A N N A L E S S O C I E T A T I S G E O L O G O R U M P O L O N I A E R O C Z N I K P O L S K I E G O T O W A R Z Y S T W A G E O L O G I C Z N E G O
V, Я —Д/2: 3—44 K ra k ó w 1981
Andrzej Śl ą c z k a, Sam Th o m p s o n III
A REVISION OF THE FLUXOTURBIDITE CONCEPT BASED ON TYPE EXAMPLES
IN THE POLISH CARPATHIAN FLYSCH
(PL I—VI and 15 Figs.)
R ewizja pojęcia jluksoturbidyt, w oparciu o przykłady z polskich K a rp a t fliszowych
(PI. I—VI i 15 fig.)
Andrzej S ł ą c z k a , S a m T h o m p s o n III: A revision of th e flu xotu rb id ite concept based on tyjpe exam p les in the P olish Gaxpajfchiiam Flysch. Ann. Soc. GeoL Poloniae, 51— 1/2: 3— 44, 1981. Kraików.
A b s t r a c t : A flu xotu rb id ite is redefined as th e depositional product of com posite sedim ent, gravity flow , w ith a gravity grain flo w (or related type) in th e low er part and a turbidity flow in the upper part. A m odel of a com plete flu xotu rb id ite (FT) bed is constructed; it consists o f a 5 m com posite bed of conglom erate and san dston e w ith a th in m udstone at th e top. The low er (F) part is gen erally m assive (internal lam ination is absent) w ith coarser grains dispersed am ong th e finer; th e transport m echanism is considered to be a grain flow , although som e zones m ay b e produced by liqu efied sedim ent flow . The upper (T) part is essen tially a Boum a seq u en ce (Ta to Te), and represents deposition from a turbidity flow .
Fluxoturhidites form sign ificantly coarser parts of subm arine can yon -fan de- posdtional system s th an norm al turbidites, and m ay exten d into distal parts of th e fan. Fluxoturbidites gen erally are cleaner sandstones and conglom erates, and constitute better reservoir objectives in petroleum exploration th an norm al tu r
bidites w hich g en erally are muddy.
K e y w o r d s : fluxoturbidite, fluxotu rb id ite m odel, gravity flow , flysch, Carpathians
Andrzej S ł ą c z k a : In stytu t N auk G eologicznych, U n iw ersytet Jagielloński, ul. O leandry 2a, 30-30063 Kraków, (Poland)
Sam T h o m p s o n III: N ew M exico Bureau of M ines and M ineral Resources.
Socorro, N ew M exico 87801, USA m anuscript received: M ay 1980
l*
accepted, July, 1980
— 4 —
T r e ś ć : B adania typow ych osadów flu k soturbidytow ych polskich Karpat flisz o w y ch w sk azu ją, że (tworzenie się law ie fluksoturbidytow ych było w y n ik iem złożo
n ego procesu sedym entacyjnego rozpoczynającego się potokami piaszczystym i, a kończącego się norm alnym i prądami zaw iesin ow ym i. Zaproponowany został k o n cepcyjny m odel pełnego fluksoturbidytu. Osady fluksoturbidytow e są charaktery
styczn e dla proksym alnych części stożków podm orskich, a niekiedy budują praw ie ca łe stożki turbidytow e.
INTRODUCTION
A fter th e concept of fluxoturbidite was introduced by Dzulynski, Ksiqzkiewicz, and K uenen (1959), m any w orkers recognized deposits of a sim ilar type associated w ith norm al turbidites in several deep- m arine basins around the world. In general, fluxoturbidites are cha
racterized by thick beds (several m eters) of sandstone and conglomerate th a t tend to be nongraded and lacking in in tern al stratification (at least in the low er part), in contrast to the norm al turbidites th a t are graded and contain a sequence of internal layers defined in the model of Bouma (1962).
F or m an y units of flysch in th e C arpathian M ountains of Poland, Dzulynski and others (1959) listed several different examples of fluxo
turbidites. The mechanism of sedim entary tran sp o rt was inferred tp be interm ediate betw een subm arine slum ping-sliding and tu rb id ity flow, b u t several processes were implied. The fluxoturbidites in the Istebna Beds were described in detail by U nrug (1963), and the sedim entary processes w ere interpreted; th a t paper rem ains one of the best docu
m entations of the fluxoturbidite concept in the type area.
Some geologists, for exam ple W alker (1967, 1970), recom mend th a t th e term “flu x o tu rb id ite” should be abandoned and th a t the concept be incorporated into “proxim al tu rb id ite ”. Not all agree, for exam ple Schlager W. and Schlager M. (1973); and some would keep the te rm b u t m odify th e concept of the sedim entary mechanism, for exam ple C arter (1975). In this paper, we w ill review these concepts and p ro blems, and propose revisions.
In addition to the significance of fluxoturbidites in sedimentology, we are also concerned w ith th e ir im portance in the exploration and developm ent of petroleum resources in deep-m arine basins. The rese r
voir quality of the cleaner sandstones and conglomerates in flu x o turbidites tends to be m uch b e tte r th a n th a t of norm al turbidites. In Poland, the fluxoturbidite reservoirs have produced up to 3,900 barrels of oil per day, averaging 300 to 400 barrels p e r day, w hereas those in norm al tu rb id ites usually produce 10 barrels p er day or less. Con
trastin g ra te s of petroleum production also are reported in o th er basins.
We plan to discuss this subject fu rth e r in a subsequent paper.
— 5 —
A t Sl^czka’s invitation, Thompson m ade th ree vacation trip s to Po
land to see w ith him several of the typical exam ples of fluxoturbidites in th e C arpathian Flysch. Based on the first two reconnaissance trips in 1972 and 1973, a prelim inary model for fluxoturbidites was presented at the International Congress of Sedim entology in Nice (Slqczka and Thompson, 1975). D uring the th ird trip in 1977, the key exposures w ere described in detail and the im proved model of the present paper w as developed.
We are indebted to m any geologists whose w ork and guidance have facilitated our stu d y of fluxoturbidites. Only a few of them are m en
tioned specifically in this brief paper. Expecially we are g ratefu l to S. Dzulyriski and R. U nrug for th e ir stim ulating discussions and th e ir suggestions for im proving the first d ra ft of th e m anuscript. We regret the passing of Ph. H. Kuenen, who was one of the greatest advocates of the fluxoturbidite concept.
REGIONAL SETTING
The A lpine-C arpathian m ountain chain passes through the so uthern
most p a rt of Poland. As is characteristic of th e rest of the chain, the tectonic style of th e Polish C arpathian M ountains consists of nappe stru ctu re s (Fig. 1) developed during E arly to Middle Miocene tim e.
