FISHERIES AND MARINE SERVICE
Translation Series No. 4452
The history of the Lunz Lakes, bogs and forests
by H. Gams
Original title: Die Geschichte der Lunzer Seen, Moore und Walder Vorlaufige Mitteilung
From: Int. Rev. Gesamten Hydrobiol. Hydrogr. 18: 305-387, 1927
Translated by the Translation Bureau (OK) Multilingual Services Division • Department of the Secretary of State of Canada
Department of the Environment Fisheries and Marine Service Freshwater Institute Winnipeg, Man.
1978
10d1 pages typescript DEPARTMENT OF THE SECRETARY OF STATE SECRÉTARIAT D'ÉTAT TRANSLATION BUREAU BUREAU DES TRADUCTIONS
MULTILINGUAL SERVICES DIVISION DES SERVICES DiVISION CANADA MULTILINGUES
CLMNrS NO. DEPARTMENT DI VI SI ON/BRANCH CI TV N° DU CLIENT MINISTÉRE DI VISION/DIRECTION VILLE 1486902 Environment Freshwater Institute Winnipeg Manitoba BUREAU NO. LANGUAGE TRANSLATOR (INITIALS) N° DU BUREAU LANGUE TRADUCTEUR ( INI TI ALES) 1 8 1979 1486902 German OK JAN
GAMS , H.: "Die Geschichte der Lunzer Seen, Moore und Wglder, Vorlâufige Mitteilung," Internationale Revue der gesamten Hydrobiologie und Hydrographie, Band 18, pp. 305-387, 1927. [From the Biological Station Lunzl. With 4 PLATE Supplements and 12 TEXT Figures.
1 (305) H. GAMS (Wasserburg at Lake of Constance)
THE HISTORY OF THE LUNZ LAKES, BOGS AND FORESTS
Preliminary Communication
With contributions by Fr. HUSTEDT (Bremen) and Fr. STEINECKE (KUnigsberg)
INTRODUCTION
During the period from 1906 to 1910 Mining Director GE,TZINGER has in- vestigated the morphometry of the Lunz Lakes in an exemplary manner and, fur- thermore, through quite a number of soundings, he has established the distri- bution of both the bottom surface sediments and the nonsedimented areas. Like Albert HEIM before him, GUTZINGER determined the rate of present-day sedimen- tation with the aid of mud chests. Even though the methods of that time per- mitted no more than a predominantly mechanical and chemical investigation of the superficial sedimentation, GUTZINGER yet suggested as early as in 1912 to obtain information "about the mode of sedimentation of mud in suspension, the nature of stratification, the velocity of sedimentation during the post-glacial period and also the amount of denudation and erosion in the catchment area of the lake through borings into suspended matter." But up to now this task has not been carried out for the mud in suspension.
ED1r-:D TRAM For inTorrnMion ch.11%,e
. TRADUCT'iON NON R. ';'.1i5F2 Information seu!arnant
SOS-200-10-91
7530-21-029-5332 2 (305)
A first period of research into the Lunz Lakes has been completed
by the contributions published in the InternationaleRevue from 1912 to 1917.
In the meantime many new problems have arisen and have partly found their so-
lution with the aid of new research methods. The stratigraphy of the lakes in
particular has been explored by L. VON POST, R.SANDEGREN and, mainly, by G. (306)
LUNDQVIST and by H. THOMASSON, who linked it most closely with bog stratigra-
phy; by elaborating the micropalaeontological methods worked out by C.A. WEBER
and N.G. LAGERHEIM, they promoted these studies in a manner unsuspected up to
quite recently and as yet little known outside of Scandinavia.
Already prior to the War, SCHREIBER, ZAILER and WEBER had investigated
many bogs of the Eastern Alps in a cursory, explorative manner and, during re-
cent years, it was particularly Fr. FIRBAS who has greatly increased our know-
• ledge about the structure and age of the East Alpine bogs, the silvan and cli-
matic history of the Eastern Alps, by providing numerous random samples of
pollen analyses. None the less, however, a systematically planned stratigra-
phic investigation of Alpine bogs is still lacking; and above all, the boring
technique and the analyses of microfossils by means of which chiefly LUNDQVIST
has opened up entirely new ways for inquiries into the history of lakes have
been applied - outside of Sweden - to a very small number of water bodies. Thus,
in the Plattensee [Lake of Plattenl the 15 - 25 m long Yopre profiles drilled \\ Ç
by the Balaton Commission (L6CZY 1916, TREITZ and others 1911) have been sub-
jected only to a mechanical and chemical as well as qualitative analysis for
diatoms (by PANTOCSEK). Beginnings of microstratigraphic investigations, how-
ever, have been conducted, for example, at the Baldegg Lake, Zurich Lake (NIP- • KOW), plus Lake of Constance and Walchen Lake. 3 (306)
During the first post-war years, after having repeatedly visited quite
a number of Swiss and Bavarian bogs and having carried out a monographic inve-
stigation of a smaller West Alpine area, I came to know many Scandinavian bogs,
frequently in the company of Norwegian and Swedish friends; I also inspected
Alpine bogs, beginning with Western Switzerland and then proceeding as far as
to the Salzkaumiergut and the Lungau. Results of these studies have been partly
incorporated in "Post-glacial dimatic changes and crustal Earth movements in
Central Europe" (1923), written in conjunction with R. NORDHAGEN.
In the fall of 1924 I began to study the higher vegetation of the Lunz
Lakes and soon extended this research to the entire Dürrenstein area, paying a
particular attention to the history of that vegetation as it can be reconstruc-
ted from deposits in the bogs and lakes. The publications already on hand prove • that the region of the Lunz Lakes islmost highly suited for this type of studies; especially so subsequent to the newly published investigation by BREHM & RUTTNER
of the biocoenoses of the Lunz water bodies. Thanks to the support by the Kai- (307)
ser Wilhelm Gesellschaft zur Fiirderung der Wissenschaften [KAISER WILHELM SO-
CIETY for the Promotion of Sciences 1 and the NOTGEMEINSCHAFT der Deutschen Wis-
senschaft [Emergency Society for German Sciencesl, chiefly, however, due to the
quite extraordinary obligingness of the [Lunzl Station Director Professor Dr.
F. RUTTNER and his technical coworkers Karl HERRMANN and Joseph AIGNER, this my
research has already progressed to a point where it appears desirable that cer-
tain results of a general interest should already be published now; thereby I
could simultaneously repay at least a part of my debt of gratitude to the above-
named gentlemen and other workers of the Lunz Station. Among these personali- • ties Dr. F. HUSTEDT has assisted me through determinations of fossil diatoms 4 • (307) Dr. F. STEINECKE through identifications of recent and fossil algae, rhiseods
and Rotatoria; Prof. Dr. A. THIENEMANN through determinations of some fossil
larvae of the Chironomidae; Dr. E. WASMUND through the analysis of a drill pro-
file from the Rehberg Bog; Miss S. RUOFF and Dr. H. WALTER helped me in com-
piling the inventories of vegetation. In this latter work I was also allowed to (308)
use photographs by Prof. Dr. KNOLL. I am furthermore obliged to Prof. RUTTNER
and Mr. H. KRAWANY for the photographs added here. The publication in this pa-
per of a few maps and bore profiles is intended to chiefly aid the above-named
as well as other coworkers in their future research activities. It will yet re-
quire several years of effort to complete the research program as planned. •
F i g . 1 . Drilling of 'i ore profile E from the ice of the Untersee [Lower Lakel. In the background Seehof, spikes of Maiss Mountain and • the Scheiblingstein. - Phot. H. G A M S. 4 March 1927. 5 • (308) Both during the compilation of vegetational inventories plus mappings
as well as during drilling activities through bogs, from the quaking moss car-
pet of the Obersee [Upper Lunz Lakel and the ice cover of the Untersee [Lower
Lunz Lake], I have been using measurement lines of a 200 m length. The peat
auger for drillings, constructed by K. HERRMANN essentially after the HILLER
model and manipulated by K. HERRMANN and J. AIGNER during every yearly season
with an undiminished working enthusiasm (see F i g . 1 ), has a 50 cm long
chamber, a 3 cm clear-diameter drill hole, plus 10.5 m tubing, so that, for in-
stance, the yearly layers of varved clays and numerous macrofossils can be ex-
tracted uninjured from depths of up to 11 m. The methods of investigation as
such are the same as used by the Swedish bog geologists, so that it will suf-
fice to refer the reader to the representations of LUNDQVIST in the Textbook • of Abderhalden (1926) and in LUNDQVIST's "BinnengewNsser" [Inland Watersl of 1927.
THE COLUMNAR `BORE PROFILES OF LUNZ
the shore banks of the Untersee [Lower Lakel
Up to now we have tyre profiles taken from the ice of the following
shore spots (cf. the maps of GUTZINGER in InternationaleRevue of 1912, Plate
18; 1926 [XVI, 5/6 ] , pp. 284):
Northern bank between P. VI and VII (profile 11 of map p. 284 at the
fisher house Deuretsbacher), designated as A and Da - Dd . (The point profiles
A, B and C were drilled in March 1925, the line profiles D, E, F in March 1927; • from the former samples were removed at intervals of only every 50 cm, from 6 • (308) the latter at every 25 cm, or spaced yet nearer to each other).
Northern bank between P. XIII & XIV through the bog at the Steinbauern-
line, designated as E - E a d (see F i g . 1 ).
Southern bank at P. III at the Schlegelberg, designated as B and F - a F (point B lies somewhat more to the east than F and F , hence falls out of c b c the line profile F but has yet been marked into it, as seen in F i g . 2 .
Southern bank at P. IX, near the fish tank, designated as C.
