Petrographic variability of Carpathian sandstones and the problem of sandstone classification

A N N A L E S DE L A SOCIETE G EO LOG IQUE DE PO LO G N E

T o m ( V o l u m e) X X X V I I — 1967 Z e s z y t (F a s c ic u l e ) 4 K r a k ó w 1967

M A R IA N K A M IE Ń SK I, C Z ESŁAW PE SZ A T , JA C EK R U T K O W SK I

ZMIENNOŚĆ PETROGRAFICZNA PIASKOWCÓW KARPACKICH I ZAGADNIENIE ICH KLASYFIKACJI

(4 fig.)

Petrographic v a ria b ility of Carpathian sandstones and the p ro b le m of sandstone classification

(4 Figs.)

STRESZCZENIE

Wstępne badania petrograficzne piaskowców godulskich, istebniań- skich, magurskich oraz piaskowców fliszu podhalańskiego wykonane w Katedrze Złóż Surowców Skalnych AGH wykazały, że ich jakościowy skład m ineralny bez względu na poziom stratygraficzno-facjalny i obszar występowania jest do siebie zbliżony. Zmusza to do badań ilościowych, które stanowią podstawę petrograficznej klasyfikacji piaskowców. Zagad­

nienie to zostało potraktowane bardzo szeroko w literaturze omówionej m iędzy innym i przez M. T u r n a u - M o r a w s k ą (1957), G. K l e i n a (1963) i W. D. S z u t o w a (1965). Piaskowce karpackie w św ietle w y ­ konanych badań (około 500 analiz planimetrycznych) odznaczają się zmiennością w ilości poszczególnych składników. D otyczy to nie tylko piaskowców pochodzących z danego poziomu stratygraficzno-facjalnego (fig. 2, 3, 4), ale także próbek z tego samego odsłonięcia, a naw et w pew ­ nym stopniu z jednej i tej samej ław icy (fig. 1), które często znajdują się w dwóch sąsiadujących ze sobą polach trójkąta projekcyjnego, repre­

zentujących różne odmiany piaskowców.

Zmienność w obrębie poszczególnych ław ic wiąże się w znacznym stopniu z w ielkością ziarna materiału klastycznego. Ilość okruchów skał obcych jest na ogół wyższa w próbkach gruboziarnistych niż w drobno­

ziarnistych, bowiem w tych ostatnich uległy one dezintegracji. Odwrotnie zachowują się glaukonit, łyszczyki i spoiwo, których ilość zazwyczaj wzrasta w miarę zmniejszania się wielkości ziarna. Związane z tym ilo­

ściowe zmiany składu mineralnego mogą być rzędu kilku, a naw et kilku­

nastu procent. Powoduje to, że piaskowce gruboziarniste posiadają za­

zwyczaj bardziej szarogłazowy charakter, a drobnoziarniste są bardziej kwarcowe. U wydatnia się to szczególnie dobrze w przypadku w arstw o­

w ania frakcjonalnego. Przy normalnym warstwowaniu frakcjonalnym próbki ze spągowej części ław icy są wzbogacone w okruchy skał obcych, a w ięc z tego tytułu przybierają bardziej szarogłazowy charakter.

W związku z przedstawioną zmiennością podział trójkąta projekcyj­

nego na liczne, a tym sam ym bardzo wąskie pola mające przedstawiać różnego rodzaju odmiany piaskowców, jak to czynią niektórzy autorzy, w ydaje się mało uzasadniony. Stąd też w pracy zastosowano stosunkowo prosty podział M. T u r n a u - M o r a w s k i e j (1957), który został nieco

zm odyfikowany (fig. 1).

3*

W zastosowanej klasyfikacji piaskowce z poziomu dolnego warstw godulskich stanowią najczęściej piaskowce oligomiktyczne i kwarcowe, rzadziej szarogłazowe (fig. 2). W poziomie środkowym są to zazwyczaj piaskowce szarogłazowe, rzadziej arkozowe, oligomiktyczne i szarogłazy.

