Geo log i cal Quar terly, 2017, 61 (4): 934–945 DOI: http://dx.doi.org/10.7306/gq.1383
A new mag netic anom aly map of Po land and its con tri bu tion to the rec og ni tion of crys tal line base ment rocks
Zdzis³aw PETECKI1 and Olga ROSOWIECKA1, *
1 Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Rakowiecka 4, 00-975 Warszawa, Po land
Petecki, Z., Rosowiecka, O., 2017. A new mag netic anom aly map of Po land and its con tri bu tion to the rec og ni tion of crys tal - line base ment rocks. Geo log i cal Quar terly, 61 (4): 934–945, doi: 10.7306/gq.1383
Mag netic to tal field mea sure ments ac quired in Po land be tween 1974 and 2011 have been com piled in a new dig i tal da ta base that pro vides a com plete pic ture of mag netic anom a lies of the coun try. The data com pi la tion and fur ther pro cess ing pro ce - dures used to cre ate the mag netic anom aly da ta base and maps that ac com pany this ar ti cle are briefly sum ma rized. The re - duced-to-the-pole and pseudogravity anom aly maps were com puted to ac cu rately lo cate anom a lies above their caus ative bod ies as well as to sim plify anom aly pat terns and em pha size prin ci pal mag netic do mains within the base ment. An in ter pre - ta tion of the mag netic maps re veals a lot of mag netic base ment prov inces and do mains in di cat ing base ment di vi sion into blocks and struc tural el e ments, which are im por tant for un der stand ing the re gional tec tonic set ting of Po land.
Key words: mag netom etry, Earth’s to tal mag netic field map, pseudogravity, crys tal line base ment, Po land.
INTRODUCTION
A num ber of high-res o lu tion mag netic sur veys have been con ducted in Po land over the last three de cades. Un for tu - nately, the large amount of mag netic data has not been com - piled into a map that cov ers the whole coun try (Petecki et al., 2003). It was there fore dif fi cult to in ter pret these mag netic data on a re gional scale and to com pare with neigh bour ing coun - tries.
To ob tain a con sis tent mag netic anom aly map of the Earth’s to tal mag netic field in ten sity for the whole Pol ish ter ri tory, the mag netic data have been com piled into a 1 km grid. The map is based on 10 semi-de tailed (2–4 pts/km2) ground- and ship- borne sur veys (Fig. 1).
The pres ent pa per in cludes a short de scrip tion of the his tory of mag netic sur vey ing in Po land, new mag netic data used in the com pi la tion of the maps, and re duc tion and pro cess ing meth ods.
Fur ther more, a brief dis cus sion of the re gional anom aly pat tern and its re la tion ship to the tec tonic el e ments of Po land is given.
HISTORY OF MAGNETIC SURVEYING IN POLAND
Mag netic field in ves ti ga tions in the area of Po land have been con ducted for more than hun dred years. The first mea sure -
ments, ex e cuted in the for mer East Prus sia (pres ent NE Po land), re sulted in the dis cov ery of a dis tinct bound ary be tween a mag - netic re gion east of the Wis³a River and a non-mag netic re gion west of it (Tornquist, 1908), which even tu ally be came to be known as the Teisseyre-Tornquist Zone (D¹browski, 1971; see also the re view in Narkiewicz et al., 2015). A sys tem atic re gional mag netic sur vey started be fore the Sec ond World War and was fin ished in the mid-1950s. It was char ac ter ized by a low data point den sity (0.06–0.7 pts/km2) and low ac cu racy of mea sure - ments of the ver ti cal com po nent Z of the geo mag netic field. On the 1:2,000,000-scale map, con structed on the ba sis of this re - gional sur vey (D¹browski and Karaczun, 1958), the two above-men tioned sep a rate mag netic re gions were more pre - cisely de ter mined: NE and E Po land be ing part of the East Eu ro - pean Craton (EEC), with the strongly dif fer en ti ated mag netic field, and the re main ing part of Po land be ing char ac ter ized by the weak or very weak mag netic field. More in tense anom a lies in the lat ter re gion were de tected only in the Sudetes, the Fore-Sudetic Block and along the NE bound ary of the Up per Silesian Block.
Ini tially, var i ous for mu las for a nor mal field have been ap - plied when re duc ing the data ob tained from sep a rate mag netic sur veys. In or der to pro cess the data in a uni form way, the an a - lyt i cal for mula for a nor mal field of the area of Po land has been cal cu lated based on the Tay lor’s for mula in con sid er ation of the sec ond de gree ex pres sions (Karaczun, 1965). It be came the ba sis for the de vel op ment of a new ver sion of the mag netic anom aly map of Po land by Karaczun et al. (1978).
Nu mer ous mea sure ments of the Z com po nent were made in the area of NE Po land, es pe cially dur ing the 1960s and 1970s. Two kinds of sur veys have been ap plied: a sur vey with the ir reg u lar point dis tri bu tion with den sity of 4–6 pts/km2, and a pro file sur vey with the point spac ing of a few tens of metres. In both cases, the mea sure ment ac cu racy was ~6 nT. All these mea sure ments were uni fied ap ply ing a mag netic ref er ence
* Corresponding author, e-mail: opol@pgi.gov.pl
Received: April 18, 2017; accepted August 28, 2017; first published online: September 19, 2017
point net work, re duced to ep och 1957.5 us ing DGRF (De fin i tive Geo mag netic Ref er ence Field) and or ga nized in a da ta base.
The weakly dif fer en ti ated mag netic field in west ern and cen tral Po land, with only re gional anom a lies of rel a tively small am pli - tudes, dis cour aged sub se quent, more de tailed in ves ti ga tions in this area.