From south to n o rth the m ain nappes in the outer p a rt of the Polish Carpathians are: Magura, Silesian, sub-Silesian, and Skole.
!9°E 2 0 ° E 2I°E 2 2 ° E 2 3 °E
Fig. 1. Tectonic sketch m ap of th e Carpathian M ountains in the southern part of Polaindi. Tectonic units are: 1 — Tatra, 2 — P od h ale Flysch, 3 — pHeniny klippen belt, 4 — M agura nappe, 5 — Fore-M agura nappe (Dukla), 6 — S ilesian nappe, 7 — su b -S ilesia n nappe, 8 — Skole nappe, 9 — M iocene and younger
foreland beds. (Modified from K siążkiew icz, 1962)
Fig. 1. Szkic tektoniczny Karpat: 1 — Taitry, 2 — Flisz podhalański, 3 — P ie niński Pas Skałkow y, 4 — Płaszczowiiina magurska, 5 — Jednostka przedm agurska i dukielska, 6 — Płaszczowiina śląska, 7 — Jednostka podśląska, 8 — P łaszczo- w ina skolska, 9 — Przedgórze Karpat. (W oparciu o pracę Książkiewiicz 1962)
The O u ter C arpathians are built of flysch sequences totaling n early 6000 m in thickness and ranging in age from latest Jurassic to E arly Miocene. P aleobathym etric depths generally range from 200 to 600 m (Książkiewicz, 1975). These sequences consist of norm al turbidites, fluxo- turbidites, and other deep-m arine deposits (Fig. 2). Three flysch fo r
m ations w ith abundant fluxoturbidites are th e L ow er Istebna Beds (Upper Senonian) (Fig. 3a, b), Ciężkowice Sandstone (Paleocene-Lower Eocene) (Fig. 4), and Krosno Beds (Oligocene).
More detailed tre a tm e n t of the geology of the Polish C arpathian M ountains is given by Książkiewicz (1962, 1963, 1968) and others.
IOOO -i m
0 -
Scale
J u r a s s i c
Lower Krosno
F C i ę ż k o w i c e
Lower I s t e b n a
Lower L go ta
1 2 - - - 3
■ 1 0 11 12 _J---I—
t-. \ J —L-- 16 F-17
ORIGINAL CONCEPT OP FLUXOTURBIDITE
A lthough the te rm f l u x o t u r b i d i t e was first published by K uenen (1958, p. 332), the original definition of th e concept is given by Dżułyński, Książkiewicz, and K uenen (1959, p. 1114):
“A different ty p e of sedim entation is encountered am idst norm al tu rb id ites in m any places. In th is type the grain size is large and the beds tend to be less m uddy. The bedding is thick and ra th e r irregular, and th e shales betw een are silty to sandy and th in or even absent.
C urrent sole m arkings are scarce, load casting is m ore common, and coarse cu rren t bedding of som ew hat variable direction is encountered.
Indications of slum ping are found, and grading is absent, repetitive, irregular, or even inverted, and irre g u lar lenses of coarser grain occur inside the beds. These sandstones m ay occur as large lenses betw een norm al flysch or shales. In other cases th e m aterial or th e direction of supply contrast w ith those of the norm al surrounding flysch of the same age”.
"Because characteristics of deposition from tu rb id ity cu rren ts appear to be m ixed w ith evidence for sliding, we p re fe r to call this kind of bed a «fluxoturbidite»”.
“We suggest th a t th e cause for this abnorm al type of flysch can be eith er a deepening of the basin and steepening of the slope, or a quick
ening of the supply, or a change in position of the supply, for instance th e building of a new d e lta ”.
“B ut w hatever th e cause, the mode of tran sp o rtatio n has changed.
Instead of a w ell-m ixed tu rb u le n t tu rb id ity c u rre n t carrying alm ost
Fig. 2. Schem atic stratigraphic colum n of th e S ilesia n nappe. Sedim entary units are:, 1 — Low er C ieszyn Beds, 2 — C ieszyn Limestan.es, 3 — U pper C ieszyn Beds, 4 — Grodiischt Beds, 5 — W ierzow ice Shales, 6 — Low er Lgota Beds, 7 — U pper Lgota Beds, 8 — radiolarite beds (and red mudsitanes), 9 — Godula Beds, 10 — Low er Isitebna Beds, 11 — Upper Istebna Beds, 12 — C iężkow ice Sandstones, 13 — H ieroglyphic Beds, 14 — Mendlite Beds, 15 — Krosno Beds — thdck sandstones, 16 — K rosno Beds — thinner sandstones and m udstones, 17 —
U nits containing fiuxotu rb id ites
Fttg. 2. Schem atyczna kolum na stratygraficzna jednostki śląskiej. 1 — Łupki cie
szyń sk ie dolne, 2 — W apienie cieszyńskie, 3 — W arstw y cieszyńsk ie górne, 4 — W arstw y grodziskie, 5 — Łupka wńerzowskie, 6 — W arstw y lgockie dolne, 7 — W arstw y lgockie górne, 8 — W arstw y radiolarytow e z czerw onym i łupkam i, 9 — W arstw y godulskie, 10 — Warsitwy istebmiańskae dolne, 11 — W arstw y isteb n iań sk ie górne, 12 — P iask ow ce ciężkowickiie, 13 — W arstw y hieroglifow e, 14 — W arstw y m en ilitow e, 15 — W arstw y krośnieńskie — litofacja grub oław i- cow ych piaskow ców , 16 — W arstw y krośnieńskie — Litofacja p iask ow ców średnio- ć aienkoław icow ych oraz łupków , 17 — Odcinki profilu zaw ierające flu k so-
turb id yty
— 8 —
2 g ~ ) 3 f ^ 5 ^ 6
M ? < tID > 8 Trmr9 — ► io U / 12 ® (j
Pig. 3a. Paleogeographie m ap of the Low er Istebna Beds (Upper Senonian).
