New mag netic anom a lies of the Outer Capathians in NE Slovakia and their re la tion ship to the Carpathian Con duc tiv ity Zone
Ľudovít KUCHARIČ1, *, Vladimír BEZÁK2, Pe ter KUBEŠ1, Vlastimil KONEČNÝ1 and Ján VOZÁR2
1 State Geo log i cal In sti tute of Dionýz Štúr, Bratislava, Mlynská dol ina 1, 817 04 Bratislava, Slovakia
2 Geo phys i cal In sti tute of the Slo vak Acad emy of Sci ences, Dúbravská cesta 9, 845 28 Bratislava, Slovakia
Kucharič Ľ., Bezák V., Kubeš P., Konečný V. and Vozár J. (2013) New mag netic anom a lies of the Outer Capathians in NE Slovakia and their re la tion ship to the Carpathian Con duc tiv ity Zone. Geo log i cal Quar terly, 57 (1): 123–134, doi:
10.7306/gq.1079
Hith erto un known mag netic anom a lies have been de tected while as sem bling a mag netic pic ture of the Slovakian ter ri tory.
An im pres sive mag netic anom aly was rec og nized in the northeasternmost part of Slovakia as so ci ated with sed i men tary rocks of the flysch belt. This is a rare phe nom e non, be cause the flysch se quence in Slovakia typ i cally lacks mag netic rocks.
Thus, an ig ne ous body in truded into the flysch might cause the anom aly. The shape and the char ac ter of the anom a lous body sug gests that its source is lo cated at shal low depth be neath the sur face. The anom aly has been mod elled in 2D space. It is in ter preted as a Neo gene vol ca nic neck made of in ter me di ate rocks. Such an in ter pre ta tion is sup ported by re sults of ther - mo met ric in ves ti ga tion of fluid in clu sions, vitrinite reflectance and fis sion tracks. Fur ther mi nor anom a lies within this area, might also be caused by small near these subvolcanic bod ies. The Carpathian Con duc tiv ity Zone is lo cated near these new ob served mag netic anom a lies, which there fore pro vide a new view on the im por tance of this zone. The re gion as a re sult may have po ten tial for metalogenesis, un der ground stor age of car bon di ox ide, and hy dro car bons.
Key words: West ern Carpathians, flysch belt, mag netic anom a lies, Neo gene subvolcanic bod ies, Carpathian Con duc tiv ity Zone.
INTRODUCTION
The West ern Carpathians rep re sent a com pli cated moun - tains range, which con sists of var i ous tec tonic units and blocks (e.g., Bezák et al., 2011). The ba sic par ti tion into Outer and In - ner Carpathians re flects Neoalpine tec tonic evo lu tion dur ing the Neo gene when the col li sion of the In ner Carpathian Block with the Eu ro pean Plat form formed the Outer Carpathian Flysch Belt. The Pieniny Klippen Belt (PKB) makes up the bound ary be tween the Outer and In ner Carpathians.
The In ner West ern Carpathians rep re sent a Palaeoalpine (Cre ta ceous) nappe sys tem of Pa leo zoic and Me so zoic rock com plexes and su per im posed youn ger sed i men tary de pos its and large Neo gene vol ca nic fields. The Outer Carpathians rep - re sent a Neoalpine (mostly Neo gene) nappe sys tem of Ju ras - sic–Paleogene flysch de pos its where Neo gene vol ca nic rocks are rare. There are sep a rate in tru sive bod ies such as dikes, sills, and laccoliths ex tend ing from Moravia (Krejčí and Poul, 2010) to south ern Po land in the Pieniny area (Birkenmajer et al., 2004; Birkenmajer and Lorenz, 2008) and con tin u ing to Ukraine and Ro ma nia (Pécskay et al., 2009; Fig. 1). Mišík (1992) de scribed mul ti ple small oc cur rences of in ter me di ary
Neo gene vol ca nic rocks (dykes) in the west ern and the east ern part of the PKB. Be sides this, there are lo cal oc cur rences of Ju - ras sic-Cre ta ceous vol ca nic rocks (e.g., Golonka, 2004).
Se quences of Carpathian flysch (Slovakian part) have for de - cades been con sid ered as rock successsions with out any sig nif i - cant mag netic prop er ties cre at ing mo not o nous and smooth pic - tures of the Earth mag netic field ob served above ar eas where these rocks are de vel oped (Ondra and Hanák, 1989). From the geomorphological point of view, the area is lo cated in the Bukovské vrchy hills, very close to state bound aries with Po land and Ukraine (Fig. 2). New mag netic mea sure ments have been car ried out in the last few years (Kubeš et al., 2008) in the area sit u ated within the Dukla Unit of the Outer Carpathian Flysch Belt in NE Slovakia. The re sults of these mea sure ments re vealed some in ter est ing new fea tures of the Earth’s mag netic field which are not typ i cal for the flysch rocks. Part of the mag netic map of NE Slovakia (Kubeš et al., 2008) is shown in Fig ure 3. The map is mainly char ac ter ized by a typ i cal of low in ten sity mag netic field.
The only ex cep tions are in the east ern most part of Slovakia, where one may dis tin guish an im pres sive neg a tive anom aly that is al most con cen tric in shape and two di min u tive pos i tive anom a - lies (more ex ten sive anom a lies lo cated in the S and SE part of the pic ture re lated to Neo gene vol ca nic rocks on the sur face within the In ner Carpathians).
On cur rent knowl edge this mag netic anom a lies can not be to as signed to any lithostratigraphical mem ber of the flysch se - quence. The larg est anom aly of this area (the neg a tive one) has been mod elled in 2D space.
* Corresponding author: ludovit.kucharic@geology.sk Received: February 1, 2012; accepted: November 6, 2012; first published online: March 15, 2013
The re sults show, that a rock body, which is not a strati - graphic mem ber of the flysch se quence, may be the source of the mag netic anom aly. This rock body is more consistent with a dis cor dant hypa bys sal vol ca nic body. In this pa per we pro vide a model of the geo log i cal body that might be re lated to this un - usual mag netic anom aly, and high light the im pli ca tions of this model for better un der stand ing of the evo lu tion of the Outer Carpathian realm.
GEOLOGICAL SETTING
The prin ci pal tec tonic di vi sion of the West ern Carpathians into Outer and In ner ones (e.g., Bezák et al., 2004) is based on ef fects of the last im por tant tec tonic ac tiv ity dur ing the Neo - gene. A sub stan tial vol ume of the crust in the In ner West ern Carpathians is formed by Hercynian crys tal line com plexes, which are com po nents of Palaeoalpine tec tonic units: Tatricum, Veporicum, Gemericum (e.g., Bielik et al., 2004). The con fig u -
ra tion of Palaeoalpine struc ture of the In ner Carpathians is sup - ple mented by su per fi cial nappes, com posed mostly of Me so - zoic, per haps even of Up per Pa leo zoic, rock se quences (e.g., Plašienka et al., 1997).