Typowe piaskowce górnogodulskie reprezentują piaskowce oligomiktyczne, rzadziej arkozowe i szarogłazowe, w yjątkow o kwarcowe. Odrębny cha­

rakter mają gruboławicowe i gruboziarniste piaskowce tworzące w B es­

kidzie Śląskim wkładki w najwyższej części górnych w arstw godulskich, reprezentujące szarogłazy i piaskowce szarogłazowe. Piaskowce istebniań- skie znajdują się w polach piaskowców arkozowych, oligom iktycznych i szarogłazowych (fig. 3). Piaskowce trzeciorzędowe posiadają na ogół podobny charakter jak piaskowce środkowogodulskie. Piaskowce magur­

skie stanowią najczęściej piaskowce szarogłazowe, w m niejszym stopniu arkozowe. Znacznie rzadziej w ystępują tutaj piaskowce oligomiktyczne, szarogłazy i arkozy (fig. 4). Piaskow ce fliszu podhalańskiego stanowią piaskowce szarogłazowe, rzadziej szarogłazy (J. B r o m o w i c z, Z. R o ­ w i ń s k i , 1965).

Wśród badanych piaskowców Karpat fliszow ych najczęściej reprezen­

towane są piaskowce szarogłazowe, stanowiące 39% uw zględnionych pró­

bek, w m niejszym stopniu piaskowce oligomiktyczne (26%) i -arkozowe (24%). Rzadziej i tylko w niektórych seriach w ystępują szarogłazy (6%) i piaskowce kwarcowe (4%), a sporadycznie arkozy (1%).

Na tle przeprowadzonych badań należy stwierdzić, że określenie charakteru i zmienności piaskowców fliszow ych musi się opierać na licz­

nych próbkach. W inny być one pobierane z uw zględnieniem zmian uziarnienia w obrębie poszczególnych ławic, kierunków z jakich m ateriał klastyczny był dostarczany do zbiornika sedym entacyjnego oraz procesów dia- i epigenezy.

K a t e d r a Z ł ó ż S u r o w c ó w S k a l n y c h A k a d e m i i G ó r n i c z o - H u t n i c z e j w K r a k o w i e

*

* *

A b s t r a c t . In th e p r e sen t stu d y, th e v a r ia b ility in m in e r a l com p o sition of so m e sa n d sto n e s fro m th e P o lish F ly sc h C arpathians is d iscu ssed , to g eth er w ith th e p rob lem of th e ir c la ssifica tio n . T h is v a r ia b ility is so m e tim e s v e r y m ark ed , b eco m in g co n sp icu o u s in p a rticu la r stratigrap h ic and fa cie s horizon s and e v e n w ith in s in g le beds. A lth o u g h su ch v a r ia b ility calls for the ap p lica tio n of a r e la tiv e ly sim p le p etrograp h ic c la ssifica tio n , sa n d sto n es fro m th e sa m e stra tig ra p h ic and fa cie s h o r i­

zon u su a lly occur in se v e r a l fie ld s, r e p r e se n tin g d iffe r en t p etrograp h ies. F urtherm ore, sa m p les from o n e and th e sa m e bed m ay re p r ese n t d iffe r en t 'types of san d ston e. T h is a rises fro m ch a n g es in g r a in -size , cau sed by th e e x is t e n c e of graded b edding. In th e P o lish F ly sc h C arpathians, g r e y w a e k e — sa n d ston es p red o m in a te, and to a le s s e r e x te n t, olig o m ictic and arkosic sa n d sto n e s occur. G re y w a ck es and q u artz sa n d sto n e s are fou n d m ore ra rely , and a rk oses seld o m occur.

IN T R O D U C T IO N

In this preliminary study, attention is drawn to only one problem of the lithology of the Carpathian sandstones, nam ely that of their varia­

bility, and connected w ith this, the problem of their classification. The

discussion is based on around 500 planim etrie analyses carried out in the Department of Non- Metallic Mineral Deposits, Academy of Mining and Metallurgy, Kraków. Here the follow ing are considered: the Go­

dula Sandstones (Turonian — Lower Senonian), th e Istebna Sandstones (Senonian — Paleocene), the Magura Sandstone (Eocene) and the Pod­

hale F lysch sandstones (Eocene). The stratigraphic position of the Carpathian sandstones are discussed by F. B i e d a et al. (1963). Problem s of the palaeogeography and sedimentation of the sandstones are consider­

ed by M. K s i ą ż k i e w i c z , in a 1960 paper and w ith other authors in the Stratigraphic and Facies Atlas of the Carpathians, edited by the last-m entioned author (1962), and also by R. U n r u g (1963).

