ran domly ar ranged and of ten ter mi nated abruptly. The av er age thick nesses of Jul1, Jul2 and Jul4+5 were about 0.5, 1.5 and 4 m, re spec tively. Vein Jul4+5 split in its up per sec tion into two sim i lar-sized bod ies of Jul4 and Jul5.
The pegmatites were es sen tially undeformed and showed no fea tures of se quen tial em place ment in places where they cross-cut one an other. Am phi bo lite, typ i cally weakly fo li ated, of - ten showed strong schistosity when ap proach ing the peg ma tite con tacts. The schistosity was par al lel to the con tact and its ori - en ta tion var ied due to the ir reg u lar course of most of the peg - ma titic bod ies. In gen eral the pegmatites had sharp con tacts with the host rock. Thin peg ma titic veinlets rarely pen e trated along the am phi bo lite schistosity. Thicker peg ma titic bod ies de - vel oped a dis con tin u ous bi o tite en ve lope up to a few centi - metres thick. No other exocontact fea tures were ob served.
Based on the ex tent of tex tural and geo chem i cal dif fer en ti a - tion, the pegmatites could be ten ta tively grouped into: (1) prim i - tive quartz-feld spars-bi o tite pegmatites with ac ces sory gar net,
es sen tially ho mo ge neous with lo cally de vel oped graphic tex - ture (e.g., Jul1); (2) more evolved gar net-, tour ma line- and in places also mus co vite-bear ing pegmatites that pos ses tex tur - ally and min er al og i cally dif fer en ti ated seg ments as well as ho - mo ge neous por tions (e.g., Jul2 and Jul3) and (3) the most com - plex zoned pegmatites with the rich est min eral as sem blage (Ta ble 1), in which pri mary mus co vite suc ceeds bi o tite in the cen tral zones (e.g., Jul4 and Jul5). The de gree of tex tural dif fer - en ti a tion es sen tially cor re lates with the peg ma tite’s di men sions.
Usu ally the thick ness of the most prim i tive bod ies does not ex - ceed 30 cm.
The ide al ized zone se quence (Fig. 5) be gins with a dis con - tin u ous gran u lar bor der zone up to a few centi metres thick. It com prises fine- to me dium-grained (<5 mm) plagioclase of po - lyg o nal shape, plates of bi o tite and mostly in ter sti tial quartz (Fig. 6). Sub or di nate K-feld spar oc curs spo rad i cally. The bor - der zone is suc ceeded by a wall zone, where crys tals are coarser by an or der of mag ni tude than in the bor der zone and show pre ferred ori en ta tion and ar range ment re sult ing from uni - di rec tional growth (Fig. 6). Elon gate, lath-shaped bi o tite crys tals tend to be ar ranged ei ther par al lel or per pen dic u lar to the peg - ma tite-am phi bo lite con tact. The par al lel ar range ment is ob - served only lo cally in the out er most por tion of the wall zone, whilst the per pen dic u lar type be comes dom i nant in wards.