The Paleogene and Neo gene sed i men tary infill of bas ins su per im posed on the Al pine thrust-fold belts (Tari and Horváth, 2006) and the Neo gene vol ca nic rocks in the In ner Carpathians rep re sent suc ces sions formed af ter em place ment of the In ner Carpathian Palaeoalpine nappes. Ba sin for ma tion as well as the vol ca nic ac tiv ity was con nected with the youn gest tec tonic de vel op ment of the In ner West ern Carpathians (asthenolite as - cent, thin ning of crust, ac ti va tion of faults and in creas ing heat flow). The de vel op ment of Neo gene vol ca nism in time and space has been widely de scribed (e.g., Csontos et al., 1992;
Lexa and Konečný, 1998; Konečný et al., 2002; Pécskay et al., 2009).
The Outer Carpathians are com posed of a stack of nappe sheets ex tend ing along the Carpathian arc, which may be up to six kilo metres thick. There are sev eral opin ions as to the dis - Fig. 1. Po si tion of the Carpathian Con duc tiv ity Zone and oc cur rences of Neo gene vol ca nic bod ies and in ter preted subvolcanic
bod ies in the Outer Carpathians (geo log i cal scheme based on Biely et al., 1996; Lexa et al., 2000)
tance of thrust ing of the Outer Carpathians nappes over the south ern part of the North Eu ro pean Plate (e.g., over 70 km, Golonka et al., 2005). The lat est pa per ana lys ing these prob - lems is Gągała et al. (2012). These nappes be came de tached from the base ment dur ing overthrusting. Behrmann et al.
(2000) con cluded about 260 km short en ing in the NE Outer Carpathians. The nappe suc ces sion from high est to low est ones com prises Magura Nappe, Fore-Magura group of nappes, Silesian Nappe, Subsilesian Nappe, and Skole Nappe.
The Outer Carpathian nappes are cut by sev eral ma jor faults of dif fer ent or i gin. The last tec tonic phase that af fected the Outer Carpathians took place in the Mio cene. The tec tonic mo bil ity in this pe riod oc curred dur ing col li sion be tween the over rid ing ALCAPA Block and the North Eu ro pean Plate (Cieszkowski, 2003).
There are two nappes of the Outer Carpathians Flysch Belt de vel oped in NE Slovakia: the Magura Nappe and the Dukla Nappe. The Magura Nappe sys tem is the larg est tec tonic unit of the West ern Carpathians and con sists of sev eral nappes (from
the south to the north): the Krynica Nappe, the Bystrica Nappe and the Rača Nappe (Ślączka et al., 2006).
The Dukla Nappe emerges from be neath the Fore-Magura nappes (Ślączka, 1970). Bore holes (Smilno-1 and Zboj-1) show, that these nappes ex tend be neath the Magura Nappe far to the south (Ďurkovič et al., 1982; Leško et al., 1987). The area of our in ves ti ga tion is en tirely lo cated within the Dukla Nappe that con - tains in this area the Sub-Menilite, Cisna and Łupków beds.
RESULTS OF PREVIOUS WORK
A gen er al ized geo log i cal map of the study area, based on Lexa et al. (2000), is shown on the Fig ure 2.
More de tail ap pears on the 1:50 000 geo log i cal map of this part of the flysch belt in (Koráb, 1983). The map cov ers a more ex ten sive re gion than that of the anom aly and con tains no re - cords of about oc cur rences of mag netic min er als or rocks. In Fig. 2. Geo log i cal map of the east ern part of Slovakia (based on Lexa et al., 2000)
the geo log i cal cross-sec tion of this area (Koráb, 1983) the Sub-Menilite Beds and Cisna Beds cre ate a synclinal struc ture on the Łupków Beds (cf. Fig. 5). At this lo cal ity, that re gional strike of beds (NW–SE) is in this part of the flysch belt changes al most into a N–S di rec tion.
Fur ther knowl edge has been gained from the deep bore - hole Zboj-1, drilled not far from this anom aly (Ďurkovič et al., 1982), at a time when the mag netic anom aly was un known. The bore hole was sited ap prox i mately 6 km SW of the anom aly in the Zboj Spring Val ley (see Fig. 4) within the Dukla Unit. Data from this bore hole, of fi nal depth 5002 m, were used in mag - netic anom aly in ter pre ta tion. The bore hole pen e trated the fol - low ing units (Ta ble 1).
The up per 3800 m were within the Dukla Unit. The Zboj Beds found be low this level com pare with the Obidowa–Slopnice Unit (Ďurkovič et al., 1982), but these beds might also rep re sent the in ner most part of the Silesian Unit (Ślączka et al., 2006).
The bore hole was eval u ated not only as re gards li thol ogy and struc ture but also in terms of hydrogeology and hy dro car -
bon oc cur rences. No ta bly, there is a po ten tial for hy dro car bons (meth ane; Rudinec, 1989). Re sults of drill core log ging and tem per a ture mea sure ments, were later in cluded into the At las of Geo ther mal En ergy of Slovakia (Franko et al., 1995).
This part of the Outer Carpathian Flysch Belt has lately been in ves ti gated re gard ing hy dro car bon po ten tial (Hrušecký et al., 2003), us ing a va ri ety of meth ods. Vitrinite reflectance, fis sion track and fluid in clu sion data from near the Zboj-1 bore hole as well as from the bore hole core have shown that this area was af - fected by in creas ing tem per a ture dur ing the Neo gene.
The first mag netic mea sure ments in this area de rive from syn op tic air borne map ping of for mer Czecho slo va kia 1:200 000 at scale, mag netic and ra dio met ric mea sure ments, 2 km flightline spac ing. The re sults com prise 1: 200 000 aero mag net ic maps (Mašín, 1963). The mag netic mea sure ments were car ried out with low ac cu racy (±25 nT) and there fore in ter pre ta tion of the mag netic field within ar eas of nar row vari a tion in am pli tude is prob lem atic.
Fig. 3. Mag netic map of the NE part of Slovakia (ac cord ing to Kubeš et al., 2008)
The east ern part of the flysch belt in Slovakia has been sub - ject of hy dro car bon pros pect ing in the sec ond half of 20th cen - tury, mostly us ing seis mic re frac tion and re flec tion sur vey ing.
Eval u a tions of seis mic in ves ti ga tion within this area are given by Mořkovský et al. (1992) and Gągała et al. (2012). How ever, these pro files are not re li able for in ter pre ta tion, be cause they ended in the area and there fore are af fected by tech ni cal prob - lems in sig nal pro cess ing. Magnetotelluric mea sure ments are sit u ated out side of this lo cal ity (Ryłko and Tomaś, 1995;
Stefaniuk, 2006). How ever, for de cades this area has been known to pos sess im por tant re gional (Carpathian) geo phys i cal anom a lies: an axis anom aly of the Carpathian Con duc tiv ity Zone – CCZ (e.g., Berdichevski and Dmitriev, 1976; Červ et al., 1984) and the south ern edge of the Carpathian Grav ity Low Zone (Tomek et al., 1979; Bielik, 1998). The sit u a tion of the lo -
cal ity with the mag netic anom a lies and with these re gional anom a lies is shown in Fig ure 4.
The mag netic anom aly source map of the Carpathian–Pan - nonian re gion dis tin guishes the fol low ing mag netic sources (Pospíšil and Ádám, 2006): (a) sources of plat form or i gin, (b) Neo gene vol ca nic rocks, (c) Al pine and Neo gene sources.