Sym bols are: 1 — sandstone and conglom erate (turbidites and fluxcrturbidiites), 2 — sandstone, 3 — sandstone and m udstone, 4 — red m udstone, 5 — calcareous red m udstone, 6 — subm arine fain, 7 — subm arine m udflow , 8 — p ositive e le m ents, 9 — northern border of geocyncline, 10 — paleocurrent directions, 11 — present northern lim it o f Carpathian M ountains, 12 — location of Pig. 3b, 13 — locality num bers from Fig. 5. (PaLinspastic reconstruction m odified from K siąż-
kiew icz, 1962, sheeit 7)
Fig. 3a. Szkdc paleogeograficzny basenu K arpat fliszow ych w czasie sedym entacji w arstw istebniańskich dolnych (sanon górny). 1 — P iask ow ce i zlepieńce (turbi- d yty i fluksoturbidyty), 2 — Piaskow ce, 3 — P iask ow ce i m ułow ce, 4 — p str e łupka, 5 — P stre m argle, 6 — P odm orskie stożki, 7 — S p ływ y m ułow cow e, 8 — Obszary w ypiętrzone, kordyliery, 9 — P ółnocna granica geosynkliny, 10 — K ie
runki paleotransporitu, 11 — W spółczesna granica północna orogenu karpackiego, 12 — P ołożen ie fig. 3b, 13 — N um eracja opisyw anych odsłonięć, patrz fig. 5
(rekonstrukcja oparta na K siążkiew icz 1962, częściow o zm ieniona)
th e entire load in suspension, one can imagine a tu rb id ity cu rren t in which m ost of the sand and gravel moves in a w ate ry slide along the base. The c u rre n t is too poor in clay to raise this load in suspension, and the slope is too steep for the load to come to rest u n til it has spread out in a la y e r”.
“A tru e tu rb id ity cu rren t can be likened to a d ry avalanche, and a norm al slum p is the equivalent of a w et avalanche rem aining in contact w ith the ground. We believe th a t an interm ediate type of
— 9 —
SW NE
m 1 0 0 0 t •=-
5 0 0 -
^ 2 m u s
ftig. 3b. P aleogeographic cross section of the L ow er Istebna Beds iin th e Silesian Basin. Sym bols are: 1 — calcareous m udstone faoies, 2 — m udstone and sh aly facies, 3 — sandstone — conglom erate facies Kturbidites and fluxoturbidites).
N ote that the san dstone-conglom erate facies contact w ith th e m udstone and shaly facies wiiithouit an in tervenin g sandstone ("distal”) facies
Fig. 3b. Przekrój paleogeograficzny (schem atyczny) w arstw istebniańskiich dolnych.
1 — Facja m arglista, 2 — Facja łupkow a i m ułow cow a, 3 — Facja piask ow cow o- zlepieńcow a (turbidyty i fluksoturbidyty). Zwraca u w agę bezpośredni kontakt lateraln y facji piaskow cow o-zlepieńcow ej z facją m ułow cow o-łupkow ą, a brak
dysitalnej facji piaskow cow ej
O 25 5 0k m
» *
Fig. 4. Paleogeographic map of the C iężkow ice Sandstones (Upper P aleocene to L ow er Eocene). Sym bols are sam e as for Fti.g. 3a. (Palinspastic reconstruction
m odified from K siążkiew icz, 1962, sheet 9)
Fig, 4. Szkic paleogeograficany basenu Karpat fliszow ych w czasie sedym entacji piaskow ców ciężkow ickich. O bjaśnienia jak w fiig. 3b. (rekonstrukcja oparta na
K siążkiew icz 1962, częściow o zm ieniona)
— 10 —
m ovem ent is also possible and suggest th a t the resulting deposit be called a flu x o tu rb id ite”.
The first quoted p arag rap h above describes so clearly w h at a fluxo
turbidite looks like th a t no illustration is needed to visualize it; how ever, th e “indications of slum ping” are not clear. Nevertheless, w ith th is description m an y subsequent w orkers have been able to recognize fluxo
tu rb id ite in o th er deep-m arine basins.
The other quoted paragraphs discuss the processes th a t produce fluxoturbidites. T hat discussion was adequate for its time, b u t con-?
sidering m ore recent advances in sedimentology some p arts are now out dated. In the sam e pap er (p. 1095), they used the te rm “slum ping”
in a general sense approxim ately synonym ous w ith “subm arine sliding”, and considered “subaqueous m udflow s” as “slum ps” and m ud “slides”.
These im precise usages have caused some com munication problem s w ith subsequent workers.
Some additional rem ark s m ay help in understanding th e ir conceptual fram ew ork. In th a t paper, th e y w ere discussing m ainly turbidites in flysch, paleogeography, and paleocurrent directions; the fluxoturbidite discussion w as only a m inor subject. Indeed, th e y noted th a t th e m ost im portant ty p e of flysch consists of norm al turbidites, and the abnorm al, subordinate ty p e called “flu x o tu rb id ite” comprises only 15% of th e thickness and less of the areal ex ten t of the C arpathian Flysch. A ppar
en tly “slu m p ” deposits w ere considered as com prising an even less common ty p e of abnorm al flysch. T hat usage of “flu x o tu rb id ite” as a type of flysch, r a th e r th a n as only an individual deposit in a flysch sequence, has also caused problems.
These few problem s w ith the original concept resu lt from the lack of an explicit definition. Although the general description of a fluxo
tu rb id ite bed is adequate fo r recognition, specific descriptions and illustrations of type exam ples are needed to determ ine the range of diagnostic characteristics so th a t a model and a m ore rigorous definition m ay be form ulated.
TYPE EXAM PLES
Dżułyński and others (1959, p. 1095) listed the Ciężkowice Sandstone, th e Istebna Beds, and the low er p a rt of the Lgota Sandstone as con
taining the m ost representative exam ples of fluxoturbidites. They also listed the G rodischt Sandstone, Pasierbiec Sandstone, low er p a rt of th e Krosno Beds, and some p a rts of the M agura Sandstone as interm ediates betw een exam ples of turbidites and fluxoturbidites. They did not de
scribe or illu strate details of sedim entary stru ctu res at specific loca
lities.
— 11 —
U nrug (1963) provided th e first detailed sedimentologic analysis of typical exam ples of fluxoturbidites in his paper on the Istebna Beds;
he presented several line draw ings and photographs of the sedim entary structures. He sum m arized (p. 86):
“F luxoturbidite deposits are characterized by lenticular shapes of beds, coarseness of d e trita l m aterial, great thickness of beds, low pelite content, prevalence of sym m etrical, m ultiple, and discontinuous grading over other types of bedding, and occurrence of non-graded beds, traces of strong erosion, lack of sole m arkings, and poor developm ent of pelitic sediments. Occurrence of arm ored shale balls arranged in reg u lar layers p arallel to the bedding planes w ithin sandstone beds points out to the transition of sand flows into tu rb id ity c u rre n ts”.
He introduced (p. 64) th e concept th a t fluxoturbidites are th e deposits of “sand flows”, b u t also considered the process as an interm ediate type of mass m ovem ent betw een tru e slum ps and tu rb id ity currents after Dzulyriski and others (1959). L a te r (Unrug, 1965) he added the observations th a t Polish fluxoturbidites are form ed during tim es of rapidly rising cordilleras both on the m argins and w ith in the geo
synclinal troughs, th a t steep slopes on th e flanks of the cordilleras provided the setting for the initiation of th e sand flows, and th a t fluxo
tu rb id ites m ay be d istrib u ted in subm arine fans extending across the basin; th a t is, th e y are not only confined to the “p roxim al” p arts of fans.