Samples of the sandstones investigated came exclusively from the western part of the Polish Flysch Carpathians. The greatest number of samples investigated (185) came from the Godula Sandstones. Sandstones of the Lower Godula Beds horizon (70 samples) w ere sampled in the Bielsko-Biała region (Wisła, Obłaziec, Czantoria, Straconka) at Porąbka as w ell as at Zagórnik and Rzyki near Wadowice. Sandstones from the middle horizon of the Godula Beds (80 samples) w ere selected for sampl­

ing in the Bielsko region (Brenna and Szyndzielnia), in the W adowice region (Rzyki, Barwałd, Sułkowice) at Wierzbanowa, near M yślenice, and at Bieśnik, near Czchów. Samples (40 in all) of typical Upper Godula sandstones w ere taken in the stream Gołaszowski (Bielsko region), as w ell as in the W adowice area (Mucharz and Sułkowice).

Samples of the Istebna Sandstones (140 samples) w ere collected in the regions of Bielsko (Wisła Głębce, Istebna, Straconka), Żywiec (Kamesz­

nica), W adowice (Mucharz, Kalwaria, Sułkowice), M yślenice (Droginia), Bochnia (Wiśnicz, Królówka, Muchówka, Sobolów, Lipnica) and Czchów (Czchów, Melsztyn, Charzewiee). The Istebna Sandstones from the Boch­

nia and Czchów regions are considered on the basis of samples described by K. S k o c z y l a s - C i s z e w s k a and M. K a m i e ń s k i (1959).

The Magura Sandstone is represented by 160 samples taken from the region of Żywiec (Korbielów), M yślenice (Lubień and Tenczyn), Lima­

nowa, as w ell as N owy Sącz (Klęczany, Kamionka, Wierchomla). Here also the results of studies made by S. S i l i w o ń c z u k (1965) in Ka­

mionka, near N owy Sącz, are utilised. Podhale Flysch sandstones of the N owy Targ region are described after J. B r o m o w i c z and Z. R o w i ń ­ s k i (1965).

The qualitative mineralogical compositions of Carpathian sandstones, irrespective of stratigraphic and facies horizon or locality, are, as a rule, similar. This is particularly true for quartz, feldspars, micas and glauco­

nite, and to a lesser degree for rock fragm ents and cement. The cem ent of Carpathian sandstones is fairly variable, both in composition and in the amount present. It is necessary to emphasize, however, that certain types of cement are characteristic for particular series. Among the components of the cement, strongly crushed, fragmental material, w ith diameters less than 0.01 mm. („matrix”) should be mentioned. Silica is another component of the cement, occurring in the form of microgranular aggregates of quartz, quartz-chalcedony or chalcedony-opal, and also being developed as m inute regeneration rims. A common constituent of the cement is calcium carbonate, recrystallized to a very variable degree.

This either fills the voids betw een the grains or forms the bulk of the rock. To a markedly lesser degree, chloritic material, glauconite and iron compounds, w hich usually play the role of colouring pigm ents w ithin

the rooks, occur as cement components. The cement constituents m ention­

ed seldom occur separately, and are usually seen in varying proportions.

Thus the cem ent of Carpathian sandstones also possess a polym ineralic character. The amount of cement present is very variable and w ithin the lim its of particular beds sometimes fluctuates w idely. This factor is related to the conditions of sedimentation as w ell as to diagenetic and epigenetic changes. As a result of the latter, fragm ents of lim estone som e­

tim es undergo recrystallization and grains of quartz and feldspar are resorbed, thus enriching the cement.

The qualitative study of mineralogical composition does not generally lead to the same kind of results as those arising from quantitative work, upon w hich latter rest the petrographic classifications of sandstones. The problem of a genetic classification of sandstones has been w idely discussed in geological literature (e. g. K. Ł y d k a 1955, M. T u r n a u - M o r a w - s k a 1957, G. K l e i n 1963, E. F. M c B r i d e 1963, R. H. D o t t 1964, V. D. S h u t o v 1965, G. N. B r o v k o v and A. E. M o g i l e v 1965). In the m ajority of studies, authors show variability in mineralogical composition of sandstones on a triangular projection. The constituents located at the vertiotes of the triangles, as w ell as the boundaries of the fields adopted for particular varieties of sandstone, are very variable.