All of the line profiles run nearly accurately N - S, perpendicularly
to the length axis of the lake and also the direction of the prevailing west- (309)
erly wind. As such the latter circumstance is undesirable, but it could not be
avoided because, as is shown by the 1912 map of bottom facies (Pl. 18), the
boring of deeper line profiles is rendered unfeasible by the creek gravel at
the weather side in the east and the exposed Opponitz lime at the sheltered side
in the west. Like in LUNDQVIST, in my F i g • 2 , the wind exposure is indica-
ted by hatched lines, the profile orientation by an arrow, both traced into
the compass cards.
As could be anticipated already by the representations of GUTZINGER
and of RUTTNER, also by findings of LUNDQVIST in Swedish lakes, the shore bank (310)
is of an entirely different composition at the four drilling points: in parts,
bore profile D consists of wonderfully layered glacial clays and lacustrine
Cretaceous of a more than 5 m thickness; bore profile E of but indistinctly
stratified sands and clays upon Opponitz lime, exposed lakeward, plus Lunz
sandstone, from which, it would seem, originate the massive sand layers, over-
lain shoreward by a remarkable flat-bog formation; bore profile F consists of • a lime-rich, coarse-detritus gyttja with numerous intercalations of coarse
7 • (309)
U1, 14“ 7 1?Y9 1!.1 1P,U07 1:1 1Vm
.. , . Ikne (1),1-7 mnm WM L2M ----1 MM --- Tonytteuma . Anst thentler Soho t mki reinlond EiÀnderton Ung .c$chicht , Ton— mit . _ Pole Gerell Seter Ton Uhl.: fete is en I I (2),1-7 uag KM2 oem MA MgM MO Mil Schkeciimm Grotkle I ritus DrIf tell tits 1..40 tio reindevitul• SgtIttum .1 g.lhgetia Gtdit. &udder/ ( 1) (IYILl. ttltemin 1 - 7: solid rock; rock debris fine sand; varved clay; unlayered clay; & gravel; • clay with iron sulphide; clay gyttja (2) 1 - 7 : lime gyttja; snail gyttja; general coarse drift gyttja; foliage detritus; gyttja; fine-detritus gyttja; sedge & marshy peat;
.i, .i., a, H f 4.fr-Mi .et, '' ■.f `V"'"V> t i t 11 1 1 1 Ant irsat J.,. ch.9ra-a.. flocks Potamogeton Polamageton £quisetum Sehamoplec. 5n(ipyrelira ci.denva prelonsus ',deans 9 I inunutta itf7 Legere., 1 – TX iV''..e.ele Iii gnitiitesruleng** 4- j. i• fr4ain ur Bohrpi ffil. ejelet rizont0a. ge Pleapnitea Care, infla14, Saltx p.micuiate,tke,. ringrea u.a. raceJalar Vegetation Came-unit self-explanatory ,_ '>----boring profile; **=guide horizons I - IX; ***=profile orientation C. F i g . 2 . '4ore profiles through shore banks of the Lunz Untersee [Lower Lakel. Circles not characterized by letters designate mere probings. The hatchings in the compass cards (N at the top) that indicate the orientation of the profile mark the exposure to the predominant westerly wind. Further explanations in the text.
drift material and gravel; bore profile C is built up of rock debris from
slopes and overlain but lakeward by lacustrine Cretaceous. 8 • (310) Due to the fact that up to now only a smaller number of the'or:e>le pro-
files have been analysed for pollen and other microfossils, 1 do not include
the results of individual analysed sections but reproduce merely certain pol-
len diagrams (Fig. 3 ; see also Fig. 11, p. 359). ***)
I regard as synchronous horizons of a provisionally purely local signi-
ficance the ones I list in the following;(even for the Obersee [Upper Lakel
they are not more than partly valid);
I. A layer of clay with abundant intercalations of black iron sulphide;
at point Dd it tops the series of varved clays that comprise more than 300 year-
ly layers (see F i g . 11 ). In a sample taken therefrom I was unable to find
more than one single pollen grain of Pinus, even after having treated the sample
with hydrochloric and hydrofluoric acids (10 cm higher 1 Pinus and 1 Salix).
U. The first profuse occurrence of Pinus and Larix, plus the first ap-
pearance of Betula, Corylus and Picea pollen (spruce comes somewhat subsequent
to birch and hazel, which, in contrast to Picea pollen, strongly decrease again
later).The significance of this horizon, thus far ascertained exclusively in
bore profile D, will reveal itself only when compared with corresponding deposits
at the Rehberg [Roe-deer Mountain] near the Obersee and the Rotmoos [Red moss
Bogl; see F i g • 11 .
III. The first occurrence of oak/mixed-forest, the constituents of which
(elm, linden and oak) appear nearly simultaneously. At first elm pollen pre-
dominates regularly over linden; later (approximately in Horizon IV) the
***) TRANSLATOR'S NOTE. All page references indicate German text pages, as in- dicated in parentheses at the top and right-hand margins of the trans- lation pages. 9 110 (310)
relationship is reversed. In none of the thus far analysed 'bore profiles from \C
the Lunz area, however, oak pollen attains more than two per cent.
IV. The first occurrence of silver fir (Abies) and beech (Fagus)which,
in the discussed area as well as the greatest part of the northern Alps and
their foothills regularly appear together and are relatively very early here. (312)
At first Abies is habitually dominant, whereas only between Horizons VI and VII
the relationship is reversed.
V. The hazel climax, when the Corylus pollen always attains 30 to about
40% of the entire forest pollen (Corylus not included).
VI. The first point of intersection between the fir curve and the spruce
or fir curve. It would seem that, depending on the exposure of the forests
above the liv)re profile, at first either spruce or fi r becomes dominant; in or-
• der, however, to eliminate purely local influences, a greater number of analy-
ses would be required. Horizons III to VI succeed very rapidly one after the
other. The fact that only about 1 - 2 m of sediment has been formed during the
time spanned by these four horizons in the thus far investigated profiles may
be explained either by the shortness of the period or by a relatively slow se-
dimentation.
VII. The first point of intersection between the spruce and the beech
curves.
VIII. The absolute beech climax which,in bore profile B, lies 21/2 m
above Horizon VII.
IX. The resumed ascent of the spruce and fir curves.
For the time being it is impossible to make a statement on the absolute • age of these Horizons; they are proposed merely in order to suggest a relative • •
40 20 159 510 se e0 ID ZO SO 10 20 30 LI0 50 50 I 1 - 1 1 1 1. I I g7. :,:77,, JJ1111
Profil A Profil -Ea' •
10 2.0 30 40 50 60 70 00 90 rUI
10 20 30 40 50 60 70 SO VIII 1 I I 1 t
Profil C
1 I Lower Lake bore profiles Iiiiterseeprofile
F i g . 3 . Pollen diagrams from the shore banks of the Untersee [Lower Lake] (See Figs. 2 and 11 for symbol explanations. 11 • (312) chronology which, possibly later, may be transformed into an absolute correla-
tion by connecting the horizons with datable bog profiles from the same area and
other regions (cf. p. 362).
It follows from the analyses thus far on hand that, at the north shore,
the formation of the shore banks has begun immediately upon the ice retreat
from a part of the Untersee. Since, at bore-profile point D I was able to count d' at least 300 yearly layers in the varved clays, a minimum of just as many years
must have elapsed from the moment the lake opened up until the total recession
of the ice. It is very likely that this time interval will turn out to be longer
subsequent to borings into yet deeper layers. (Ice conditions in March 1927 have
precluded such an undertaking).
After its first melting the Seebach [Lake Creek] Glacier has no longer
• reached the Untersee. Contrary thereto, however, a decrease in most of the micro-
fossil groups, comlined with an increase in coarser mineral particles between Ho-
rizons II and III, seems to indicate a glacier advance at a greater altitude, a
fact detectable indeed in the bore profiles from the Obersee and the Rotmoos
(see V i g • 11 , p. 359).
The formation of the shore banks at the southern shore must have started
only after the immigration of the oak/mixed-forest (III) and must have lasted
in point B as long as beyond Horizon IX, probably even as long as into the (313)
present time, whereas in C as well as also in A it was over already before
the beginning of the true beech period (VII).
Consequently, here we are in the presence of old sediments, a fact not
to be wondered at when we consider GUTZINGER's findings, namely that large ex-
panses of the lake bottom are formed by solid rock; a similar situation has been
established in Swedish lakes. 12 • (313) ' Bore profiles D, F and C have hit larger masses of gravel and crushed
rock. Whereas the latter - to the extent that probings undertaken up to now
admit of concluding - seem to rest in D and C directly upon solid lime, this is
not the case in bore profile F : here, yet 1.8 m of mud deposits are subjacent
to the debris, the accumulation of which has taken place only between Hori-
zons V and VI.
bore profile E cuts throughavery remarkable bog formatio n,
unique in the entire Untersee area. My assumption - based upon a mere external
examination - that, at this spot, we are not in the presence of a young deltaic
build-up but of a fossil bog now in the process of erosion has been fully con-
firmed by the borings; moreover, the latter have also provided an explanation
for the thus far incomprehensible fact why, precisely here at this spot and ex-
• clusively here, such a massive peat formation was able to develop (we established
as maximum thickness 1.45 m, the greater part of which lies below today's
lake surface).
This entire swamp is a flat bog, built up mainly of Carex species (gra-
cilis, paniculata, of Davalliana and others), with a dense ground mat of Cli_
macium dendroides and Acrocladium cuspidatum. Lakeward Dryopteris thelypteris
and Menyanthes are found among others as well as also shrubbery of willow (par-
ticularly Salix cinerea) and alder. Similar species constitute the totality of
the peat layer.