Wedge-shaped feld spar crys tals are ori ented per pen dic u lar to the con tact with the ver tex point ing to the wall. The thick ness of both the bor der and wall zones reaches 40 cm. Two in ter me di - ate zones can be dis tin guished. The outer one is com posed of both potassic feld spar-quartz and plagioclase-quartz graphic inter growths. It also con tains char ac ter is tic gi ant bi o tite laths, usu ally flar ing to wards the cen tral parts of the dikes. The amount of bi o tite de creases in wards, giv ing way to gar net and tour ma line lo cally ac com pa nied by mus co vite and beryl. The tran si tion to the in ner in ter me di ate zone is marked by the dis ap - Fig. 4. The Julianna peg ma titic sys tem
A – sche matic hor i zon tal and ver ti cal cross-sec tions; quartz cores that were iden ti fied in veins Jul2, Jul3 and Jul4 are marked;
B – in an about 18 m long hor i zon tal cross-sec tion veins Jul4 and Jul5 with a short apophysis be tween in a hor i zon tal cross-sec tion on the 360 a.s.l. level; C – view of the Jul1–3 veins from the 340 a.s.l. level along the 50 m long frag ment of the quarry's wall
Min eral name Fine-grained
bor der zone Coarse-grained wall zone
In ter me di ate zones
Quartz core graphic zone blocky
microcline
Al bite + + + +
Al la nite-(Ce) + +
Almandine + + + + +
Ar seno py rite +
Bar ite + +
Bavenite + +
Beryl + + +
Betafite group + +
Bi o tite + + + + +
Bismite +
Bis muth na tive +
Bis muthi nite +
Bismutite + + +
Calciosamarskite + +
Cas sit er ite +
Chal co py rite + +
Cheralite + + +
Clinochlore + + + + +
Colum bite-(Fe) + + +
Colum bite-(Mn) + + +
Dravite + + +
Epidote + +
Euxenite-(Y) + +
Ferriallanite-(Ce) + +
Ferrowodginite +
Fluorapatite +
Fergusonite-(Y) + +
Fersmite + +
Gadolinite-(Y) + +
Ga lena + +
Goethite + + + + +
He ma tite + +
Hingganite-(Ce) +
Hingganite-(Y) +
Hya lo phane + +
Ikunolite +
Il men ite + +
Ishikawaite + +
Ixiolite + +
Keiviite-(Y) +
Microcline + + + + +
Microlite group + +
Monazite-(Ce) + + +
Mus co vite + + + +
Phenakite +
Plagioclase £An39 + + + +
Polycrase-(Y) + +
Py rite + + +
Pyrochlore group + +
Pyrophanite + +
Pyrrhotite + +
Quartz + + + + +
T a b l e 1 Min er als of the low- to mod er ately-frac tion ated pegmatites of the Julianna sys tem from Pi³awa Górna
Min eral name Fine-grained
bor der zone Coarse-grained wall zone
In ter me di ate zones
Quartz core graphic zone blocky
microcline
Samarskite-(Y) + +
Schorl + + +
Spessartine + + +
Ver mic u lite + + + + +
Vikingite Ag4Pb8Bi14S31 +
Vikingite group (?) –
Ag5Pb4Bi17S32 +
Tantalite-(Fe) + +
Thorite + +
Ti tan ite + +
Ti tan ite group (?) –
Ca[Ti0.33(Al0.33Ta0.33)][SiO4]O +
Uraninite + +
Vuagnatite group (?) –
(Ca0.5Y0.5)Al[SiO4](O0.5OH0.5) +
Xeno time-(Y) + +
Zir con + +
Zoisite + +
The ones for which the Julianna peg ma titic sys tem is, ac cord ing to the au thors’ knowl edge, the first Pol ish oc cur rence as well as pos si ble new min eral spe cies are in bold. Min er als iden ti fied only from the most evolved Li- and Cs-en riched pegmatites (see the text for de tails) are not in cluded in the ta ble due to the in com plete data on the as sem blage and the po si tion in the zon ing se quence
Tab. 1 cont.
Fig. 5. Sche matic cross-sec tion of the Julianna-type peg ma tite vein
Fig. 6. The con tact of the Jul4 vein with am phi bo lite Tran si tion be tween the out er most bor der zone and the wall zone is marked by larger crys tal di men sions and pre ferred ori en ta tion with lon ger crys tal axes more or less per pen dic u lar to the con tact plane (de tails in the text); a small am phi bo lite xe no lith de tached from the wall is em bed ded in the peg ma tite; the ori en ta tion of the con tact plane shown in the fig ure is 280/35; the ham mer is 27 cm long
pear ance of graphic tex ture al though crystallisation of in di vid ual feld spar crys tals pro ceeded un in ter rupted across the tran si tion bor der. The in ner in ter me di ate zone is es sen tially de void of plagioclase and con tains mainly mas sive (blocky) K-feld spar.