An investigation of mineralogical composition shows that the Carpath­

ian sandstones are generally characterized by a great variability in the proportions of particular constituents, frequently seen as a scattering of projection points over a considerable part of th e triangle. This is shown not only by sandstones from a given stratigraphic and facies horizon (Fig. 2, 3, 4), but also samples from the same exposure, and to a certain degree, even from one and the same bed. In Fig. 1, the last-m entioned type of variability is shown for m aterial representing different sandstone series. The separate points indicating samples taken from the very same bed are joined by lines. Variability w ithin a bed m ay be fairly marked, and this phenomenon is seen in all the sandstone series investigated.

The variability of mineralogical composition in particular sandstone beds is to a marked degree related to the sizes of the clastic mineral grains. First and foremost, this concerns fragments of exotic rocks, the proportion of w hich is generally higher in coarse-grained samples than in those w hich are made up of fine grains. It is a proven fact that in the fine fraction, fragm ents of exotic rocks are m ainly seen as their disinte­

gration products, monomineralic constituents. On the other hand, the amounts of glauconite, micas and cement usually increase in proportion to a decrease in the size of the clastic material. In connection w ith this last point, the quantitative differences in mineralogical composition m ay be in th e order of several or even a dozen or more percent. This means that samples of coarse-grained sandstone have th e character of grey- wacke-sandstone, w hile those of fine grain-size are more quartzose. This is particularly conspicuous in the case of beds showing graded bedding, a characteristic feature of flysch sandstones. It should here be m entioned that attention has already been called to the relationship betw een m inera­

logical composition and grain-size by, for instance, G. F i s c h e r (1934).

The existence of this type of variation in mineralogical composition w ithin particular beds and also w ithin stratigraphic and facies units has great significance for the classification of sandstones. Furthermore, the division of the projection triangle into numerous, narrow fields to repres­

ent different types of sandstones appears to be artificial and poorly sub­

stantiated. Thus as a basis for further considerations, the relatively simple classification scheme o f M. T u r n a u - M o r a w s k a (1957) is used in the present study, w ith only slight ammendments (Fig. 1). M. Turnau-Moraw- ska’s quartz-sandstone (loc. cit.) included rocks w ith more than 80%

quartz, w hile here the term is restricted to sandstones w ith more than 90% of this constituent. Here also rocks containing 80— 90% quartz are

KWARC QUARTZ

ROCKS FRAGMENTS ’ O FELP3PARS

♦ MICAS

Fig. 1. Z m ien n o ść sk ład u m in e r a ln e g o w obrębie p oszczeg óln y ch ła w ic p ia s k o w c ó w na tle tró jk ąta k la s y fik a c y jn e g o sto so w a n e g o w pracy: 1 — p ia s k o w c e g o d u lsk ie;

2 — p ia sk o w c e iste b n ia ń sk ie; 3 — p ia s k o w c e m ag u rsk ie. L in ia m i p o łączon o p u n k ty o d p o w ia d a ją c e próbkom p o ch o d zącym z jed n ej i tej sa m e j ła w ic y : I — p ia s k o w c e k w a rc o w e; II — p ia sk o w c e o lig o m ik ty c z n e ; III — p ia sk o w c e szaro głazow e; IV —

p ia s k o w c e a rkozow e; V — szarogłazy; V I — a rk ozy

Fig. 1. V a r ia b ility in m in e r a lo g ic a l com p osition in th e lo w e r p arts of p articu lar sa n d sto n e beds, sh o w n on th e c la ssific a tio n tr ia n g le adopted in th e p r e sen t study:

I — G odula San d ston e; 2 — Isteb n a S an d ston e; 3 — M agura S a n d sto n e. L in e s jo in in g p o in ts in d ica te sa m p le s co m in g fro m th e sa m e bed. I — q u a rtz-sa n d sto n es;

II — olig o m ictic sa n d sto n es; III — g r e y w a c k e -sa n d s'to n e s; IV — arkosic sa n d ston es;

V — g r e y w a c k e s; V I — arkoses

termed oligomictic sandstones. In spite of this simplification in subdivis­

ion, samples collected by the authors from one bed frequently occur in two neighbouring fields of the triangular projection, representing differ­

ent types of sandstone.