Subjacent thereto is a quite thin layer of dendroid sand and lime-rich
drift material, underlain in its turn by a massive deposit of but indistinctly (see F i g . 2 ) stratified clay, which is only bottomward somewhat sandy/.1t would seem that II/ this fossil-devoid, up to 5 m thick deposit is of glacial origin.
13 • (313) Already the diverging character in comparison with the much more sandy
deposits upon the shore bank, as well as the further circumstance that in bore
profile at point Ec - outside of the entire bog formation - solid rock was hit
as rapidly as at a 95-cm depth, would justify the assumption that, for a long
time,a separate basin, independent of the lake, has existed here.
It is nothing else but the lower continuation of the clay trough near the Stein- (314)
bauer farm. For a longer period, either the surface level of the Untersee was
by about 1 m lower than today, or the separating rock-bar (a continuation of the
Steinbauer sunmdt) was higher and decreased later maybe by shore erosion, which,
as is shown in the bore profile, has also worn away a part of the bog. I would
regard the latter alternative as more likely.
The bog formation must have taken place at a period when this small ba-
sin was still separate and possessed a lower water table than today. By pollen
analysis this period can be determined.
Unfortunately, all of the constituent peat, especially the lowermost
and uppermost layers, are decomposed to a degree that the pollen of deciduous
wood is partly destroyed and no longer quantitatively determinable. None the
less, even the analysis of three samples from depths of 45, 120 and 130 cm at
point Eal permit a sufficiently certain age determination. We might give here
only the percentage figures for conifers and beech, since a good part of the
alder, hazel and oak/mixed-forest pollen can no longer be safely identified
(see also F i g • 3 ):
depth : Pinus Picea Abies Fagus • 45 mn 3 32 53 13 120 mn 7 36 42 12 • 130 mn 0 29 39 20 14 • (314)
These figures make it sufficiently obvious that the bog formation must
have taken place during the time between Horizons VI and IX, very likely even
merely between VIII and IX because of the insignificant percentage of fir, plus
the decline of the beech curve.
Hence a very wide gap yawns between the eacial infilling of the basin
and the bog formation. It might probably be interpreted as follows: at first the
entire little basin was filled with clay and sand; and only later, when the sur-
face level of the Untersee was already lying lower than the height of the then-
present rocky ridge, the basin got completely eroded through rain and percola-
ting water. An alder swamp developed there in the beech-horizon period. Still
later, either the rock-bar at boring point E was sufficiently lowered, or the c • surface level of the lake rose so high that a further growth of peat became im- possible and that, much rather, parts of the formerly developed and probably
strongly decomposed peat was again worn away due to repeated droughts; this si-
tuation continues even into the present time after the wilful elimination of
the willow and alder copses for the purpose of replacing them with a vegetation (315)
that produces litter. Consequently, the entire bog formation bears a fossil cha-
racter and has nothing to do with a progressing deltaic formation at the Untersee.
As we shall see, similar conditions prevail also at the Obersee bogs .
In respect to the reasons why we have such differing ages in the sedimen-
tation banks of the Untersee, mere conjectures are possible for the time being,
as long as the conditions of lake currents have not been explored (pertinent in-
vestigations are in progress). The lack of younger strata upon several shore
banks is relatively easy to explain: normally, there is no longer any sedimen- • tation above a certain minimum depth; this depth seems to have been reached, 15 • (315) for instance, in bore profile D as early as prior to the time interval of
Horizon VII. Where the depth exceeds this limit of sedimentation, the sediment
either remains unchanged, is reworked, or is carried away. A sliding-off must
be chiefly supposed at the steep rocky slip-off slopes in the western half of
the lake (bore profiles E and C). At the northern shore, a preponderance of ero-
sion due to water and ice movements may have occurred (E; to a lesser extent also
D). The "zoogenous sand and mud," which GUTZINGER figures for a particularly wide
area at the northern shore, is to its largest part no "molluscan gyttja" in nor-
mal stratification, but an accumulation of partly whole, partly broken-up Val-
vatae, Limanaeae and Pisidia; this mass is of a very inconsiderable thickness,
just a washed-in agglomerate in a mostly secondary bedding that can be compared
with the shell zones in North German and Danish lakes (cf. WASMUND 1926).
It is also easily explainable that, for example, at the eastern shore,
in l ore profile F, such an active sedimentation is found of predominantly coarse
drift material. LUNDQVIST enlarges upon the fact that, especially in shallow
lakes with a rich bottom vegetation, the strongest sedimentation takes place
due to wind pressure at the shore exposed to the prevailing winds; contrasting
therewith, in deeper lakes, it occurs through counter currents at the opposite
shore. Obviously, the latter condition is also present in the Untersee. This
situation is further enhanced by the Seebach and other smaller creeks at times
carrying at the eastern shore a lot of coarse material into the lake.
It seems, however, more difficult to interpret the lack of older sedi-
ments at the southern shore. Possibly, prior to the formation of the shore banks,
depth currents have been more active here in opposition to the surface currents • produced by the prevailing westerly winds (cf. also EKMAN 1914). 16 • (316) Except for modelling the shores, the above-described occurrences are
likewise of greatest significance for the present-day vegetation. Since, in
anothi context, I am going to deal circumstantially with the vegetation, a few
indications may suffice at this point. The most luxuriant plant growth (Schoeno-
plecteta lacustris, Potamogetoneta natantis, Elodeeta, etc.) is found at the
northeastern shore, where three favourable circumstances combine: a strong se-
dimentation, due - on the one hand - to wind pressure; on the other hand to the
creeks; furthermore, fertilization through the canal water so rich in nutritive
substances. In like manner, at the place where the water trickles out, favourable
current conditions and a certain, even though less marked, fertilization result
in a rather lush vegetation (cf. bore profile 9 in BREHM & RUTTNER 1926, p.298).
Quite inversely, the shores with an insignificant sedimentation and, all
• the more, those exposed to erosion, carry a very scant vegetation. The following
plants in particular are lacking here on wide expanses: Phragmites, Schoenoplec-
tus and Potamogeton natans; in contrast and naturally, the chars with their ac-
cumulations of capsules find favourable conditions just in these places. Here,
Carex inflata forms its beds nearly exclusively upon the well-drained gravel banks.
Ultimately, we turn to a few findings concerning the history of immi-
gration of some inhabitants of the lake. More precise data thereon will not be
obtained before, on the one hand, the macrofossils are disaggregated by elu-
triation of larger sedimentary samples and, on the other hand, the microfossils
in their entirety are ascertained through quantitative analyses; for this, the
co-operation of several specialists is required.
As revealed by a comparison with the Obersee and Rotmoos bore profiles, • a great number of diatoms make their appearance already somawhat anterior to
17 • (316) Horizon II, which corresponds to the last (or penultimate ?) interstadial [in-
terglacial]; (these diatoms are, among others: Cyclotella species and Campylo-
discus noricus); also Desmidiaceae (Cosmarium, Eurastrum and Staurastrum species);
furthermore Myriophyllum spicatum, Bosmina coregoni and larvae of Chironomidae
(probably tanytarsids). Between Horizons II and III the diatoms decrease marked-
ly and the first Molluscs appear. I found the first Fontinalis leaves in TV,
where the Mollusca too (Valvata alpestris, Pisidia) are already more numerous.
Cyclotella bodanica begins before V, and it was here that I also found a pollen
grain of an Iridacea (Iris pseudacorus or Narcissus radiiflorus ?). Spongilla
lacustris seems to have arrived only between VI and VII.
