Rodingite from Nas³awice and the other oc cur rences of these rocks in Lower Silesia (SW Po land)
Wies³aw HEFLIK1, Lucyna NATKANIEC-NOWAK1 and Magdalena DUMAÑSKA-S£OWIK1, *
1 Fac ulty of Ge ol ogy, Geo phys ics and En vi ron men tal Pro tec tion, AGH Uni ver sity of Sci ence and Tech nol ogy, Al. A. Mickiewicza 30, 30-059 Kraków, Po land
Heflik W., Natkaniec-Nowak L. and Dumañska-S³owik M. (2014) Rodingite from Nas³awice against the other oc cur rences of these rocks in Lower Silesia (SW Po land). Geo log i cal Quar terly, 58 (1): 31–40, doi: 10.7306/gq.1126
Rodingites from Nas³awice of the Jordanów-Gogo³ów ser pen tin ite mas sif in SW Po land are com posed of augite/di op side, grossular and hornblende/tremolite. The ac ces sory com po nents are rep re sented by vesuvianite, adu laria, ba saltic horn - blende and picotite. Ap a tite, millerite?, sphalerite, ga lena, Fe-sulphides, Ni-sulphides and Ni-ar se nates were also ob served as trace phases in these rocks. Gen er ally, rodingites from Nas³awice are en riched in nu mer ous polymetallic com pounds of Cu, Ag, Fe, Ni, Co, Fe, Pb, Zn, As and Bi, and show a sim i lar min eral as so ci a tion and tex ture as rodingites from the other oc - cur rences in SW Po land, i.e. from the Szklary and Braszowice-BrzeŸnica mas sifs. They most prob a bly de vel oped from a mafic protolith (fine-grained gab bro) in trud ing into serpentinized ultra mafic rocks un der metasomatism con di tions. The sec - ond ary pneumo-hy dro ther mal post-gra nitic ac tiv i ties also af fected the fi nal for ma tion of these metasomatic rocks.
Key words: rodingite, Nas³awice, Sudetes, polymetallic com pounds, mafic protolith.
INTRODUCTION
Rodingite is a rare, gar net (grossularite, hydrogrossularite, an dra dite)-di op side (diallage) rock formed by metasomatism. It can be en riched in other Ca-sil i cates, like epidote, prehnite and vesuvianite. The world wide bib li og ra phy on this rock is quite rich; in clud ing pa pers as early as e.g., Bell et al. (1911) and Benson (1914). Some pa pers pres ent the oc cur rences of rodin - gites in var i ous parts of the world, as e.g. Bloxam (1954), Bilgrami and Howie (1960), Vuagnat and Pusztaszeri (1964), Seki (1965), Coleman (1966), O’Brien and Rodgers (1973), Ev - ans et al. (1979), Barriga and Fyfe (1983), Sivell and Wa ter - house (1986), Schandl et al. (1989), O’Hanley et al. (1992), Mogessie (1994), Kobayashi et al. (1997) and the lat est ones, as e.g. Schandl and Mittwede (2001), Kobayashi and Kaneda (2010), Perraki et al. (2010) and ref er ences therein. In Po land, rodingites are as so ci ated mainly with ultra mafic and mafic rocks of ophiolitic com plexes within the Góry Sowie Block (Gunia, 1996; Kryza, 2011). The char ac ter is tics of the rodin - gites from the Jordanów-Gogo³ów Mas sif (Majerowicz, 1979, 1984; Heflik and ¯abiñski, 1980; Heflik, 1982; Heflik and Sob - czak, 1988; Dubiñska, 1989, 1995, 1997; Dubiñska et al., 1991, 2004; Dubiñska and Gunia, 1997; Ga³uskin and Sze³êg, 2003)
and the Braszowice-BrzeŸnica Mas sif (Gunia, 1986a, b, 1989, 1992) are well-known. How ever, rodingites from the Szklary Mas sif seem to be less known; they were de scribed by Heflik and Natkaniec-Nowak (1987, 1989) and Dubiñska et al. (1991).
The over rid ing pur pose of the study is to de scribe the pres - ence of new min eral phases in rodingites from Nas³awice and to give a short sum mary of the gen eral data about rodingites from Lower Silesia (SW Po land).