Each of these sources is char ac ter ized by a typ i cal con fig u ra - tion of mag netic field. The out crop of the Magura and Dukla nappes on the mag netic map show anom a lies char ac ter is tic of plat form and Al pine Paleogene sources that oc cur out side of Slovakia. This is rep re sented by an ex ten sive mag netic anom - aly de tected south of Dukla vil lage (Po land) where the Rača, Dukla and Silesian nappes are pres ent at the sur face (Woźnicki and Šucha in Poprawa and Nemčok, 1988–1989).
Fig. 4. The mag netic anom a lies of the area stud ied and the Carpathian geo phys i cal anom a lies
Depth [m] The rock com plex
0–300 SUB-MENILITE BEDS – sandy gray and green-gray non-cal car e ous or weak cal car e ous claystones al ter nat ing with mica silts (age: Paleocene)
300–800 CISNA BEDS – de vel oped as typ i cal flysch se quence; the share of sand stones is from 30–80%, beds are only slightly tec toni cally de formed (age: Paleocene).
800–3800 ŁUPKÓW BEDS – claystones-sandy flysch; the ra tio claystones: sand stones is 4:1; the col our of claystones is dark grey; cal car e ous share in sand stones is very vari able 1.4–35.7% (age: Cre ta ceous–Paleogene)
3800–5002 ZBOJ BEDS – main lithotype the mas sive sand stones with ho mo ge neous tex ture (the con tent of SiO2 is 53–89%); the top of beds is tec tonic de com posed (age: Up per Eocene to Lower Oligocene?)
T a b l e 1 The sim pli fied geo log i cal pro file of the bore hole Zboj-1 (mod i fied af ter Ďurkovič et al., 1982)
New ad di tional mag netic mea sure ments have been car ried out in the last years (Kubeš et al., 2008), by ground ap pli ca tion of pro ton mag netom etry with a den sity of 1–3 points/km2 (Kubeš et al., 2008). The ac cu racy of these mea sure ments en - ables com pi la tion of a mag netic map with isolines at 10 nT in - ter vals. The den sity of the mea sure ments is suf fi cient for a con - struc tion of a map at the scale of 1:50 000. All mea sure ments were re duced to the nor mal mag netic field (IGRF 1995 – In ter - na tional Geo mag netic Ref er ence Field). Thus, a com pre hen - sive da ta base of mag netic anom a lies DT has been pro duced, which is the ba sis for the new mag netic map of the Slo vak Re - pub lic. Geo log i cal in ter pre ta tion of this mag netic map is given in Kubeš et al. (2010).
GEOPHYSICAL 2D MODELLING
The anom aly un der dis cus sion on the mag netic map of Slovakia (Kubeš et al., 2010) is char ac ter ized by neg a tive am - pli tude, which reaches a value al most 100 nT (see Figs. 3 and 4). The anom aly pos sesses an ap prox i mately con cen tric shape and rel a tively steep mag netic gra di ent. No signs of mag - netic rocks have been re corded at the sur face in that area, which top o graph i cally com prises a de pres sion (see Fig. 4).
The neg a tive mag netic anom aly was mod elled us ing OASIS MONTAJ soft ware in 2D space. We have used only the mag netic part of this code, be cause grav ity mod el ling in such an area of fers many in ter pre ta tions. Grav ity maps for dif fer ent vol ume den si ties and with dif fer ent fil ters have been pro cessed from the grav ity field but with out con clu sive re sults. The mag - netic mod el ling though is more ob jec tive, due to the nar rower scale of in her ence of mag netic rocks. Be cause spe cific mag - netic data of the in ferred anom aly – pro duc ing body was not avail able, we used in di rect in for ma tion from pre vi ous work. Ev i - dence of a ther mal event dated to Neo gene (Hrušecký et al., 2003) sug gest the source of this anom aly may be mag matic.
The shape of this anom a lous field ex cludes to con sider pres - ence of a mag netic ob ject of sed i men tary or i gin, while the gra di - ent of the anom aly ex cludes the pres ence of mag netic rock on the sur face. A typ i cal fea ture of Neo gene vol ca nic rocks in Slovakia is mul ti ple al ter na tion of mag netic field po lar ity and many rocks bod ies (mostly andesites) are ex pressed in a mag - netic field by neg a tive anom a lies (Filo et al., 2003). Ther mal remanent mag netic polar is ation, which is char ac ter is tic of ig ne - ous rocks, can pro duce a re versed mag netic field – hence we uti lized remanent mag ne ti za tion when mod el ling. Mod el ling was un der taken de spite good co in ci dence be tween the ob - served and cal cu lated curves af ter a tech ni cal in ter pre ta tion (Fig. 5). It was im por tant to clar ify the or i gin of the mag netic anom aly and to in te grate the in ter preted geo log i cal cause of the anom aly into its lithological and struc tural con text in the area. In the terms of our pre vi ous in ter pre ta tion (Kubeš et al., 2010) we were able to as sign al most all mag netic anom a lies from the West ern Carpathian area to an ap pro pri ate geo log i cal unit. The pat tern of the mag netic anom aly and sur round ing mag netic field in di cates that the body re spon si ble for the anom aly did not reach ground the sur face. In plan the anom aly is al most cir cu - lar. Miss ing pos i tive val ues of the mag netic field in di cated, sug - gest that rocks with remanent mag netic po lar iza tion cre ated that anom aly. In the West ern Carpathians area (Kubeš et al., 2010), such mag ne ti za tion is typ i cal of youn ger Ce no zoic mag - matic rocks (flysch rocks also pos sess remanent mag ne ti za tion but usu ally of very low in ten sity). Hence the fi nal geo phys i cal model took the form of a tube of di am e ter around 2 km, dip ping to the NE. Our in ter pre ta tion con tains am bi gu ities re gard ing the
depth, thick ness and pre cise mag netic prop er ties of the dis turb - ing body. It is clear, though, that the shape and the in cli na tion of anom a lous body is dis cor dant to the flysch strata (as sum ing a mag netic sus cep ti bil ity of around 1000 ´ 10–6 [cgs units]). The anom a lous body there fore may rep re sent a subvolcanic neck of in ter me di ary com po si tion of Mio cene age, with in flu ence of thermoviscous po lar ity. A geo log i cal cross-sec tion adopted from older data (Koráb, 1983) us ing the re sults of 2D mag netic mod el ling is shown in Fig ure 5.
Two other anom a lies have been rec og nized in this area.
Both are sit u ated to the SW of the main one on the op po site side of the CCZ (see Fig. 4) near the vil lages of Stakčínska Roztoka and Ulič. They show sim i lar fea tures: small rel a tive pos i tive am pli tudes of mag netic field (20–30 nT) and lin ear shapes lo cated in val leys. The 2D shapes of the anom a lies, sug gest thin dykes of in ter me di ate com po si tion. The top of the bod ies lie closer to the sur face and we in fer that the val leys were es tab lished along fault zones that fa cil i tated magma as - cent to wards the sur face.
GEOLOGICAL INTERPRETATION
The prin ci pal out puts of 2D mag netic mod el ling for geo log i - cal in ter pre ta tion are as fol lows:
– the anom aly is caused by a cy lin dri cal body with a width of al most 2 km in clined to the north-east;
– the roof of the anom a lous body is sit u ated at a depth of about 1 km and its sur face is al most subhorizontal;
– mod el ling used remanent mag netic po lar iza tion.
The anom a lous body may rep re sent a subvolcanic neck (Fig. 5).