The diatoms of the interstadial and stadial lacustrine Cretaceous of (317)
bore profile Dc (Horizons II to IV) are listed in the following compilation, • most graciously identified by Dr. Fr. HUSTEDT (symbols - ss = very scarce; s = scarce; z = scattered; zh = rather frequent; h = frequent; sh = very frequent;
m = in masses) : Lower Lake Unterseeprofil De .... , w Interstadial Stadial Poste. 5 à E e P bore profile Dc g› g W I.' Depth Tide in cm • 620 595 570 545 520 495 0 W U Achnanthos trinodis Am. — z ss z r — zh ss • 0 Amphora ovalis Kg.. . . z h h h I z __ h Amphora ovalis var. pedi- culus Kg. • — — — ss • s — h Anomoeoneis exilis (Kg.) --- - - — — ss h Anomoeoneis sphaerophura . (Kg.) — .---- . — — ss — fehlt h al ent Caloneis alpestris (Grun.) ' ss __. • __ Caloneis latiuscula (Kg.) — — — zh • • h Caloneis obtusa W. Sm.. . ss z sh fehlt Caloneis silicula var. ge- nuina CI z z s z Campylodiscus noricus
Ehrenb s z ss — — • s • h Cocconeis placentula Ehrenb ss ss s — h Cyélotella autiqua W. Sin. . — — ss • — .fehlt. Cyclotella bodanica Eul — — — — ss h Cyelotella distinguenda nov. . • spec. (s. S. 320) m sh zh h .— • sh fehlt Cymatopleura elliptica ' (Bréa.) W Sm • — s s Cymatopleura elliptica • var. constricta Grun. . . — -- z z z s h Cymatopleura Solea (Bréb.) W. Sm — — ss s —r. —• h __ .à Cymbella ae qualis. W. SM. ,, s' Cymbella amphicephala . . : Naeg ...... .. . ss ss .- ss — : .— Cymbella austriaca Grun — .—,/ — ss s Çymbella cistula Hempr ss -- sS — — -- h Cymbella dolicatula Kg. • -- s ss zli ---7 - - h Cymbella Ehrenbergii Kg s Ai m sh sh — • h - Cymbella helvetica Kg. — — — ss — ss h Cymbella leptoceros (E ) . Grun z s s s z s z
• 18 (318)
. . . ; ,,, ' ; ci Lower Lake Unterseeprofil. De ;1, ,-z: 4-1 0 , I ""•--‘' ,_,. 52; 0 81 bore profile Dc Interstadial Stadial. Postst.I.3 cz, r--- cr.) P depth Tide in cm 6 20 1_ 695 L 570 545 520 i - 495 P 0 , — — ______ : 0 Cymbella microcephala 1 -1-- i 0 Grun SS h Cymbella sinuata Greg, SS ■■■■•• Cymballa ventrieosa Kg. sit ; h ; Denticula tennis Kg.. • zh Zil h h Diatoma hiemale var. Ina- so don (Ehrenb.) Grun. . SS ss SS h Diploners domblittensis
var. sabconstrieta A. Cl. SS li Diploners elliptica (Kg.) Cl. z s S h Epithemia argus Kg. . . SS SS sh ss Epithemia Mblleri Fricke SS • — h SS Epithemia sorex Kg.. . . SS ! II Epithemia zebra var. por-
cellus Grua. s I S ---- I SS Eucocconeis; tlexella (Kg )
Cl zh z • z h • Eunotia circus Ehrenb. h h h sh Fragilaria capucina Desm. ss Fragilaria construens (Ehrenb.) Grun. zli sh h _ Fragilaria construens var. binodis Grun. h z z z , Fragilaria cons truens var, venter Grun h z Fragilaria Harrissoni (W. Sm.) Grun. _a ^_- SS z
Fragilaria pinnata Ehrenb. li zli z Frustulia styriaca Gram. , SS Gomphonemaconstrictum Ehrenb SS it Gomphonema intrieatum ;Kg 83 h Gomphonema intricatum var. pumila Grim, . , , ; z h • Gornphonerna olivaceurn Lyngb. •■■•■■■■■ SS s. Gomphonema parvulup Kg. -7- SS - Gomphonemasubclava- lum var. montanum • Schiun . SS
19 (319)
Lower Lake Untersee nora De ,u u
bore profile Dc -a' (a Interstadial Stadial Postst. E Depth Tiefe in cm 620 595 570 545 520 495 0 o0 Gyrosigma acurninaturn 0 (Kg.) h Gyrosigma attenuatum
(Kg.) - z zli h Ii Mastogloia Smithi var: Li- eus tri s Grun Meridion circulare (Grey ) Ag SS h Navicula cryptocephala Kg. SS h Navicula cuspidata Kg, ss • • Navicula cuspidata var. a m b ig u a Ehrenb __ . __ ss _ Navicula oblonga Kg. . z z h — su h Navicula placentula Ehrb. __ __ ss Navicula pupula Kg. . __ ss s s h Navicula pupula var. ree- tangularis Grun SS • Navicula radiosa Kg. . $ S S h Navicula tuscula Ehrenb. SS s ss z SS h Navicula viridula Kg, • SS h Navicula vulpina Kg. - z s SS h Neidium affine (Ehrenb.) Neidium iridis (Ehrenb.) h zh h Neidium productum (W. Sm.) h •Nitzschia angustata var. , ac.uta Grun, h • Nitzschla denticula Grun. zh Nitzschia recta Hantzsch . ss Nitzsehia sinuata var. tabollarla Onu. ss fehltl absent Pinnularia Brehissoni Kg. SS Pinnularia maier Kg. - h Pinnularia mesolopta var. stauronelfermis Grun„ z zh z, ,PInnularia viridis (Nitzseh) zh Rhopalodiagibba(Ehrenb.) o. Müll. ss Rhopalodia parallela . (CiTIM,) 0. Mtill„ . Sti I Z Steuroneis parvula (L'un. SS — I S • 20 • (320)
_ ■•■■• Unierseeprofil De a■ Lower Lake , bore profile De hiterstadial Stadia' Postst. o _ • in cm 620 595 I .570 545 I 520 495 PCk) °W depth Tide '-'------ 0 0 Stauroneis Phoenicente- ron Ehrenb. Stephanodiscus Astraea ss (Ehrenb.) Grun. SS 511 h Surirella biseriala Bra. SS Surirella dellealisshna . . • SS absent Surirella linearis W. Sm. . Surirella linearis var. con- 7. Ii stricte (Ehrenb.) Dust. zli Synedra Ulna var. danica h (Kg.) • 1 - Tabellaria floeculosa SS (Roth) Ag. -- SS SS •
F i g . 4 . Cyclotella distinguenda HUSTEDT (Magnif. x 1000). Authorts original.
Diagnosisof Cyclotella distinguenda HUSTEDT nov. spec.
Cells flatly drum-shaped of a 10-35 - l.t diameter. Shells with broad mar-
ginal zone, flat throughout, and with sharply outlined central field that pro-
jects distinctly above the marginal zone or is correspondingly sunk and tangent-
ially undulate. Marginal zone uniformly and radially striped, without shade
lines or tubercles; within 10 p 12-14 striae. Central field either laevigate, or
more or less coarsely and confusedly punctate.
h) The bog on the Rehberg Saddle
The small bog on the Rehberg Saddle above the Lunzer Seehof, at an alti-
tude of about 780 m (approximately 170 m above the Untersee) has already been 21 • (320)
.,/, ■\\ z.,,,- .• /,-- \\\ ■TII /ir
\\» e .- e eo - _f ,
' ..-:' ‘-:' --'' 1. /(,. ‹ •I_S --S—sS .---,k —,'—,4,',7,4'.‹s.-.4' ,-,' *--..,, z..-t5 /*".:,. /7— -----e-, tr-7. - S e..• 4 4 4 11`,1,i'4,',e.",,'r il■ ,:_,I.:: - --- R „Ç''-, 4 l• t, ,t.%, 4* v I.„ 4 i 'i. --
,t, '..+4 + v j , ' At v * v ' ,-„_.. ,z, , it,. ,, v , 4
-- •-- • - 4 s4',' 4, '4'' v \:---\\ - ....,_,...-,- _, / s v „,..,..,,, , •k.....,e A /1, s..* V. 4 .1, T•Sn, .., \ e:..,:i:s1r.,-"Ii ‘l.-1/4i's,-s " ,i, ,I\ -s:• -s .'.' 1....‘ ' ''' 1 -- 't-7 's 4 '''' I V., vi}, .1'■ —5 , '
‘ AS sY s5 • \ "ritli fi\e' \‘ :ç\ ' ..., -9 to 29 3 0 4.0 son,
• V .., IT
----Niecterrnoopearicetal'lvtoliniaNarcisiusrvo'it'flornfi)lygotunn 6istorea
** e'rr, Übergangsmoor ;4Callunela Poly? richeld,9sillarclefa viiaceinien s Sali.rautita u.a.A.ellaus glu/. ,t, Picea
Lariz deciclua T Abies alha ?Tagros Obstbâtune *** Line 5 =Strass.3 Dune TLeittingsmasten eUc5e x Bohrpunk t 1-5 * flat bog; ** = transitional swamp; *** = fruit trees Line 5, 1-5: 1=highway; 2=fences; 3=transmission poles; 4=blocks 5=boring point F i g 5 . Vegetational sketch of the Rehberg Bog.
briefly described by GCTZINGER (1912, p.33) and FUCHSIG (1924, p. 192). Upon
Lunz sandstone the bog fills an entirely flat, oval trough, about 150 m long
and 100 m broad; GUTZINGER has correctly assumed that this trough was infilled (321)
with a small ice-margin lake. It has not been established as yet at what point
of time the glacier receded from here, the lake was formed and what shape it pos- • sessed. After its deltaic build-up, at first a mossy swamp developed, thereupon 22 • (321) a typical silvan raised bog, with a rather well-developed lagg, where Drepano-
cladus species, Polygonum bistorta, etc. were growing. Today a great part there- (322)
of is deforested and has been considerably transformed through hay-cropping,
pasturing and the installation through the bog of a high-voltage transmission
(see F i g . 5 ).
Several borings through the southern raised-bog part provided in accord-
ance the following profile from top to bottom:
About 3/4 to 1 m : Sphagnum magellanicum/ Eriophorum vaginatum peat, with
wood; thereuder coniferous stumps.
About 2 m : radicellose peat and radicellose moss-peat.
About 1 m : lacustrine Cretaceous (lime gyttja), upwards poorer in lime.
About 1 m : glacial varved clays.
A pollen analysis conducted under my supervision by E. WASMUND provides
the following, quite normal picture (later on I shall deal with the age of the
individual horizons):
The lacustrine Cretaceous, containing Pisidia and, as early as in the
lowermost strata Chara oiispores, has been developed entirely during the fir-ho-
rizon period, between Horizons II and III of the Untersee scale. Whether the
lowermost layer, where Betula is represented with 15%, while there is no Picea
as yet, would correspond to the interstadial of the Untersee cannot be decided
before more samples will be analysed. The lacustrine Cretaceous contains Rhizo-
poda (among others Arcella vulgaris), remains of chironomids, diatoms (it seems
they occur only in the lowermost and uppermost strata) and moreover everywhere
abundant green algae. According to the investigation of two samples from 350 • and 375 cm depths by Fr. STEINECKE, a species, designated provisionally as 23 (322)
Tetraedron minimum, is markedly dominant. (More details about this in the Chap- ter dealing with the Rotmoos, p. 354). As isolated specimens Fr. STEINECKE found Scenedesmus quadricauda as well as the following Desmidiaceae which, with the exception of the four last-named ones, are found again in the interstadial
Rotmoos gyttja:
Cylindrocystis brebissonii, Cosmarium botrytis, crenatum, eranatum,
laeve, pseudogranatum, pseudopyramidatum and undulatum var. minutum;
Cosmarium arctoum var. tatricum and regnellii, Arthrodesmus incus f. minor, Staurastrum muricatum.
