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 A N N A L E S D E L A S O C I f i T f i G f i O L O G I Q U E D E P O L O G N E
T o m ( V o l u m e ) X X X I X — 1969 Z e s z y t ( F a s c i c u l e ) 1—3 K r a k ó w 1969
F R A N K S I M P S O N *
INTERFACIAL ASSEMBLAGES 1 OF FORAMINIFERA IN THE CARPATHIAN FLYSCH
(PI. X C —XC III, 2 Figs.)
O m iędzyrytm ow ych zespołach o tw o r n ico w yc h 1 w e fliszu karpackim
(Tabl. X C — X CI II , 2 fig.)
A b s t r a c t : A gg reg a tes of sm all, b enthonic Fora m in ifera occur at the in te r fa ce s b e tw e e n th in , fin e -g r a in e d sa n d sto n e and sh a le la yers of su c c e s s iv e beds in se q u e n c e s o f E o cene fly s c h b e lo n g in g to the M agura Series, P o lish W estern C arpa
thians. T h ese interfacial a ssem b la g e s are fre q u en tly se en as in te r m itte n t layers of th ick n ess equal to the d iam eter of a sin gle test. For de sc rip tiv e purposes, four d ifferen t types of in'terfacial a s sem b la g e w e r e nam ed after the m ost c o m m o n ly occurring genera.
V arying degrees of la teral d isp la c e m en t of f o r a m in ife r a l tests by th e currents w h ic h deposited fin e sand a b o ve the in terfa ces m ay be deduced. In m a n y cases, h o w ev e r , lateral d isp lacem en t of tests w a s at a m in im u m and the in terfacia l a s s e m blages are residua, form ed w h e n bottom m u d s w e r e s e le c tiv e ly eroded by s a n d - -b e a r in g currents. The b urrow ing ac tivities of larger in v erteb rates w e r e e ff e c tiv e in the disruption o f interfa cia l a s sem b la g e s a n d in the m e c h a n ic a l fr a g m e n ta tio n
of tests.
IN T R O D U C T IO N
N e s t e r o f f (1961, 1963) described pelitic elem ents of beds from deep-sea cores of Recent turbidites, divisible into two pa^ts: a lower layer, in which the microfauna is either im poverished or absent, and an upper layer, characterized by the presence of pelagic Foraminifera and pteropods. Where the succeeding bed begins w ith fine-grained sand or silt, the tests m ay be concentrated in a band, of thickness equivalent to the diameter of a single test, occurring at the mud /sand interface.
N e s t e r o f f (1961, 1963) and N e s t e r o f f and H e e z e n (1963) deduced deposition of the layer of tests from the tail of a turbidity
1 P o w ie r zc h n ia m iędzyry'tmowa odpow iad a „ in te r fa ce ” sen su D ż u ł y ń s k i i S i m p s o n (1966, p. 197). P o j ę c ie „ r y tm u ” w y j a ś n ia autor w pracy ( S i m p s o n , 1970)..
In terface se n su D ż u ł y ń s k i and S i m p s o n (1966, p. 197). O ther term s c o n cern in g stratification, used here, are giv en by S i m p s o n , 1970.
* Address: Dr F rank S i m p s o n , D e p a r tm e n t of M in era l R eso urces S u b surfa ce G eological Laboratory 2G1-E, D e w d n e y Ave., Regina, S a s k a tc h e v a n , Canada.
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current and furtherm ore, concluded that pelagic deposits are generally eroded away by succeeding turbidity currents ( N e s t e r o f f and H e e - z e n, 1963). An alternative explanation was subsequently provided by K u e n e n (1964), who suggested that the removal of Clay from the sea- -bottom by a turbidity current lacking the energy required to lift the tests gave rise to a thin concentrate of shells, forming a „pavem ent”
at the base of the turbidite sand. Though no fossil pavem ents have been hitherto recorded as such in the volum inous literature pertaining to flysch and flysch-like deposits, K u e n e n ’ s hypothesis is attractive in that it is supported by some experim ental and theoretical evidence (K u e n e n, 1964, p. 242).
Organic remains from the interfaces betw een flysch sandstones and the shales beneath them have been previously reported as assem blages occurring on the soles of sandstones. A brief survey of these occurrences is follow ed by a detailed account of interfacial assem blages from the Eocene of the Magura Series. The sedim entation of the flysch form ations of the Magura Series, to which reference is made in this account, is considered in detail by S i m p s o n (1969).
K s i ą ż k i e w i c z (1960, p. 743 and Plate III, Figs. 12, 13) described, under the name ,,Halimeda” *, ram ifying, chain-like arrangements of siliceous, capsulate bodies, found on sandstone soles in the Istebna Beds and in the Cretaceous and Palaeocene of other units. As pointed out by K s i ą ż k i e w i c z (op. cit.), these chains correspond in shape to system s of negative sole structures described by F u c h s (1894). Both occurrences are probably referrable to the Aschemonellci B r a d y (see N e a g u, 1964, p. 586). An occurrence of tubes of Bathysiphon M. S a r s on the soles of thin sandstones belonging to the Istebna Beds was reported by K s i ą ż k i e w i c z (1961, pp. 23— 25 and Plate I, Fig. 1). Tubes up to 4 cm. in length are aligned in parallelism w ith the principal current direction and exhibit a preferred orientation, w ith their pointed ends downcurrent (see also B i e d a , 1948, Plate IV, Fig. 5).
K s i ą ż k i e w i c z (1961) also described groove moulds with Bathy siphon at their downcurrent ends (see also D ż u ł y ń s k i , 1963, Plate XXVIII, Fig. 3) and linguoid ridges of the sole, downcurrent w ith respect to the feathysiphon tubes w ith which they make contact. The former structures may have arisen as a result of the dragging action of the current, w hile the latter ^jnay be interpreted as current-form ed scours, eroded either before or after the deposition of the tests ( K s i ą ż k i e w i c z , 1961).
Sim ilar occurrences of Bathysiphon have been recorded from the Ciężko
wice Sandstone of the central Polish Carpathians b y Ś l ą c z k a (1964, p. 203). Aligned tests of the Bolivina argentea at the base of a graded sandstone layer from the subm arine Santa Barbara Basin, off southern California, are figured by H a r m a n (1964, Fig. 6, p. 86).
Assem blages of Foraminifera have been found on the soles of flysch sandstones belonging to the Upper Senonian of the eastern Carpathians by D a n y s h (1966), who describes ,,needle-like” (probably Hyperam- mina or a related form; see also op. cit., p. 21), „w orm -like” (an indeter
minate, tubular form), „rosary-like” forms (Aschemonella or a related form). On some sandstone soles, the tests are aligned parallel to the lineation given b y interfacial sedim entary structures ( D a n y s h , 1966,
1 T h e apostrophes a re used by K s i ą ż k i e w i c z (op. cit., p. 743).
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p. 20). Species of the branching, Dendrophryna Vi a 1 o v and Aschemo- cella V i a l o v , as w ell as straight tubes of Aciculina V i a l o v reach
ing up to 12 cm. in length, were described by V i a l o v (1966) from the soles of Upper Cretaceous flysch sandstones in the northern Carpathians.