T E R M IN O LO G Y OF THE S A N D S T O N E S D IS C U S S E D

The greatest number of samples investigated by the authors from among the previously mentioned Carpathian sandstones came from th e Godula Beds. The variability in mineralogical composition of the three horizons here distinguished is shown in Fig. 2. The sandstones from the

lower horizon have the highest quartz content, as w ell as the low est amounts of feldspar, exotic rock fragments and micas. Their projection points are in the oligomictic and quartzose sandstone fields, and rarely in that of the greywacke-sandstones. The sandstones from the middle horizon have a lower and more variable quartz content, and more rock fragm ents and micas. These are m ainly greywacke-sandstones, rarely arkosic sandstones, oligom ictic sandstones and greywackes. The typical

KWARC QUARTZ

ROCKS FRAGMENTS FELDSPARS

+ MICAS

Fig. 2. Z m ien n ość p ia s k o w c ó w godulskich : 1 — poziom dolny; 2 — poziom środ k o w y ; 3 — poziom górny

Fig. 2. V a ria b ility in th e G odula Sa n d ston e: 1 — L o w e r H orizon, 2 — M id d le H orizon, 3 — U p per H orizon

Upper Godula sandstones are characterized by a som ewhat higher and less Variable quartz content and usually represent oligom ictic sandstones, rarely arkosic sandstones and greywacke-sandstones, and seldom quartz- -sandstones. The thick-bedded and coarse-grained sandstones forming intercalations in the uppermost par of the Upper Godula B eds display a variable character. These rocks (6 samples), exposed in the stream Goła- szowski (near Bielsko), occupy a separate field in the triangle, comprising exclusively greywackes and greywacke-sandstones.

W ithin the Istebna Sandstones, w hich rest stratigraphically upon the Godula Beds, upper and low er levels are distinguished. The samples investigated prelim inarily by the authors, representing both of these horizons, show no great differences in petrographic composition and thus appear together on the graph (Fig. 3). B y comparison w ith the Godula Sandstones, they have a som ewhat low er quartz content and their pro­

jection points occur in the fields of arkosic sandstones, oligomictic sandstones and greywacke-sandstones. It m ay also be m entioned that the field in which the Istebna Sandstones appear occupies the axial part of the triangle.

The Tertiary sandstones investigated displayed in the triangular projection a character similar to that of the Middle Godula Sandstone.

The Magura Sandstone showed a variable quartz content and is repres­

ented by projection points most frequently found in the greywacke-sand- stone field, and to a lesser degree in the arkosic sandstone field (Fig. 4).

Markedly more rarely found are oligom ictic sandstones, greyw ackes and arkoses. The Magura Sandstone of Babia Góra was the subject of petro- graphic investigations by T. W i e s e r (1963, 1966). This author employed

K W A R C Q U A R T Z

ROCKS FRAGMENTS r ELDSPARS

+ MICAS

Fig. 3. Z m ien n o ść p ia sk o w c ó w iste b n ia ń sk ich Fig. 3. V a r ia b ility in th e Isteb n a S a n d sto n e

K W A R C Q.UARTZ

+ MICAS

Fig. 4. Z m ien n o ść n ie k tó r y c h p ia sk o w c ó w p aleogeń sk ich : 1 — p ia sk o w c e m a gu rsk ie;

2 — p ia sk o w c e flis z u p od h a la ń sk ieg o

Fig. 4. V a r ia b ility in so m e P a la e o g e n e san d ston es: 1 — M agura S a n d sto n e; 2 — sa n d sto n e s from th e P o d h a le F ly sc h

the triangular projection of C. Gilbert (H. W i l l i a m s , F. T u r n e r , C. G i l b e r t 1954) and his results are not at variance w ith those obtained in the present study.

The Podhale Flysch sandstones are considered on the basis of tjhe work of J. B r o m o w i c z and Z. R o w i ń s k i (1965). These rocks show a markedly sm aller variation in mineralogical composition. Their project­

ion points lie in the field of greywacke-sandstones and only in insigni­

ficant numbers enter th e greywaoke field.

A. Ś l ą c z k a and R. U n r u g (1966) used a triangular projection similar to the one employed in the present study (Fig. 1), but subdivided the triangle in a som ewhat different manner. The study made by the last-m entioned authors dealt w ith some Eocene-Oligocene sandstones from th e eastern part of the Polish Carpathians. The small number of samples from the particular horizons studied by these authors does not, however, permit a broad comparison w ith the material described in the present study. It is only possible to remark that in the classification scheme used in the present account, the Mszanka Sandstone represents oligomictic and quartz-sandstones, w h ile the Cergowa Sandstone is found in the greywacke and greywacke-sandstone fields. The Kliwa Sandstone comprises quartz-sandstones, oligomictic sandstones, greywacke-sand­

stones and greywackes. The sandstones from the M enilitic Shales are quartz-sandstones.