Also, the upper gyttja layers contain remains of Chydoridae, eggs of
Gastrotrichia and seeds of a small Potamogeton species.
The radicellose peat contains the pollen horizons IV to VI (cf. p. 310); at the time of the linden immigration, which tree represents here the oak/mixed
forest almost alone and attains at a depth of 1.5 m up to 12% of the entire fo- rest pollen, the pool is of a complete deltaic build-up. The low and transi- tional swamp was covered with willow shrubbery, with isolated alder and ash plus Dryopteris thelypteris, which still grows today at the Untersee, and it (323) was surrounded by a spruce/fir forest.
Even before the beech gained dominance - this must have occurred here a little later than at the Untersee - the swamp dried up and was overgrown with a forest; later, however, it became waterlogged again. This was accompanied by the immigration of Scheuchzeria palustris, characteristic - in other places too - of the lowermost strata of the younger Sphagnum peat, but living at pre- sent merely scantily at the Obersee and abundantly in the Rotmoos. Consequently, the raised bog covered with Polytrichum strictum, Oxycoccus, Calluna and Molinia is quite young. 24 • (323) Due to the fact that too few samples have been analysed from this bog
and that, except for the listed plant species, they have not yielded anything
remarkable, I do not report the detailed results of the analyses.
c) The Obersee [Upper Lake] and its quaking bogs
(See thereto PLATES I- III )
The Obersee, lying 1113 m above sea level, 505 m above the Untersee,
is one of the most interesting Alpine lakes, as is already evidenced by the des-
criptions of it by GUTZINGER, p. 107 ff. in 1912, FUCHSIG (1924, p. 178 ff.)
BREHM & RUTTNER (1926, p. 331), to which we refer the reader in regard to the
lake's present condition. It does not possess, as stated in the thus far avail-
able representations, one unique but, instead, three or four rock islands; I
have named them as follows: Grosse Insel [Large Island] (sketched in all the
maps of the lake), Latschen Insel [Dwarf Pine Island], (named "Bliicke" at P 14
on GUTZINGER's maps), and Moorinsel [Bog Island] (between P 12 and R on my map).
The fourth rock island, between Y and Z of the map, at boring point U, does not
attain the surface of the lake, but forms a bar, with its apex lying 41/2 m
below the low-water level of the lake.
A principal task of my investigations consisted in clarifying the nature
and the history of formation of its quaking bogs. GUTZINGER (1912, p. 108) de-
signates them as "typical flat bogs" and remarks that the deltaic build-ups at
the southern shore of the lake "have not progressed, since their outlines have
seemingly not been modified" during the time of observation. FUCHSIG and other
authors, in contrast, speak of a raised bog and assume that it has been formed • upon the flat bog with an emerging vegetation of fresh delta facies and that 25 • (3 23) it continues its growth lakeward.
As a matter of fact, however, one can speak of a raised bog only in two
places: upon solid rock, on the Moorinsel [Bog Islandl a small silvan bog has (324)
developed, with Sphagnum magellanicum, Eriophorum vaginatum and Pinus montana ;
secondly, upon the mightiest part of the quaking bog, between GUTZINGER's points
T and Z, my boring points A and J, where at least fragments are present of truly
raised-bog associations upon the transiti onal bog, which, by
the way, forms the quaking carpets.
Since, in a later work, I shall give a detailed description of the en-
tire Obersee vegetation, I want to merely call attention here to a few phenome-
na of the quagmire margins: • In the first place, the precipitous declivity, recognizable already from the boat and outlined in the structure sections of F i g . 7 , testifies quite
unquestionably against a noteworthy progression of deltaic deposits, but repre- (325)
sents much rather an erosional margin, just like the bog margin
in bore profile E of the Untersee; among other features, this is also proved by that the fact/the high water of 1926, called forth in the main through an artificial
danmdng-up, has torn off lumps of the shaking carpet from the Grosse Insel
[Large Island] and has drifted them to the northern shore of the lake.
Secondly, I point to the differing nature of the quagmire margins: at
the narrow quag fringes of the Grosse Insel [Large Islandl and the northern shore
of the lake, also at the boundary of the large quaking bog in the south towards
the Cariceta of the high-water belt, the margins are formed throughout by a (326)
Calamagrostis lanceolata/ Sphagnum teres association ; in contrast, it is lack- • ing at the northern margin of the large quaking bogs, hence the southern shore ▪•
26 (3 24) • outlet jj 1-lut of Biol. Stat. Outlet of anterior D Hutto der *)11.0'etae' V'e * ) 2 Rotmoos • , Per rnol‘n ..„Itgu°a,e e & Hunter's cot-\ - y • tage e e e g 4 •e e e ' .•1 Outlets of e '7. • •r":' Abfk,om, • - • • - ' e Irn postericy .."4.-.•rk,'„?•ee„,] f rotmoos • 1.0h.ab,,*)3
-e*)4 Ii :,.et Explanations: leichenerltlâ rime: ' e,s\ • • OS erdtil fflj Fl.7,1 .er<.r.i. ukrpe, 1,1Forl eabrpsoldc ■ lP ,- 1.-t.:t ,t, , -F -F-ie . ,,,„,,, e,,,,,■■.4 c,,,,,,,,,,, -.-1;iop I .11,0, 0 , 4 1 ,o,s, 5 I -''',, ‘..el.'; ee,?,. er"- - Lare qua A..A A AA' Ver *fr.e.-V. 11111 mire .1c.e51--. 6 vegetation:ge e=41z.,v, ikwefeMag:)7 A 'es ise dal I >•. 'Z›. :`.7 ..., 'I, eit, YYY 941 *)8 I. ct en 4e ts C: li:lot.n 11411o, r..,2eiG4o.la ( P...1 Foram (/A& 0,S,,, Mallstab, rszel,r) .111,91 44y) e So IOU 150 ZOO ot ..L. 4-. v - ? &dead
1,eg end:
• s'1ne14,•te• • iffll-'*) 1 Former boat shed; ,,esmdem. 2 *)9.' *) 3 path to Herrnalm [Master's alpine pasturel; *) 4 Loiser's haymaking; *) 5 Dwarf-pine Island; *) Bog Island; ,,e) 6 7 deer lairs; *) 8 inflow from cataract; *) 9 bog hollow; *) inflow from the Lueg and the Schattenplatz D= shady place]. Line I, 1-5: Bank consisting of solid lime; sources and source creeks; gyttja near banks; depth gyttja; boring points. Line II, 1-5: Cariceta of inundations; interspersed Cariceta and Moli- nieta; Calamogrostideta lanceolatae; quagmire Sphagneta; dwarf-pine humus.
Vegetation : self-explanatory.
F i g . 6 . Map depicting the vegetation and the sediments of the LUNZ Obersee 1:5000. Drawn by the author in accordance with CCITZINGER's, KNOLL's and his own surveys. •
27 • (325) i
.jo . Lângeprofil , .•,,,\ ---,.------Long tudunal struc Y u_r_e section - , le
. •,,,, ,b. s ° ''''' \""71eegegUeeeMeeeee7eieeee»-. ' " sf'1*1-ef'Wer
Nb. cross section .}itirdliches Querpro f il .m."--- 'a eliei."‘"$see" geigeMeee • "
10 2.0 30 00 50 60 70 60 90 100 110 17.0 130 140 150 160 170 180 190 000 en Hun r —1 •------r- end IiliM1 112.M (1) to (7) Line I: Anslellender Fussed Mnderlen %Winder Ton5y1113 Kalkgyllja Ochnecken- • Fels Gyllja em em mum. --, mm ezm umn (1) tO (7) Line II: Grcbdeledus Drilegyllja Laubyydja Gedere FeinJelnlus- lead ■ cellen. ,,p4g,,,-, allqemem Heiser 6y14.3 Ton nadeellen- Torilsoffle VYV un -J,e-g- 44 ramie) cm.-Aek me.._ pot,....gm, cd . pi,' Vegetation: elude/Ism ege/wyee lanceema erce.sa I - ,...« ,.. ,•■•■ eY ? (;) * x * * SP4ea• (fuez ,Pe- ' Bohrpree Leilhorilonle • Aymnpellosel u.e) Line I : (1) solid rock; (2) fine sand; (3) varved clays; (4) streaks of clay; (5) clay gyttja; (6) lime gyttja; (7) snail gyttja;
Line II : (1) generally coarse detritus; (2) drift gyttja; (3) foliage gyttja; (4) larger wood pieces; (5) fine detrital gyttja; (6) radicellose clay; (7) Sphagnum radicellose peat (quaking-bog peat).
Vegetation : self-explanatory;
*) boring profiles; **) index horizons I - IX.
F i g • 7 • Structure sections of bore profiles through the quaking bogs of the LUNZ Obersee. The boring points are designated in the same manner as on map F i g • 6 • The upper sections are superelevated by 5 times, the • lower, more diagrammatic ones, are according to scale 1: 2700. 28 • (326) of the Obersee, where, for long stretches, it is replaced by a Sphagnum-rich
Carex diandra association. This state of affairs can scarcely be caused by che-
mico-physical circumstances, since all of these margins are floating in the
same manner, but it must be related to the formative history of the quagmires.
In order to clarify this history, the line profiles noted in F i g . 6
and depicted in F i g • 7 were drilled.
We begin with the sediments of the lake: in them too synchronous pollen
horizons are ascertainable; I am going to describe them provisionally as fol-
lows, without intending to thereby state whatsoever concerning their absolute
age or an equivalence in age with those of the Untersee:
I. Beginning of the Pinus curve, directly superjacent to the glacial
varved clays (see F i g • 11, p. 359).