Other tubular forms were reported from the lower surfaces of Miocene sandstones in the western Ukraine by V i a l o v and P i s h v a n o v a
(1967).
Also relevant to the present discussion are certain interfacial accum u
lations of graptolites, described by J a w o r o w s k i (1964, 1966) from the Silurian of eastern Pomerania. J a w o r o w s k i (1966) deduced bottom traction of graptolite rhabdosomes from considerations of short groove moulds and prod moulds evidently formed by these on the sole of a thin (6 mm.) siltstone layer and concluded that the rhabdosomes w ere transported by weak currents of low density (compare w ith K h a 1 e t s k a y a, 1967).
From this brief review , several general considerations emerge:
1. Occurrences of the remains of pelagic and benthonic organism s have been reported from the soles o f flysch and flyschoid sandstones.
2. There is reason to believe that some of these occurrences are fairly common (see, for instance, K s i ą ż k i e w i c z , 1960, p. 743), though the distribution of organic remains on a given sole is usually sparse.
3. Interpretative emphasis has hitherto rested upon the sandstones, on the soles of which the fossils are found. Thus erosion of the organic rem ains from the bottom muds, followed by redeposition at som e more distal point from a sand-bearing current has been deduced (K s i ą ż k i e- w i c z, I960, 1961; J a w o r o w s k i , 1966).
4. The microfauna of the shales im m ediately underlying such sand
stones has not been investigated.
EOCENE IN T E R F A C IA L A S S E M B L A G E S OF THE M A G U R A SE RIES
By interfacial assemblage is m eant a concentration of foram iniferal tests occurring as a layer, usually of thickness equal to the diam eter of a single shell, and coincident w ith the erosional shale/sandstone inter
face, where successive beds make contact. These assem blages are only found where fine-grained sandstones rest upon shales; in instances, w here either the sandstone is m edium - or coarse-grained or w here the shale contains a significant proportion of the coarser size fractions, interfacial assem blages o f microfossils do not norm ally occur. For descriptive pur
poses, four different typ es of interfacial assem blages are here named after the genus usually predominant among those com m only appearing in a given assemblage:
1. Aschemonella assemblage, 2. Bathysiphon assemblage, 3. Hyperammina assemblage, 4. Sphaerammina assemblage.
It is emphasized that, by definition, such an assem blage is character
istic for a part of a given interface on ly and is not necessarily typical as a w hole for either the sandstone or shale elem ents respectively of the beds in contact at that interface. Also, a genus predom inating in a particular
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assemblage m ay appear in reduced proportions in a different assemblage.
An interfacial assemblage carries no age connotation.
L O C A L I T Y S T R E A M 1 « STRYSZAWA -R O Z T O K I 2 ZAWOJA - JAWORZYNA 3 ZAWOJA - JAWORZYNA
- POLICZ NE
4 ZAWOJA - K O Ń S K I E 5 K O J S Z d W K A -
W IE P R Z C Z A N K A 6 OSIELEC - OS IE LEC
CHRZANÓW O
WADOWICE
o
K R A K O W
®
M YŚ LEN ICE
o
S U C H A O ZAWOJA O
fc n .
O M A K tJ W JORDANÓW
50 KM
Fig. 1. S k e tc h m ap s h o w in g location of m a in points w h e r e in te r fa cia l a ssem b lag e s found
Aschemonella assemblage
This assemblage is known from a single occurrence in the Beloweza Beds, exposed in the stream Przywarowka, NW of Lipnica Wielka (locality beyond the area shown in Fig. 1). Test of Aschemonella B r a - d y are irregularly distributed as fragments up to 3 cm. long, showing
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random orientation in the plane of the interface. They frequently occur at the upcurrent ends of flute marks or are partially enclosed by sm all current crescents. The m aterial described was not located in situ and therefore the m icrofaunal composition of the underlying shales is not known. The absence of a preferred orientation w ith respect to the linea- tion defined by current-form ed interfacial structures suggests the possi
b ility that the tests underwent a m inimum of lateral displacem ent by the sand-depositing current. This interfacial assem blage (Plate XC, Fig. 1) is also known from the Inoceramian Beds and Variegated Shales of the Polish Western Carpathians (M. K s i q z k i e w i c z , personal communication, 1967).
Bathysiphon assemblage
An interfacial assem blage consisting exclusively of narrow, elongate and tapering tubes, referable to the genus Bathysiphon M. S a r s (fide L o e b l i c h and T a p p a n, 1964, p. 186), is of fairly common occur
rence in the Hieroglyphic Beds and in fine-grained com plexes belonging to the Osielec Sandstone. The tubes are made up of fine-grained siliceous m aterial held together by a chalcedonic cement. They m ay reach lengths of 7 cm., as in the uppermost Hieroglyphic Beds, exposed in the stream Wieprzczanka, near Kojszowka; tubes of lengths up to 3 cm. are most com m only seen. Tests are generally laterally compressed and buckled, so as to give hour-glass and C-shaped cross-sections. Further evidence of the flexib ility of these tests is provided by the common occurrence of tubes bent so that, in each case, an acute angle is described by two connected portions of the tube. On the other hand, Bathysiphon tests are frequently transected by fractures at right angles to the w alls and divid
ing the tubes into sections up to 1— 2 mm. in length (see P late XC, Fig. 2). These sections correspond in size to fragm ents of Bathysiphon found as part of the microfauna yielded by disaggregated shales.
The m icrofaunal composition of this interfacial assem blage is unvar
ying, comprising tests of Bathysiphon only. The most striking variation exhibited by the assem blage is in population density, w ith different interfaces characterized by rare, common or abundant tests.
In relatively sparse assemblages, tests frequently show a w ell devel
oped preferred orientation. The lineation so defined usually corresponds to that given by sedim entary structures at the same interface or to the direction of m axim um dip for cross-lam inae in the sandstone above the interface. Current-formed structures at these interfaces include grooves at the upcurrent ends of tests (Plate XC, Fig. 3) and downcurrent scours as described by K s i ^ z k i e w i c z (1961), as w ell as current crescents developed at the upcurrent ends of tests (Plate XC, Fig. 4). P late XC, Fig. 4 shows a concentric arrangement o f Bathysiphon tests, evidently formed by the action of vertical vortices, follow ing entrapm ent of the
tests in a depression of the mud surface.