DISC USSIO N S OF LOCALITIES
F rom the m an y localities w here fluxoturbidites have been identified by M. Książkiewicz and others w orking th e Polish C arpathian Flysch, we have chosen some of th e b e tte r exposed ones in the stratigraphic u nits listed by D żułyński and others (1959) as type exam ples (see lo
cation map, Fig. 5, and Table 1). Instead of the Lgota Beds, we have chosen the low er p a rt of th e Krosno Beds as it is a th ic k er and more w idely exposed u n it w ith m any good exam ples of fluxoturbidites (Dżu
łyński and Slączka, 1959), and the dominance of sandstone provides a contrast w ith th e Istebna Beds and Ciężkowice Sandstone w hich are m ore conglomeratic. In addition to the representative stratigraphic distribution, we have also attem pted to space the localities geographic
ally, and provide the distribution of fluxoturbidites w ith in th e sub
m arine canyon-fan systems.
F or th e exam ples, we are presenting colum nar sections of the sequences of sedim entary structures, cross sections of th e bedding relationships, and photographs of significant features. Because o u r w ork
— 12 —
Table 1. Main type examples of fluxoturbidites (see locality numbers on Fig. 5)
Loc.No. Name . Stratigraphic Unit
Roznow Lower Istebna Beds
('.'Rawsh-noove") Upper Cretaceous,
63 km‘ SE of Senonian
Krakow* near Roznow Lake
Mucharz ("Mu-hazgh") 40 kra SW of Krakow, on Skawa River
Lower Istebna Beds Upper Cretaceous,
Senonian
Remarks
Principal type example of fluxoturbidite. Zones of gravel segregations and mudstone clasts die out laterally within grain-flow deposits, which are gradational with overlying turbidites.
Good exposure in quarry.
Channel deposits of conglomerate; sandstones from margin "slumped"
(by fall or slide) into flows. Good exposure N in stream cut.
Ciężkowice ("Chairn-skow- veet-sah") 80 km SE of Krakow
Odrzykon ("Awd-gee- cawn") 14 5 km SE of Krakow
Ciężkowice Sandstone Paleocene to Lower
Eocene
Ciężkowice Sandstone Paleocene to Lower
Eocene
Zones of gravel segrega
tions above dispersed gravels in grain-flow deposits. Channels with trough laminae; some horizontal lamination.
Fair to good exposure in park.
Zones of gravel segrega
tions up to 20 cm thick.
Fair exposure at castle.
Koniakow ("Cawn-ee-ak- ov") 85 km SW of Krakow
Polana
("Poh-lahn-ah") 175 km SE of Krakow
Krosno Beds Lower Oligocene
Krosno Beds Lower Oligocene
Grain-flow deposit gradationally overlain by complete turbidite sequence. Good exposure in quarry.
Massive (debris?) flow deposit is gradational with overlying
turbidite. Good to fair exposure in quarry .
is of a reconnaissance nature, only macroscopic observations generally w ere made; m ore detailed sedimentological investigations could provide additional docum entation.
Descriptions and interpretations of the turbidites encountered in these sections follow the Ta to Te model of Bouma (1962). G rain-flow deposits (Middleton and Southard, 1977, p. 8.4—8.6) are recognized as conglomerates or sandstones th a t are associated w ith turbidites, b ut are generally w ithout grading, in te rn a l stratification, or a m ud m atrix.
— 13 —
IS^E 20°E 21°E 22°E 23°E
Fig. 5. L ocation map of typ e exam p les of Jluxoturbidites. Locality num bers, 1 — Rożnów, 2 — M ucharz, 3 — Ciężkowice, 4 — Odrzykoń, 5 — K oniaków , 6 — Polana, 7 — Borzęta, 8 — M uchówka, 9 — T ylm anow a, 10 — Kom ańcza,
11 — S leszow ice
Fig. 5. Mapa lokalizacji opisyw anych fluksoturbidytów . 1 — Rożnów, 2 — M u
charz, 3 — Ciężkowice, 4 — Odrzykoń, 5 — K oniaków , 6 — Polana, 7 — B o
rzęta, 8 — M uchówka, 9 — Tylm anow a, 10 — Komańcza, .11 — Sles^owdce
Bedding and lam ination description follows the system of Campbell (1967). In terp re tatio n of horizontal, current-ripple, and tro u g h lam ina
tion produced by m igrating bed form s is based on H arm s (1975).
R o ż n ó w (Loc. 1; Fig. 6; PI. I; PL II, Fig. 1)
S. Dżułyński inform ed us th a t the Rożnów locality is the principal type exam ple w here the fluxoturbidite concept was originally developed.
U nrug (1963) described and illustrated m any of the sedim entary fea
tures. This long abandoned q u arry near Rożnów Lake contains some of the best exposure of fluxoturbidites seen in our study.
Two thick beds (Fig. 6a, 0.00 to 2.73 m and 2.73 to 6.47 m) contain grain-flow deposits (F) w ith zones of m udstone clasts and segregations of gravel, and upw ard transitions into turbidites (Ta to Tc). On the basis of such observations, we w ill propose la te r th a t a fluxoturbidite be considered as a composite bed of a grain-flow or related deposit and a tu rb id ity -c u rren t deposit.
In th e grain-flow deposits, pebbles of igneous or m etam orphic rock generally are dispersed evenly through ithe sand m atrix, b u t locally they m ay be found in clast-supported clusters. M udstone clasts sank w ithin each flow to form a zone on top of a surface of density contrast, in some cases m ark ed by the transitional contact of sandstone above
— 14 —
С с RЧ- с°Е M l
Lithdogic Column
Description
Tc"
Tb
Ta-
6A7.6-42
5 3 2
5l87/
SS above ,
t o m f e r a i o S W ? ISSIde
SS:n o g ra v e l;s a n d (1 0 0 % ), m g m ax ;so m e partings of m udstone, carbonaceous m aterial; horizontal la m r
^ S S : as below, but graded nation
indefinite surface
S S : gen. no g ravel, few MS clasts in lo w e r p a rt;sa n d (100%l vcg m ax, eg m odal, no grading,larger gruins dispersed,
no internal stratification
ТЬДс Tb Та-"
3.72 3A2 3.17.
2B8
2.73
o . \ a 0Г9 '0'
-S
2.%.
О■o l О• о pr -У-,- 2.43226,
2.21
1.46 1.26
0 5 6 0 5 0
о О о ООО о * о *о *о о*
"Ж Ф.