Grey quartz fills in ter stices be tween feld spar crys tals. The in ter - me di ate zones con tain pods of symplectic inter growths of gar - net-quartz, tour ma line-quartz and mus co vite-quartz. Well-de - vel oped tour ma line, gar net, beryl and colum bite are the main ac ces sory min er als. The thick ness of both in ter me di ate zones reaches up to 2 m al though the pro por tions of the two units vary. Sev eral sep a rate quartz cores oc curred roughly in the ax ial parts of the Jul2, Jul4 and Jul5 veins (Fig. 4). The larg est one mea sured 1 ´ 2 ´ 3 m. Smaller segregations of quartz were dis trib uted less reg u larly within the in ter me di ate zones. Mas - sive grey quartz con tains euhedral beryl, tour ma line, gar net, K-feld spar and book-like ag gre gates of mus co vite pro ject ing from the sur round ing peg ma titic zones.
The zon ing se quence de scribed above of ten de vi ates from the ide al ized scheme be cause some units are re duced or miss - ing in the veins. It be comes strongly asym met ri cal in sub-hor i - zon tal seg ments of the pegmatites. In that case the thick ness of the outer zones di min ishes strongly in the hang ing wall part and the core is dis placed up wards. Be sides the in ter nal units of pri - mary or i gin, the pegmatites also con tain ran domly dis trib uted bod ies whose na ture is am big u ous, be ing ei ther pri mary or sec - ond ary. They vary in size and are dom i nated by mus co vite or saccharoidal, rarely platy al bite (cleavelandite). Other com mon min er als in clude gar net, tour ma line and Nb-Ta ox ides. Scarce frac ture fill ings are lim ited to al bite- or quartz-dom i nated thin (<1 cm) bod ies found mostly in the in ter me di ate zones. Quartz fill ings are of ten rooted in the quartz core. They lo cally con tain small crys tals of tour ma line, gar net and mus co vite as well as grains of ox ide and sul phide min er als.
MINERALS OF THE JULIANNA PEGMATITIC SYSTEM
The pegmatites of the Julianna sys tem are dom i nated by veins with a low to mod er ate de gree of frac tion ation that con sist of the rock-form ing feld spars, quartz and micas ac com pa nied by tour ma line, gar net and beryl. The as sem blage of ac ces sory min er als com prises colum bite-, samarskite-, euxenite- and il - men ite-group min er als, fergusonite-(Y), cas sit er ite, mona - zite-(Ce), xeno time-(Y), mem bers of the pyrochlore supe - rgroup, gadolinite-(Y), ti tan ite, base metal sulphides, Ag-Bi sulphosalts and oth ers (Ta ble 1). Rare lith ium- and cae - sium-rich min er als, in clud ing Li-rich tour ma lines and micas, spodumene and pollucite, were iden ti fied in pegmatites that at - tained an ex cep tion ally high de gree of frac tion ation (Pieczka et al., 2010c). How ever, they were found only in a few loose rock frag ments with lit tle in di ca tion of a broader geo log i cal con text.
There fore nei ther a com plete de scrip tion of the Li- and Cs-bear ing min eral as sem blage nor its po si tion within the peg - ma titic zon ing se quence can be given at pres ent.
FELDSPARS
White to grey ish white potassic feld spar con sti tutes most of the pegmatites’ vol ume. It shows op ti cal fea tures of perthitic microcline though the pres ence of orthoclase in some veins can not be ruled out. In the out er most peg ma titic zones K-feld - spar of ten con tains Ba-rich do mains that are usu ally de vel oped close to sec ond ary al bite re plac ing pri mary K-feld spar. The rel - a tive abun dance, mode of oc cur rence and crys tal size of
K-feld spar de fine the over all tex tural zon ing of the peg ma titic bod ies. Large crys tals (>40 cm) with well-de vel oped faces, en - coun tered in the in ner in ter me di ate zone, pos sess cores of graphic inter growths sur rounded by quartz-free perth ite (Fig. 7B, D). They gen er ally show a stout tab u lar habit that evolves into elon gate col umns pro ject ing from the footwall into the quartz core in the subhorizontal apophyses (Fig. 7C, D). Al - though feld spar is typ i cally euhedral against quartz of the quartz core, the op po site ten dency is some times also ob served. In such cases the feld spar-quartz con tact shows a sur face which is cor ru gated in a way sim i lar to growth sur faces in graphic K-feld spar-quartz inter growths.