GEOLOGICAL SETTING
Nas³awice Quarry is lo cated within the Jordanów-Gogo³ów ser pen tin ite mas sif (Fig. 1), which is the larg est of the three ultra mafic bod ies of the Sudetic ophiolite (Dubiñska et al., 2004). This mas sif oc curs close to the north ern bor der of the Góry Sowie Block (Fig. 2). In the north, serpentinites of the mas sif dis play ther mal-metasomatic con tacts with Variscan granitoids of the Strzegom-Sobótka Mas sif (Majerowicz and Pin, 1989). The Jordanów-Gogo³ów Mas sif is com posed mainly of serpentinites and sub or di nate fresh or slightly al tered peri dot - ites. The serpentinites are con sid ered to be the lower part of the Œlê¿a ophiolitic se quence (Narêbski and Majerowicz, 1985) of Early De vo nian age (Dubiñska et al., 2004; Kryza, 2011). The pri mary min er al ogy of ultra mafic rocks sug gests that serpenti - nites were de vel oped from harzburgites and lherzolites (Dubiñ - ska and Gunia, 1997). Sev eral oc cur rences of rodingites and other leucocratic rocks were found within the serpentinized rocks of the Jordanów-Gogo³ów Mas sif (Gunia, 1996). Dubiñ - ska (1995) iden ti fied two types of rodingites within the mas sif:
* Corresponding author, e-mail: dumanska@agh.edu.pl
Received: February 14, 2013; accepted: September 7, 2013; first published online: October 26, 2013
boninitic rodingite and plagiogranite rodingite. More de tailed ge ol ogy and a geo log i cal sketch map of this re gion was pre - sented by Dubiñska (1995) and Dubiñska et al. (2004).
METHODS
Mi cro scopic and Raman spec tros copy in ves ti ga tions were car ried out at the lab o ra to ries of the Fac ulty of Ge ol ogy, Geo - phys ics and En vi ron men tal Pro tec tion, AGH Uni ver sity of Sci - ence and Tech nol ogy in Kraków, Po land. Stan dard op ti cal ex - am i na tions were car ried out with an Olym pus BX 51 po lar iz ing mi cro scope. Back scat tered elec tron ob ser va tions were con - ducted on pol ished sec tions us ing a FEI Quanta 200 FEG scan - ning elec tron mi cro scope with an EDS de tec tor. The sys tem of SEM op er ated at 20 kV ac cel er at ing volt age, 50 mA cur rent, in a high vac uum mode, i.e. 6 ´ 10–5 – 7 ´ 10–6 Torr.
Raman spec tra of se lected rodingite com po nents were re - corded with a Raman Thermofisher Sci en tific spec trom e ter cou pled with a DXR mi cro scope equipped with 50´, 20´ and 10´ mag ni fi ca tion lenses. The sam ples were ex cited with the 514.5 nm line of a Spec tra-Phys ics Ar+ la ser. The la ser power and ex ci ta tion time was ac com mo dated to the op ti cal char ac ter of the sam ples. It should be noted that no sam ple prep a ra tion was per formed. Un for tu nately, the vast ma jor ity of rock re gions could not be used due to the la ser-in duced sam ple flu o res - cence.
FORMER AND PRESENT STUDIES OF SUDETIC RODINGITES
JORDANÓW-GOGO£ÓW SERPENTINITE MASSIF
Min er al og i cal and petrographic stud ies of serpentinites from this mas sif have been con ducted since the end of the 19th cen - tury. The pos si bil ity of oc cur rence of rodingites in Sudetic ophiolites, es pe cially within the Jordanów-Gogo³ów Mas sif, was first men tioned by Traube (1885, 1888), and then by Sachs (1902) who con nected these rocks with Weisssteins (term used by Ger man ge ol o gists for white aplite veins in ter sect ing var i ous, dark col oured rocks from the Niemcza Zone). An in ter est in this prob lem was sub se quently con tin ued by Gawe³ (1957) and Heflik (1967). In ves ti gat ing the al tered leucocratic zone in Jordanów Œl¹ski, Heflik (1967) found that there is an as so ci a - tion of grossular with vesuvianite, di op side, zoisite and prehnite, which was later rec og nized as rodingite (Heflik and ¯abiñski, 1980). At Jordanów Œl¹ski, rodingite oc curs in the north west ern and east ern walls of the quarry, in the form of ir reg u lar lenses, 1 ´ 0.25 m in size. In the vi cin ity of Jordanów Œl¹ski, a sim i lar min eral paragenesis was also ob served in both the ser pen tin ite quarry in Nas³awice (Heflik, 1968; Gunia, 1996) and a small quarry lo cated south of the vil lage of Œwi¹tniki (Majerowicz, 1979, 1984). Within the Jordanów-Gogo³ów Mas sif, rodingites were also ob served be tween Glinica and Jordanów Œl¹ski, near Uliczna (Czernica Hill; Gunia, 1996).