Jo.ooJ—
Zone of MS clasts, max 50cm long/16cm wide, various orientations inSS; base of density contrast o f S$/CGL;zone disappears to S COL: gravel(6 0 4 ), 5mm max, hints of segregation; sand (40%)matrix SS . gravel segregations in low er part,poorly graded in uPP®|'Qrj CGL-.gravel (80%), 8mm max, 2mm mode, dispersed in sand m atrix,
^5harp,erosional surface, load features 3 to 4cm convex top
l deep, flam e structures _ . .___
: NSS. hor, laminae; to S unit thins to21cm,with wedging and ripple laminae T/w H O T^^m t^ae^Sx^cm ^m bde 0,5cm thick,carbonaceous
m aterial along laminae
S S ’.gravel (10 %*). small pebbles in segregated xonei leu them lcm thick; sand(90%-)Jvf- vcg, in zones 2 to3cm thick
Zone of MS clasts, max 30cm long, various orientations, 'mSS SS: mudstone clasts, max 20cm long,5 cm wide, scattered;sand
(100 %■)■■ vf to vcg; no grading or internal stratification Zone of MS clasts,5 cm long, in SS
SS: gravel (10% + 1, 4m m m ax.,in segregated lones few mm thick, sand (90 % - ): vf to vcg
sharp, erosional surface, load features 5 cm wide, 4cm deep MS and CGL below
Hig. 6a. C olum nar section a/t R ożnów (Loc. 1) of Low er Istebna beds (Upper Cretaceous). T w o flu xotu rb id ite beds sh ow m any characteristic features. T hin zones of g ravel segregations occur in the gra in -flo w deposits. M udstone clasits gen erally appear to b e confined to zones m arking boundaries of density contrast w ith in the flo w s. The tops of the gra in -flo w deposits (F) are gradational w ith th e overlying turbidriity-current deposits (Ta- in terv a ls are thin). Sym bols are
th e sam e kim. th e follow ing colum nar secltions
Fig. 6a. P ro fil odsłonięcia w arstw isfcebniańskich dolnych w R ożnow ie (lok. 1).
Obie ła w ice flu k soturbidytów w ykazują liczne cechy charakterystyczne. C ienkie strefy segregacji żw irow ej w idoczne są w osadach potoków piaszczystych. Klasity m uł owe ow e zw iązane są zw yk le zie strefam i granic gęstościow ych w obrębie prą
du. Osady potoków piaszczystych ,(F) przechodzą stopniow o ku górze w osady prądów zaw iesin ow ych (in terw ał Ta jest cienki). Sym b ole na w szystkich załączo
nych kolum nach są rtakiie sam e
— 15 —
& " ■=«= ^.=0° Speciol Symbols:
VJJh Rippl« lamination Ł —sl Horizontal lamination
(both in sondston*)
SYMBOLS
CGL*Congtomerarte ss-
Sandstone ■2-: Ms-
Mudstone
& Mudstone chut
Armored rruJbatl j Ripple lamriation -^r; Urite I Horizontal lam. -n.
Erosion
' surface . Definite
sirfloc® ___ Indefinite sgrfaw
kiteiprvtation: Tb-e • tirbkfity ■ current deposit F>9vi~flow (or related) deposit
Fig. 6b. Cross section, north-souith, of quarry w a ll at Rożnów. Fig. 6a is located on le ft side. Principal bedding surfaces occur at 0.00 m, 2.73 m, and 6.47 m.
Lateral variability w ith in beds is show n. In low er bed (0.00 to 2.73 m) are lenses and load pockeits o f gravel in gradn-flow deposits. Zones of gravel segre
gations and m udatooe clasts die out laterally. C onglom erate at base of upper bed thickens locally w ith a con vex top indicating a buildup over a sligh tly higher part of th e bottom . Sym bols gen erally are th e sam e as th o se used in
colum nar sections; special sym bols are indicated Fig. 6b. Przekrój północ-południe kam ieniołom u w R ożnowie.
Fig. 6a. reprezentuje lew ą część przekroju. G łów ne pow ierzchnie uławicenda w y stępują na poziom ach 0.0 m, 2.73 m, i 6.47 m. W idoczna jest pozioma zm ienność w obrębie ław ic. W dolnej ław icy (0.00—2.73) w idoczne są soczew k i żw irów w osadach potoków piaszczystych. S trefy segregacji żw irów i k la stó w m ułow co- w ych lateralnie w yk lin o w u ją się. Zlepieńce w dolnej częśai w yższej ła w icy lok al
n ie zw iększają m iąższość, ich w ypu k ła górna pow ierzchnia w skazuje na nad
budow ę. Sym bole są ogólnie tak ie sam e jak w profilach, sym bole odm ienne są objaśnione obok rysunku
— 16 —
and conglomerate below. Thin sheets of gravel segregations are found w ithin th e sandstones and m ay be th e resu lt of liquefied flow. Both the zones of m udstone clasts and th e gravel segregations die out la te rally, so th e y do not represent norm al layers of bedding or lam ination.
Description
Covered by stream deposits (som e S3 to E in stream ) revel' mg; no grading or in tern al stratification
rface 3
SS: gravel (10 %-),2gpnirpxydis^r2e»dj5mm mode; sand (9 0 % )mg;
, SS:.no , definite si
fto gradinc .indefinite surface
.'—CGL, .-as below but with armored m udballatbase
Indefinite ---te surface „ , . , „
' Hffig n o r n q \ a»tГо!Ш са1?Ь1ПГТ1 moae'9 rea*® 10 *°P 50c*11 M n u p - jL * g ra v e ft7 O “/0 2cm m o d e ; sorid [3 0 % )л о gra d in g
^definite irregular surface,bat not erosional
C G L : gra ve l (7 0 % ),2 0 c m т а и , 6cm m ode of m etam orphic rockt, rare L i,3 c m m ode o f q u a rtz ; hints o f imbrication, 10* т а к Inct.. aligned p a r a lle l to ctahfiol axis (N17E1 in lo w e r p art, tra n * v e r s e (N 9 0 E )4 n u p p e r p a r t ,
p a le o e u rre n t t o N N E ; s a n d (30%) in r re trix ; n o g ra d ln fio r In te rn a l
s t r a t if ic a t io n .