Tests of sim ilar dim ensions tend to occur together in these sparse assem blages and bent tests are rare or absent. Furthermore, fragm ents of Bathysiphon are extrem ely rare in the shales below the interface.
Thus the relatively sparse Bathysiphon assem blages display a number of features w hich suggest that the tests have undergone lateral displa
cem ent by the currents from which sand was deposited. Assem blages of this type are known from the Osielec Sandstone, exposed in the stream
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Roztoki, Stryszawa, and the stream Osielec, Osielec Górny, from the uppermost H ieroglyphic Beds in Roztoki, and from the Below eza Beds of Ochlipów, Zubrzyca Górna.
A ssem blages richer in individuals reflect a dim inished influence of current activity upon a given population. For instance, in the upper part of the Hieroglyphic Beds exposed in Końskie, Zawoja, shale elem ents in the order of 3— 6 cm. in thickness and containing abundant B a th y si phon, visible in hand specimen, are each succeeded in vertical sequence by sandstones in w hich Bathysiphon is rare or absent. A t the interfaces between beds, Bathysiphon tubes are found in rich assem blages showing a low degree of preferred orientation. Bent tests are fairly common. Tool markings are rare and scour structures absent. Thus the Końskie assem blages are considered to be autochthonous, as are certain Bathysiphon assemblages in the upper part of the Hieroglyphic Beds of the stream Wieprzczanka, near Kojszówka.
Hyperammina assemblage
A ssem blages in which the predominant form is Hyper am m ina B r a d y are found throughout the Hieroglyphic Beds. They are seen as tran
sitions betw een an im poverished fauna, comprising m ainly scarce tests of Hyperammina, and a rich assemblage, consisting of numerous, closely packed tests o f Hyperammina w ith subordinate amounts of other benthonic forms.
In the relatively sparse assem blages, tests of Hyperammina, up to 4 mm. in length, are frequently oriented in parallelism w ith the current- -direction given by flute-lineation and rare current crescents (Plate XC, Figs. 5, 6). Som etim es low, elongate scours are located at the downcurrent ends of tests. The tests are often bent into gentle sigmoid curves (Plate XC, Fig. 6). The minimum extent of current influence upon the assemblage is thus seen as rotation of tests into positions o f stability and widespread entrainm ent of bottom mud.
These current effects are further developed in the richer H y p e r a m mina assemblages. An extrem e exam ple is provided by an interfacial assemblage from near the top of the H ieroglyphic Beds in Wieprzczanka, between Wieprzec and Kojszówka. Here Hype ra mm ina predom inates in an assemblage comprising both tubular and m any-cham bered forms. The former are represented by Hype r am m ina, Psammosiphonella A v n i m e - 1 e c h (see P f l a u m a n n 1964, pp. 49— 54), Rhizammina B r a d y and fragments of Bathy siphon ; the latter by Sphaerammina, Trocham- minoides C u s h m a n , Haplophragmoides C u s h m a n , Recurvoides E a r 1 a n d, Lituotuba R h u m b l e r , Glomospira R z e h a k, and Aschemonella B r a d y .
Though the population density of the assem blage and its composition tend to vary within the interface, tests are closely spaced throughout.
Tubular forms and scarce fish -teeth (Plate XC, Figs. 5, 6; Plate XCI, Figs. 1, 2) are oriented parallel to the current direction given by the maximum dip of sandstone cross-lam inae above the interface (Plate XCI, Fig. 3) and by the trend of groove m oulds on the sandstone sole (Plate XCI, Figs. 1, 2). Hyperammina occurs as bent, som etim es bilobed tubes, found in a fragmented condition. The fragile, term inal sw elling of the tube, or proloculus, is som etim es present and usually indicates the up- current direction. Numerous, sand-filled grooves, exhibiting a preferred
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orientation in agreem ent w ith that of the elongate tests and bilobed like Hyperammina, are of common occurrence. These were presum ably formed as a result of bottom traction of Hyperamm ina tests. Psammosiphonella occurs as straight, undeform ed tubes, w hile Rhizammina in seen as Y-shaped, branching forms. Bathysiphon is present as scarce tubes up to 5 cm. in length and more com m only a® sm all, laterally folded frag
m ents found characteristically at the downcurrent ends of paired groove- -sets (Plate XC, Fig. 5; Plate XCI, Fig. 1). The m any-cham bered forms, taken as a single sub-population, show poor sorting and the proportions of the genera present vary over relatively short distances on the interface.
The presence of sm all, fragile tests of Aschemonella which show no preferred orientation, suggests this form suffered a m inim um of lateral displacem ent.
The closely packed foram iniferal tests and associated tool m arkings do not occur w here either o f two types of interfacial structure are found:
1. organic trails of Palaeophycus type, formed after the deposition of the sand layer,
2. flat-bottom ed, m ultiple groove-m oulds, up to 2 cm. in w idth and 0,5 cm. in depth.
These structures mark unfossiliferous, relatively sm ooth areas of the sandstone sole (Plate XCI, Fig. 2). In the case of Palaeophycus, rejection of tests by a sedim ent-eating burrower is indicated. The com paratively sm ooth surfaces of groove-m oulds evidence a much low er density of Foram inifera at only short vertical distances 'below the layer of tests presently preserved at the interface. W ithin the sandy infilling of a groove, but at the level of the interface on either side of the groove- -m ould, tests of Bathysiphon are frequently localized. Above the inter
face, for a distance of 4— 6 cm., organic rem ains are scarce (<C 1%). At this level, however, the amount of organic m aterial in the sandstone sharply increases (6%) in the form of tests seen at the interface, among
which Bathysiphon is conspicuous.
The faunal composition of the shale underlying the interface is as follows: Sphaerammina, Trochamminoides, Recurvoides, Psammosipho
nella, fragments of Bathysiphon and indeterm inate tubular forms (pro
bably Hyperammina). The most striking feature here is the extrem ely low proportion of Hyperammina, which m ay be explained in one of three ways:
1. the tests of Hyper amm ina were m ostly destroyed during prepa
ration of the shale;
2. Hyperammina was allochthonous;
3. Hyperammina was autochthonous, but was confined to the upper
most, eroded part of the mud.
The first possibility is considered to be unlikely, since samples from other beds treated in a similar manner yielded varying proportions of Hyperammina. The presence of the fragile proloculus on tests in the interfacial assemblage is taken to indicate a m inimum of lateral displace
ment. Thus the third possibility is held as being most lik ely (see also N y h o 1 m, 1957, Fig. 1, p. 76, for the modes of life of some tubular, sm all Foraminifera).
Sphaerammina assemblage
Interfacial assemblages characterized by the predominance of Sph ae
rammina C u s h m a n are fairly common in the Hieroglyphic Beds.