In the early 1960s, re search ers from the Geo phys i cal De - part ment of the Pol ish Acad emy of Sci ences con structed the
first Pol ish pro ton mag ne tom e ter, which was able to mea sure the ab so lute to tal mag netic field T value. It al lowed a rad i cal in - crease in the ac cu racy of mag netic mea sure ments (0.1 nT) as well as sim pli fi ca tion of fur ther data pro cess ing. These new tech niques to gether with more de tailed sur vey lay outs led to the sec ond gen er a tion of mag netic map ping pro grams in Po land.
The first semi-de tailed ground sur vey in the west ern part of Po land, ex e cuted us ing pro ton mag ne tom e ters, was car ried out in the south ern part of the Fore-Sudetic Monocline be tween 1972 and 1974 (Ta ble 1, No. 1). This study be gan ac qui si tion of the pres ent semi-de tailed sur vey cov er ing the whole area of Po - land.
The mag netic T off shore sur veys in the south ern Bal tic Sea have been car ried out by sev eral com pa nies. The larg est off - shore sur vey (with re spect to the area and the num ber of data points) was com pleted be tween 1976 and 1982 by the Inter-Un - ion Re search In sti tute of Ma rine Ge ol ogy and Geo phys ics WNIMORGEO, upon a com mis sion from the in ter na tional group PETROBALTIC, Gdañsk. Re sults were re pro cessed by the Geo phys i cal Ex plo ra tion Com pany (PBG) in 1993–1994, and a com puter da ta base was cre ated. To tally, a dataset of 490,000 ma rine mea sure ments was ac quired (Ta ble 1, No. 5).
Aero mag net ic mea sure ments were ac quired be tween 1977 and 1981 in the area of the Sudetes, the Fore-Sudetic Monocline, and the Carpathians and their fore land. Mea sure - ments were col lected along 1 km spaced flight lines in ter sected per pen dic u larly by 10 km spaced tie lines. Un for tu nately, the whole orig i nal dataset was af fected by a strong noise mainly of in dus trial or i gin. As a re sult of works aimed at the elim i na tion of those dis tur bances, the mag netic field was rad i cally smoothed.
For a long time, strong ar ti fi cial noise, caused by elec tri fied rail ways, posed a se ri ous ob sta cle for the ac qui si tion of uni - formly dis trib uted data points. A field work method en abling the elim i na tion of the de scribed noise was de vel oped by Kosobudzka (1988). The so-called dif fer en tial method com - prises the mea sure ment of mag netic field vari a tions in two mea sure ment points, si mul ta neously with the use of two syn - chro nized mag ne tom e ters, work ing at an ac cu racy of 0.1 nT.
Us ing this method there is still a lack of mea sure ments right at rail way lines and the char ac ter is tic “ze bra” pat tern of mag netic sta tions in the 8 km wide zones on both sides of them (Fig. 2).
Fig. 1. Location of semi-detailed surveys used during map construction
1 – Fore-Sudetic Monocline; 2 – Szczecin Trough and Fore-Sudetic Monocline; 3 – West ern, cen tral and south east ern Po land; 4 – NW Po land; 5 – Bal tic Sea; 6 – west ern, cen tral and southeast ern Po - land; 7 – margin zone of the Pre cam brian Plat form; 8 – Carpathians and their fore land; 9 – Sudetes; 10 – NE Po land
No. Area of sur vey Year Point den sity
[pts/km2] Pur chaser Con trac tor
1 Fore-Sudetic Monocline 1974 1.0 AGH Uni ver sity of Sci ence
and Tech nol ogy
PBG Geo phys i cal Ex plo ra tion Com pany 2 Szczecin Trough and Fore-Sudetic
Monocline 1989 4.0-4.5 Pol ish Oil and Gas Com pany
(PGNiG) 3 West ern, cen tral and south east ern
Po land I 1992 2.0-3.0 Pol ish Geo log i cal In sti tute
4 NW Po land 1994 1.0 State Com mit tee for Sci en tific
Re search Pol ish Geo log i cal In sti tute
5 Bal tic Sea 1994
Min is try of the En vi ron ment PBG Geo phys i cal Ex plo ra tion Com pany 6 West ern, cen tral and south east ern
Po land II 1997 2.0
7 Mar gin zone of the Pre cam brian
Plat form 2002 2.0
8 Carpathians and its fore land 2005 2.0
9 Sudetes 2007 4.0–13.0
10 NE Po land 2011 3.7
T a b l e 1 Mag netic sur veys of to tal field, used to com pile the pres ent to tal in ten sity mag netic map (for more de tails re fer to Petecki et al., 2003)
936 Zdzis³aw Petecki and Olga Rosowiecka
Rou tine mag netic mea sure ments, with the ap pli ca tion of the dif fer en tial method, started in 1981 in the north ern part of the Fore-Sudetic Monocline and the south ern part of the Szczecin Trough (Ta ble 1, No. 2). The re sults ap peared to be so prom is - ing that a de ci sion to ex pand mea sure ments across the whole area of west ern and cen tral Po land (1985–1992) was made (Ta ble 1, No. 3). The pro ject was sup ple mented by re search in the Szczecin area as part of a grant fi nanced by the State Com - mit tee for Sci en tific Re search (Ta ble 1, No. 4). Be tween 1995 and 1997, the pro ject was con tin ued in the area of south-east - ern Po land (Ta ble 1, No. 6).
A next stage in the mag netic data ac qui si tion was made by ex pand ing the sur vey into the area of the EEC mar ginal zone (Ta ble 1, No. 7). All the so far men tioned semi-de tailed sur veys of DT were com piled into a map at a scale of 1:500,000 pre sent - ing the north ern part of Po land (Petecki et al., 2003). The south - ern part had to wait un til com ple tion of lack ing sur veys in the Carpathians and Sudetes. Since 2002, a semi-de tailed sur vey cov er ing the Carpathians and their fore land has been ac quired (Ta ble 1, No. 8). The co or di nates of mea sure ment points were based on the di rect field mea sure ments us ing GPS re ceiv ers. A sim i lar sur vey in the Sudetes was per formed be tween 2005 and 2007 (Ta ble 1, No. 9).