32 Wies³aw Heflik, Lucyna Natkaniec-Nowak and Magdalena Dumañska-S³owik
Fig. 1. The lo cal iza tion of Nas³awice Quarry within the Œlê¿a com plex (mod i fied af ter Majerowicz, 1984)
Rodingite from Jordanów Œl¹ski is white in col our and con - tains gar net (grossular) with saponite (Heflik and ¯abiñski, 1965). Lo cally, it can also be com posed of gar nets with py rox - enes (di op side), lo cally intergrown with tremolite, form ing ag - gre gates with a ra dial tex ture (Fig. 3). Crystallisation of this as - so ci a tion took place in stages. De creas ing tem per a ture led to the crystallisation of the fol low ing phases: first di op side and grossular, and then tremolite. Rodingite of this mas sif is lo cally cut by thin magnesite-talc veins (Fig. 4). Min eral com po si tion of rodingites from other lo cal i ties in Lower Silesia is very sim i lar to that of Jordanów-Gogo³ów metasomatic rocks.
In the early 1980s, the se nior au thor men tioned the pres - ence of min er al og i cal paragenesis in Nas³awice, which are iden ti cal to those from Jordanów Œl¹ski (Heflik, 1982). In 2009, in the south east ern part of the Nas³awice Quarry, he found an about 20-cm-thick vein com posed of in tensely al tered fine- grained gab bro, which con tained green-white rodingite en - claves. Sam ples col lected from these rocks are the ob ject of the pres ent stud ies. The rocks are com monly por phy ritic, con - sist ing of diallage and strongly al tered hornblende pheno - crysts set in the fine-grained di op side and am phi bole (tremo - lite–actinolite) groundmass. The pheno crysts are also rep re - Fig. 2. The dis tri bu tion of ba sic and ultrabasic rocks within the Niemcza Zone
(mod i fied af ter Smulikowski and Teisseyre, 1957)
Fig. 3. Py rox enes with ra dial tex ture in rodingite from Jordanów Œl¹ski (crossed polars)
Fig. 4. Car bon ate vein in rodingite from Jordanów Œl¹ski, (crossed polars)
sented by nu mer ous tab u lar forms, which are most prob a bly fine-grained ag gre gates of pyroxene with gar net crysta lised prob a bly af ter pri mary ba sic plagioclase. The ma jor ity of phenocrystals are strongly al tered, only the diallage is rel a - tively fresh; al though the pe riph eral parts of some of the crys - tals are amphibolitized to some ex tent.
The pres ence of main com po nents of this rock, i.e. grossu - lar and di op side was con firmed by mi cro Raman spec tros copy (Fig. 5). The pres ence of grossular is man i fested by the bands at 370, 423, 545, 819 and 876 cm–1. The bands 423, 546 and 819 and 876 cm–1 are re lated to Si-O bend ing and stretch ing vi bra tions, re spec tively (Kolesov and Gei ger, 1998, 2005).
The band at 370 cm–1 could be mixed T/R(O4H4) and T/R(SiO4) vi bra tions. The char ac ter is tic bands at 138, 660, 675 and 1009 cm–1 can be at trib uted to di op side. Richet et al.
(1998) as signed bands 660–675 cm–1 and 1009 cm–1 to a mixed stretch ing bend ing mode of the Si-O-Si bridg ing bond and Si-O stretch ing vi bra tions with non-bridg ing ox y gen, re - spec tively. The band of 138 cm–1 is as so ci ated with the de for - ma tion mode of the sil i cate chain.