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Other forms often present as minor constituents in this assem blage are Trochamminoides, Haplophragmoides, Hyperammina and Psammosipho- nella. Near the top of the Hieroglyphic Beds exposed in the stream Ja
worzyna, Zawoja-Policzne, 'interfaces w ith the Sphaerammina assem blage are of common occurrence in com plexes of beds w here fine-grained sandstones, 1— 6 cm. thick, are succeeded by shales of similar thickness.
The sandstones are usually made up entirely ripple-drift cross-lam inae and interfaces are relatively even. The assem blage is also frequently found in similar com plexes belonging to the Hieroglyphic Beds, seen in Końskie, Zawoja-Gołynia.
D ifferences are seen from one interface to another in population density, in associated current-formed, interfacial structures and in degree of disruption due to burrowing activity. On the basis of these three variables, four arbitrary subtypes of assemblage m ay be distinguished.
These subtypes may occur separately or to varying degrees mixed.
1. Sphaerammina and other m any-cham bered forms are randomly distributed within the interface (Plate XCI, Fig. 4). Sorting of m any- -chambered tests is poor. The only evidence of current action upon the assemblage comes from the preferred orientation of scarce tubular forms.
This is the most common variant of the assemblage, occurring w idely in Jaworzyna and Końskie.
2. There is relative uniform ity of distribution of Foraminifera w ithin the interface, but lateral displacem ent by the sand-bearing current is evidenced b y short, sand-filled grooves, each with a test at its down- current end (Plate XCI, Figs. 5, 6). The grooves are up to 2 mm. in length and the m axim um w idth corresponds to that of the adjacent test.
Throughout the Policzne section of Hieroglyphic Beds in Jaworzyna, grooves of sim ilar dim ensions are found on the soles of fine-grained sandstones, but w ithout the tools responsible for their formation. Clearly these structures evidence bottom traction of m any-cham bered Foram i
nifera. Plate XCI, Fig. 5 and 6 show Sphaerammina tests at the dow n- current ends of short grooves on the sole of a 7 cm. layer of convoluted sandstone from Policzne. The faunal composition of the shale below the interface is: abundant Sphaerammina, w ith Trochamminoides, ? Haplo
phragmoides and ? Hyperammina.
Therefore in this case, although some lateral m ovem ent of the tests is clearly indicated by interfacial structures, the assem blage is considered to be essentially autochthonous. It was concentrated prim arily in response to a vertical component of displacem ent, attendant upon the selective erosion of bottom muds b y the sand-bearing current.
3. Sphaerammina and other many-cham bered forms are som etim es concentrated by current action in depressions of the mud surface and by the activities o f burrowing organisms in postdepositional trails. In the Hieroglyphic Beds at Policzne, for example, closely packed concen
trates of tests occur as infillings of prod moulds, and in the Końskie section, Sphaerammina is concentrated in flute moulds (Plate XCII, Fig. il). Tests of m any-cham bered forms are som etim es found as accum u
lations in current-excavated trails of predepositional origin (compare w ith K s i ą ż k i e w i c z , I960, p. 739). These trails are usually of Sub- phyllochorda and Spirophycus types (see Plate XCII, Fig. 2— 4), showing localized fluting and w ith cross-lam inated infillings.
Likewise, tests m ay be concentrated in trails, post-depositional with
— 41719 —
respect to the sandstone above the interface. Plate XCII, Fig. 5 and 6, for example, show tests of Sphaerammina concentrated in a trail of Pa- laeophycus type, w hile in Plate XCIII, Fig. 1 and 2, tests occur abundantly in the system s of sand-filled tubes belonging to an irregular Paleodictyon network (sensu S e i l a c h e r , 1962, Fig. 1, p. 230). In the latter exam ple, the sandy tubes w ith Sphaerammina are also found in the uppermost part of the shale below the interface.
In all cases considered above, tests seen at the interface exhibit poor sorting, adult forms occurring w ith juvenile stages. The elongate shape of the tubular forms effectively excludes them from both the current- -form ed and organically generated types of assemblage.
4. Closely packed aggregates of many-chamibered Foraminifera, forming a discontinuous basal layer of thickness equal to the diameter of a single test, are seen on the soles of some fine-grained sandstones exposed in Końskie (Plate XCIII, Fig. 3, 4). Sim ilar aggregates, differing in that the tests are not so closely spaced, are also found on the upper surfaces of the underlying shales. Presum ably this splitting of an inter- facial assem blage is a result of unevennes in the distribution of cement, due to irregularities in the packing of tests. These aggregates comprise tests of Sphaerammina and extrem ely scarce tubular forms, usually represented by Hyperammina. The m any-cham bered tests are poorly sorted. In the shale sampled for a vertical distance of 1 cm. below such an interface, the faunal composition was: abundant Sphaerammina, w ith Trochamminoides and indeterm inate tubular forms. Thus a strong pre
dominance of Sphaerammina is a feature common to both the interfacial assem blage and the upperm ost part of the shale below the interface.
Rare, branching tests of Rhizammina, reaching up to 3 cm. in length (Fig. 2 and P late XCIII, Fig. 5), have been discovered in the same inter
faces as the sheet-like aggregates of Sphaerammina. T h e s e d e l i c a t e f o r m s , w e l l p r e s e r v e d a n d s h o w i n g n o s i g n s o f d e f o r m a t i o n , c a n n o t h a v e s u f f e r e d d i s p l a c e m e n t , e i t h e r v e r t i c a l o r l a t e r a l .
Fig. 2. D elicate, b r a n ch in g test of R h i z a m m i n a sp. on sa n d sto n e sole. H ie r o g ly p h ic Beds, M id d le Eocene. Stream Konsikie, Z a w o ja — (xolynia. T h e sa m e sp e c im e n is
sh o w n in PI. X C III, Fig. 5
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A ny one of the above subtypes may be found at a given interface, either separately or m ixed to varying degrees with one or more of the other three. The only exception here is that sheet-li'ke aggregates of tests (subtype 4), though frequently associated w ith random ly scattered, isolated tests (subtype 1) and often transected b y post-depositional burrows packed w ith m any-cham bered forms (subtype 3), are nowhere found together w ith current-form ed sedim entary structures (see sub- type 2).