In or der to com plete a ho mo ge neous anom aly dataset for Po land, a mag netic sur vey in NE Po land was con ducted be -
tween 2008 and 2011 (Ta ble 1, No. 10).The re sult ing mag netic da ta base has been sup ple mented with the ar chi val data from the years 1967–1992, cov er ing se lected anom a lous ar eas.
DESCRIPTION OF SOURCE DATA AND PROCESSING
For the pres ent com pi la tion, 10 ground- and ship-borne sur - veys were used, which were con ducted be tween 1974 and 2011. The char ac ter is tics of in di vid ual sur veys are sum ma rized in Ta ble 1. The reader is also re ferred to Fig ure 1 for more de - tailed ac count of sur vey lo ca tion.
Data pro cess ing of ground mag netic data in cluded re moval of the ef fects of time-vary ing ex ter nal fields such as micropulsations, mag netic storms and di ur nal vari a tions, re - moval of the In ter na tional Geo mag netic Ref er ence Field, and gridding. Di ur nal re moval was achieved by sub tract ing the time-syn chro nized mag netic field, re corded at a sta tion ary base-sta tion mag ne tom e ter, from the sur vey data. Af ter the base-sta tion cor rec tion and ad just ment to the 1982.5 geo mag - netic ep och, the to tal-field mag netic anom aly DT was ob tained by sub tract ing the mag ni tude of an ap pro pri ate DGRF 1982.5 re gional field from the to tal field mea sure ment to ob tain the crustal anom aly field. No ta bly, the DGRF 1980 model was se - Fig. 2. Distribution of all magnetic stations (black dots) used for the present map compilation
lected as the best ref er ence model for Eu rope (Wonik et al., 2001), which was re cently used by Ga briel et al. (2011) dur ing com pi la tion of the mag netic anom aly map of Ger many. Fi nally, the data were gridded at 1 km spac ing us ing a min i mum cur va - ture method. Nearly 1.4 mil lion data points were used to pre - pare the grid (Fig. 2).
To pro duce a mag netic anom aly map of Po land, some Z mea sure ments were used as well. In two re gions, the en vi rons of War saw and large part of Up per Silesia (Fig. 2), where new mea sure ments were not achiev able be cause of strong in dus - trial noise, the data se lected from the Z re gional sur vey (Karaczun et al., 1978) were used to fill gaps in the data point dis tri bu tion. Since mag netic anom a lies were cal cu lated in that case in ref er ence to the lo cal geo mag netic level, they were re - cal cu lated to the DGRF, ep och 1957.5 ref er ence field. The ver - ti cal-com po nent data have been con verted to the to tal-field data by means of 2-D fil ter ing (Gunn, 1975). It was per formed in the wavenumber do main us ing the MAGMAP™ soft ware of Geosoft Ltd., and as sum ing that sources of mag netic anom a - lies are mag ne tized par al lel to the Earth mag netic field di rec -
tion. As a next step, the mag netic to tal in ten sity grid has been used as the “mas ter grid” for merg ing with DZ con verted to DT grid, ap ply ing an other tool (GridKnit™) of the Geosoft Oasis montaj soft ware. Fi nally, a com bined grid was ed ited for man ual elim i na tion of re main ing er rors. Fig ure 3 shows the to tal in ten - sity mag netic anom aly DT map of Po land.
MAGNETIC DATA FILTERING
Uti li za tion of mag netic data dur ing geo log i cal in ter pre ta tion is dif fi cult in Po land since mag netic anom a lies usu ally do not lie di rectly above their caus ative sources. Dis place ment be tween anom a lies and their sources re sults from di rec tions of the geo - mag netic field and source mag ne ti za tion, which are not ver ti cal be yond the mag netic poles (Blakely, 1995). To cor rect for this dis tor tion, the mag netic data should be re duced to the pole or trans formed to the pseudogravity field by the ap pli ca tion of math e mat i cal fil ters to ob served data (Baranov, 1957; Baranov and Naudy, 1964).
Fig. 3. Total intensity magnetic anomaly map of Poland, and a sketch of main geological discontinuities and blocks
BF – Bia³opole Fault; DF – Dubienka Fault; EEC – East Eu ro pean Craton; FSB – Fennoscan - dia–Sarmatia bound ary (af ter Bogdanova et al., 2015); HCS – Holy Cross Su ture; KLFZ – Kraków–Lubliniec Fault Zone; MB – Ma³opolska Block; MSSZ – Moravo-Silesian Su ture Zone; OFZ – Odra Fault Zone; TTZ – Teisseyre-Tornquist Zone (af ter Narkiewicz et al., 2015); USB – Up per Silesian Block; white line – pro file A–A’ (see Fig. 6)
REDUCTION TO THE POLE
A shape of a mag netic anom aly re sults from the body’s mag ne ti za tion di rec tion as well as in cli na tion and dec li na tion of the lo cal Earth’s mag netic field. Re duc tion to the pole (RTP) is a math e mat i cal ap proach pro posed by Baranov (1957) and Baranov and Naudy (1964), which sim pli fies the anom aly shape. It re cal cu lates the ob served anom aly into the anom aly that would be ob served at the mag netic pole, i.e. as sum ing verticality of the mag ne ti za tion and am bi ent field. Thus, mag - netic in ter pre ta tion be comes sim pler, since the re duc tion to the pole cen tres the anom a lies over their caus ative struc tures.