IL First occurrence of Picea, Corylus and Betula which, later on, dis-
appear again. This horizon is regularly represented by an approximately 5-cm
thick gyttja layer, overlain by an about 15-cm thick glacial clay, with but a
scanty amount of Pinus montana and Salix pollen. Consequently, layer II is a
typical interstadial .
III. Reappearance of the spruce pollen in an insignificant amount. It
is regularly detected in clay- or lime-gyttja, where two thin, reddish clay-
lamina are intercalated.
IV. Speedy rise of the spruce curve and reappearance of hazel, followed
very soon by elm, linden and oak (the latter species only scarcely less than
the others).
V. Hael climax, attaining at the Obersee only 15-25% and following im-
mediately upon the intersection between the fir and spruce curves (see F i g s . 41› 29 • (326)
8 and 11 ). Nearly simultaneously, even though just a little earlier, appear
also Abies and Fagus.
VI. First spruce maximum.
VII. First fir maximum.
VIII. Absolute beech maximum.
IX. Disturbed horizon where, in many cases, older strata (IV-V) rest on
younger ones (VI-VII). (Several of them are present in bore profile E ( F i g .
8 ), where one of them lies under VIII).
X. Second beech climax.
10 ZO 30 10 50 60 70 90 10 20 30 40 50 60 70 90 90 I I I I I I I 1 MI, 11111 I I I I • 11111
É
1111
(
t A 1 1 Upper Lake profiles Inersoeprofile
F i g • 8 . Pollen diagrams from the 0 b er s e e (explanation of symbols and position of the bore profiles in F i g s . 6, 7 and 11 ).
The disturbed horizon IX is particularly distinct in the northern • transverse structure section on the interval G - J where, at first, an old 30 • (327 ) lime-gyttja and, further lakeward, a sandy coarse-detrital gyttja overlie a younger
fine-detrital gyttja. This striking overthrust becomes comprehensible if one
considers that in the Obersee too, at boring point L, for instance, where Hori-
zons VIII - X are lacking, old deposits are bared at the shore in many cases.
Unfortunately, there are as yet no age determinations for the "viscous red su-
spension mud," described by GUTZINGER from greater depths.
Among the very numerous but flot as yet more circumstantially investiga-
ted microfossils (among others Rhizopodia and Cladocera, but seemingly neither
diatoms nor Desmidiaceae), occurring as early as in the interstadial gyttja I
and II, the well-preserved heads of Eu-Tanytarsus larvae are particularly re-
markable (in addition there are isolated ones of a Tanypine; determinations by
Professor THIENEMANN); they persist even through the following horizons, even
though decreasing rapidly from about Horizon IV and nearly lacking from about
IX; there replaced in the main by chironomids s. str. and Culicoidinae (Bezzia (328)
etc.). Spongilla lacustris, present in the Obersee in such masses today, seems
to appear only subsequent to Horizon IX, in contrast to Daphnia longispina, al-
ready so strongly represented through Ephippiae in the plankton of Horizon III.
This change in the fauna of chironomids signifies a similar modification
in the metabolism of the Obersee, as was established, for example, by LUND-
QVIST through detailed sedimentary and microfossil analyses for the lakes of
Vxje). in Sweden, namelyarapidly increasing eutrophiation.
There, the causes for these phenomena were found to lie in the considerable
settlements of the bronze period, while here I consider them to have been brought
about by the fertilization through game, in particular deer and chamois; in
periods of low water this is strôngly noticeable even today upon the dried-up 31 • (328) mud surfaces. But low-water conditions will also have occurred at the Obersee
in post-glacial warmth periods, particularly often and mainly during the
Subboreal. It can scarcely be imagined that the stock of game was smaller then
as it is today. Here oxygen deficiency is caused especially by the iron content
of the depth water.
The slide manifested in Horizon IX may have been caused by high water
following a longer period of drought; it might even be connected with a first
uplift of the quaking carpets.
Sphagnum remains appear for the first time between Horizons VI and VII;
but the formation of quagmire peat does not start anywhere before IX. From the
bore profiles represented inFigs. 7 and 8 the initially surprising fact is
manifest that the Sphagnum radicellose peat is not overlying anywhere pure ra-
dicellose peat, but that, much rather, the situation is reversed by sphagnate
radicellose peat lying underneath and following directly upon coarse-detrital
and drift-gyttja. In many cases the lowermost layer is rich in Equisetum limo-
sum, which still grows at present in the lake, plus on isolated spots in the
quaking bogs, but in contrast, not among the Cariceta inflatae of the
inundation belt.
Consequently, the Sphagna (teres, amblyphyllum, etc.) have not colo-
nized flat bogs but ( at least temporarily) dried-up lacustrine mud.
Only in exceptional cases the thickness of the quagmires exceeds 2 m
(maximum 2.1 m), and the depth of the mud surfaces below them exceeds but ex-
ceptionally 3 m below the present-day low-water point of the Obersee. Where (329)
the open space between the bottom border of the quagmire and the lake bottom
exceeds 1 m, it is easily possible that the interval has widened due to a 32 • (329) posterior outflow of the mud.
In case the quagmires would be growing out into the open water, or have
been doing so in former timEs, they ought to be found over deeper water as well
and be thinning out lakeward. Both of these features are not present, however,
but much rather, the quags wedge out landward. Furthermore, here, they are regu-
larly overlain by the red radicellose peat of the Caricetum inflatae, hence they
are older, at least in their older parts, than these Cariceta.
At the time when the present-day quagmires were established, the early-
suumier inundations cannot have possessed the same intensity, or at least flot an
equal duration, as the high waters of today.
Consequently, the shaking bogs have been formed upon solid ground • and have been lifted off therefrom at a later point of time. This might have oc- curred approximately during the period of Horizon X, but need not have been com-
pleted in one occurrence. Seemingly, a marked increment in breadth has not
taken place thereafter and, since that period, the upward growth in its turn
might scarcely have amounted to more than about one third of the total present-
day thickness of the quagmires.
In the southern basin, the drift and gyttja deposits are partly rather
compact, considerably firmer in their major part than those of bore profile
F of the Untersee; among other reasons, this might have been caused by the pres-
sure of the swamp cover and an outflow of the softer gyttja masses. That a bog
could form upon such a firm ground is all the less remarkable as, in many cases
(at boring points U, Y, Z) Even spruce have established themselves. Contrary to
my initial assumption and as proved by the borings, the trees do not root upon • rock, but in viscous detrital gyttja. 33 (329)
It is very likely that the quaking carpets at the southern shore of the
lake were of a greater expanse than nowadays and had been torn asunder later
by a similar high-water erosion as that of the 1926 summer which, in its turn,
has also rent considerable gaps into the Cariceta. I presume that many of the
quagmire fringes at the northern shore of the lake and at the Large Island have
not been growing at these places, but represent torn-off drift lumps, rooted
there only later.
To what extent interferences of man - for example, by the first erecting at the,outlet of a retaining dam/rather long ago - have also participated in bringing about (330)
these events is not as yet accessible to our knowledge.
Even at this point, however, I feel rather certain that the quagmires
of the Obersee are the result of an old, probably Subboreal formation of deltaic
• no longer grow in breadth but are subject to an deposits and that, today, they
erosional condition.
Further on we shall investigate to what extent similar statements can
also be made concerning other quagmire formations.
d) The Rotmoos[Red Moss Bog] and its eruptions
(see thereto PLATES III and IV)
The position of the Rotmoos is shown best by the photographs of PLATE I,
for which I have to thank Professor H. KRAWANY; furthermore, it is seen on
PLATE III; its divisional plan is represented in the map F i g . 9 . The en-
tire, about 800 m long valley that lies only just 9 - 12 m above the Obersee
comprises three totally separated basins, lacking any surface outlet. The nor- • thernmost small one, called "at the Kreuzfeichten" [name obscure and
34 • (331) THE STRING OF THE ROTMOOS BOGS
Der flotmoos.zug „ Bet 1' ./....eretafetchtdno aufgenommen 1926 von H. GAMS 'f=1, 1926 survey by H.. GAMS 44 4 Y hi der 4 Bocksbartmauer iiqui lachen 4 4\ 4 [Goat's-Beard' Legend: Wall] A (1) old road; 4 (2) riding path to Obersee Hut; (3) dry valleys in solid rock; Y'g4 r (4) basins lacking a surface outlet ';:;- ,>1 4 t Vorde t'r e s i‘ h and filled with rock debris from slopes and moraines, with depo- sits from lakes and bogs; (5) source and vanishing hole (po- nor)[=unidentifiable word]; (6) direction of mostly subsurface outlets towards the Upper Lake; Legende: Ittuto Trockentâler im ( 7 ) place where deer wallow in the mire; twin anstellendett Fels. ( 3 ) bog-burst craters with Caricetum -. Von Gehângo- und (8) t 4Iorânenschutt, See- ( 4) • ■ inflatae; & urtit ,itttla?iralpgerucen '' entteur'itIscelicenenAgfruett. ( 9 ) lagg associations; 9 Quelle. A Schwiddluch (Pow). (5) (10) flat-bog Cariceta/Deschampsieta ' -i Hinteres gitlitungftiFlitung der groBeneaten-- „ , teds untemr dischen ( 6 ) and deer lairs; /,114 R 0 t !no 0 e Aunüsse zum Obersee. u Hirschuhle. ( 7 ) (11) Sphagnum flat bog; 'fiiosterior -. Moorausbrunnim iq Rotmoos „.w f",'g"10,6reen,111710;1,1,7.e. 9 (12) Molinieta and Nardeta upon dead , Niedermoor-Carkeia, ( raised bog; 4 _ eel 7A:eh:ekes/do und \ 10 ) mrsaagen (11) (13) Sphagneta upon dead raised bog; e Sphagnum- Niedermour. eruptive complexes of raised V v Nohiliela und Wanida (12) (14) V v au( totem llochmoort (13) bogs (mostly quaking swards); ii I I I ‘15;:tleenf (oachmuroor. a (15) spruce; ED eePrino°F.I■feeMe ( 1- 4) mist echwingrasen),s (16) stands of mountain pine; f et Fichten. (15)(17) Lycopodium inundatum. '''. Leg fdhrenbestânde. ( 16 ) _,.. ,e,propoLeimiierem. (17)
Scale Malistab: 50 e,-ev ç Me' • Fig. 9 . Vegetational map of aeRotmoos string of bogs 1:4000. 35 (330)
untranslatablei, does not concern us. The two larger basins were occupied by
two larger lakes, subsequent to the melting away of the glacier, which, probab-
ly, had despatched from the Lueg one of its lobes into this little valley and
remained for quite some time separate from the glacier of the Obersee; the two
lakes owed their origin to the caulking-up by glacial clay of the markedly cleft
karst topography of the Hierlatz lime.