O R IG IN OF IN T E R F A C IA L A S S E M B L A G E S
Four different origins are conceiveable for the interfacial assem blages of m icrofossils described:
1. The layer of foram iniferal tests w as laid down during the final depositional phase of the current, w hich formed the bed im m ediately below the interface. A ny pelagic deposits later formed were eroded away by the n ext suspension current, w ithout disruption of the layer. This approach, analogous to the view expressed by N e s t e r o f f (1961, 1963) and N e s t e r o f f and H e e z e n (1963), is not acceptable here because of the extrem ely poor sorting of tests making up a given inter
facial assemblage. For exam ple, coarse silt and all sand grades are frequently represented by tests of Sphaerammina in assem blages where this form is common. As pointed out by R u s n a k (1957, pp. 387— 389), differences in effective density and shape of current-borne organic re
mains of similar sizes give rise to differences in hydraulic behaviour (see also R u s n a k and N e s t e r o f f , 11964, pp. 489— 493). However, w here t e s t s c o n f i n e d t o a p a r t i c u l a r g e n u s , abundant in a given interfacial assemblage, display poor Size sorting, it is unlikely that th ey were transported any great distance prior to deposition.
2. The tests w ere eroded from bottom muds and carried b y a sand- -bearing current, to be deposited and concentrated as the coarse-grained fraction (compare w ith P h 1 e g e r, 1960, p. 98) at a more distal point.
Certainly evidence of tests having acted as tools during bottom traction and the concentrates of tests, found as infillings o f various types of interfacial structure, indicate that lateral displacem ent took place. H ow
ever, the strikingly poor sorting of tests, the good preservation of delicate tubular forms, such as Hy pera mm ina and particulary R h iz ammi
na, and good qualitative correspondence betw een the interfacial fauna and that of the underlying shale suggest that, in many cases, lateral m ovem ent was at a minimum. Clearly the degree of displacem ent of tests w ill vary from one interface to another, according to the consistency of the bottom sedim ent and the flow characteristics of the sand-depositing current.
3. In many cases, the m icrofossils w ere concentrated prim arily by vertical m ovem ents of tests, consequent upon the w innow ing aw ay of clay from the bottom muds (see K u e n e n, 1964) by a sand-bearing current. A minimum of lateral displacement, in the form of rotation of tubular forms into preferred orientation and perhaps lim ited rolling of many-cham bered forms, to give closely packed aggregates, took place.
This explanation satisfies the arguments against points 1 and 2 above, and is considered to be the one most generally acceptable.
4. A final possibility is that tests from the underlying shales were concentrated at the interface by the activity of burrowing organisms.
— 481 —
Though aggregates of indisputable organic origin are known, these are exclu sively in the form of tubes, and it is difficult to envisage how a continuous layer of particles m ight be generated by organic means alone. On the other hand, the widespread disruptive effects of burrowing upon interfacial assem blages should be borne in mind. Describing the Foram inifera of the slope province in the Santa Barbara Basin, off California, H a r m a n (1964, p. 86) wrote:
„Broken tests, sporadic frequency distributions of species, abnorm ally low foram iniferal numbers and large percentages of fecal pellets m ay indicate that the larger burrowing organisms destroy some of the foram iniferal tests”.
This passage suggests that H a r m a n had in mind m echanical effects of burrowing. The displacem ent and fragm entation of tests b y burrowers is w ell demonstrated b y certain interfacial assemblages, preserved on sandstones soles exhibiting abundant trails, postdepositional w ith respect to the sandstone. Displacem ent of tests is w ell illustrated b y the exam ple already discussed, in which Sphaerammina is concentrated into the tubes of an irregular Paleodictyon network (Plate XCIII, Fig. 1 and 2).
Som e soles, characterized by numerous postdepositional trails of Scolicia type, display both displacem ent and fragm entation of tests belonging to the Sphaerammina assemblage. Where Scolicia is seen as high, positive reliefs, tests are usually absent from the surfaces of the trails, w hile occurring in fair abundance on the „unburrowed” parts of the sole.
However, where the trails are low in relief, tests of Sphaerammina and Rhizammina m ay occur at the interface. In these cases, the latter is seen as broken networks of branching tubes (Plate XCIII, Fig. 6). Thus it is lik ely that burrowing action frequently led to the fragm entation of branching, tubular Foraminifera b y m echanical means. On the other hand, chemical effects appear to have been slight or absent, even where ingestion of tests can be inferred.
C O N C L U D IN G R E M A R K S
1. A ggregates of sm all, benthonic Foram inifera occur at the in ter
faces betw een thin, fine-grained sandstone and shale layers o f successive beds in sequences of Eocene flysch belonging to the M agura Series, P olish W estern Carpathians. The sandstone layers above such interfaces are usually made up of cross-lam inae of ripple-drift type.
2. Interfacial assem blages of sm all Foraminifera are frequently seen as interm ittent layers, varying considerably in the packing density of the tests and of thickness equal to the diam eter of a single test. Concen
trations of foram iniferal tests are also found in the depressions of the interface provided by trace fossils of various types and b y current- -form ed sedim entary structures, particularly flute moulds.
3. For descriptive purposes, different types of interfacial assem blage w ere named after the m ost com m only occurring genera. Forms pre
dominant at a given interface are frequently found making up reduced proportions of another assemblage.
4. Lateral displacem ent of tests by current action is clearly evidenced where the Foraminifera of an interfacial assem blage are found at the downcurrent ends of m inute groove moulds. Rotation in response to current flow above the present interface is indicated w here the long
31 R o c z n i k G e o l o g i c z n y t o m X X X I X
— . <482 —
axes of tubular tests are oriented parallel to the direction of m axim um dip of sandstone cross-lam inae above the interface.
5. That lateral displacem ent of the tests m aking up interfacial assemblages was at a minimum in some cases is suggested by:
a) poor sorting of the tests representing a particular genus in a given interfacial assemblage;
b) the lack of preferred orientation of long axes in assem blages w’here elongate, tubular forms predominate;
c) the presence of undamaged, fragile forms, such as tests of H y p e rammina w ith the proloculus and also delicate networks of Rhizammina;
d) instances in which the predominant genera of an interfacial assem blage predominate also in the shale below the interface. Such interfacial assem blages are thought to arise largely as a result of m ove
ment of tests vertically downwards, consequent upon erosion of the enclosing mud by a sand-bearing current.
6. Those interfacial assemblages, arising prim arily by vertical displace
ment of tests, may be considered as being essen tially in situ. They evidence time intervals betw een episodes of sand deposition, during which colonization of the mud bottom by small, benthonic Foraminifera took place. This was presum ably effected under conditions of either non- -deposition or pelagic deposition and in absence of strong currents.
7. It is lik ely that the calcareous tests of pelagic Foraminifera, w ith effective densities low er than those of the siliceous benthonic forms described, were preferentially eroded from the bottom, together with pelitic grains, usually to be deposited as part o f a fine-grained sandstone layer. It is suggested that the test m aterial of any calcareous forms concentrated at the interfaces was dissolved and redistributed throughout the sedim ent during diagenesis. The plane of lithological discontinuity, provided by the interface, would facilitate this process.
8. There is evidence that the burrowing activities of larger in verte
brates were effective in the disruption of interfacial assemblages and in the fragm entation of tests.