PSEUDOGRAVITY TRANSFORMATION
Mag netic anom a lies can be trans formed to the equiv a lent grav ity anom a lies, on con di tion that the dis tri bu tion of source’s mag ne ti za tion is pro por tional to the den sity dis tri bu tion (Baranov, 1957). The trans for ma tion based on the Pois son’s re la tion ship be tween the grav i ta tional and mag netic po ten tials caused by a source of uni form den sity and uni form mag ne ti za - tion con trasts. This op er a tion is called pseudogravity trans for - ma tion that pro duces pseudogravity anom a lies.
The pseudogravity trans for ma tion, com puted as sum ing a ra tio of mag ne ti za tion to den sity of 0.5, con sists of re duc tion to the pole and ver ti cal in te gra tion. The lat ter trans form en hances long wave length anom a lies, lead ing to en hanc ing anom a lies caused by deep mag netic sources (Blakely, 1995).
The pseudogravity pro ce dure sim pli fies anom aly pat terns and em pha sizes prin ci pal mag ne tized do mains within the base - ment (Blakely and Simpson, 1986).
The afore men tioned pro ce dures were per formed on the data in the wavenumber do main us ing the MAGMAP™ soft - ware from Geosoft. Both fil ter ing meth ods re quire knowl edge of the mag ne ti za tion di rec tion and were ex e cuted un der the as - sump tion that the mag ne ti za tion is par al lel to the am bi ent mag - netic field. The re sult ing re duced-to-the-pole and pseudogravity maps are shown in Fig ure 4.
Re duc tion to the pole re sults in a slight north ward mi gra tion of anom aly max ima, and changes their am pli tudes. In west ern Po land, there has been a sig nif i cant change in the course of the isolines that now run more reg u larly along the NW–SE di rec - tion. By sup press ing strong but shal low mag netic dis tur bances, the mag netic pseudogravity map pro vides a clearer out line of re gional mag netic prov inces.
MAGNETIC ANOMALY PATTERN
Po ten tial field tech niques, es pe cially mag netic sur veys, are used com monly to map the base ment struc ture be neath the sed i men tary cover. With the ex cep tion of lo cal anom a lies caused by intra-sed i men tary sources (D¹browski and Karaczun, 1971; Karaczun and Królikowski, 1982; Nawrocki et al., 2007, 2008) the dom i nant con tri bu tion to the mag netic anom aly field of Po land is from the crys tal line base ment. There - fore, the cur rently com piled da ta base and the new mag netic anom aly maps (Figs. 3–5) of fer in sights into li thol ogy, struc tural ar chi tec ture and tec tonic char ac ter of the crys tal line base ment on both re gional and lo cal scales.
A dis tinct di vi sion into sev eral mag netic re gions, show ing quite dif fer ent mag netic char ac ter is tics, is ap par ent. These re -
938 Zdzis³aw Petecki and Olga Rosowiecka
Fig. 4. Reduced-to-the-pole (RTP) total intensity magnetic anomaly map (A) and pseudogravity anomaly map (B) Black lines – bor ders of mag netic do mains; Bd – Bal tic do main, Chd – Che³m do main, CWPd – cen tral and west ern Po land do main, Cz – Ciechanów zone, Md – Mazowsze do main, PCz – Plat form Con tact zone, PMd – Pomerania–Mazury do main, Pz – Podlasie zone, Sd – Sudetic do main, SSPI – Szczecin–Stargard Szczeciñski–Pi³a–Inowroc³aw lin ea ment, USMd – Up per Silesia–Ma³opolska do main, WPd – West ern Pomerania do main; anom a lies: 1 – Tychy, 2 – Jordanów, 3 – Nowy S¹cz, 4 – Gogo³ów–Jordanów, 5 – Nowa Ruda, 6 – Braszowice;
other ex pla na tions as in Fig ure 3
gional mag netic do mains are char ac ter ized by their anom aly wave lengths and am pli tudes, het er o ge ne ity, in ter nal mag netic pat terns and trend di rec tions, and, in many cases, are sep a - rated by out stand ing gra di ent zones. Mag netic anom a lies are mainly caused by lithological and struc tural changes in the bur - ied base ment re lated to suc ces sive stages of magmatism and
meta mor phism and as so ci ated P-T path ways. How ever, the in - flu ence of vari able source depths on anom aly shapes and am - pli tudes may also be sig nif i cant.
The area of Po land is di vided into two ma jor mag netic prov - inces by the NW–SE trending line. The north east ern prov ince, cor re spond ing to the EEC, is char ac ter ized by the pres ence of Fig. 5. RTP map of the EEC, and a sketch of main geological discontinuities and blocks
TTZ – Teisseyre-Tornquist Zone (af ter Narkiewicz et al., 2015), FSB – Fennoscandia–Sarmatia bound ary (af ter Bogdanova et al., 2015); Fennoscandia: MLSZ – Mid-Lith u a nian Su ture Zone, AMCG – An or tho - site-Mangerite-Charnockite-Gran ite as so ci a tion, Pa leo zoic mas sifs: 1 – Olsztynek, 2 – M³awa, 3 – Pisz, 4 – E³k, 5 – Tajno; Sarmatia: BPGB – Belarus–Podlasie Granulite Belt, OHB – Okolovo–Holeszów Belt, IBZ – Ivano–Borisov Zone, OMIB – Osnitsk–Mikashevichi Ig ne ous Belt (af ter Krzemiñska et al., in press); Mesoproterozoic mas sifs of Fennoscandia: 6 – Kêtrzyn, 7 – Suwa³ki (af ter Kubicki and Ryka, 1982); other ex pla na tions as in Fig ure 4
in tense mag netic anom a lies. The south west ern prov ince is part of the youn ger Phanerozoic West Eu ro pean Plat form, where the over all in ten sity of ex ist ing mag netic anom a lies is def i nitely lower, ex cept for a few par tic u lar re gions. The bound ary be - tween the two prov inces is marked by a strong gra di ent zone, roughly cor re spond ing to the Teisseyre-Tornquist Zone (TTZ), in the shape sug gested by Narkiewicz et al. (2015; Fig. 3).