The pres ence of a pos si ble subvolcanic body is sup ported by : – Small Neo gene hypa bys sal calc-al ka line andesitic dykes and sills have been ob served be tween Szczawnica and Czorsztyn in the Pieniny area of Po land along and less than 4 km from (Birkenmajer et al., 2004).
The an de site bod ies are lo cated in the Outer Flysch in the Magura Unit and Birkenmajer et al. (2004), Trua et al. (2006) in ferred a large mag matic cham ber at depths of about 10–15 km, as so ci at ing them with subduction.
Hy dro ther mal al ter ation and ore min er al iza tion have been ob served in side the an de site bod ies as well as in the ad ja cent ar eas. The ra dio met ric age range of these rocks has been de ter mined as 10.8–13.3 Ma (Pécskay et al., 2006).
– Sim i larly a clus ter of shoshonitic bas alts and andesites is de vel oped in the form of small ir reg u lar bod ies within the Beloveža Beds in the west ern part of the flysch belt around Bojkovice town ship and Bánov (Bielokarpatská Unit) in the Czech Re pub lic (see Fig.1). Krejčí and Poul (2010) gave the new est data from this area. In ten sive al - tered rocks were emplaced along the faults ac tive in the Mid dle Mio cene. The bod ies are 10–15 km from the Klippen Belt. Their ra dio met ric age range has been de - ter mined as 11.0–13.5 Ma (Pécskay et al., 2006), the same age as the vol ca nic rocks in the Pieniny area.
– At both lo cal i ties vol ca nic rocks are de vel oped along the axis of the Carpathian Con duc tiv ity Zone (CCZ) – the zone of zero value of Wiese´s vec tor (Fig. 1).
– The lo cal ity stud ied here lies in a sim i lar po si tion. The CCZ is sit u ated very close to the south ern mar gin of the mag netic anom aly. The dis tance of the anom aly from the PKB is around 25–30 km. This means that the CCZ
is a con trol ling fea ture for vol ca nic bod ies sit u ated north of the Klippen Belt. This ob ser va tion sug gests that the re la tion of the CCZ and the PKB may be re con sid ered.
Other fea tures sup port in ter pre ta tion of subvolcanic bod ies:
– The At las of geo ther mal en ergy of Slovakia (Franko et al., 1995) shows this area a tem per a ture at the depth of 1000 m on the level of 50°C. This value is sim i lar to those in sub stan tial parts of the Dan ube Ba sin and the East Slovakia Ba sin (re sults from the Zboj-1 bore hole;
Ďurkovič et al., 1982). Our in ter pre ta tion in di cates that the up per edge of mag netic body lies ap prox i mately at that level. The lower lev els of the bore hole Zboj-1 do not show anom a lous val ues of tem per a ture, con sis tent with our in ter pre ta tion of an anom a lous body dip ping to the NE (see Fig. 5).
– Rock sam ples col lected from the sur face near the Zboj-1 bore hole (Hrušecký et al., 2003) and from the core bore hole show vitrinite reflectance (Rr) val ues that are the high est in the Dukla Unit in Slovakia. Nor mal val - ues are be tween 0.48–0.59%, while reflectance val ues at the sur face close to the Zboj-1 bore hole are 1.23–1.49%, and in the Zboj-1 bore hole at a depth of 1105 m they are 1.62–1.67%. These re sults in di cate that these rocks were meta mor phosed to al most 200°C.
The vitrinite reflectance val ues sug gest an age in ter val of 10–20 Ma for this (Kotulová in Hrušecký et al., 2003).
These tem per a ture changes did not take place dur ing ba sin for ma tion or dur ing tec tonic ac tiv ity (ibid).
– Fis sion track dat ing on de tri tal apatites has also been car ried out in that area giv ing re sults sug gest ing ages within the Sarmatian or the Sarmatian–Mid dle Pannonian, the age range of 9.9–17.2 Ma (Hrušecký et al., 2003) see Ta ble 2.
– Ther mo met ric anal y sis of the fluid in clu sions has been car ried out on the sur face sam ples near the Zboj-1 bore - hole. The re sults ob tained sug gest that flu ids within joints were com posed of var i ous pro por tions of wa ter, crude oil, gas o line, meth ane and car bon di ox ide with tem per a tures of 130–220°C. This value is con sis tent with those from vitrinite reflectance of 128–178°C. The pres sure of flu ids as sessed on the base of micrometric study fluc tu ated from 1093 to 3694 bars. This pres sure con sid er ably ex ceeds the lithostatic pres sure which re - sulted in joint for ma tion (Hrušecký et al., 2003). Com par - ing the pla nar shape of the anom aly and the re lief of the ter rain (see Fig. 4) sug gests that the ridge of the Bukovské vrchy Mts. (Paleogene), ly ing al most N–S, has been “pushed” to the west at the mar gin of the Fig. 5. 2D mag netic mod el ling and geo log i cal in ter pre ta tion of mag netic data
anom aly as a con se quence of the Neo gene in tru sion.
The ridge of the Bukovské vrchy Mts. is cre ated by rigid sand stones of the Cisna Beds, while the in ferred in tru - sion stopped its as cent in the soft clay se quence of the Łupków Beds. A com bi na tion these lithological fea tures and tec tonic and ex og e nous pro cesses shaped the re - lief of the field into the form seen to day.
– These fac tors com bined with mod el ling of the mag netic anom aly, sug gests that the prob a ble source of the mag - netic anom aly is a subvolcanic body of diorite por phyry which in truded into this area dur ing the Sarmatian. Plac - ing the in ferred body into the con text of young Carpathians vol ca nic rocks, fol low ing Pécskay et al.
(2006), this anom aly might be re lated to mafic to calc-al - ka line rocks (in tru sions), age of range be tween 10–14 Ma, sim i larly to the vol ca nic rocks ob served in east ern Moravia, the Pieniny Mts., the Slánske vrchy Mts., the Vihorlat Mts. and the Gutin Range in Ukraine.
DISCUSSION
The PKB ba sin closed at the Cre ta ceous/Paleogene tran si - tion as an ef fect of strong Late Cre ta ceous (Subhercynian and Laramian) thrust fold ing. The last im por tant events in the PKB were the Neo gene transpression and Sarmatian vol ca nism rep - re sented by an de site dykes and sills, which cut mainly Paleogene flysch (Magura Nappe) and formed the so-called Pieniny Andesitic Line (Krobicki et al., 2003). We may con clude that Sarmathian vol ca nism cut the Dukla Nappe as well.
How ever, Ju ras sic and Cre ta ceous vol ca nic rocks are also pres ent within the Outer Carpathians of Transcarpathian Ukraine and in the Silesian or Subsilesian nappes within the Pol ish–Czech bor der re gion and in Żegocina SW from Kraków (Golonka, 2004; Krobicki et al., 2004). Such vol ca nic rocks, though, are un likely to lie within the area un der study. The roof of the in ter preted anom aly is at the depth of ap prox i mately 1000 m and even if we will con sider the Zboj Beds (from the Zboj-1 bore hole) as a part of the Silesian Nappe, their depth (3800 m) is too great to cause the mag netic anom aly rec og - nized. Fur ther more, an ex is tence of vol ca nic rocks older than Mio cene (Ju ras sic and Cre ta ceous) could not have di rectly in - flu enced of the Paleogene en vi ron ment.