The main com po nents of the rocks are ac com pa nied by ac - ces sory min er als of vesuvianite and adu laria with char ac ter is tic hour-glass zon ing (Fig. 6). Lo cally, sin gle crys tals of ba saltic hornblende and picotite (Fe, Mg)(Al, Cr)2O4 also oc cur in the rock. This type of hornblende is of ten found in fine-grained gab - bro; Heflik and ¯abiñski (1970) de scribed it in the rock from S³upiec in the Nowa Ruda gab bro-diabase mas sif. It was most likely formed as a re sult of iron ox i da tion un der the in flu ence of hot gases in the last stage of magma dif fer en ti a tion.
In SEM im ages, rodingite en claves from Nas³awice form a pyroxene-gar net con glom er ate in ter sected by nu mer ous thin veins. The ma trix is made of py rox enes form ing well-de vel oped thin col umns as well as spher i cal ag gre gates. SEM-EDS in ves -
ti ga tions re vealed that the pyroxene com po si tion is vari able, from di op side (sin gle crys tals) to augite (spher i cal ag gre gates).
The lat ter also shows a vari able com po si tion be tween in di vid ual do mains of crys tal, i.e. in the core, Al dom i nates over Mg, whereas in the rim, the con tent of Al de creases and the con tent of Mg in creases (Fig. 7). Sim i larly, gar nets show vari able com - po si tions of Al, Cr and Fe, typ i cal of the ugrandite group.
The veins that in ter sect rodingites are filled with gar nets (Fig. 8) or py rox enes. Hence, it is as sumed that in ad di tion to rodingite that re sulted from eins (dykes) of augite/di op side and ba sic plagioclase, there is also an other (youn ger) gen er a tion of rodingite.
34 Wies³aw Heflik, Lucyna Natkaniec-Nowak and Magdalena Dumañska-S³owik
Fig. 5. Mi cro pho to graph of groundmass made of di op side (up per Raman spec trum) and grossular
(lower Raman spec trum)
Fig. 6. Adu laria (Adl) crys tals in rodingite from Nas³awice (crossed polars)
The SEM-EDS stud ies, re vealed the pres ence of nu mer ous ac ces sory phases in rodingite from Nas³awice, i.e. ap a tite, millerite? (Fig. 9A), sphalerite (Fig. 9B), ga lena and iron sulphides (Fig. 9C). The lat ter com pounds con tain also traces of Cu and Ni. Be sides the sulphides, Ni ar se nates with Bi traces were found in the rock ma trix (Fig. 9D). Polymetallic com - pounds, rich mainly in nickel, form tiny crys tals (Fig. 10A). In the pe riph eral parts, they are rep re sented by nickel sulphides with Pb traces, whereas in the cen tral part – by nickel ar se nates with Fe and Pb ad mix ture. Lo cally, Ni sulphides with Bi, Co and Pb, are also ob served (Fig. 10B). In the vi cin ity of Nas³awice, pitticite (hy drous fer ric ar se nate sul phate) was re ported from serpentinites of Jordanów Œl¹ski (Traube, 1888).
The pres ence of na tive el e ments of the Cu-Au se ries and their com pounds in rodingites was de scribed by Spiridonov et al. (1997). In Po land, na tive cop per in rodingitizated gab bro was re ported by Gunia (1986b) from serpentinites of the Braszo - wice-BrzeŸnica Mas sif. Sim i larly, the min eral paragene sis was also found by Ga³uskin and Sze³êg (2003) in rodingites from Nas³awice. They found amal gam ates of sil ver in as so ci a tion with Cu and Ag sulphides, Ag and Cu selenides, and Cu, and na tive cop per ox ides.
SZKLARY SERPENTINITE MASSIF
In the 1980s, de tailed geo log i cal in ves ti ga tions were car ried out in the Marta’ nickel mine in Szklary near Z¹bkowice Œl¹skie (vide Heflik and Natkaniec-Nowak, 1989). The aim of these in - ves ti ga tions was to study serpentinites and other prod u cts of serpentinization, formed as a re sult of al ter ation of ultra mafic (du nite, peridotite) and mafic rocks (gab bro) (vide Natkaniec- Nowak and Pitera, 1986). Dur ing those stud ies, lenses of rocks re sem bling neph rite with the as so ci a tion of leucocratic rocks were found in Szklary (Heflik et al., 1988). A sim i lar phe nom e - non of paragenesis of rocks was de scribed by Heflik (1967) from the Jordanów Œl¹ski ser pen tin ite quarry near Sobótka.