CO N C LU D IN G R EM A R K S

From the descriptions of these preliminary investigations, it is seen that w ithin particular stratigraphic and facies horizons of the Carpathian sandstones, a variability in mineralogical composition is found, w hich as shown in the triangular projections included, is betw een 20— 35%.

This means that sandstones from the very same horizon, in spite of the use of a relatively simple classification scheme, generally occur w ithin the boundaries of three, and som etimes even four or five fields represent­

ing different types of sandstone. This variability is marked, as m entioned above, w ithin particular beds, especially in the case of graded bedding.

With normal graded bedding, samples taken from the basal part of the bed are enriched in fragments of exotic rocks, and thus have a character more approaching that of greywackes.

On the basis of work carried out up to the present time, it m ay be concluded in the Polish Flysch Carpathians, follow ing the classification adopted, greywacke-sandstones are most frequently represented, compris­

ing 39% of the sam ples investigated. Oligomictic sandstones (26%) and arkosic sandstones (24%) occur more rarely. Greywackes (6%) and quartz- -sandstones (4%) are decidedly rare, only occurring in certain series.

Samples w ith the character of arkoses (1%) occur quite sporadically.

It should also be stated that the definition of the character and variability of flysch sandstones, and also of other sandstones derived in the course of intensive erosion and orogenic movements, must be based on numerous samples. These must be selected so as to take into account

changes in grain properties w ithin particular beds, the direction from which clastic material was supplied to the sedim entary basin, as w ell as diagenetic and epigenetic processes.

T r a n l a t e d b y

B. M a r s z a l a n d F. S i m p s o n D e p a r t m e n t of N o n - M e t a l l i c M in e r a l D e p o s i ts ,

A c a d e m y of M in in g a n d M e t a l l u r g y K r a k ó w

W Y K A Z L IT E R A T U R Y R EFER EN CES

A tla s G eo lo g iczn y P o lsk i (1962), Z a gad n ien ia S tr a ty g r a fic z n o -F a cja ln e . Z. 13. K reda i sta rszy trzeciorzęd w P o lsk ic h K arp ata ch z ew n ętrzn y ch (G eological A tla s of P oland. S tra tigra p h ic and F a cial problem s. F asc. 18. C retaceous and E arly T ertiary in the P o lish E x te r n a l C arpathians). Inst. Geol., W arszaw a.

B i e d a F., G e r o c h S., K o s z a r s k i L., K s i ą ż k i e w i c z М. , Ż y t k o К . (1963), S tra tig ra p h ie des K arp ates E x tern es P o lo n a ise s (Стратиграфия В неш них П олских Карпат). Biul. Inst. Geol. 181, pp. 5— 174, W arszaw a.

B r o m o w i c z J., R o w i ń s k i Z. (1965), K ilk a u w a g o p ia sk o w c a c h flis z u p o d h a­

la ń sk ie g o (Som e rem ark s on th e sa n d sto n e s from th e P o d h a le F lysch ). K w a r t . geol.

9. nr 4, pp. 837— 856. W arszaw a.

B r o v k o v G. N. , M o g i l e v A. E. — Б р о в к о в Г. H. , М о г и л е в А. Е. (1965), К вопросу о классификации теригенны х осадочны х пород по вещ ественном у составу (То th e problem of a c la ssific a tio n of terrig en ou s se d im e n ta ry rocks b y th e ir m a te r ia l com p osition). Литология и П олезны е И скопаемы е (L i t h o l o g y and m i n e r a l r e s o u r c e s ) nr 6, pp. 67— 74, M oskw a.

D o 11 R. H. Jr. (1964), W acke, g r a u w a c k e and m a tr ix — w h a t approach to im m a tu re sa n d sto n e cla ssific a tio n . J. S e d i m e n t . P e tro l. 34, no. .3, pp. 625— 632.

F i s c h e r G. (1934), D ie P etro g ra p h ie der G rau w ack en . J. P re uss. Geol . L a n d e s a n s t . 54, pp. 320—'343. (za r. 1933). B erlin.

K l e i n G. V. (1963), A n a ly s is and r e v ie w of sa n d sto n e c la s sific a tio n in t h e N orth A m erica n g eo lo g ic a l lite r a tu r e 1940'—'I960. Bull. Geol. Soc. A m e r . 74, no. 5, pp. 555— 576.