We designate the northern basin "at the Tintenlacken" [approximately 'at
the ink pool'i as the Anterior Rotmoos (or plainly 'Rotmoos;' the following ex-
positions by STEINEOKE, for example, refer exclusively to the 'Anterior Rotmoos');
the southern one we shall call the Posterior Rotmoos. Both of them comprise se-
veral, partly amalgamated raised bogs, encircled by a common lagg; the Anterior • Rotmoos includes one bog of an about 100 m length ( PLATE IV )plus two others of a merely 30 to 40 m length. The Posterior Rotmoos consists of a similarly small
bog and two rows of moors, separated by a fragmentary creek that disappears in
many places; each of these bogs displays two to three 50-m broad marshes ( PLA-
TE III ). The uppermost part "at the Arschfeichten" [equally untranslatable] is
developed as a Sphagnum flat bog, with a quagmire abuve soft gyttja.
All of the raised bogs are dead *). Another special characteristic (332)
they all share is the absence of Calluna, Trichophorum caespitosum, Sphagnum
compactum, rubellum and fuscum. For the rest the bogs fall into two groups:
1 *) Here and in what is going to follow I conceive under 'dead raised bogs' not only those that can no longer grow at all, but all those that, for one rea- son or another, have discontinued their increment, or in which erosion ex- ceeds the latter. As regards the significance of Molinia and Nardus as hu- mus consumers, cf., for instance, RAMANN. Concerning the latest findings, • see supplement German text p. 387; translation p.102. 36 (332)
the intact ones covered with Nardeta and Molinieta and the eroded ones;
the latter in their turn are divided into such with an incipient erosion and
those with true bog bursts or eruptions. The three largest ones, among them
that tat the Tintenlackent Eat the ink pooll, belong to the latter group.
In this last group three concentric zones or complexes are regularly
distinguishable, which, in their turn, are constituted of a greater number of
associations or, more precisely, fragments of associations:
The lagg, displaying fern- and moss-rich spruce forests (among other
species, with Polytrichum commune, Plagiothecium undulatum, Sphagnum squarro-
sum, etc.), has a chain of small pools that are connected by rills only at the
time of snow melting and after heavy rainfalls. • The marginal complex that includes essentially a very steep peripheral declivity, plus parts of the original bog surface; it is formed by associations
with Sphagnum acutifolium, Cetraria islandica, Lycopodium selago, Nardus, Moli-
nia, Vaccinia and, chiefly, Pinus montana (laggward with isolated spruce). As
a rule the peripheral complex slopes rather abruptly towards the eruptio n-
a 1 complex, which, in its turn, comprises three part complexes: the
crater of bog bursts, with Caricetum inflatae in the open brown water (the
Tintenlacke and the corresponding pools in the Posterior Rotmoos,PLATE IV );
the cicatrization quagmire which, in some characters, calls to mind the one of
the Obersee, but is more acid and richer in Scheuchzeria (PLATE IV );
finally, the creeping-soil terrasses and stairs; as a rule they form a mosaic
of patches, with naked peat mud, rather often Lycopodium inundatum and peat
hummocks, carrying an association of Molinia, Lycopodium selago and Mylia • taylori; these peat hummocks replace here similar erosional complexes of other 37 • (332) places with dominating Calluna and Trichophorum caespitosum, absent here.
The thus far available description, according to which the holes, called
here 'craters of bog eruptions,' are designated as remnants of the original
lakes, is doubtlessly incorrect, which is already proved by the entire relief by and the elevation of these holes/2 - 3 m above the lagg.
This finding has also been fully confirmed by the results of the few (333)
borings carried out up to now (two in the Anterior, one in the Posterior Rot-
moos). The boring in the quaking carpet of cicatrization ( F i g . 12 ) has
produced a diagram that is easily correlated with the one from the Obersee. The
interstadial , developed here inasimilarly beautiful manner, is
distinguished by the occurrence of alder pollen and a very rich algal flora; • Dr. STEINECKE reports thereon in what is going to follow. The very marked Abies maximum is due to a purely local motivation: the
lake, at that time not yet complete in its deltaic sequences, was surrounded by
firs, the stands of which have diminished since then, very considerably repressed
by spruce. Soon after the beech had been definitely crowded out by spruce, this
bore profile is concluded.
The lacking part, containing the resumed rise of the beech and fir curves,
is present in the bore profile from the marginal complex; it is not reproduced
here. This profile, plus the upper 160 cm of the thus far sole boring profile
from the Posterior Rotmoos, consists of nearly wood-deficient,inconsiderably
humified Sphagnum peat, superjacent upon a layer of stumps; in places the latter
rests directly upon rock, in other places, however, upon gyttja formations.
During the period when the principal mass of the Sphagnum peat was formed, • the Anterior Rotmoos and most likely also the other raised bogs had most certainly 38 • (333)
transgressed far and wide over the surrounding forest ground and, in places,
directly over the limestone rock, which displays here a very marked karst deve-
lopment, rent and furrowed by numerous fissures.
The bog eruption that created the entire eruptive complex
seems to have occurred during a period between Horizons IX and X of the Obersee
profiles. The Tintenlacke and the corresponding holes in the southern eruptive
complexes are neither remains of the lakes that had completed their deltaic
build-up long before the formation of the raised bogs, nor can they be compared
with the pools of the Baltic raised bogs; they are, in fact, eruption craters
having not yet reached the stage of cicatrization. The creeping-soil steps con-
sist of the oozed-out mud masses, a part of which may have participated in the • formation of the quaking bogs. It is an extremely striking fact that here, within such a restricted
space, bog eruptions, perfectly conforming to one another, abound to such an ex-
tent, whereas similar eruptions have not been described as yet from the Alpine
area (as to their real occurrences in other Alpine bogs see p. 372). I believe (334)
to have found an explanation for this remarkable situation: once more it is
the abundant stock of game. The two bog basins display today no
fewer than four spots where "deer wallow in the mire" (drinking stations) (cf.
F i g . 9 ), two of which are lying on raised-bog parts not flown-out as yet.
Due to the trampling, resting and the excrements of the large game, the bog sur-
face, anyhow no longer markedly growing and not - like in other dead raised
bogs - consolidated through beds of Calluna, is injured, and at such spots the
erosion, generally observable in dead Alpine bogs, is readily at work. • It is not excluded that we ourselves may see a bog explosion in the 39 (334)
long-extended, already distinctly eroded bog on the western side of the Poster-
ior Rotmoos. It is true that the uniformity of the phenomena in the already
erupted bogs (there has also been an erùption between the two southern ones,
but of a somewhat diverging character, so that it may be older) would testify
to an approximately simultaneous occurrence of the three big explosions, but in
consideration of the indicated causes, we may reckon with further eruptions.
As regards the recent and fossil associations of micro-organisms in the
Anterior Rotmoos, I am indebted to Dr. Fritz STEINECKE of Miningsberg for the
following explanations: in July of 1925 and 1926, he collected the recent samples
exclusively in the Anterior Rotmoos, particularly in the eruptive complex. For
comparison, a few samples were investigated from the lagg, some from the moss
carpets on the ground and some from the lime blocks in the surrounding forest.
The shallow hollows at the margin of the cicatrisation quagmire display, among
other features, massive congregations of Natrium digitus. These pools do not
possess true plankton; but under this designation species are combined, which
Dr. STEINECKE has especially found suspended in open water. The "depth mud"
from the Tintenlacke originates from a depth of about 1 m; the rill, flowing
out northward from the Tintenlacke, is named "outlet ditch;" it is filled with streaming filamentous algae. The figures mean the estimated amunt(1 = very
scarce; 2 = isolated; 3 = rather abundant; 4 = abundant; 5 = in masses). Na- turally, the noninvestigated flat-bog parts of the Posterior Rotmoos (with Des- champia caespitosa, Carex elongata, etc.) contain moreover entirely different associations of micro-organisms.