sheb-p eration su rface,uneven channels and p ockets,axes trend N E - S W C G L : os below , g ra v e l 1cm m a x ,g r a d in g a t top
indefinite su rfa c e , th o rp elsewhere
C G L: gravel (7 0 % ), 3 cm m ax, 1cm mode; sand (3 0 % ) in m a trix ; no mud; d efin ite g ra d in g , no in tern al s tra tific a tio n
sharp, uneven surface,erosional scours over 10 cm in relief SS : eg to veg, no visible grading
covered by soil and vegetation (m ore SS below )
Fig. 7a, Colum nar section at Mucharz (Loc. 2) o f Low er Istebna Beds (Upper Cretaceous). From 0.00 to 0.60 m is the upper, truncated pant of a flu xotu rb id ite bed. From 0.60 to 3.70 m, and 3.70 to 4.35 m are tw o, thick, norm al turbidite beds (Ta). From 4.35 m fto 8Л8 m is a seq u en ce of flu xotu rb id ite beds (F) w ith th e upper (T) parts m issing. The d efin ite stratification surfaces at 6.25, 6.65, and 8.08 m are depositional discontinuities w ith no evid en ce of erosion; possibly ithey m ay be lam ination surfaces w ith in a com plex flu xotu rb id ite bed. The in d efin ite surfaces at 7.45 and 7.65 m are recognized by graiin-size contrasts, but show no evidence o f depositional discontinuity; th ey are interpreted as boundaries
produced by internal variations of grain concentrations w ith in the flo w Fig. 7a. P rofil odsłonięcia w arstw listebmiańskich dolnych w Mucharzu (lok. 2).
Odcinek 0.00— 0.60 m reprezentuje górną, częściow o zerodowaną część ła w icy fluksoturbidytow ej. Odcinek od 0.60 do 4.35 obejm uje d w ie grube ław ice n or
m alnych turbidytów . Od 4.35 do 8.18 m w y stęp u je serlia ław ic fluksoturbidytów (F) z brakującym i w yższym i partiam i (T). W yraźne pow ierzchnie u w arstw ienia na poziom ach 6.25, 6.65 i 8.08 m reprezentują strefy nieciągłości jednak bez śla dów erozji; m ogą one być pow ierzchniam i lam in w obrębie jednej złożonej ła w icy fluksoturbidytu. N iew yraźne pow ierzchnie na poziom ie 7.45 i 7.65 m są zw iązane ze zm ianą w ielkości ziarn; P ow ierzchnie te są interp retow an e jako
granice spow odow ane zróżnicow aną koncentracją ziarn w prądzie
— 17 —
M. Książkiewicz inform ed us th a t the locality on the Skaw a River is one of th e m ain exam ples th a t he, S. Dżułyński, and Ph. H. K uenen
M u c h a r z (Loc. 2; Fig. 7; PI. II, Fig. 2; PI. III, Fig. 1)
1 L 1 1 <
Fig. 7b. Cross section, south—southw est — north — northeast, ait Mucharz. S tru c
tural dip is 40° south. Bedding surfaces at 0,60, 4.35, 6.25, 6.65, and 8.08 m above base of colum nar section are labelled
Fig. 7b. Przekrój SSW — NNE odsłonięcia w M ucharzu. Upad w a rstw 40° ku S.
G ranice w a rstw na poziom ach 0.60, 4.35, 6.25, 6.65 i 8.08
E
Figs, 7a , fcW
Fig. 7c. Cross section, east—w est, v ie w dowindip, at Mucharz. Figs. 7a, b are located near m iddle. Surface at 4.35 m is base of flu xotu rb id ite channel, buit
m uch o f th e relief and irregularity ds the result of loading
Fig. 7c. Praekrój E—W odsłonięcia w Mucharzu. Przekrój poprzedni (fiig. 7b) 1 kolum na <fig. 7a) odpow iadają częśai centralnej. P ow ierzchnia 4.35 jest dnem
kanału częściow o zm ieniona w efek cie w ystępow an ia pogrązów
studied during th e developm ent of the fluxoturbidite concept. Although w e did not find com plete fluxoturbidite (FT) beds here, we did see some im portant relationships w ithin sequences of grain-flow (F) depo
sits. This section is in one of the coarsest facies of fluxoturbidites;
m any beds contain 50% to 70% gravel.
N orm al tu rb id ites are present w ithin the m ain exposure and in nearb y outcrops. In grain-flow deposits, elongate pebbles tend to be
2 — R o czn ik P T G 51/1—2
— 18 —
oriented p arallel to the flow direction, and flat ones tend to be im b ri
cated to dip upcurrent. This fabric indicates deposition from a clast dispersion, w ith no bed-load rolling (Walker, 1975, p. 146).
No sh e ar surfaces of sliding (or slumping) were recognized, b u t th e presence of sandstone boulders suggests erosion into subjacent tu rb id ites and falling or sliding of blocks into th e flow. One exposure indicated breaking and sliding of sandstone blocks into a mudflow. These features
1
2 £ -Дч- с Я c о о E a.£
• 0 ł-H
э 1 3 1
|х ,
Lithologic Column
Description
9.43 F ?
743
О О О О О ' о/ О О'*
О ’ О О О О 0.0 О О
О . Ó О . О
о ’ О о о
Та ТЬ Та
6 3 3 6.18^1
Т Ь
Та 465 -3.75
О О О О О О О О* О . О 'О ’ О ■
у о ; ? ^
2.90
О о о о о о
Q 80- 0.00
О О О О О О о о о о о о
о о о о о о
* о • о • 6 • о*
о ' О ' о *0*0
о * о • о •9
.Presen t erosion surface
C G L gravel (5 0% \ in segregaded zones; sand {50У,}/
as below ; p oo rly ex p o sed .sh arp , uneven su rfa ce
SS ; sand (1 0 0 % ) 1mm m ax, hint of grading, nonlam inate J CGL: gravel (10 % -) 1c m max y g raded ;sand (90% la s above;
no internal stratification
"sharp, uneven surface with flam e structures
S S ig rq ve l flO%-) in basal 43cm,1cm m «,5m m modal,with normal inverse, and lateral grading;sand (90/£■*),2mm max grading up to 0.1mm max; non laminated in lower part, larrtinated .sharp sJFV<5%® witR'rrlinor ^o^onM m of section present toN),flute
cast hdicating paleocurrent to NNE . . . .