Al though the oc cur rence of in tru sive rocks in front of the PKB are rare, our in ves ti ga tion sug gests that such ob jects may
ex ist in the subsurface. Birkenmajer et al. (2004) interpered this event as a com po nent of melange of the Outer Carpathians.
The Pieniny Mts. andesites, which oc cur at or near to the Outer/In ner Carpathian tec tonic junc tion, find their equiv a lents in the west in the Moravian Carpathians and, in the east, in Transcarpathian Ukraine, the Vihorlat Mts., Gutai (Baia Mare re gion, NW Ro ma nia), and as a subvolcanic unit at Toroiaga, Radna and Borgon (NW Ro ma nia). The an de site in tru sions at these lo ca tions be long to the out er most (north ern most) post-collisional late Mid dle Mio cene (Sarmatian) vol ca nic arc of the West Carpathian orog eny that is some 400 km long – the Pieniny Vol ca nic Arc (Birkenmajer et al., 2004).
Ma jor and trace el e ments chem is try of the in tru sive rocks in di cate subduction-re lated magma sources, as in vol ca nic rocks of the Carpathians. The three in tru sive phases dis tin - guished within the in ter val have been dated as 14.76 ± 1.18 Ma to 11.04 ± 1.21 Ma (with eastwards age mi gra tion along the Carpathian arc; Pécskay et al., 2006).
In tru sive ac tiv ity con tin ued in Ro ma nia to 11.5–8.0 Ma (Pécskay et al., 2009), clearly in di cat ing mi gra tion of the subduction zone from west to east. This is a sim i lar trend of mi - gra tion of the in tru sive ac tiv ity as in vol ca nic ac tiv ity in the main vol ca nic chain.
The in tru sive rocks are gen er ally af fected by postmagmatic al ter ation. The bo ron geo chem is try of the an de site in tru sions is typ i cal of subduction re lated calc-al ka line rocks. Subduction flu - ids un der the Moravian and the Toroiaga re gions (Ro ma nia) prob a bly orig i nated from the crust, while in the Pieniny they de - rived from subducted flysch de pos its (Gmélin et al., 2007).
How ever, ac cord ing to Jurewicz and Nejbert (2005) the geotectonic po si tion of the Pieniny andesites sug gests con nec - tiv ity with deep crust faults rather than with pro cesses of subduction.
Re gard ing the oblique course of Neoalpine col li sion and the grad ual mi gra tion of the subduction zone along the Carpathian arc to the east and to the south-east it is highly prob a ble, that in - di vid ual vol ca nic cen tres formed in dif fer ent geotectonic en vi - ron ments (Lexa and Konečný, 1998). These au thors have clas - si fied the West ern Carpathians volcanics into two groups: the first one linked to a subduction zone (east Slovakia) and the sec ond is re lated at the asthenolite as cent and ex ten sion pro - cesses (cen tral Slovakia). The prov e nance of vol ca nic bod ies at the tail of the subduction zone is pos si ble to ex plain ei ther with con tin u ing ex ten sion af ter re gres sion/mi gra tion of the subduction zone to the south-east, or via faults sys tems that orig i nated ear lier above the subduction zone. This lat ter seems to more fea si ble be cause the subduction zone than was else - where with a dif fer ent ori en ta tion.
Be sides the main mag netic anom aly in ques tion, small pos i - tive anom a lies to the south sug gest that the pres ence of ig ne - ous rocks be hind the PKB lo cally (e.g., the Morské Oko vol cano in the Vihorlat Mts.) is in a sim i lar set ting.
THE RELATIONSHIP BETWEEN CARPATHIAN CONDUCTIVITY ZONE AND THE PIENINY KLIPPEN
BELT AND MAGNETIC ANOMALIES
Sev eral fac tors need to be taken into con sid er ation in interpretating the Neo gene vol ca nic bod ies that lie within the zone of the PKB and be hind this zone in the flysch belt. The PKB is mostly re garded as rep re sent ing the sur face of the Eu - Geo log i cal unit Num ber of
sam ples Min.age
[Ma] Max.age
[Ma]
Transcarpathian
De pres sion 4 13.9 24.8
In ner Carpathian
Paleogene 18 23.3 36.9
Klippen Belt 1 12.3 –
Krynica Unit 16 12.0 28.7
Rača Unit 16 14.5 25.0
Dukla Unit 9 9.9 17.2
T a b l e 2 Dis per sion of fis sion track dat ing in sed i ments (ap a tite)
the geo log i cal units of the east Slovakia (af ter Hrušecký et al., 2003)
ro pean Plat form mar gin, and hence the bound ary of subduction dur ing Neoalpine oro gen esis (e.g., Oszczypko et al., 2002).
The po si tion of known and in ter preted vol ca nic rocks in re la - tion to the CCZ is de picted in Fig ure 6. How ever, the depth of CCZ is greater than the depth of the ig ne ous bod ies. In our in - ter pre ta tion this zone rep re sents a deep-seated fault sys tem, along which magma in truded into the flysch de pos its.
The course of the CCZ has been us ing magnetotelluric mea sure ments along the whole Carpathian arch from the Vi - enna Ba sin to Ro ma nia (Berdichevski and Dmitriev, 1976; Červ et al., 1984; Stanica et al., 1999; Ádám, 2001; Hvožďara and Vozár, 2004). Most of these au thors agree that this is a deep-seated fault zone, which en abled flux of heat and of ten of min er al ized flu ids from the man tle. These flu ids were en riched in CO2 and CO, re duc tion of which pro duced car bon films in the rock. This zone is de tected at depths of 5–25 km, as part of the crust com pris ing crys tal line blocks. Its man i fes ta tion in the con - duc tive sed i men tary unit of the flysch rocks is prac ti cally neg li gi - ble (Hvožďara and Vozár, 2004). The or i gin of such a re mark - able large-scale struc ture is pos si ble to ex plain by the move - ment of large tec tonic blocks only. We con sider this took place by oblique move ment of the In ner Carpathian Block and the Eu - ro pean Plat form, or of its rifted blocks.
The spa tial po si tion of the CCZ is in de pend ent of the PKB (see Fig. 1). In the cen tral part of Slovakia, the CCZ is dis placed to the south and in the east ern and west ern part of Slovakia it is lo cated to the north of the PKB. This may in di cate in ter fer ence of plat form seg ments be low the In ner West ern Carpathians.
This pos si bil ity is con sis tent with iso static ris ing of the Tatra Mts. and Malá Fatra Mts. (Maglay et al., 1999). It sug gests that the real mar gin of the Eu ro pean Plat form (EP) is the CCZ, and the PKB seems to be a shal low struc ture de tached from the In - ner West ern Carpathians.
As re gards re gional tec ton ics, there are sev eral sig nif i cant points. The in ter pre ta tion of the geo log i cal cross-sec tion through the east Slovakia (Fig. 6) sug gests on the ba sis of geo phys i cal data, that the plat form, be fore col li sion com prised an other block and that the PKB is not the real mar gin of the plat form. The CCZ may have been cre ated by hor i zon tal dis place ment at the con - tact be tween the In ner West ern Carpathians blocks and blocks de rived of Eu ro pean Plat form and the plat form it self.