White plagioclase, abun dant in the out er most parts of the pegmatites, can be the only feld spar in the bor der and wall zones (Fig. 7A). The wall zone of ten hosts wedge-shaped crys tals, per - pen dic u lar to the con tact. The amount of plagioclase de creases through out the outer in ter me di ate zone and the blocky feld spar zone is plagioclase-free near the quartz core (Fig. 7B).
Plagioclase shows pro gres sive so dium en rich ment to ward the vein cen tre from An39–12 in the mar ginal zones to An16–0 in the in - ter me di ate zones. Pri mary al bite (An5–0) is com monly ob served as plagioclase rims and tab u lar in clu sions in microcline. White, slightly blu ish and colour less platy al bite crys tals (<2 cm) form pods dis trib uted ir reg u larly within the in ner in ter me di ate zone and are pres ent in the in ter stices be tween gi ant crys tals of K-feld spar in the larg est Jul4 and Jul5 dikes.
Albitization of pri mary feld spars is wide spread and al though its ex tent var ies through out a sin gle peg ma tite body it is par tic u - larly in ten sive in the out er most peg ma titic zones. In the in ter me - di ate zones or quartz core, veinlets and streaks of sec ond ary al - bite cut plagioclase and K-feld spar mark ing fluid mi gra tion paths. In places sec ond ary al bite forms more vo lu mi nous ir reg - u lar pods lo cally as so ci ated with fine-grained mus co vite and tour ma line. Pro found albitization of K-feld spar re sults in cre at - ing small (<2 cm) voids which may be filled with clay min er als.
MICAS
Micas are black to dark brown bi o tite and colour less to sil - very-white mus co vite. In the prim i tive veins bi o tite is the only pri mary mica from the mar gin up to the quartz core. Ex cept for the gra nitic bor der zone, it usu ally forms strongly elon gated (<60 cm) laths (Fig. 8). Pseudohexagonal plates oc cur rarely.
Chloritization of bi o tite is wide spread. In more evolved pegmatites mus co vite grad u ally suc ceeds bi o tite in the outer in - ter me di ate zone and is found up to the quartz core (Fig. 9).
Short apophyses that branched from vein Jul5 to wards Jul4 were ex posed on the 360 a.s.l. quarry level (Fig. 7A, B), and were par tic u larly abun dant in mus co vite. In di vid ual mus co vite blades rarely ex ceed 10 cm. In con trast to bi o tite, they are dis - trib uted less reg u larly and form large (<15 cm) book- and ro - sette-like ag gre gates. Pods of cha ot i cally ar ranged crys tals and plumose ag gre gates are rare. In ter me di ate zones host also mus co vite-quartz symplectites. Pri mary mus co vite is com - monly ac com pa nied by gar net, tour ma line and beryl. A later gen er a tion of fine-grained mus co vite cov ers the faces of other min er als, mainly K-feld spar, beryl and tour ma line or is pres ent in frac ture fill ings and along part ing and cleav age planes. It can - not be ruled out that at least some of the podiform ag gre gates of fine-grained mus co vite may be of sec ond ary or i gin.
QUARTZ
Quartz, usu ally grey, smoky and milky, rarely colour less and rose, is pres ent in all the peg ma titic zones, al though its rel a tive
Fig. 8. Biotite laths from the outer in ter me di ate zone The ham mer is 33 cm long
Fig. 7. Feld spars
A – a slice of peg ma tite con tact ing with am phi bo lite af ter re ac tion with cobaltinitrite that stains K-feld spar yel low (mod i fied method of Bailey and Stevens, 1960), close to the con tact the peg ma tite con tains only plagioclase, K-feld spar ap pears at some dis tance from the con tact; B – a slice of the peg ma tite at the tran si tion be tween the graphic outer in ter me di ate zone and the blocky K-feld spar with euhedral ter mi na tions, apart from microcline the graphic zone con tains quartz-plagioclase inter growths; C – co lum nar crys tals of microcline, the lens cover is 5 cm across; D – typ i cal crys tals of microcline (up to 8 cm) with quartz-intergrown cores
abun dance and habit var ies. Ir reg u lar anhedral grains are typ i - cal of the gran ite-tex tured bor der zone. In ter sti tial quartz in the spaces be tween ear lier crys tal lised phases is very com mon.