Mazur et al. (2015) mod i fied the TTZ-shape in its north ern part by mov ing it fur ther to the north-east and east. Thus, the TTZ runs through the elon gate pos i tive anom aly of the PCz unit de - scribed later in this ar ti cle.
Inhomogeneity of both prov inces as well as their di vi sion into smaller do mains can be ob served. As a first step, a sim ple re gional iden ti fi ca tion of their geo met ri cal shapes based on dis - tinct in ter nal struc tural pat terns has been per formed. In most cases, the geo graph ical ex tent of these do mains can be de ter - mined based on mag netic anom aly pat terns or, more ob jec - tively and ac cu rately, by trac ing the max i mum hor i zon tal gra di - ent mag ni tudes of pseudogravity (Cordell and Grauch, 1985;
Blakely and Simpson, 1986). The bound aries of dis tin guished do mains are marked by black lines in Fig ures 4 and 5.
The de tailed de scrip tion of mag netic do mains is be yond the scope of this pa per, as the main goal is to pres ent a new com pi la - tion of mag netic data of Po land. Nev er the less, a brief de scrip tion of main mag netic do mains is given be low, along with some in for - ma tion on their geo log i cal con text. Al though the geo log i cal im - por tance of some of mag netic do mains and anom a lies has been stud ied (Cieœla and Wybraniec, 1998; Petecki, 2001, 2008;
Grabowska and Bojdys, 2001; Dziewiñska and Petecki, 2004;
Królikowski, 2006; Grabowska et al., 2007, 2011; Lemberger et al., 2008; Wiszniewska and Petecki, 2016), many fea tures still re main to be in ves ti gated to find a closer re la tion ship be tween the mag netic field and crys tal line base ment ge ol ogy.
EAST EUROPEAN CRATONIC PROVINCE
Sev eral units within the EEC prov ince have been dis tin - guished based on geo phys i cal and geo log i cal data by Kubicki and Ryka (1982) and Ryka (1998). Sub se quent in ves ti ga tions of fun da men tal im por tance for the knowl edge about the Pre cam - brian crys tal line base ment have been per formed in the next years (e.g., Dörr et al., 2002; Wiszniewska et al., 2002; Bagiñski et al., 2007; Wil liams et al., 2009; Krzemiñska et al., 2009a;
Demaiffe et al., 2013). These re sults, sup ple mented with the new est geo chem i cal, iso tope and U-Pb dat ing stud ies of bore - hole sam ples, with the mag netic and grav ity data used to set geo log i cal bound aries, en abled com pi la tion of a novel geo logic map of the crys tal line base ment in the Pol ish part of the East Eu - ro pean Plat form (Krzemiñski et al., 2014; Krzemiñska et al., in press). The pre vi ous lithostratigraphic di vi sion, with a large num - ber of meta mor phic for ma tions and lo cal groups es tab lished by Kubicki and Ryka (1982) and Ryka (1998), has been re placed by a more up-to-date chronostratigraphic clas si fi ca tion. The ar eal ex tent and geo log i cal im por tance of these do mains to gether with their sub di vi sion are fur ther de vel oped be low.
Within the EEC mag netic prov ince, the fol low ing do mains are dis tin guished: Plat form Con tact zone (PCz), Che³m do main (Chd), Podlasie zone (Pz), Mazowsze do main (Md), Ciechanów zone (Cz), Pomerania–Mazury do main (PMd), and Bal tic do main (Bd; Fig. 4).
PLATFORM CONTACT ZONE
The Plat form Con tact zone (PCz) is con toured in mag netic im ages (Fig. 4) as a sep a rate elon gate unit, be cause the lay out
and di rec tion of its mag netic anom a lies is dif fer ent from those in the neigh bour ing units. It is char ac ter ized by broad pos i tive anom a lies of mod er ate am pli tudes and spreads across hun - dreds of kilo metres. A se ries of pos i tive mag netic anom a lies oc - cur ring in this zone is bor dered to the SW by a well-ex pressed mag netic gra di ent zone. South west ward of this line, there is a prom i nent mag netic low. The char ac ter of the mag netic field in - di cates a ma jor lithological and/or tec tonic bound ary in the base ment.
The blurred shape of anom a lies and their gra di ents in di cate a deep lo ca tion of mag netic sources re lated to a deep en ing of the crys tal line base ment rocks. Their di rec tion is in gen eral com pat i ble with the di rec tion of the gra di ent zone, es pe cially in its south ern part where these anom a lies are strongly sep a rated from the NE–SW-trending anom a lies of Chd. North of War saw, the anom a lies of the west ern bor der of PMd and Cz ter mi nate within PCz.
CHE£M DOMAIN
In the Che³m do main (Chd), lo cated in SW Po land, the anom a lies trend mainly SW–NE and, subordinately, NW–SE (Fig. 4). Geo log i cally, the do main be longs to Sarmatia (Bogdanova et al., 2006), which is ap prox i mately equiv a lent to the Ukrai nian part of EEC in clud ing the Ukrai nian Shield. The north west ern bor der of Sarmatia is de fined along the Hanna Fault (¯elichowski, 1972; Bojdys et al., 2003; Krzemiñska et al., in press), bound ing the £uków El e va tion from the south.