This in ter pre ta tion is sup ported by seis mic mod els of the CEL-11 pro file (Janik et al., 2011), part of the CELEBRATION 2000 pro ject, where the Eu ro pean Plat form mar gin is sit u ated north of the Klippen Belt and where, in the space be tween the Eu ro pean Plat form and the Klippen Belt, a newly in ter preted Pieniny crustal seg ment has been in serted.
SIGNIFICANCE OF THE PROPOSED INTERPRETATION TO APPLIED GEOLOGY
Aside from dis cus sion of the gen e sis of this pos si ble Neo - gene ig ne ous body, there are sev eral im pli ca tions for ap plied ge ol ogy in par tic u lar as re gards metalogenesis, pos si bil i ties for CO2 stor age and hy dro car bon po ten tial.
An de site dykes in the Pieniny Mts. (Po land) cause the con - tact meta mor phism in neigh bour ing rocks. The fi nal prod ucts may in clude at small de pos its of gold, sil ver and lead. These ores had been briefly ex ploited at the be gin ning of the 18th cen - tury (Szeliga and Michalik, 2003; Birkenmajer et al., 2004). A cor re la tion be tween in tru sion em place ment and min er al iza tion has be ing dem on strated (Birkenmajer et al., 2004).
Sim i larly, ig ne ous rocks in the Czech Re pub lic (Mid dle Mio - cene) are in ten sively al tered (propylitisation) and con tact meta - mor phism has been ob served in the neigh bour ing flysch de pos - its (Krejčí and Poul, 2010).
There are fur ther oc cur rences of min er al iza tion in Ro ma nia, where ore de pos its are as so ci ated with intrusives rep re sent ing Sb-As-Ag-Zn-Pb-As-Cu vein min er al iza tion and dis sem i nated cop per – en riched ore (Cu-Zn-Pb,) in the Tibles area and argillic hy dro ther mal al ter ation as so ci ated with Cu-Pb (Au) min er al iza - tion in the Rodna–Bargau area (Pécskay et al., 2006).
Hence a sim i lar type of min er al iza tion might be ex pected in the exo- and endo-con tact of the in tru sive body in ter preted.
Con sid er ation of un der ground stor age of CO2 has par al lels with hy dro car bon ge ol ogy. Vol ca noes emit large amounts of vol ca nic gas exsolving from the erupt ing magma dur ing ex plo - sive and ef fu sive erup tion and non-erup tive con tin u ous de gas - sing. De gas sing of large vol ume of non-erupted magma can cause con sid er able de gas sing; the erupted magma rep re sents Fig. 6. Sche matic cross-sec tion of the crust in the east ern part of Slovakia (adapted from Bezák et al., 1997)
only a small por tion of the magma that drives vol ca nic ac tiv ity (Shinohara, 2008).
We may ex pect a large vol ume of rocks to have been af - fected by de gas sing of magma, be cause the in tru sion has lost ki - netic en ergy at the lithological bound ary within the Łupków Beds, the magma than cool ing and crys tal liz ing. Vol a tile bub bles, as - cend ing through buoy ancy, will have ac cu mu lated in the up per part of the in tru sive body. Crys tal li za tion of mag mas con cen - trates vol a tile com po nents in the melt, caus ing vol a tile sat u ra tion – bub ble for ma tion (Shinohara, 2008). As the body re mains unerupted, is rea son able to sup pose that the vol ume of rocks in - clud ing vol a tile com po nents may be re mark able (see Fig. 5).
Per me able magma foam can form to al low gas es cape once bub bles be come in ter con nected. Magma per me abil ity can be much higher than wall-rock per me abil ity, and so ver ti cal gas loss can be an im por tant es cape path, in ad di tion to gas loss through the con duit walls (Sparks, 2003).
The lo cal stress field and com plex in ter ac tions of buoy ancy forces, host rock re sis tance to frac ture, elas tic de for ma tion of coun try rock, magma hy dro static pres sure and fluc tu at ing magma pres sure, magma vis cos ity and weight of over bur den con trol the em place ment pro cess (Planke et al., 2003). On a lon ger time scale, the dom i nant pro cesses near in tru sions in - clude re lease of min eral-bound flu ids, pore pres sure in crease and hydrofracturing. Hydrofracturing oc curs when the rate of fluid pro duc tion ex ceeds the rate of fluid mi gra tion (Svensen et al., 2004). Part of the sec ond ary po ros ity ob served in this area may re sult from this pro cess.
We may refere inter ref or ma tion of per me able en vi ron - ments within the up per part of the ig ne ous body, per haps at the con tacts.
Data from the Zboj-1 bore hole sug gests some po ten tial for hy dro car bons, es pe cially within the Zboj Beds (Rudinec, 1989).
The in ferred in tru sion may en hance this.
CONCLUSIONS
New mag netic mea sure ments re veal sev eral small mag netic anom a lies and one large one in the NE part of the Slovakian flysch belt. These ob jects are in ter preted as subvolcanic bod ies of Neo gene age. Their po si tion is sim i lar to those of known ig ne - ous bod ies within the flysch zone of Moravia and Po land. The po - si tion of these ig ne ous rocks near the Carpathian Con duc tiv ity Zone, sug gests an im por tant shear zone at the bound ary be - tween the Eu ro pean Plat form and blocks of the In ner West ern Carpathians. Other fault sys tems, which likely en cour aged as - cent of magma, were con nected with this zone, fol low ing mi gra - tion of subduction fur ther along the Carpathian arc to the Easter Carpathians.
Con se quences of in ter pre ta tion of these mag netic anom a - lies in the Carpathian Flysch Belt for ap plied ge ol ogy in clude min er al iza tion, CO2 stor age, hy dro car bons, and the gen eral im - por tance of the CCZ. How ever, test ing of our hy poth e sis re - quires fur ther work. This might in clude fur ther geo phys i cal in - ves ti ga tions in other parts of the Carpathian arc along the CCZ and the PKB to de velop a better un der stand ing of re la tion be - tween the Carpathians and the Eu ro pean Plat form.
Ac knowl edge ments. This work was sup ported by pro ject No. 1307 – Quan ti ta tive pa ram e ters of se lected geo log i cal struc - ture suit able for CO2 stor age – Min is try of En vi ron ment of Slovakia, by the grant VEGA No. 2/ 0088/12 and by the Slo vak Re search and De vel op ment Agency un der the con tract No.
APVV-0194/10 and 0724/11. The au thors ex press their thanks to J. Grabowski, J. Golonka and P. Krzywiec for con struc tive crit i - cism and help ful com ments dur ing the prep a ra tion of this manu - script and to T. Peryt for over all im prove ment of this pa per.
REFERENCES
Ádám A. (2001) An at tempt to map the depth of the elec tri cal asthenosphere by deep magnetotelluric mea sure ments in the Pannonian ba sin (Hun gary). Acta Geologica Hungarica, 44:
197–192.
Behrmann J.H., Stiasny S., Milička J., Pereszlényi M. (2000) Quan ti ta tive re con struc tion of orogenic con ver gence in the north ern Carpathians. Tectonophysics, 319: 111–127.
Berdichevski M.N., Dmitriev V.I. (1976) Distorsion of mag netic and elec tri cal fields by near-sur face lat eral inhomogenities. Acta Geodaetica, Geophysica et Montanistica Academiae Scientarium Hungaricae, 11: 447–483.