How ever, the most prom i nent tex tural va ri ety is cu ne i form quartz graph i cally intergrown with feld spars of the outer in ter - me di ate zone (Figs. 7B, D and 10A–C). The thick ness of the quartz rods in creases to wards the cen tre of the dikes and also from the cen tre to wards the mar gins of in di vid ual feld spar crys - tals, in places ex ceed ing 2 cm. Mas sive peg ma titic cores rep re - sent the lat est gen er a tion of pri mary quartz (Fig. 10D). The quartz core usu ally en vel ops well-formed crys tals of K-feld spar, micas, gar net, beryl and tour ma line that ei ther pro ject from the ad ja cent in ter me di ate zone or are com pletely sub merged in quartz. How ever, in some parts of the in ter me di ate zone, quartz turns at least partly euhedral against K-feld spar and shows well-de vel oped lo cally stepped pris matic and rhombohedral faces. Quartz frac ture fill ings can be rooted in the quartz cores.
GARNET
The almandine-spessartine va ri ety of gar net (Nejbert et al., 2010), with colours rang ing from dark brown through var i ous shades of red to yel low ish-or ange, is com mon in both the in ter - me di ate zones and the quartz core (Fig. 11). Large euhedral crys tals (<5 cm) form com bi na tions of rhombic do deca he dra and trap e zoidal icositetrahedra, in places grouped in string-like ag gre gates (Fig. 11). Skel e tal gar net intergrown with quartz, more rarely with K-feld spar and mus co vite, oc curs in the outer in ter me di ate zone. The inter growths form oval pods, some over 10 cm long. Sim i lar gar net-quartz inter growths con sti tute the cores of larger crys tals with quartz-free euhedral mar gins.
TOURMALINE
Tour ma line of the schorl-dravite se ries (Pieczka et al., 2010b) forms euhedral pris matic crys tals ter mi nated with trigonal pyr a mids or/and a pedion face (Fig. 12). It oc curs from the outer in ter me di ate zone up to the quartz core and its abun - dance var ies in versely with that of bi o tite. Spec tac u lar gi ant crys tals up to 70 cm long and 7 cm across were found in vein Jul4+5, strad dling the bound ary be tween the two in ter me di ate zones. Com mon fun nel-shaped ag gre gates spread out to wards the dike cen tres. Tour ma line-quartz symplectites oc cur as up to 20 cm large oval pods in the outer in ter me di ate zone. In di vid ual crys tals are lo cally bro ken with frag ments dis placed and the frac tures sealed by quartz. In thin sec tion tour ma line crys tals re veal an in ter nal tex ture that con sists of a core with blue to colour less pleochroism and a rim with pleochroic colours rang - ing from ol ive-green through brown to colour less. A late gen er a - tion of finer-grained tour ma line forms 2–3 cm long thin and of - ten flat tened prisms which oc cur along the cleav age and part ing planes of feld spars.
BERYL AND OTHER Be MINERALS
Green, pale yel low, rarely white or slightly blu ish beryl (Fig. 13) ap pears from the outer in ter me di ate zone up to the quartz core. It is par tic u larly abun dant in mus co vite-rich por tions of the pegmatites. Beryl forms hex ag o nal prisms ter mi nated by hex ag o nal pyr a mids or pina coids, up to 15 cm long and sev eral centi metres wide. Ex cep tion ally well-de vel oped crys tals oc - curred in the quartz cores of veins Jul4 and Jul5. Char ac ter is tic ici cle- and pear-shaped crys tals thick en ing to wards the peg ma - Fig. 9. Mus co vite
A – ran domly-ori ented ag gre gates, the lens cover is 5 cm across; B – mus co vite-quartz symplectites (15 ´ 10 cm);
C – ra dial ag gre gate in microcline (10 ´ 10 cm); D – frag ment of a larger book-like ag gre gate (10 ´ 10 cm)
Fig. 11. Gar net
A – gar net-quartz symplectites (3 cm); B – crys tal with the form of a rhombic dodecahedron mod i fied by sub or - di nate trap e zoidal icositetrahedron faces (4 cm); C – string-like ag gre gate of crys tals up to 1 cm long in quartz;
D – crys tal with the form of a rhombic dodecahedron com bined with trap e zoidal icositetrahedron (1.5 cm) Fig. 10. Quartz
A – quartz-feld spars inter growths in the core of a large feld spar crys tal man tled by quartz-free perth ite, the coin is 2 cm large; B – typ i cal cu ne i form quartz rods intergrown with feld spars from the outer in ter me di ate zone, the pol ished sur face is about 18 cm long; C – coarse quartz rods in graphic inter growths, the coin is 2 cm across;
D – quartz core in the Julianna Jul5 vein in plan view, the ham mer is 33 cm long
titic cores are com mon. Some beryl crys tals con tain in clu sions of bavenite and phenakite (£odziñski et al., 2010).