The SW-trending anom a lies of Chd ap pear to ter mi nate against the re gional anom a lies of PCz. The anom aly pat tern in - di cates that the li thol ogy and ar chi tec ture of the crys tal line base ment is strongly di ver si fied (Grabowska and Bojdys, 2001). Sev eral faults ap pear across the area. They are both per pen dic u lar and par al lel to PCz (Fig. 4). Two of them are the Dubienka and Bia³opole faults traced in the POLCRUST-01 seis mic data (Malinowski et al., 2015).
The new geo logic map of the crys tal line base ment in the Pol - ish part of EEC sug gests the ex is tence of two Paleoproterozoic do mains: Osnitsk–Mikashevichi Ig ne ous Belt and Ivanovo–Bori - sov Zone in Chd (Fig. 5; Krzemiñska et al., in press).
PODLASIE ZONE
To the north of Chd, an ob vi ous NE–SW-trending mag netic field fab ric is ob served (Fig. 4). This area, la belled herein as the Podlasie zone (Pz), is char ac ter ized by a set of sev eral belt-shaped anom a lies ex tend ing from Po land to west ern Belarus.
Their bound aries can be clearly marked us ing the mag netic data pat terns. These strong lin ear mag netic highs and lows de lin eate the Belarus–Podlasie Granulite (BPGB) and Okolovo–Holeszów (OHB) belts (Fig. 5; Krzemiñska et al., in press). These belts are re garded as a south ern frag ment of the Fennoscandian part of EEC, bor der ing Sarmatia from the NW (Bogdanova et al., 2006;
Krzemiñska et al., in press). How ever, ac cord ing to the new tec - tonic sub di vi sion of the South Bal tic re gion (Bogdanova et al., 2015), the BPGB and OHB be long to Sarmatia.
MAZOWSZE DOMAIN
The broad mag netic Mazowsze do main (Md), bound ing Pz from the north, is char ac ter ized by a neg a tive low am pli tude anom aly of RTP data (Fig. 4). Ac cord ing to the new geo log i cal data, this mag netic do main cor re sponds mainly to granitoids and paragneisses (Wil liams et al., 2009; Krzemiñska et al., in
940 Zdzis³aw Petecki and Olga Rosowiecka
press). On top of the sub dued re gional field level, there are prom i nent lo cal mag netic anom a lies. These cor re spond to var i - ous rock types char ac ter ized by dis tinct mag netic prop er ties, mainly syenites and am phi bo lites, whereas gran ites and gneiss es with low mag netic sus cep ti bil ity dom i nate else where in the do main. For ex am ple, neg a tive lo cal mag netic anom a lies are re lated to the Pa leo zoic syenite mas sif of E³k (Wybraniec and Cordell, 1994), while pos i tive anom a lies to the Pa leo zoic gab bro-syenite mas sif of Pisz and the com pos ite, small carbonatite-syenite mas sif of Tajno (Fig. 5, e.g., Krzemiñska et al., 2006).
Char ac ter is tic fea tures of Md are nar row, lin ear anom a lies, usu ally strik ing NW–SE, and thus par al lel to the TTZ. They may be re lated to mag matic dykes. The geo graphic ex tent of Md mostly over laps the Late Svecofennian Mazowsze orogenic do - main (Fig. 5; Krzemiñska et al., in press).
CIECHANÓW ZONE
The NNE-trending Ciechanów zone (Cz) is a prom i nent pos i - tive mag netic belt of mod er ate to high am pli tudes, bound ing Md in the north-west (Fig. 4). This re gional fea ture ter mi nates to the SW within PCz. The Pa leo zoic syenite in tru sion of M³awa oc curs within the belt (Fig. 5). This is ex pressed as a lo cal anom aly with a re duced am pli tude value. Note that Cz is now sup posed to be - long to the geo log i cal Mazowsze Do main ac cord ing to the re cent geo log i cal stud ies (Krzemiñska et al., in press).
POMERANIA–MAZURY DOMAIN
In the north and north-west, Md and Cz bor der the E–W trending Pomerania–Mazury do main (PMd) that has a com pli - cated struc ture and a very di ver si fied mag netic pat tern (Fig. 4).
This is a belt-shaped Mesoproterozoic do main ear lier termed as the Mazury Com plex that is com posed of rocks as so ci ated with AMCG mag matic rocks emplaced along an E–W trending lin ea ment in north ern Po land and south ern Lith u a nia (Wiszniewska et al., 2002). Char ac ter is tic fea tures of this zone are dis tinct mag netic anom a lies re lated to the dif fer ent groups of in tru sive rocks (Wiszniewska, 2002; Skridlaite et al., 2003;
Bagiñski et al., 2007; Krzemiñska et al., 2009b, in press). The strong neg a tive mag netic lo cal anom a lies are re lated to the Mesoproterozoic an or tho site mas sifs of Kêtrzyn and Suwa³ki (Fig. 5; Cieœla and Wybraniec, 1998; Cieœla et al., 1998;
Wiszniewska et al., 2002). The lat ter con sists also of gab - bro-norite, gab bro and diorite, host ing Fe-Ti-V ore de pos its (Wiszniewska and Petecki, 2014). The pos i tive anom a lies co in - cide with gab bro, norite, monzodiorite and granodiorite in tru - sions, as con firmed by nu mer ous drillings (Wiszniewska, 1995).
The Pa leo zoic syenite mas sif of Olsztynek is also dis tin guished in this do main.
BALTIC DOMAIN
The Bal tic do main (Bd) is char ac ter ized by a re gional mag - netic high with a su per im posed mo saic pat tern of strong pos i - tive mag netic anom a lies (Fig. 4) as so ci ated with early Mesoproterozoic AMCG magmatism. It is sep a rated from PMd by a nar row lat i tu di nal zone of mag netic low. This mag netic do -
main is now de fined as the Late Svecofennian Pomerania-Blekinge Belt (Fig. 5; Krzemiñska et al., in press).