A C K N O W L ED G E M E N T S
The author g r a te fu lly a c k n o w le d g e s his in d eb ted n ess 'to Prof. dr. M. K s i ą ż - k i e w i c z, for reading the m a n u scrip t and for the loan of three sp ecim en s figured in the present account, and to Doc. dr. St. G e r o c h, for m a n y h elpfu l discussions.
Prof. dr. F. B i e d a kin d ly su g g e ste d som e a m en d m e n ts to the t e x t prior to publication. Research w a s carried ou t during ten ure o f a F e llo w sh ip a w a rd ed by the Polish M in istry of Education.
D e p a r t m e n t of Ge ol ogy , Jagi el lo ni an U n i v e r s i t y , K r a k ó w , O l e a n d r y Str. 2a
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Rocz. Pol. T o w . Geol. (Ann. Soc. geol. Pol.), 18: 151— 179.
D a n y s h V. V. — JJ,a ii bi m B. B. (1986). O K p v n H b i x ( J j o p a M H H H c l J c p a x b K a p n a T C K O M
$ .TH me (Large F o ra m in ifera in the C arpathian flysch). ITa^eoHT. C6oipHHK, 3:
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D ż u ł y ń s k i St. (1963), W skaźniki k ie r u n k o w e transportu w osadach flis z o w y c h (Directional structures in Flysch). S t u d i a geol. poi., 12: 136 pp.
D ż u ł y ń s k i St., S i m p s o n F. (1966), E x p e r im e n ts on in terfacia l current m a rk in gs. Geol. R om a n a , 5: 197— 214.
F u c h s T. (1895), Stu d ien über F ucoiden und. H iero gly ph en . De nk sc hr . Ak a d . Wiss.
Wie n, M at h .- Na t. CL, 62: 369— 448.
H a r m a n R. A. (1964), D istribution of Foram in ifera in the Santa Barbara Basin, California. M i c r o p al eo n to l og y, 10: 81— 96.
J a w o r o w s k i K. (1964), S truktury nagrom adzeń grap tolitó w na po w ie r z ch n ia c h w a r s t w o w a n ia (Structures o f g raptolite a m a ss m e n ts on stratification planes).
K w a r t , geol., 8: 91— 101.
J a w o r o w s k i K. (1966), Sole m ark in gs produced by graptolite remains. Bull.
Acad. Pol. Sei., Ser. sei. geol. дёодг., 14: 151— 153,
К h а 1 e t s к а у a O .N . — Х а л е ц к а л О. Н. (1967), Р асполож ени е граптолитов как показатель условий отложения осадков (The localization of grao to lites аз an in d e x of s e d im en ta ry conditions). Докл. Акад. Наук СССР, 173: 173— 174.
K s i ą ż k i e w i c z М. (1960), О niek tórych prob lem aty k a ch z fliszu K a ro a l p ol
skich: Część I (On som e problem atic organie traces from the fly sch of the Folish Carpathians: Part I). K w a r t , geol., 4: 735—747.
K s i ą ż k i e w i c z М. (1961), О niektórych s e d y m e n ta c y jn y c h strukturach fliszu karpackiego (On some s e d im e n ta ry structures in the Carpathian Flysch). Rocz.
Pol. T o w . Geol. (Ann. Soc. geol. Pol.), 31: 24— 36.
К u e n e n Ph. H. (19S4), The sh ell p a v e m e n t b elow oceanic turbidites. Ma r ine Geol., 2: 236— 246.
L o e b l i c h A. R. Jr., T a p p a n H .(1964), P rotista 2, in: M o o r e R. C. (Editor), T reatise on invertebra te pa leo nto logy, Part C. 900 pp.
N e a g u T. (1964), D uże otw o r n ice a g lu ty n a ją c e z k am p a n u K arpat ru m u ń sk ich (Large size agg lutinated F ora m in ifera from the Carpathians of Rumania). Rc c z.
Pol. T o w . Geol. (Ann. Soc. geol. Pol.), 34: 579— 588.
N e s t e r o f f W. D. (1961), La „sequence t y p e ” dans les turbidites terrigenes m o dernes. Re v . Geogr. p hy s. Geol. dyn. , (2), 4: 263— 268.
N e s t e r o f f W. D. (1963), Essai d ’interpretation du m ec a n is m e des courants de turbidite. Bull. Soc. geol. France, 7: 849— 855.
N e s t e r o f f W. D., H e e z e n B .C . (1963), E ssais de com paraison entre les tu r bidites m odern es et le flysch. R ev . Geogr. phy s. Geol. dyn., (2), 5: 113— 125.
N у h o l m K. G. (1957), O rientation and binding pow er of R ecent m o n o th a la m o u s F oram inifera in soft sedim ents. Mic r op a le on t ol o gy , 3: 75—76.
P f l a u m a n n U. (1964), G eo log isc h -m ik r o p a lä o n to lo g isch e U n te r su c h u n g e n in der F ly sch -O b e r k r eid e zw isch en W artach und C h iem see in Bayern. Ph. D. Thesi s, Univ. München, 180 pp.
P h i e g e r F. B. (1960), Ecology and distribution of R ecen t F oram inifera. J o h n H o p ki n s Press, B al t im or e, 297 pp.
R u s n a k G. A. (1957), T h e orientation of sand grains under conditions o f u n i
directional fluid flo w . Part I, T h eory and e x p e r im en t. J. Geol., 65: 384— 409.
R u s n a k G. A., N e s t e r o f f W. D. (1964), Modern turbidites: Terrigenous a b yssa l plain v e r su s bioclastic basin, in: M i l l e r R. L. (Editor), P a p e r s in m a r i n e g eol ogy ( S he par d C o m m e m o r a t i v e Vol.), 488— 507.
S e i l a c h e r A. (1962., P aleo n to lo gical studies on turbidite sed im en tation and erosion. J. Geol., 70: 227— 234.
S i m p s o n F. (1970), O se d y m e n ta c ji środkow eg o eocen u serii m agursk iej w p ol
skich Karpatach zachodnich (S edim enta tion of the M iddle Eocene of the M agura Series, Polish W estern Carpathians). Rocz. Pol. T o w . Geol. (Ann. Soc. дго1.
Pol.), 40.
31*
S 1 ą с z к a A. (1964), B u d o w a g eo lo g ic zn a jed n ostk i śląsk iej m ię d z y B ie ls k ie m a T ab aszow ą (G eology o f the S ile s ia n un it b e t w e e n B ielsk o and Tab aszow a, P o lish Carpathians). K w a r t , geol., 8: 199— 210.
V i a l o v O. S. — В я л о в О. С. (1966), О крупных ф орам иниф ерах S ilic in if era из верх не мелового флиш а Карпат (Large siliceous F o r a m in ifer a S ilic in ifer a fro m the Upper Cretaceous fly s c h o f the Carpathians). Палеонт. Сборник, 3:
27— 36.