COLUMBITE AND OTHER ACCESSORY MINERALS
Colum bite-group min er als pre dom i nate over (Y, REE, Nb, Ta, Ti)-rich ox ide min er als and in clude colum bite-(Fe), colum - bite-(Mn) and tantalite-(Fe) (Pieczka et al., 2010a). They are usu ally as so ci ated with beryl and oc cur as black platy crys tals, up to 7 cm long and 1 cm wide (Fig. 14) in the in ter me di ate zones and in the quartz core and as thin nee dles in more dif fer - en ti ated veins (e.g., vein Jul4+5). Zir con, xeno time-(Y), monazite-(Ce), cheralite, samarskite- and euxenite-group min - er als (Fig. 15) along with al la nite(-Ce), (Nb,Ta)-en riched cas sit - er ite, ti tan ite and il men ite are rel a tively com mon, the other ac - ces sory min er als be ing rare.
LITHIUM- AND CAESIUM-RICH MINERALS
Li-rich min er als are rep re sented mainly by spodumene, le - pido lite, and tour ma lines of the elbaite-olenite-rossmanite se - ries along with rare lithiophilite and prob a bly also liberite and eucryptite (Pieczka et al., 2012). A very high de gree of Mn-Fe frac tion ation is also re flected by the com po si tion of gar net close to the spessartine end-mem ber (Nejbert et al., 2010) and the oc cur rence of colum bite-(Mn) and tantalite-(Mn). Cs-rich beryl reaches a com po si tion cor re spond ing to pezzottaite. The whole as sem blage is closely as so ci ated with pri mary al bite and may
rep re sent a dis tinct late con stit u ent of the zon ing se quence de - scribed above.
Pollucite oc curs to gether with Li-rich micas, quartz, zeolites and clay min er als in up to 30 cm large pods within the graphic-in ter me di ate zone. At the pres ent stage of study it is not pos si ble to state whether the pollucite-bear ing pods are pri mary or sec ond ary.
FINAL REMARKS
Pub lished data on the tex tural and min er al og i cal char ac ter - is tics of the peg ma tite oc cur rences that were mined in his tor i cal times in the fore land do main of the GSB unit (Lis and Sylwestrzak, 1986 and ref er ences therein) as well as stud ies of his tor i cal sam ples stored in min er al og i cal mu se ums sug gest that the great ma jor ity of these bod ies rep re sent a sin gle and rel a tively uni form peg ma tite pop u la tion. Mi nor dif fer ences seem to be a re sult of var i ous de grees of geo chem i cal and tex tural dif fer en ti a tion of in di vid ual pegmatites. The newly dis cov ered low to mod er ately evolved pegmatites from the Pi³awa Górna Quarry are in all re spects rep re sen ta tive of that pop u la tion. At the same time the large scale of the Julianna peg ma titic sys tem shows that the po ten tial for sim i larly evolved pegmatites in GSB has been un der es ti mated (e.g., Mikuszewski et al., 1976).