Bezák V., Šefara J., Bielik M., Kubeš P. (1997) Mod els of the West - ern Carpathians litho sphere. In: Geo log i cal Evo lu tion of the West ern Carpathians (eds. P. Grecula et al.): 25–34. Mineralia Slovaca-Mono graph, Bratislava.
Bezák V., Broska I., Ivanička J., Reichwalder P., Vozár J., Polák M., Havrila M., Mello J., Biely A., Plašienka D., Potfaj M., Konečný V., Lexa J., Kaličiak M., Žec B., Vass D., Elečko M., Janočko J., Pereszlényi M., Marko M., Maglay J., Pristaš J.
(2004) Tec tonic map of the Slo vak Re pub lic 1:500 000. ŠGÚDŠ Bratislava.
Bezák V., Biely A., Elečko M., Konečný V., Mello J., Polák M., Potfaj M. (2011) A new syn the sis of the geo log i cal struc ture of
Slovakia – the gen eral geo log i cal map at 1:200 000 scale. Geo - log i cal Quar terly, 55 (1): 1–8.
Bielik M. (1998) Anal y sis of the grav ity field in the West ern and East ern part of Carpathian junc tion area: den sity mod el ling.
Geologica Carpathica, 46: 75–83.
Bielik M., Šefara J., Kováč M., Bezák V., Plašienka D. (2004) The West ern Carpathians – in ter ac tion of Hercynian and Al pine pro - cesses. Tectonophysics, 393: 63–86.
Biely A., Bezák V., Elečko M., Kaličiak M., Konečný V., Lexa J., Mello J., Nemčok J., Potfaj M., Rakús M., Vass D., Vozár J., Vozárová A. (1996) Geo log i cal map of Slo vak Re pub lic 1:500 000. GÚDŠ Bratislava.
Birkenmajer K., Lorenc W.M. (2008) Lower Cre ta ceous ex otic intraplate basaltoid olistolith from Biała Woda, Pieniny Klippen Belt, Po land: geo chem is try and prov e nance. Studia Geologica Polonica, 131: 237–246.
Birkenmajer K., Pécskay Z., Szeliga W. (2004) Age re la tion ships be tween Mio cene vol ca nism and hy dro ther mal ac tiv ity at Mt.
Jarmuta, Pieniny Klippen Belt, West Carpathians, Po land.
Studia Geologica Polonica, 123: 279–294.
Cieszkowski M. (2003) The Outer Carpathians thrustbelt. Pub li ca - tions of the In sti tute of Geo phys ics, Pol ish Acad emy of Sci - ences, Mono graphic, 28 (363): 107–110.
Csontos L., Nagymarosy A., Horváth F., Kováč M. (1992) Ter tiary evo lu tion of the intra-Carpathian area: a model. Tectonophysics, 208: 221–241.
Červ V., Pek J., Praus O. (1984) Mod els of geo phys i cal anom a lies in Czecho slo va kia. Jour nal of Geo phys ics, 55: 61–168.
Ďurkovič T., Koráb T., Rudinec R., Gašparíková V., Snopková P., Kőhler E., Zakovič M. (1982) Hlboký štruktúrny vrt Zboj-1.
Regionálna Geológia Západných Karpát, 16: 1–76.
Filo M., Konečný V., Kubeš P., Šimon L., Dublan Š., Kaličiak M., Lexa J., Gluch A. (2003) Zdroje magnetických anomálií v neovulkanitoch Slovenska. Geologicke Práce – Správy, 107:
47–172.
Franko O., Remšík A., Fendek M., Fusán O., Kráľ M., Bodiš D., Drozd V., Vika K., eds. (1995) At las of geo ther mal en ergy of Slovakia. GÚDŠ Bratislava.
Gągała Ł., Vergés J., Saura E., Malata T., Ringenbach J.-C., Werner P., Krzywiec P. (2012) Ar chi tec ture and orogenic evo lu - tion of the north east ern Outer Carpathians from cross-sec tion bal anc ing and for ward mod el ling. Tectonophysics, 532–535:
223–241.
Gméling K., Németh K., Mar tin U., Eby N., Varga Z. (2007) Bo ron con cen tra tions of vol ca nic fields in dif fer ent geotectonic set - tings. Jour nal of Vol ca nol ogy and Geo ther mal Re search, 159 (1–3): 70–84.
Golonka J. (2004) Plate tec tonic evo lu tion of the south ern mar gin of Eur asia in the Me so zoic and Ce no zoic. Tectonophysics, 381:
235–273.
Golonka J., Aleksandrowski P., Aubrecht R., Chowaniec J., Chrustek M., Cieszkowski M., Florek R., Gawęda A., Jarosiński M., Kępińska B., Krobicki M., Lefeld J., Lewandowski M., Marko F., Michalik M., Oszczypko N., Picha F., Potfaj M., Słaby E., Ślączka A., Stefaniuk M., Uchman A., Żelaźniewicz A. (2005) The Orava Deep Drill ing Pro ject and post-Palaeogene tec ton ics of the North ern Carpathians. Annales Societatis Geologorum Poloniae, 75:
211–248.
Hrušecký I., Kotulová J., Baráth I., Kubeš P., Ďurkovič T., Fejdi V., Pereszlényi M., Nemčok M., Janočko J. (2003) Uhľovodíkový potenciál východoslovenského neogénu a priľahlých oblastí flyšového pásma. Manu script. Geofond, ŠGÚDŠ Bratislava.
Hvožďara M., Vozár J. (2004) Lab o ra tory and geo phys i cal im pli ca - tions for ex pla na tion of the na ture of the Carpathian Con duc tiv - ity Anom aly. Acta Geophysica Polonica, 52: 497–508.
Janik T., Grad M., Guterch A., Vozár J., Bielik M., Vozárová A., Hegedüs E., Kovács C.A., Kovács I., Keller G.R., Cel e bra tion 2000 Work ing Group (2011) Crustal struc ture of the West ern Carpathians and Pannonian Ba sin: seis mic mod els from Cel e - bra tion 2000 data and geo log i cal im pli ca tions. Jour nal of Geodynamics, 52: 97–113.
Jurewicz E., Nejbert K. (2005) Geotectonic po si tion of the so-called “Pieniny Mts. andesites”. Min er al og i cal So ci ety of Po - land, Spe cial Pa per, 25: 179–183.
Konečný V., Kováč M., Lexa J., Šefara J. (2002) Neo gene evo lu - tion of the Carpatho-Pannonian re gion: an in ter play of subduction and back-arc diapiric up rise in the man tle. EGU Stephan Mueller Spe cial Pub li ca tion Se ries, 1: 105–123.
Koráb T. (1983) Geo log i cal map of the Nízke Beskydy Mts., scale 1:50 000 – East ern part. GÚDŠ, Bratislava.
Krejčí O., Poul I. (2010) Ev i dence of Mid dle Mio cene thrust tec ton - ics in the Bílé Karpaty Unit (Carpathian Flysch Belt). Geologické Výzkumy Moravy a Slezska: 58–63.
Krobicki M., Golonka J., Aubrecht R. (2003) Pieniny Klippen Belt:
gen eral ge ol ogy and geodynamic evo lu tion. Pub li ca tions of the In sti tute of Geo phys ics, Pol ish Acad emy of Sci ences, Mono - graphic, M-28 (363): 25–33.