SS sand (Ю О ^ С И т т m at, (may hate mud m atr i x), g rad. e d, I a пф 0,5 tolcm thick in lower part, 2to3mm in upper part
SS: no gravel,sand (1 0 0 % ): 1mm max, nint of gradrg/nonlarrinatec sharp surface, no evident erosion,armored mud balls occur locally
below surface (down to 20cm)
CGL: gravel (2 0 % ),as below, long axes geahorizontaI,some inclined to SSW an d NNVVgravel in segregated zones 5cm max thick
ness, disappear laterally;sand ( 80 % ), -as before,butlm m max in upper 9 0 cm ,3 0 cm zones betw een grgvel segrega .indefinite fla t surface tions, some h o rizo n tal lam eLlae
CGL:gravBl (50%+) , 1.5cm max, 27m m mode, dispersed in sd,not g"aded,not segregated'sand (50^-), 2mm max, m atrix ---— --- --- in о mual Covered below
Fig. 8a. Colum nar section at S ow a in C iężkow ice area (Loc. 3) of C iężkow ice Sandstone (Paleocene to Low er Eocene). From 0.00 to 2.90 m is th e upper part a fluxoturbidite bed. T he basal exp osu re from 0.00 to 0.80 m is a conglom erate w ith gravel dispersed through the sand m atrix. The overlying in terval from 0.80 rto 2.90 m is a conglom erate w ith gravel segregations and some horizontal lam ellae in the upper part that have d iffu se boundaries. Three normal turbidite beds are present b etw een 2.90 and 7.43 m. At the top of (the sequence, from 7.43 to 9.43 m, is the low er part of a possible fluxoturbddite bed, but iit is
poorly exposed
Fig. 8a. P rofil piaskow ców ciężkowictoich w skałce Sow a. Skam ieniałe m iasto koło C iężkowic. Odcinek 0.00—2.90 m reprezentuje górną część ław icy flu k so - turbidytu. Część dolną (od 0.00 do 0.80 m) stanow i zlepieniec z rozproszonymi dużym i ziarnam i kwarcu w m atrix piaszczystym . Interw ał w yższy (0.80—2.90 m) to zlepfieniec z poziom am i żw irow ym i, a w wyższej części horyzontalnie lam ino
w any. W in terw ale 2.90—7.43 m w ystępu ją trzy ła w ice norm alnych turbidytów . Górną część profilu stanow i doLna część ła w icy przypuszczalnie fluksoturbidy-
tow ej
— 19 —
m ay have suggested th e process interm ediate betw een “slum ping” and norm al tu rb id ity currents proposed by Dzulynski and others (1959) for th e deposition of fluxoturbidites.
Fig. 8b. Block diagram , v ie w southeast, at Sow a. Fig. 8a is located on right side. S everal beds are truncated by erosion surfaces of m oderate relief. (Modified
from Koszarski, 1956, 1963)
Fig. 8b. B lok diagram skałki Sow a, w idok ku SE. Zwraca uw agę ścinanie ław ic przez pow ierzchnie erozyjne (wg K oszarski 1956, 1963, nieco zm ienione)
On the colum nar section (Fig. 7a) at 6.25 m above the base, a bedding surface separates a low er conglom erate from an u p per one w ith a sm aller modal size of gravel clasts. The surface is irre g u la r and no erosion is evident (PI. Ill, Fig. 1). A pparently, th e u p p er bed was de
posited from a low er velocity flow th a t eith er was incapable of eroding coarser m aterial in the substratum , or was dum ped so rapidly th a t there was insufficient tim e to erode the irre g u la r surface.
2*
— 20 —
In the national p ark , Skam ieniałe Miasto, are exposures of the Cięż
kowice Sandstone a t its type locality. This form ation was recognized as one of th e m ain exam ples of fluxoturbidites (Dżułyński and others,
1959).
A t Sowa, in the m iddle of the park, is one of the best exposed sedi
m e n tary sequences (Fig. 8a, b; PL VI, Fig. 2). Some of the sedim entary stru ctu re s w ere described and illu strated previously by Koszarski (1956, 1963). The base of the lowest grain-flow deposit is not exposed, b u t th e lowest exposed p a rt is massive conglom erate wiith dispersed pebbles (0.00 to 0.80 m). N ext above (0.80 to 2.90 m) is a conglom erate w ith gravel and sand segregations, and th in horizontal lam ellae (Fig. 8c) w ith diffuse boundaries th a t m ay also be products of liquefied flow, or m ay be products of lam ellar flow shearing, o r m ay be crude lam ination developed d u rin g a brief tractional phase prior to deposition. No erosion
C i ę ż k o w i c e (Loc. 3; Fig. 8; PI. III, Fig. 2; PL IV; PI. VI, Fig. 2)
Fig. 8c. Cross section, north w est—southeast, of prom inent exp osu re at Ratusz an Ciężkowtice area. Structural dip is about 12° south. On left (northwest) are ,two thick flu xotu rb id ite beds com posed m a in ly of m a ssiv e san dston e w ith d i
spersed pebbles. Ait top of low er bed are erosional channels filled w ith trough lam inae, dmdacatimg associated traction currents. Largest trough is 4 m w id e and 1 m deep. On right, relationships in low er part are questionable because of weafthering and vegetation cover, but in upper part ab ove a basal conglom erate
is a sandstone w ith lam ination
Fig. 8c. Przekrój NW—SE skałki Ratusz. Skam ieniałe M iasto koło Ciężkowic.
Upad około 12° ku S. Po lew ej d w ie grube ła w ic e flu k soturbidytów reprezento
w anych g łów n ie przez m asyw n e piask ow ce z rozproszonym i żw iram i. Na granicy ławtic obecne są k an ały erozyjne w yp ełn ion e piaskow cam i skośnie w arstw o w a
nym i, co w sk azu je na obecność prądów (trakcyjnych. N ajw ięk szy kanał posiada szerokość 4 m, a głębokość 1 m
— 21 —
is evident at the top of th e grain-flow deposit in th e line of section (2.90 m, Fig. 8a), b u t erosional rem nants are seen to th e n o rth east (Fig. 8b).
SW NE
Fig. 8d. Cross section, sou th w est—northeast, on southeast side of exp osu re at R atusz. Trough and horizontal Iamimaitdom are present. Foresets in troughs in
dicate a paleocurrent to SW. Sm all fau lt com plicates relationships
Fig, 8d, Przekrój SW— NE (ścianka SE) skałki R atusz. W idoczne lam inow anie h o
ryzontalne i skośne. To ostatnie w sk azu je na kierunek paleoprądu ku SW. Zwraca u w agą częściow e zróżnicow anie struktur po obu stronach n iew ielk iej d yslokacji
A t Ratusz, in th e southw estern p a rt of th e national park, is a compli
cated exposure of probable g rain flow and other deposits (Fig. 8c, 8d;
PI. VI, Fig. 2). Channels w ith trough lam inae are seen at th e tops of some grain-flow beds (PI. IV) and probably w ere produced by traction currents. A transverse view of the troughs (Fig. 8d) shows foresets indicating a paleocurrent to the southw est. To explain th e troughs, Książkiewicz (1975, p. 320, 349) postulated a filling of the basin up to n ear wave base so th a t the stru ctu re s could be form ed in shallow w ater.
A lthough unusual, large channels w ith tro u g h lam inae have been reported in other deep-m arine basins, and we see no need for shallow
ing.