The Julianna veins were emplaced dur ing a sin gle event in a zone of tectonized am phi bo lite. Blocks of the coun try rock be - haved in a rigid man ner at the time of in tru sion. The over all ge - om e try of the Julianna sys tem and re la tions to the host rock fab - Fig. 12. Tour ma line
A – tour ma line-quartz symplectites (17 cm long); B, C – fun nel-shaped ag gre gates of pris matic crys tals, the lens cover is 5 cm large; D – frag ments bro ken crys tal are dis placed and re-sealed with quartz (7 cm);
E – ideal pris matic crys tal (8 cm)
ric sug gest that the in tru sion post dated re gional ret ro grade meta mor phism un der am phi bo lite fa cies con di tions and brit tle de for ma tion and took place through pas sive fill ing of tec tonic frac tures. The NNE–SSW ori en ta tion of the peg ma titic veins con forms to the sys tem of frac tures su per im posed on larger NW–SE ori ented fault planes in the fore land GSB do main (¯elaŸniewicz, 1985; Cymerman et al., 1988; Cymerman, 1989). Large veins show a well-de vel oped clas si cal zon ing pat - tern with uni di rec tional and skel e tal so lid i fi ca tion tex tures in - clud ing comb-like feld spars, bi o tite and tour ma line, quartz-feld - spar graphic inter growths as well as quartz-mus co vite, quartz-gar net and quartz-tour ma line symplectites. Such fea -
tures re sult from sub stan tial undercooling and rapid crystallisation of a peg ma titic melt in trud ing into cooler coun try rocks (e.g., Lon don, 2009 and ref er ences therein). These ob - ser va tions are in ac cor dance with the model pro posed by
¯elaŸniewicz (1987, 1990), in which the pegmatites rep re sent syn-ex hu ma tion dikes that sealed sub-ver ti cal ten sion-re lated frac tures.
The Julianna sys tem rep re sents the rare-el e ment (REL) class pegmatites (see Èerný and Ercit, 2005) and ex hib its high vari abil ity in de gree of frac tion ation and min er al ogy. The beryl-colum bite sub type pre vails al though among the most frac - tion ated veins al bite-spodumene and per haps also com plex Fig. 13. Beryl
A – pear-shaped crys tal (8 cm); B – pris matic crys tals (6 cm); C – frag ment of a beryl prism ter mi nated by a basal pina coid (10 ´ 12 cm); D – short pris matic crys tal ter mi nated by de formed pyr a mid (4 cm); E – short prism ter mi - nated by basal pina coid (7 cm long); F – pris matic crys tals ter mi nated by mul ti ple pyr a mids (10 cm long); G – pris - matic crys tal ter mi nated by a com bi na tion of pyr a mid and pina coid (5 cm)
REL types could be dis tin guished. The cur rent petro gen etic clas si fi ca tion of gra nitic pegmatites dis tin guishes be tween two dis tinct LCT (en riched in Li, Cs and Ta) and NYF (en riched in Nb, Y and F) fam i lies and pegmatites with a hy brid NYF + LCT geo chem i cal sig na ture (Èerný, 1991; Èerný and Ercit, 2005).
The ma jor ity of the Julianna veins, which dis play a low to mod - er ate de gree of frac tion ation, con tain typ i cal NYF-sig na ture ac - ces sory min er als, such as al la nite-(Ce), colum bite-, euxenite- and samarskite group min er als, fergusonite-(Y) and gadolinite-(Y). How ever, with in creas ing frac tion ation, the min - eral as sem blage of the most evolved pegmatites dis plays the LCT sig na ture as shown by the pres ence of spodumene, le - pido lite, pollucite and other Li- and Cs-rich min er als. There fore the en tire peg ma titic sys tem is as signed to the mixed NYF + LCT fam ily. Ge netic sce nar ios pro posed to ex plain the mode of or i gin of hy brid NYF + LCT pegmatites in clude par tial melt ing of an only par tially de pleted crustal source, anatexis of mixed de pleted and undepleted lithologies as well as var i ous pos si bil i ties of ex ter nal con tam i na tion (Èerný, 1991; Èerný and Ercit, 2005; Mar tin and De Vito, 2005; Novák et al., 2012).