In Szklary, the out crops of leucocratic and neph rite-like rocks are lo cated in the north ern part of the mine, in the west ern wall (lens of 5 ´ 2 m in size), and about 200 m to the north in the east ern wall (zone of 12 ´ 2 m in size). Al tered gab bro with in - clu sions of rodingites was ob served in this re gion (vide Heflik and Natkaniec-Nowak, 1989). In its im me di ate vi cin ity, white- col oured, crum bly albitites (Muszyñski and Natkaniec- Nowak, 1993, 1992) and crys tal line schists (tremolite and bi o - tite–actinolite–ver mic u lite) were also found. All these rocks oc - cur within the in tensely al tered serpentinites. In this leucocratic zone, the min eral as so ci a tion in cludes grossular, augite/di op - side, plagioclase (al bite–oligoclase), tremolite, clinozoisite, clinochlore, ser pen tine, prehnite and talc.
Fig. 7. Vari able com po si tion of a pyroxene crys tal:
1 – core, 2 – rim (BSE im age)
Fig. 8. Gar net vein in ter sect ing rodingite from Nas³awice (crossed polars)
36 Wies³aw Heflik, Lucyna Natkaniec-Nowak and Magdalena Dumañska-S³owik
Fig. 9A–D – ore-bear ing phases in rodingite from Nas³awice (BSE im age)
A – nickel sul phide (1); B – sphalerite (2, 3); C – ga lena (4), iron sul phide (5); D – Ni ar se nates (6)
Fig. 10A and B – polymetallic com pounds in rodingite from Nas³awice i.e. nickel sulphides with Fe and Pb traces (1), nickel ar se nates with Fe and Pb ad mix ture (2), Ni sulphides with Bi, Co and Pb (3, 4) (BSE im age)
Heflik and Natkaniec-Nowak (1989) thor oughly de scribed lenses of strongly and weakly al tered gab bro with rodingite in - clu sions. Green ish (light type) and grey (dark type) rodingites form spher i cal bod ies within the in tensely al tered gab bro. They show heteroblastic (grano-, poikiloblastic) and mas sive, lo cally rel ict tex ture. Rodingites are mainly com posed of gar net (grossu lar), which is intergrown with pyroxene crys tals (augi - te/di op side). The tex ture of these min eral inter growths is char - ac ter is tic of eutectic sys tems, de scribed e.g. from gab bro pegmatites (Heflik and ¯abiñski, 1970). Gar nets are the most prob a ble prod ucts formed as a re sult of garnetization of ba sic plagioclases, the main com po nents of protolithic gab broid. The main phases of this rock are ac com pa nied by elon gate crys tals of tremolite, lo cally form ing ra dial ag gre gates. Rodingite is in - ter sected with thin veins of prehnite and clinozoisite.
BRASZOWICE-BRZEZNICA SERPENTINITE MASSIF
Rodingite from serpentinites near Miko³ajów was first de - scribed by Gunia (1986a, b), even though many years be fore, Traube (1889) found grossular in this mas sif at the Mnich Hill.
The pos si bil ity of rodingite oc cur rences in this re gion was also con sid ered by Dziedzicowa (1979) and Jamrozik (1981).
Rodingites crop out in the up per part of the wall of the ser - pen tin ite quarry, on the south west ern slope of the Mnich Hill (Kozie Chrzepty). In strongly frac tured serpentinites, pink-grey mylonitized rodingite forms en claves, 3 ´ 0.4 m in size. Be - tween the rodingite and the ser pen tin ite, there is a chlorite con - tact rim of the “black-wall”. Lo cally, in the im me di ate prox im ity to the oc cur rences of rodingites, sin gle opal-chal ce dony veins can be ob served. Rodingites show grano-, porphiroblastic and mas - sive tex tures. Grossular ap pears as a main com po nent of these rocks, while di op side, chlorite and vesuvianite are sec ond ary phases. Gar nets reach sizes of up to 0.15 mm, and they are a lit tle bit larger (ca. 0.5 mm) only in the con tact zone with chlorite rocks. Sin gle chlorite crys tals oc cur also in the gar net ma trix of the rock. Di op side forms idiomorphic crys tals up to sev eral cm in size. Vesuvianite fills in ter stices in the grossular groundmass (Gunia, 1986a).