V i a l o v О. S., P i s h v a n o v a L. S. — В я л о в О. С. , П и ш в а н о в а JT. С.
(1967), О некоторых кремистых фор ам ини ф ерах из миоц ен а западных о б л а стей У С С Р (On so m e siliceo u s F oram in ifera from th e M iocen e of wes'tern regions o f the U krSSR). Палеонт. сборник, 4: 35— 42.
STRESZCZENIE
We fliszow ych utworach eoceńskich serii magurskiej polskich Karpat zachodnich w ystępują nagromadzenia m ałych, bentonicznych otwornic, które usytuowane są na m iędzyrytm ow ych powierzchniach cienkich ła
wic drobnoziarnistych piaskowców i łupków (fig. 1, 2; tabl. XC— XCIII).
W ław icach piaskowców, które w ystępują ponad takim i powierzchniam i m iędzyrytm ow ym i, zazwyczaj spotyka się tylko struktury złożone ze wspinających się riplem arków (tabl. XCI, fig. 3; tabl. XCIII, fig. 4).
Miąższość skupień równa się średnicy skorupki pojedynczej otw ornicy.
Nagromadzenia skorupek otwornic obserw uje się także w zagłębieniach m iędzyrytm ow ych powierzchni, które mają charakter różnego rodzaju hieroglifów organicznych (tabl. XCII, fig. 2— 6; tabl. XCIII, fig. 1, 2) lub erozyjnych struktur prądowych, a szczególnie jamek w irow ych (tabl. XC, fig. 4; tabl. XCII, fig. il). Przy opisach poszczególnych, wyróżniających się typów om aw ianych skupień autor posługuje się nazwam i rodzajowym i dom inujących w nich otwornic. Formy dominujące w danym typie sku
pień mogą jednak w ystępow ać podrzędnie w innych typach.
W yróżniono następujące typ y skupień otwornic:
il. Zespół z Aschemonella, 2. Zespół z Bathysiphon, 3. Zespół z Hyperammina, 4. Zespół ze Sphaerammina.
W niektórych przypadkach w ystępow anie skupień otwornic w od- prądowych partiach śladów wleczenia (tabl. XC, fig. 3; tabl. XCI, fig. 1, 5, 6) wskazuje na lateralne przemieszczenia skorupek przez prąd. Również ułożenie najdłuższych osi rurkowatych skorupek rów noległe do kierunku m aksym alnego upadu w arstew ek skośnych osadów spoczyw ających po
w yżej św iadczy także o działalności prądu (patrz tabl. XC, fig. 5, 6). N a
tom iast o tym, że lateralne przem ieszczenia skorupek otwornic m usiały być na ogół minimalne, dowodzi: a) złe w ysortow anie skorupek danego rodzaju w danym skupieniu m iędzyrytm ow ym (tabl. XCIII, fig. 3), b) brak orientacji najdłuższych osi skorupek w skupieniach złożonych 2 podłużnych, rurkowatych form (tabl. XC, fig. 2), c) obecność nie uszko
dzonych, kruchych form, jak np. skorupek Hyperammina z zachowaną pierw szą komorą, lub delikatnych skorupek Rhizammina (fig. 2;
tabl. XCIII, fig. 5), d) przypadki, w których rodzaje przeważające w m ię
dzyrytm ow ym zespole dominują także w łupku poniżej powierzchni m iędzyrytm ow ej. Takie m iędzyrytm ow e zespoły utworzone są przeważ
nie w w yniku w ym yw ania przez prąd i m ają charakter residuum. Po
w stały one w rezultacie działalności tego samego prądu, który deponował
— 484 —
— 48’5 —
następnie w yżejległe osady piaszczyste. Owe m iędzyrytm ow e zespoły w y stępują zatem niem al in situ. Zespoły te świadczą o istnieniu przerw m iędzy epizodami depozycji piasku, w czasie których zachodziła koloni
zacja dna przez małe, bentoniczne otwornice. Przypuszczalnie miało to m iejsce w warunkach albo braku depozycji dennej albo depozycji pela- gicznej, a także przy nieobecności silnych prądów.
Jest prawdopodobne, iż skorupki wapiennych, pelagicznych otw ornic, które mają m niejszy ciężar w łaściw y aniżeli krzem ionkowe skorupki om aw ianych otwornic, zostały wybiórczo wyerodowane z dna wraz z m a
teriałem pelitycznym . Niezależnie od tego wapienne skorupki otwornic, o ile zachow ały się na powierzchniach m iędzyrytm ow ych, m ogły później zostać stosunkowo łatwo rozpuszczone podczas procesów diagenezy.
W badanych osadach można stwierdzić, że w skutek działalności w ięk szych zwierząt bezkręgowych skupienia otwornic b yły deform owane, a skorupki ulegały przy tym połamaniu (tabl. XCIII, fig. 6).
E X P L A N A T I O N OF P L A T E S
A l l photographs, w it h only tw o e x c ep tio n s m en tio n e d in e xp la n ation , s h o w lo w e r surfaces of sandstones. S c a le in m illim e tr e s . A rrow indicates direction of curren t from w h ic h sand deposited.
P la te X C
Fig. 1. B r an c h in g tes'ts o f A s c h e m o n e l l a B r a d y . A s c h e m o n e l l a a ssem b la ge.
S p ecim en fo u n d by Prof. Dr. M. K s i ą ż k i e w i c z . V ar ie g a le d S h ale s, P a la eo cen e. G u b ern a só w k a , L ipnica M ała
Fig. 2. T ests of B a t h y s i p h o n M. S a r s s h o w in g lack o f preferred orientation.
B a t h y s i p h o n assem blag e. H ie r o glyp h ic Beds, M iddle Eocene. Str ea m K ońskie, Z a w o ja — G ołynia
Fig. 3. T est o f B a t h y s i p h o n at d o w n c u r re n t end of groo ve mould. B a t h y s i p h o n a ssem bla ge. H iero g ly p h ic Beds, M iddle Eocene. S trea m Roztoki, S tr y sz a w a Fig. 4. In centre and on r ig h -h a n d side in fillin g of cu r r en t-fo r m ed scour w i t h con cen trica lly arranged tests of B at h y s ip h o n . On le f t -h a n d side, current crescen t fo rm ed around B a t h y s i p h o n test. B a t h y s i p h o n a ssem b lag e. H ie r o glyphic Beds, M iddle Eocene. S tream W ieprzczanka, W ieprzec
Fig. 5. Tests of H y p e r a m m i n a B r a d y s h o w in g preferred orientation and sm a ller proportions o f m a n y -c h a m b e r e d forms. L a rg er-sca le, double ridges are groove m ould s w i t h fra g m e n ts of B a t h y s i p h o n tests at the d ow n c u r re n t ends. H y p e r a m m i n a a ssem blage. H ie r og lyp h ic Beds, M iddle Eocene. Strea m W ieprzczanka, W ieprzec
Fig. 6. D e ta il from surface sh o w n in Fig. 5. R ight of centre is oriented fish tooth
P la te X C I
Fig. 1. G roove m o u ld w i t h f r a g m e n t of B a t h y s i p h o n test at d o w n cu rren t end.