Above the troughs, exposed in cliffs, are probable horizontal lam inae th a t m ay have been produced by traction cu rren ts developed in over- bank areas, or during the latest stages of channel filling, or a fte r th e channels w ere buried. In a m ore accessible exposure tow ard the south
east, sim ilar featu re s appear to be horizontal lam ellae or segregations of fine sand w ithin conglomeratic sandstones.
F a rth e r southeast are exposures of red pelagic m udstones overlying the Ciężkowice sandstones. These pelagites support th e in te rp retatio n of deep-m arine deposition.
— 22 —
On the n o rth side of the castle, Odrzykoń, is another w ell-know n exposure of Ciężkowice w ith fluxoturbidites. G rain-flow deposits (Fig, 9, 0.00 to 2.20 m) pass upw ard into tu rb id ites (2.20 to 4.50 m) w ith m ultiple grading. A conglom erate wedge, w ith gravel up to 1.5 cm in diam eter,
O d r z y k o ń (Loc. 4; Fig. 9)
4> d
gLrthologic Colimn
Description
7 2 5 F ?
F
O k j Ta-
Ta-_
F
5,75■ о d 6 6 o'o
ООО ООО о о о о
2,90 2,20
ОО
... о • “■ .• О ... * . 0 . .
' 'О * * * 4 •
о ■ • О • * о
• 'О • • о * * ■
. о • 1 О . ■ » О
Т~ о . . о . -
О ■ о * •
• о • • <а • « i
О * . о - ■ о *
- - о • ♦ о • • о . . о • • о
• • о • • о - ■
о * * О • • о *
- • о • * о ■ о * • о - - о
• - о • • о • о . , о . -
CG L above in castle w all
sharp, erosion surface, minor relief
SS: (no gravel),sand as below,no internal structure (about 5 m to W see channel 1m deep with trough lam in ae)
sharp surface
OGL . gravel (AO%),zones 20cm max, thick, gravel segregations;
sand (6 0 2 ),zones 25cm max thick; no internal stratification sharp, erosion surface
, S S : minor gravel sand as below; C G L ip wedgej 1,5cm max,not graded xou sharp,erosion sa’rTace', load features with 10cm relief
CGL-. gravel (3 0 % to 10% at top^ 4m m max, 3m m modal,graded;
sand (ТОУгЗОХ) , 2 mm to 1 m m max, graded; no internal stratificcr
. indefinite surface ^Ю*"1
CGL-, gravel ( 30?» to 10 % a t top)7 to 5mmmaj.1albac,qrade«J1sand (70/i to 90/2 2 to 1mm m ax at top; no internal stratification
-indefinite surface,gradational boundary
CGL'. grovel (3 0 % ) H em max, 5 m m m od al, nongraded, dispersed pebbles, not oriented; sand (7 0 % ),
2m m m ax, 1mm m odal, m atrix o f egl; no internal stratification
covered by soil and vegetation
Fig. 9. Colum nar section at Odrzykoń (Loc. 4) ot C iężkow ice Sandstone (Paleocene to L ow er Eocene). Low er flu xotu rb id ite bed (0.00 ito 4.50 m) contains tw o in ter
v a ls of Ta-. W edge and trough lam inae are seen in upper beds
Fig. 9. P rofil p iask ow ców ciężkow ickich w odsłonięciu pod zam kiem w Odrzy- koniu. D olna ła w ica fluksoturbidytow a (0.00—4.50 m) zaw iera dw a in terw ały Ta.
W ystępują k anały erozyjne ii w y k lin o w y w a n ie się ław ic
m ay be a grain-flow deposit (F?) scoured into a norm al tu rb id ite (Ta, 4.50 to 4.75 m). G ravel segregations up to 20 cm th ick are p resen t in a higher grain-flow bed (4.75 to 5.75 m). The sandstone above contains channels 1 m deep w ith trough lam inae indicating deposition from associated traction currents.
To the south east in the national park, Prządki, are additional expo
sures of massive sandstones and conglomerates several m eters thick which show no grading or in ternal stratification. These rocks probably are grain-flow deposits, b u t exposure quality is only fair and no t u r bidites were recognized in th a t area.
— 23 —
In th e q u arry a t this locality is one of th e best exposures of a fluxo- tu rb id ite sandstone bed, w ith grain-flow deposits gradationally overlain by a complete tu rb id ite sequence (Fig. 10a). A t th e base of the m ain bed (0.00 to 0.20 m) is a sandstone w ith hints of grain segregations;
the transitional boundary above is not a bedding surface, b u t is uneven K o n i a k ó w (Loc. 5; Fig. 10; PI. V)
eg
I
il
c Lithologic -3 ColumnE
Description
ray-
T©/
Tb
uzą
1V10-
No.70
SS-. as below, coarser, no internal stratification sharp erosion surface , ,
^“ MS: deeply weathered, dork gray
^ S S - as below, horizontal laminae .
SS : as below, Cj 1mm max grain size, current ripple laminae S S #. as belcrvy Q5mm max grain size, horizontal laminae
■definite lamination surface
T a - SS ; as below, but decrease in max grain size to 0,5mm, graded,inc.in mica,no internal stratification
620 ... indefinite surface, g ra d a tio n a l
SS: as below (no grave I), grain segregations, no internal stratification
3.20 • *—1_. indefinite su rface, gradational . ^ o. . •
* • Q • « • ... ..
.SS). Q ^ «
0 . 2 0 j ^ 0.00
SS : gravel (10%), 5mm max decreasing to 3 mm at top, dispersed; mudstone clasts 20cm to 5cmgen.max,
1,5 Cm modal some inclined to SE, sand (9 0 % ); 1mm max, no internal stratification
indefinite surface, uneven as result of loading, gradational
:___SS (1QQ%).0'5mrri rTvax.3^njey eg aticnsini<M'ef- part_________________
sharp, flat erosion surface
MS,SS b e lo w (r a r m a l t’jrb;dites
Fig. 10a. Columnar sectio n at K oniaków (Loc. 5) of Krosno Beds (Lower Oligo- cene). B est typ e ex a m p le of a flu xotu rb id ite bed that is dom inantly sandstone (0.00 to 11.20 m). In upper part (6.20 to 11.20 m) is a com plete turbidite sequence
of Boum a (1962) from T a- (no erosional base) to Te
Fig. 10a. P ro fil w a rstw krośnieńskich z kam ieniołom u w K on iak ow ie (lok. 5).
N ajlepszy przykład ła w ic y fluksoturbidytu składającego się głów n ie z piasku (0.00—11,20 m). W częśai w yższej (6.20— 11.20 m) wysitępuje ław ica turbidytow a
z w szy stk im i interw ałam i Boum y (1962) od Ta do Te