INTERPRETATION AND DISCUSSION
Rodingites from Lower Silesia seem to be sim i lar in form, tex ture, and min eral com po si tion to the other Ca-rich, SiO2- undersaturated rocks formed as a re sult of serpentinization (e.g., Sivell and Wa ter house, 1986; Kobayashi and Kaneda, 2010). They form veins (in the NW and E wall of the Jordanów Œl¹ski Quarry and the SE wall of the Nas³awice Quarry) or ir reg - u lar lenses (in the W and E walls of the aban doned Szklary mine). The larg est iso lated en clave of rodingite (2.5 ´ 3 m) was noted on the NW wall of the Jordanów Œl¹ski Quarry. Sim i larly, smaller en claves were ob served in the west ern part of the Szklary mine and on the west ern wall of the ser pen tin ite quarry near Miko³ajów.
All of them show com plex, heteroblastic (grano-, poikilo - blastic), mas sive, lo cally cataclastic or rel ict tex ture. They are com posed mainly of gar nets (grossular), py rox enes (augite/di - op side) and vesuvianite. Tremolite and Fe-rich chlorite are sec - ond ary phases. This min eral paragenesis is char ac ter is tic of a Ca-rich me dium ge net i cally re lated to ba sic magma (Gawe³, 1957; Heflik, 1967).
Rodingites from Nas³awice are en riched in polymetallic phases. Com pounds of Fe, Ni, and Co are as so ci ated with an
ultra mafic protolith, even though the pres ence of phos pho rus seems to be re lated to mafic rocks, as a max i mum amount of P2O5 is char ac ter is tic of gab bro magma. Cu and Ag com pounds are also typ i cal of a mafic protolith (gab bro, ba salt). It should be noted that in the vi cin ity of Nas³awice, in Pustków Wilczkowski, there are oc cur rences of Cu phos phates (tur quoise) (e.g., Heflik et al., 1976). Hence, it is as sumed that cop per com - pounds are quite wide spread in the rocks of the re gion and the pres ence of Cu must be as so ci ated with the host, ultra mafic and mafic rocks of Lower Silesia. How ever, Cu and Ag sul - phides could crys tal lise also dur ing the hy dro ther mal stage of magma dif fer en ti a tion at a much lower tem per a ture range.
Ga³uskin and Sze³êg (2003) sup pose that crystallisation of Cu-Ag min er als from sulphides be gins at 200°C, then, un der the low sul phur ac tiv ity, they are sub sti tuted by selenides and, fi nally, na tive Cu is sub sti tuted by ox ides, whereas Ag re mains in a na tive state.
Dur ing the hy dro ther mal stage, also Fe and Pb com pounds could crys tal lise. How ever, Zn, Pb, As and Bi com pounds are as so ci ated rather with acid pneumo-hy dro ther mal em a na tion.
Bis muth with cop per and nickel are fre quently in cor po rated into Pb-Ag com pounds. In rodingites from Nas³awice, Bi oc curs in ar se nates. Adu laria is also a hy dro ther mal prod uct.
Based on our stud ies and lit er a ture data (Dubinska et al., 2004), it was noted that rodingites from Nas³awice are en riched mainly in Ca and Mg, and show some con tents of Fe and Ti (Dubiñska et al., 2004), which sug gests that their or i gin could be re lated to a mafic protolith. The pres ence of main min eral phases, ac ces sory polymetallic com pounds of Fe, Ni, Co, Zn, Pb, Cu, Ag, As, Bi and P and the tex ture of these rocks could also sup port this the sis. It is as sumed that rodingites from the other oc cur rences in Lower Silesia could con tain sim i lar poly - metallic com pounds (e.g., Gunia, 1986b, noted the pres ence of cop per in rodingites from the Braszowice-BrzeŸnica Mas sif).