H y p e r a m m i n a assem blage. H iero gly p h ic Beds, M iddle Eocene. Stream W ieprzczanka, W ieprzec
Fig. 2. In centre, groo v e m ou ld w it h r e la tiv e ly sm ooth surface and w ith o u t fo r a - m in ifer a l tests; on either side, num erous tests o f Fo ram in ifera cover sole.
Crossing, postdeposition al burrows w ith o u t tests. Top, le ft-h a n d side: o r ie n ted test of B a t h y s i p h o n . H y p e r a m m i n a assem bla g e. H iero gly p h ic Beds, M id dle S trea m W ieprzczanka, W ieprzec
Fig. 3. P o sitiv e print of X - r a y photograph, s h o w in g part of v e r tica l cr o ss-sec tio n through la y er of fine grained sandstone. L o w e r surface w it h in te r fa cia l
— 486 —
a ssem blage. In section are seen clim b in g ripples w ith erosion of upcurrent sides. H ie r o g lyp h ic Beds, M iddle Eocene. Stream W ieprzczanka, W ieprzec Fig. 4. D iso rderly arran g em en t of tests o f S p h a e r a m m i n a C u s h m a n . S p h a e
r a m m i n a assem bla ge. H ie r o g ly p h ic Beds, M iddle Eocene. Stream Jaw orzyna , Za w o j a— P o l i c zn e
Fig. 5. T ests of S p h a e r a m m i n a at d o w n c u r re n t ends of m in u te g r o ov e m oulds.
S p h a e r a m m i n a assem blage. H ie r oglyp h ic Beds, M iddle Eocene. Strea m J a w orzyna, Z a w o ja —P o lic z n e
Fig. 6. T ests of S p h a e r a m m i n a at d o w ncurrent ends of m in u t e groove m oulds. Other data as in Fig. 5
P la te XC II
Fig. 1. Erosional depression of interface c on tain in g tightly p a ck ed tests of S v h a e - r a m m i n a . S p h a e r a m m i n a a ssem b lage. H iero gly p h ic Beds, M iddle Eocene.
S'tream J a w orzy n a , Z a w o ja — P oliczne
Fig. 2. P r edepositional burrow of Scolicia type eroded by current and fille d w i t h tests of S p h a e r a m m i n a . S p h a e r a m m i n a a ssem b la ge. H iero gly p h ic Beds, M iddle Eocene. S trea m J a w o rzy n a, Zatwoja v illa g e
Fig. 3. P red ep osition al 'burrow of S p i r o p h y c u s type, p a rtially eroded by current and fille d w ith tests of S p h a e r a m m i n a . S p h a e r a m m i n a a ssem b la g e . S p e c i
m e n found by Prof. Dr. M. K s i ą ż k i e w i c z . H ie r o gly p h ic Beds, M iddle Eocene. Strea m K ońskie, Z a w o ja — G ołynia
Fig. 4. P r edepositional burrow of Spirophycu-s type filled w i t h 'tests of S p h a e r a m mi na . O ther data as in Fig. 3
Fig. 5. Postdepositio n a l burrow of P a l a e o p h y c u s type filled w it h tests of S p h a e r a m m i n a . S p h a e r a m m i n a assem blage. H ierog lyp h ic Beds, M id dle Eocene.
Stream Jaw o rzy na , Z a w o ja —P o lic z n e
Fig. 6. Po stdepo sitio n a l burrow of P a l a e o p h y c u s type filled w it h tests of S p h a e r a m mina. L atter s h o w m ark ed d ifferen ces in m a x im u m diam eter of test. O ther data as in Fig. 5
P la te XCIII
Fig. 1. N e tw o r k of p ostdeposition al, „irregular P a l e o d i c t y o n ”. Fora m in ifera occur both on th e flat sa n d ston e so le and in tubes m a k in g up the network.
S p h a e r a m m i n a a ssem blage. H ierog lyph ic Beds, M iddle Eocene. S tr ea m J a w o rzyn a, Z a w o ja v illa g e
Fig. 2. Part of „irregular P a l e o d i c t y o n ” n etw o rk containing tes't of S p h a e r a m m i n a . S p h a e r a m m i n a assem blage. H ie r oglyp h ic Beds, M id dle Eocene. S tr ea m J a w orzyna, Z a w oja v illa g e
Fig. 3. D iscontinous la y e r of S p h a e r a m v i i n a tests w ith rare tubular forms, probably H y p e r a m m i n a . S p h a e r a m m i n a assem blage. H ierog lyp h ic Beds, M id d le Eocene.
Stream K ońskie, Z a w o ja — G ołynia
Fig. 4. P o s itiv e print of X - r a y photograph; part of v e r tica l cr o ss-sec tio n through layer, the sole of w h ic h is sh ow n in Fig. 3. L o w er surface w ith S p h a e r a m m i na a ssem blage. In section rip p le-d rift and trough cro ss-la m in a e . H ie r o glyp h ic Beds, M iddle Eocene. Stream K ońskie, Z a w o ja — G ołynia
T ig. 5. D elicate, branching test of R h i z a m m i n a sp. S p h a e r a m m i n a assem blage. H ie r o glyphic Beds, M iddle Eocene. Stream K ońskie, Z a w o ja — G ołynia. Com pare w ith Fig. 2, p. 479.
Fig. 6. F oram iniferal te s t s ( p r o b a b l y R h i z a m m i n a ) fra g m e n ted as the result of b urrow ing action of larger in v erteb ra tes w h ic h g a v e rise to postdeposi'tional trails of Scolicia type. S p h a e r a m m i n a assem blage. H ie r o gly p h ic Beds, Middle Eocene. Stream Jaw o rzyna , Z a w o ja—'Policzne
R o c z n i k Pol. T o w , Geol., t. X X X I X z. 1— 3 Tabl. X C
F. S i m p s o n
R o c z n i k Pol. T o w . Geol., t. X X X I X z. 1— 3 Tabl. X C I
F. S i m p s o n
R o c z n i k Pol. T o w . Geol., t. X X X I X z. 1— 3 Tabl. X C I I
F. S i m p s o n
R o c z n i k Pol. Tovo. Geol., t. X X X I X z. 1— 3 Tabl. X C I I I
F. S i m p s o n