WEST EUROPEAN PLATFORM PROVINCE
The West Eu ro pean Plat form prov ince strongly dif fers from the East Eu ro pean Cratonic prov ince mainly by its weakly dif - fer en ti ated mag netic field. The fol low ing main do mains can be dis tin guished: Up per Silesia–Ma³opolska do main (USMd), Sudetic do main (Sd), Cen tral and West ern Po land do main (CWPd), and West ern Pomerania do main (WPd; Fig. 4).
UPPER SILESIA–MA£OPOLSKA DOMAIN
The Up per Silesia–Ma³opolska do main (USMd) of mod er - ate mag netic in ten sity and sev eral mag netic highs of re gional im por tance (Fig. 4) gen er ally con sists of the Up per Silesian Block (USB) and the SW part of the Ma³opolska Block (MB) (Fig. 3; Dadlez et al., 1994). The NE bound ary be tween the USB and MB cor re sponds to the Kraków–Lubliniec Fault Zone (KLFZ) which is marked by the belt of lo cal anom a lies con - nected with bi modal in tru sive rocks (Bu³a et al., 1997; ¯aba, 1999). The south ern part of the do main is dom i nated by the pos i tive Tychy, Jordanów and Nowy S¹cz anom a lies (Fig. 4).
The lat ter two are as so ci ated with the south ward-dip ping Pre - cam brian base ment of the Outer Carpathians (Grabowska et al., 2007, 2011).
SUDETIC DOMAIN
The Sudetic do main (Sd) com prises the Sudetic Mts., the Fore-Sudetic Block and the SW part of the Fore-Sudetic Monocline as far as the Dolsk Fault Zone. The do main has low mag netic field am pli tudes with the ex cep tion of sev eral in ten - sive re sid ual anom a lies as so ci ated with the serpentinized ultra - mafic, diabase or am phi bo lite rocks, e.g. Gogo³ów–Jordanów, Nowa Ruda and Braszowice (Fig. 4; Petecki and Rosowiecka, 2016; Wiszniewska and Petecki, 2016). Nu mer ous in tense lo - cal mag netic anom a lies of small ar eal ex tent oc cur ring in the area are re lated to Ce no zoic (pre-Qua ter nary) volcanites.
One of the most prom i nent mag netic fea ture in the N part of Sd is a zone of pos i tive mag netic anom a lies trending NW–SE. These anom a lies are re lated to the sub-Perm ian Wol sztyn– Leszno High im aged as a deep crustal struc ture by the wide-an gle re flec tion and re frac tion (WARR) P4 seis mic pro file (Grad et al., 2003). The west ern ex ten sion of the zone passes into the Mid-Ger man Crys tal line High (Wonik et al., 2001; Ga briel et al., 2011). The north ern bound ary of this mag netic re gion is ex pressed by the SE-trending mag netic gra di ent zone de fined as the S³ubice–Leszno mag netic lin ea - ment (Fig. 4; Petecki, 2008) and adopted here to trace the NE bound ary of Sd. It ap prox i mately cor re sponds to the Dolsk Fault, a dis tinct crustal bound ary marked on the WARR P4 pro file, which shows a fun da men tal change in crustal struc ture (Guterch and Grad, 2006).
The east ern bound ary of Sd is less clear. How ever, a mag - netic low be tween Sd and USMd is ap par ent. The source of this low co in cides with the Staré Mìsto Belt and its north ern con tin - u a tion in the Fore-Sudetic Block, mark ing the bound ary be -
tween the Moravo-Silesian (E) and Moldanubian/Saxo - thuringian (W) parts of the Sudetes (Mazur et al., 2006), la - belled MSSZ (Moravo-Silesian Su ture Zone) in Fig ure 3.
There fore, it is here as sumed as the east ern limit of Sd.
CENTRAL AND WESTERN POLAND DOMAIN
In the area north and north-east of the S³ubice–Leszno lin - ea ment, in clud ing cen tral Po land, there is a vast mag netic low (Fig. 4) de fined here as the cen tral and west ern Po land do main (CWPd). This mag netic low is bounded to the north by the Szczecin–Stargard Szczeciñski–Pi³a–Inowroc³aw (SSPI) gra di - ent zone (Petecki, 2008). The mag netic field of CWPd has no strong lo cal anom a lies of re gional im por tance.
The ab sence of mag netic anom a lies in this do main sug - gests ei ther con sis tently lower mag ne ti za tion of the base ment rocks in com par i son to the neigh bour ing mag netic do mains, or a smooth top of the base ment at a great depth. It should be noted that the west ern ex ten sion of CWPd in east ern Ger many is also as so ci ated with pre dom i nantly neg a tive mag netic anom - a lies (Wonik et al., 2001; Ga briel et al., 2011). CWPd is char ac - ter ized by the pres ence of a thick low-ve loc ity up per crustal layer (Guterch and Grad, 2006) that could be partly re spon si ble for the gen er ally low mag netic anom aly val ues.
WESTERN POMERANIA DOMAIN
The West ern Pomerania do main (WPd) is lo cated north - east of the SSPI gra di ent zone be tween CWPd in the south - west, Bd in the north and PCz in the north-east. The mag netic field in this area is char ac ter ized by NW–SE-trending low-am - pli tude anom a lies (Fig. 4). This mag netic do main is ter mi nated to the north-east by a steep mag netic gra di ent zone that bor - ders on the re gional mag netic highs of PCz. Ac cord ing to Petecki (2001) the sub dued anom aly pat tern in this area re - flects a con sid er able depth of ~18.5 km to the top of the mag - netic base ment, es ti mated based on the spec tral method of Spector and Grant (1970). This, in turn, sug gests a con sid er -
able dis place ment of mag netic base ment along a gra di ent zone bound ing PCz to the SW, which is in ac cor dance with the WARR seis mic data (Guterch and Grad, 2006). The re sults of mag netic mod el ling (Fig. 6; Petecki, 2008) in di cate that the edge of the el e vated crys tal line base ment of EEC is sit u ated near this gra di ent zone. Prom i nent pos i tive mag netic anom a lies lo cated NE of this gra di ent zone have been mod elled as the sources show ing a con sid er able ver ti cal ex tent and steeply dip - ping edges, and re lated to the struc ture of the EEC crust in the PCz and PMd mag netic do mains (Petecki, 2008).