K s i ą ż k i e w i c z M. (1960), Z arys p a le o g eo g r a fii p o lsk ich K arp at flis z o w y c h (O ut­

lin e of th e p a leo g eo g ra p h y in the P o lish F ly s c h C arpathians (Pr. Inst. Geol. Э0, cz. II, pp. 209— 249, W arszaw a.

Ł y d k a К. (1955), Stu d ia p etro g ra ficzn e nad perm ok arb on em k r a k o w sk im (P etro- graphic stu d ies co n cern in g th e P erm o-C arb on iferou s of th e C racow R egion). Biul.

Inst. Geol. 97, pp. 1,15— 227, W arszaw a.

M e B r i d e E. F. (1963), A c la ssific a tio n of com m on sa n d sto n es. J. S e d i m e n t . Petrol.

33, no. 3, pp. 664r—669.

S h u t o v V. D. — Ш утов В. Д. (1965), О бзор и анализ минералогических класси- фикаций песчаных пород (по работам Ам ериканских и Р усск и х литологов за последни е двадцать лет). R e v ie w and a n a ly sis of m in e r a lo g ic a l c la ssific a tio n s for aren aceou s rocks in th e papers of A m erica n and R u ssia n lith o lo g ists for th e p ast tw e n ty years). Литология и полезны е иокопае-мые (L ithology and m in e r a l resources), nr 1, pp. 95—ill2. M oskw a.

S i l i w o ń c z u k Z. (1965), P ia sk o w c e m a g u r sk ie okolic K a m io n k i W ielk iej k oło N o w eg o Sącza jako m a te r ia ł b u d o w la n y (The M agura S a n d sto n e s in th e v ic in itie s of K a m ion k a W ielk a n e a r N o w y Sącz as b u ild in g m aterial). Prz. geol. 13, nr 2, pp. 60— 63, W arszaw a.

S k o c z y l a s - C i s z e w s k a K. , K a m i e ń s k i M. (1959), O fa c ji in o c er a m o w e j w a r s tw iste b n ia ń sk ich Pogórza W iśn ic k o -R o ż n o w sk ie g o (On th e In ocera m ia n F a ­ d e s of th e Isteb n a B ed s of th e W iśn ic z -R o ż n ó w R egio n (F lysch C arpathians).

K w a r t . geol. 3, nr 4, pp. 977— 995, W arszaw a.

S i ą c z k a A. , U n r u g R. (1966), Z b ad ań nad stru k tu ram i se d y m e n ta c y jn y m i i p etro g ra fią n ie k tó r y c h serii p ia sk o w c o w y c h z łu p k ó w m e n ilito w y c h K arp at (S ed im en tary stru ctu res and p etro lo g y of so m e sa n d sto n e m em b ers of th e M e n i- li'te B eds, C arpathians). Rocz. Pol. T o w . Geol. 36, z. 2, pp. 155— 180, K rak ów . T u r n a u - M o r a w s k a M. (1957), Z a g a d n ie n ie g e n e ty c z n e j k la s y fik a c ji p ia s k o w ­

c ó w (The problem of g e n e tic c la ssific a tio n of sa n d sto n es). A r c h . M in er . 20, z. 1— 2, pp. 169— 190, (za r. 1956), W arszaw a.

U n r u g R. (1963), W a r stw y iste b n ia ń sk ie — stu d iu m se d y m e n to lo g ic z n e (Istebna B ed s — a F lu x o tu r b id ity F o rm a tion in th e C arpathian F lysch ). Roc z. Pol. T o w . Geol. 33., z. 1, pp. 49— 92, K rak ów .

W i e s e r T. (1963), C h a ra k tery sty k a p etrograficzn a p ia sk o w c ó w m a g u r sk ic h z B e ­ s k id u Ś red n ieg o (P etro g rap h ica l fe a tu r e s of th e M agura S a n d sto n e s from th e M id d le B esk id R ange). K w a r t . geol. 7, nr 2, pp. 282—294, W a rszaw a.

W i e s e r T. (1966), Z p e tro g r a fii reg io n u B a b iej G óry. P r z ew o d n ik X X X I X Z jazdu P o lsk ie g o T o w a r zy stw a G eologicznego. B a b ia G óra 2— 5 c z er w ca 1966, W arszaw a.

W i l l i a m s H. , T u r n e r F., G i l b e r t C. (1954), P etro gra p h y . U n iv . of C alif.

P ress, S a n F rancisco.