Krobicki M., Golonka J., Lewandowski M., Michalik M., Oszczypko N., Popadyuk I., Słaby E. (2004) Vol ca nism of the Ju ras sic-Cre ta ceous tri ple-junc tion zone in the East ern Carpathians. Geolines, 17: 60–61.
Kubeš P., Kucharič Ľ., Gluch A., Kohút M., Bezák V., Potfaj M.
(2008) Magnetická mapa Slovenska. Fi nal re port Manu script.
Geofond, ŠGÚDŠ Bratislava.
Kubeš P., Bezák V., Kucharič Ľ., Filo M., Vozár J., Konečný V., Kohút M., Gluch A. (2010) Mag netic field of the West ern Carpathians (Slovakia): re flec tion struc ture of the crust.
Geologica Carpathica, 61: 437–447.
Leško B., Ďurkovič T., Faber P., Filkova V., Hradil F., Janku J., Losík K., Píchová E., Rudinec R., Sam uel O., Smetana J., Snopková P., Wunder D. (1987) Oporný vrt Smilno 1 (5 700 m).
Regionálna Geológia Západných Karpát, 22: 1–133.
Lexa J., Konečný V. (1998) Geodynamic as pects of the Neo gene to Qua ter nary vol ca nism. In: Geodynamic De vel op ment of the West ern Carpathians (ed. M. Rakús): 219–240. Geo log i cal Sur - vey of the Slo vak Re pub lic.
Lexa J., Bezák V., Elečko M., Mello J., Polák M., Potfaj M., Vozár J., eds. (2000) Geo log i cal map of the West ern Carpathians and ad ja cent ar eas: scale 1:500 000. Geo log i cal Sur vey of Slo vak Re pub lic, Bratislava.
Maglay J., Halouzka R., Baňacký V., Pristaš J., Janočko J., Hók J. (1999) Neotectonic map of Slovakia and ex pla na tion 1:500 000. GÚDŠ Bratislava.
Mašín J. (1963) Aeromagnetická a aerorádiometrická mapa ČSSR v měřítku 1:200000. ÚÚG Praha.
Mišík M. (1992) Pieniny Klippen Belt in re la tion ship with Me so zoic and Ter tiary vol ca nism. Západné Karpaty, Geológia, 16: 47–64.
Mořkovský M., Novák J., Lukášová R. (1992) Geo phys i cal prospectings for hy dro car bons in the Intracarpathian Paleogene and in the East Slovakian Flysch belt. Sborník geologických věd, Užitá Geofyzika, 25: 9–48.
Ondra P., Hanák J. (1989) Petrofyzikálna štúdia sedimentov východoslovenského flyša. Geologicke Práce – Správy, 89:
67–89.
Oszczypko N., Golonka J., Malata T., Poprawa P., Słomka T., Uchman A. (2002) Tectono-strati graphic evo lu tion of the Outer Carpathian ba sin (West ern Carpathans, Po land). Geologica Carpathica, Spe cial Is sue, 53.
Pécskay Z., Lexa J., Szakács A., Szeghedi I., Balogh K., Konečný V., Zelenka T., Kovacs M., Póka T., Fülöp A., Márton E., Panaiotu C., Cvetković V. (2006) Geo chron ol ogy of Neo - gene magmatism in the Carpathian arc and intra-Carpathian area. Geologica Carpathica, 57 (6): 511–530.
Pécskay Z., Seghedi I., Kovacs M., Szakacs A., Fülöp A. (2009) Geo chron ol ogy of the Neo gene calc-al ka line in tru sive magmatism in the “Subvolcanic Zone” of the East ern Carpathians (Ro ma nia). Geologica Carpathica, 60 (2):
181–190.
Plašienka D., Grecula P., Putiš M., Kováč M., Hovorka D. (1997) Evo lu tion and struc ture of the West ern Carpathians: an over - view. In: Geo log i cal Evo lu tion of the West ern Carpathians (eds.
P. Grecula, D. Hovorka and M. Putiš): 7–24. Mineralia Slovaca – Mono graph, Bratislava.
Planke S., Svensen H., Hovland M., Banks D.A., Jamtveit B.
(2003) Mud and fluid mi gra tion in ac tive mud vol ca noes in Azerbaijan. Geo-Ma rine Let ters, 23: 258–268.
Poprawa D., Nemčok J., eds. (1988–1989) Geo log i cal at las of the West ern Outer Carpathians. Scale 1:500 000. Wydawnictwa Geologiczne, Warszawa.
Pospíšil L., Ádám A. (2006) Re view of the Crust – Litho sphere re - search in the Carpathians. AAPG Mem oir, 84: 481–495.
Rudinec R. (1989) Crude oil, nat u ral gas and geo ther mal en ergy re - sources in east ern Slovakia. ALFA pub lish ing, Bratislava.
Ryłko W., Tomaś A. (1995) Mor phol ogy of the con sol i dated base - ment of the Pol ish Carpathians in the light of magnetotelluric data. Geo log i cal Quarterly, 39 (1): 1–16.
Shinohara H. (2008) Ex cess de gas sing from vol ca noes and its role on erup tive and in tru sive ac tiv ity. Re views of Geo phys ics, 46:
1–31.
Ślączka A. (1970) Ge ol ogy of the Dukla Unit (in Pol ish with Eng lish sum mary). Prace Instytutu Geologicznego, 63: 1–97.
Ślączka A., Kruglov S., Golonka J., Oszczypko N., Popadyuk I.
(2006) The gen eral ge ol ogy of the Outer Carpathians, Po land, Slovakia and Ukraine. AAPG Mem oir, 84: 1–70.
Sparks R.S.J. (2003) Fore cast vol ca nic erup tion. Earth and Plan e - tary Sci ence Let ters, 210: 1–15.
Stanica M., Stanica D., Marin-Furnica C. (1999) The place ment of the Trans/Eu ro pean Su ture Zone on the Ro ma nian ter ri tory by elec tro mag netic ar gu ments. Earth Plan ets Space, 51:
1073–1078.
Stefaniuk M. (2006) Some re sults of a new magnetotelluric sur vey in the area of the Pol ish Outer Carpathians. AAPG Mem oir, 84:
707–716.
Svensen H., Planke S., Malthe–Sorenssen A., Jamtveit B., Myklebust R., Eidem T.R., Rey S.S. (2004) Re lease of meth -
ane from a vol ca nic ba sin as a mech a nism for ini tial Eocene global warm ing. Na ture, 429: 524–527.
Szeliga W., Michalik M. (2003) Con tact meta mor phism and hy dro - ther mal al ter ations around an de site in tru sion of the Jarmuta hill, Pieniny (Po land). Geologica Carpathica, 46: 327–334.
Tari G., Horváth F. (2006) Al pine evo lu tion and hy dro car bon ge ol - ogy of the Pannonian Ba sin: an over view. AAPG Mem oir, 84:
605–618.
Tomek Č., Švancara J., Budík L. (1979) The depth and the or i gin of the West Carpathian grav ity low. Earth and Plan e tary Sci ence Let ters, 44: 39–42.
Trua T., Birkenmayer K., Serim G., Pécskay Z. (2006) Pe trog ra phy and geo chem is try of Mid dle Mio cene (Sarmatian) vol ca nic area of the Pieniny Mts., Western Carpathians. Lithos, 90: 57–76.