The south ern bound ary of the do main, de fined by the SSPI gra di ent zone, is best rep re sented as a mag netic con tact at depths of 18–23 km, us ing the Eu ler deconvolution method (Petecki, 2008). The pres ence of a mag netic low over CWPd in - di cates con sis tently lower mag ne ti za tion of the crust con sti tut - ing the do main as com pared to WPd and Sd. In ad di tion, the re - sults of mag netic mod el ling sug gest that the SSPI gra di ent zone rep re sents a NE-dip ping con tact in the mid dle and lower crust (Fig. 6), which is in ac cor dance with the lower crustal and sub-Moho re flec tors dip ping north-eastwards, re vealed on the GB-2B-96 and 25-III-82 pro files cross ing the SSPI zone (Petecki, 2003). These re sults may in di cate that SSPI rep re - sents a crustal-scale south-vergent thrust. Ex ten sion of this zone into north ern Ger many cor re lates well with the Stralsund–Anklam faults sys tem (Hoffmann and Franke, 1997).
The north ern bound ary of Sd ex pressed by the S³ubice-Leszno mag netic lin ea ment (SL in Fig. 6) has been mod elled as a con tact zone of bivergent na ture. While the mag - netic con tact in the up per part of the crust shows a NE’ward dip, the con tact in the mid dle and lower crust dips to the op po site di - rec tion (Petecki, 2008).
CONCLUSIONS
Ten mag netic sur veys made over dif fer ent por tions of Po - land dur ing the past sev eral de cades have been used to com - pile the mag netic data set and to pro duce the most up-to-date to tal in ten sity mag netic anom aly map for the whole coun try. The
942 Zdzis³aw Petecki and Olga Rosowiecka
Fig. 6. Magnetic modelling along A-A’ profile (Petecki, 2008)
SL – S³ubica–Leszno magnetic lineament; for profile location and explanations see Figure 4
global ref er ence field, DGRF 1982.5, was used to elim i nate the ef fect of the Earth’s core mag netic field from the data. The map rep re sents a sub stan tial up grade from the pre vi ous com pi la - tions of mag netic anom aly data for Po land (Karaczun et al., 1978; Petecki et al., 2003). This new com pi la tion has pro vided a view of the var i ous mag netic sig na tures re lated to the ma jor geo log i cal and tec tonic units of the coun try. The RTP and pseudogravity anom a lies were com puted to im prove po si tion - ing of anom a lies and high light mag netic fea tures with dis tinct bound aries and char ac ter is tic anom aly pat terns. These trans - for ma tions clearly show the dif fer ent anom aly sig na tures of the East Eu ro pean Craton and West Eu ro pean Plat form of cen tral and west ern Po land and in di cate the mag netic base ment di vi - sion into smaller do mains.
The new mag netic maps de scribed in the pres ent pa per al - low in te gra tion with other geo phys i cal and geo log i cal data for better def i ni tion of the mag netic base ment. They can be uti lized for a wide range of pur poses, start ing from re gional to even trans-Eu ro pean stud ies. On a re gional, coun try scale, the mag - netic data have re cently been used for con struct ing the geo log i - cal map of crys tal line base ment in the Pol ish part of the East Eu ro pean Plat form (Krzemiñska et al., in press), an a lyz ing the base ment struc ture of the Pa leo zoic Plat form in Po land (Narkiewicz and Petecki, 2017) and the Sudetes and sur round - ing ar eas in SW Po land (Petecki and Rosowiecka, 2016). The new mag netic anom aly map of Po land pro vides an op por tu nity
for fu ture ad vances in the un der stand ing of the Pol ish litho - sphere by in te gra tion of the mag netic data with other ex ist ing geo phys i cal and geo log i cal data.
Ge ol ogy knows no bor ders, so to im prove in ter pre ta tion of the mag netic anom aly pat tern it would be suit able to merge this map with mag netic maps of sur round ing coun tries. This in te gra - tion of mag netic anom aly data will be a pow er ful tool for fur ther eval u a tion of the struc ture and tec tonic evo lu tion of the ar eas that span across na tional bound aries. In this con text, the cross-bor der trac ing of such geo log i cal units as the Mid-Ger man Crys tal line Rise and crustal do mains of EEC would be im por tant for un der stand ing the re gional tec tonic set ting of Cen tral Eu rope.
Ac knowl edge ments. This pa per is based on the re sults of the pro jects funded by the Pol ish Min is try of En vi ron ment through the Na tional Fund for En vi ron men tal Pro tec tion and Wa ter Man age ment: 2.07.0002.00 “Mag netic anom aly map of Po land, scale 1:500,000”; 22.2601.1301.00.1 “Com pre hen - sive, geo phys i cal and geo log i cal in ter pre ta tion of the new im - age of the to tal mag netic field of the Earth in the area of the Sudetes and its fore land”; 21.2101.0010 “Geo log i cal map of crys tal line base ment in the Pol ish part of the East Eu ro pean Plat form, scale 1:1000,000”; 4.94.0517.26.0 “Geo phys i cal at - las of the Carpathians”. Prof. M. Narkiewicz is warmly ac knowl - edged for valu able dis cus sions. We thank S. Mazur and two anon y mous re view ers for their help ful com ments.
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