Lis and Sylwestrzak (1981) noted that peg ma tite- pneuma - tolitic prod ucts af fected the leucocratic zone within the serpen - tinites of the Nas³awice Hills. In the Jordanów Œl¹ski Quarry, they found pegmatites and aplites. The peg ma tite was com - posed of al bite, quartz, mus co vite, K-feld spar, beryl, gar net (almandine–grossular), tour ma line (dravite), gahnite, colum - bite, flu o rite, zir con and cas sit er ite, whereas the aplite con - tained quartz, K-feld spar, plagioclase, bi o tite, beryl and gar nets (almandine–spessartine). The rocks with such min eral para - genesis were also found within the ad ja cent granitoids of the Strzegom-Sobótka Mas sif. Thus, aplites and pegmatites from Nas³awice could be ge net i cally as so ci ated with granitoides of this mas sif. Sim i larly, in Szklary near the oc cur rences of rodingite, pegmatites with gem qual ity tour ma line crys tals are found (Pieczka, 1987). Sachanbiñski et al. (2000) as so ci ated them with acidic rocks of the Strzegom-Sobótka Mas sif. How - ever, based on new SHRIMP zir con age, Kryza (2011) sug - gested that aplites and pegmatites from these mas sifs show sim i lar age as granitoids from the Niemcza Shear Zone, dated at 338 +2/–3 Ma.
CONCLUDING REMARKS
In Nas³awice, the mafic protolith is rep re sented by fine- grained gab bro. This rock ex hib its dif fer ent tex ture than gab bro from the Sobótka re gion (e.g., diallage gab bro in the up per part of Œlê¿a Mt.). It forms an in tru sion re sem bling a dyke. It is as - sumed that these rocks are ge net i cally re lated to the ophiolite suites of the Góry Sowie Block. How ever, it is not clear which mag matic stage of the ophiolitic sys tem the dykes are as so ci -
ated with. Ac cord ing to the se quence of the Troodos Ophiolite in Cy prus (Varga and Moores, 1985), the fine-grained gab bro from Nas³a wice most prob a bly be longs to the sheeted dyke com plex, which in Troodos is built mainly of diabases that ex pe - ri enced greenschist- or am phi bo lite-fa cies al ter ation. The thick - ness of these dykes ranges from 0.5 to 5.0 m with 0.3–3.0 m in length. The fine-grained gab bro from Nas³awice is prob a bly ge - net i cally as so ci ated with orthoamphibolites from Sobótka, which could orig i nate from the al ter ation of diabase un der am - phi bo lite-fa cies con di tions.
To sum up, the rodingites oc cur ring around the Góry Sowie Block are re lated to a mafic protolith (fine-grained gab bro). Dur - ing the for ma tion of rodingites and other co-ex ist ing leucocratic rocks (Heflik, 1967), pneumo-hydrotermal post-gra nitic prod - ucts, as so ci ated with acidic rocks of the Strzegom-Sobótka Mas sif or the Niemcza Shear Zone, played a neg li gi ble role.
Rodingites from Lower Silesia re sem ble the rocks from New Zea land de scribed by O’Brien and Rodgers (1973), Leach and
Rodgers (1978) and Sivell and Wa ter house (1986), as well as those found in the Sartuohai chro mium de posit in China (Koba - yashi and Kaneda, 2010).
The au thors of this pa per sup pose that the rodingites from the Sudetic ser pen tin ite mas sifs share a com mon or i gin, and the vari abil ity be tween them could re sult only from lo cal events.
More over, the prob lem of gen e sis of these in ter est ing dec o ra - tive rocks is still open. Nev er the less, the au thors hope that the in ves ti ga tions pre sented herein will be fruit ful to the dis cus sion of rodingites from Lower Silesia.
Ac knowl edge ments. A. Gawe³ is grate fully ac knowl edged for his as sis tance with the scan ning elec tron mi cro scope and mi cro Raman spec tros copy. The re view ers made help ful and con struc tive com ments on the manu script. This work was fi nan - cially sup ported by AGH Uni ver sity of Sci ence and Tech nol ogy, the stat u tory grant No. 11.11.140.319.
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