The data avail able do not al low the draw ing of a co her ent model for the or i gin of the Julianna peg ma titic sys tem. Cur rent con cepts of the geo log i cal evo lu tion of the GSB re late the or i gin of mi nor gra nitic and peg ma titic bod ies to anatectic melt ing of the source rocks that com prise both supracrustal and man - tle-re lated lithologies (e.g., Grocholski, 1967; Morawski, 1973;
Kryza, 1981; Gunia, 1985; ¯elaŸniewicz, 1987, 1990; Kröner
and Hegner, 1998; Kryza and Pin, 2002). Such protoliths have the po ten tial to gen er ate melts with LCT, NYF as well as hy brid LCT + NYF geo chem i cal sig na tures. The anatectic GSB granitoids and pegmatites so lid i fied at about the same time at 370–380 Ma (Breemen et al., 1988; Timmermann et al., 2000).
How ever, there is no com pel ling ev i dence that they are con san - guin e ous and it re mains un known whether the peg ma titic melts were de rived di rectly from small amounts of par tial melts or were sub jected to dif fer en ti a tion pro cesses in a pluton-sized res er voir of anatectic magma.
An other im por tant is sue to be ad dressed be fore a petro gen - etic scheme for the Julianna pegmatites can be pro posed is the pos si bil ity of ex ter nal con tam i na tion of the pris tine peg ma - tite-form ing melt. In situ con tam i na tion from the man tle-re lated host am phi bo lite (Kryza and Pin, 2002; Ilnicki et al., 2012) could add NYF char ac ter is tics to the so lid i fy ing melt. How ever, abun - dant uni di rec tional and skel e tal tex tures in di cate dis equi lib rium crystallisation at high undercooling val ues and the me ter-scale thick ness of in di vid ual dikes im plies rapid so lid i fi ca tion of the pegmatites. Thus in ter ac tion of the melt with the host rocks was strongly lim ited in time. Also the sharp am phi bo lite-peg ma tite con tacts, mostly an gu lar shape of am phi bo lite xe no liths in - cluded into the pegmatites and the poorly de vel oped exocontact, only a few centi metres thick, sug gest that the ef fect of in situ con tam i na tion was of mi nor im por tance. On the other hand, the pos si bil ity of melt con tam i na tion prior its em place - ment re mains an open ques tion.
Fig. 14. Colum bite
A – the larg est known colum bite crys tal from Pi³awa (8 cm); B – 2.2 cm long pris matic crys tal; C – 3 cm frag ment of a tab u lar crys tal; D – 4 mm long pris matic crys tals over grown by iso met ric pale green cheralite
Sys tem atic min er al og i cal and geo chem i cal stud ies of the pegmatites from the Pi³awa Górna Quarry are cur rently in prog - ress. Al though pre lim i nary, the re sults pre sented here pro vide com pel ling ev i dence for the Julianna peg ma titic sys tem as a unique min er al og i cal oc cur rence in the Bo he mian Mas sif.
Ac knowl edge ments. The au thors would like to ex press their deep est grat i tude to the au thor i ties of the Dolnoœl¹skie Surowce Skalne min ing com pany for their ex cep tional and un - prec e dented help dur ing field work. We are par tic u larly very thank ful to J. £uczak, the re cently de ceased pres i dent of the
DSS Com pany, for his great un der stand ing, per sonal in volve - ment and in ter est in our re search. The peg ma titic sys tem de - scribed in the pa per is named af ter his youn ger daugh ter – Julianna. We also would like to thank M. Ro man, the cur rent DSS pres i dent, and M. Then as well as all mem bers of the com - pany’s and mine’s man age ments for con tin u ing this ex em plary co op er a tion. The au thors thank R. Mac don ald for im prov ing the Eng lish ver sion of the text and the re view ers: D. Lon don, M.
Novák and J. Janeczek for their help ful dis cus sion on the manu script. The study was fi nanced by the Min is try of Sci ence and Higher Ed u ca tion grant NN307 241737.
Fig. 15. Ac ces sory min er als
A – elon gated zir con (1 cm); B – iso met ric zir con ep i taxy on yel low xeno time (1 cm); C – xeno time-zir con inter growths (0.5 cm); D – tab u lar monazite (1 cm); E – iso met ric cheralite (up to 1 mm) on colum bite;
F – crys tals of samarskite-euxenite group min er als (<1 cm)
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