40 (335)
Compilation of the recent micro-organisms from the Anterior Rotmoos
and their distribution in the biocoenoses
Eruptive comp lex large l Ti nte n.la.Icke Samples collected and de- 10°1 -0 pool • try •H ls
0 h termined by Fr. STEINECKE r.r) ro 0 4-1 oo d -o d mu
its l p
ditc e a t mu
.0 in e w çj 4_1 le r (f) t
u-) shor 0, a)
-o ou sho marg 1 2 3 4 5 6 7 8 9 10 11 ; 1. Microphyta . . C.hroococcus turgidusnwg.,f. eha lybeus 1 222 4 Chroococcus minimus (v. KeiBler) _ 'v. turfosus Steinecke 1 1 9 Oscillatoria Frochlichii ICg. . 1 2 Isocystis infusionum (Kg.) 1 2 Nostoc' microscopicum Carm. . . 1 Anabaena augstumalis Schmidle. 1 2 1 1 2 . Hap alosiphon fontinalis (Ag.) Bor- net 22 11 2 Stigonema ocellatum (Dillw.) Thu- ret 1 1 Bodo saltans Ehrenbg. 1. I-Texan-inns pusillus Klebs . . . Synura uvella Ehrenbg • Dinobryon sertularia. Ehrenbg. , 1 3 Cryptomonas erosa Ehrenbg.. . 1 Cryptonionas ovate 1.1renbg.. 1 Englena Ehrenbergii Klebs . . . 1 Euglena elongata Schew. . 2 2. 1 2 1 1 2 Englena acus Ehrenbg. var. minor Ilansg . 3 . 1 1 Distigma proteus Ehrenbg. , 1 2 Menoidium pelfucidum Perty. . • 2 21 1 . Deteronema nous (Ehrenbg.) Stein 1 • Salpingoeca frequentissima (Zach,) Lemm. 2 - 2 Peridin ium in no nsp icu um Lemm.? 3 1 Peridinium cinctum (Intl.) Ehren- berg y, palustre Linden). 2 1 flysten (des Vorhergehenden?) . . 1 4 212 2 • Gleeotaenium filiiIIIS Pascher . 1 41 • (336)
Samples collected and de- termined by Fr. STEINECKE [See meaning of numbers below on trans- lation page 40]
l2 3-- 4 .5-- .6-- 7 8 9 10 11 %India a rcuata (Naeg.)Steinecke 1) 2 1 Luno Lia paludosa Grun. 1 Eunotia_exigua (Bra.) Babel'''. 2 1 1 1 - Runolia Lenella Grun . .1 1 2 . 1 Navicula subtilissima Cleve . . 2 2 2 4: 2 1 2 1 1 Frustulia saxonica Rabh . 3 1 2 3 1 3 2 2 Pinnularia stomaLophora Grun. 2 2 1 Pi unularia micros tauron Ehrenbg. 1 2 2 9 2 Pinnularia viridis Ehrenbg., P. bo- realis Ehrenbg. 1 Il an tzsehia a mph ioxys (Kg.) Grun. 1 Zygogonium ericetorum Kg. (Zell- sa ri failles) ce.11. sap .co1,ourle ,s i 2 2 3 . Zygogo ni uni once Lorin-Ft Kg, (Zell-
saft violett) .s'?1). YiP 1.- e .. Il 3 2 3 2 Mougeo tia lae to v irons (A. Br.) W i 1 Ir e clt ? . 1 5 5 5 5 8 2 3 • NI o u ge o 1. i a p a r v u I a I. lass 2 2 2 2 M eso Lue ni u in De tit rayi Turn.. . . Ii Al eso Laenin in m acroco count (Kg.) ç) 2 Boy et Biss. 1 1 2 2 - . NI osolnon i u in violascons Do By. 1 1 Cylindrocystis Brebissonii Me- neghini /1 2 2 .1 1 1 1 1 Ne tri u in digitus (Bréb.) Liiitkem. (Zellsaft farblos)*.a.p.c.olo.unes .1 I 6 2 1 Netrium tligi Lus (Zellsaft gelb-
- lick) sap .yetlowdsh • 2 2 1 1 ' Netrium oblongum(DeBy.)LtiLltem. - 3 2 ' 2 2 2 Penium polymorphum Perty . . . . 2 2 2 1 1 Poulton crassinsculum Do By.. , 3 2 3 4 ' 1 2 1 3 t Penium did yin ocarpumLund.. . . 1 3 1 3 2 . 1 Penium minutum (Rails) CI. .. Cos- in aHum d oui di oi des Liitkem. . . . 1 2 2 - , 1 Closterium incurvum Bréb.. . . . 1 1 i . 1 ) Diese Art. isi iden Lisch mil, R un. grau il is (Ehrenb.)Bbh. Awn von Fr Hustedt. This species ideriEical w. Note by
42 (337)
Samples collected and de- [See meaning of numbers below on trans- termined by Fr. STEINECKE lation page 40 ]
CI os L ri u w aeu tunt (Lyngh,) Bréb. nebst var. linon Te tm cm orus Brebissonii (Menegh ) Rat fs Te tmemorus rninutus De By. . Pleurotaenium Lrabe eu la (Ehren- berg) N aeg. Docidium u ndulatum Bail. var. di- 1 a La Lum (Cl.) West Eu as trum hinale (Turp.) Ehrenbg. f. GuLwinskii Sehmidle uas Uri m insigne llass. u as (iii m hum eros u . . Cos ma riu m amo e nu m Ralfs . Cosmarium bacillar° LittIcem. ( Pen ium in eons picuu In West). . Cos In arium a ngulos u m Brdb., •• • C os in a ri u10 cueurbi ta Bra, • • C os m a r i n m obliquum Nerds( . . Cosm a rium palangula Bra. , Cosmarium p a ry Id um i3rób. . . . Cos m u ri u ni s ph agn bol u m W, et G. S. West Cosmarium v e n us tum Bréb. . S t auras tru m D j chi ci Ralfs . . Staura.strum f urea Lu m (Ehrenbg ) Bréh. S ta u r as trum dejeolu m 13r6b, 'var. sub gl ab ru m Grônblad . Staurastrurn 'non tieulosum Bréb. var. biFariuin Nordst. Staurastrum nigrae-sirvao Sehmidle Staurastrum O'Mearii Arch.. • S t auras trum i n cc n spi euu m • .Nordst.
•
43 1 (338)
Samples collected and de- termined by Fr. STEINECKE [See meaning of numbers below on trans- lation page 40 ]
1 1 2 3 4---- 5 -6- : 9 110 11 St. aurastrum paradoxum Meyen. 2 1 1 1 Slaurastrum punetulatum [ira. Stauritst.t.um Iteinseliii West. . . 2 9 1 Staurastrum seabrum 13ib., . 2 3 12 1 SI aurastrum vestitum flairs. . . 1. 2 . 1 Ar throdesm US bi Brai. . . 1 Artlirodosmus con LPOVOPSUS W. et (1. S. West • 1. . • i n eus (13r(1b.) Ilass. r. Ar th ro cl es mus vu lgari ,; 1 3 1 2 1 2 Spondà•losiunt Ar°,11 1 4 2 2 1 '' 2 Gym nozyga 11101111 i 101 1111 s 11;11r1)g 9 3 2 2 3 2 3 Desmidium Swartzii Ag. : 1 Binuelearia ti. L l'all a . • 1 1 2 3 2 2 3 1 Mierospora stagnorum (Kg.) La- gerheim • 1 • 2 • Mierospora paehyderma (Wille) Lagerheim 2 1\1 loto t II a ni nion i n gi an um Nitegeli 2 4 Collot:bite° 1(10 1) a 111111 Schmidt° 4 1 Gloeoplax \•Veberi Schmidt° . • 2 3 2 3 Oedogonium 1 Lzigsohnii De By 2 2 1 3 3 1 2 Oedog. onium sp. (sien!) 2 Pandorina morum Bory .1 ' Chlainydomonas glocoeysLifor- mis Dill 2 '1 1 1 1 1 1 (11oeuti,ystis gigas (Kg.) Lager1i, 2 2 4 2 2 8 213 11 ae m a toeo crus pluvians Flot. . . 1 .An kisttudosinus B va n (Naeg.)
C: o e I as Ltunl congloinera Lu ni (v. Anet') Sicilien° 2 2 Ooeystis solitaria Wittr. . . . 2 2 1 2 2 2 • . Coceomyxa dispar Sehmidle • 1 2 : 1
• 44 (339)
Samples collected and de- termined by Fr. STEINECKE [See meaning of numbers below on trans- lation page 40]
H ScoLiella nivalis (Shunieworl,h) 2H 45 678 9 10] 11
Fritsch ? • 1 .2 1 Trochiseia granula La (Deinseh) 1-lansgirg 1 Selenoeoceus rareinalis Schmidle et Zach. 2 9 eph roey Liu to elosterioid es Bolt- lin 9 1 Kirchneriella eon Lena (Selnuidle) 13ohlin • 2. Troelliscia stagnalis Ilansg, , :1 Keratococeus eaudalus Paschal' . ophioey Lill Ill Logerlionnii Letton.
H. ilirozimi.
11 liizopo den: • • Areolla vulga ris Ehrenbg Amelia artocrea Leidy • .1 Areella discoides Ehrenhg., . 1 DirrIngia croula Leidy 2 Dirflugia varians Pénard 1 Dirrlugia elugaus PLinard 1 Dirrhigia•rubescens Pénard, . . Dirflugia globulosa Du]. . . . 2 DifrIngia piriforniis PerLy var. bryophila Pénard Di fflugia pi ri for mis var, la eus iris Pénard 2 Dimugla baeHlirertnPénard . 2 Dirflugio constricto Ehrenhg. . il 2 1 Centropyxis couleata Ehrenhg. 2 1 Con tropyxis laevigata. Pénard . 2 1 llyalosPhenia papilio Leidy. . 3 1 Ilyalosphenia degons Leidy . 1 • 1 Nehda bohenlica Tor. 1 Nebel il car i flat ci 1 .
•
45 (3 40)
Samples collected and de- termined by Fr. STEINECKE [See meaning of numbers below on trans- lation page 40
Nebe la bursella Vejd Nebela niililaris Pén Nebe la collaris Ehrenbg. . • . . Nebela tenella Pén Heleopera petricola Leidy . Heleopera pieta Leidy Ifeleopora rosea Pén Ph rygan oll a nidu1usPén. und Ph r. hemisphaerica Pén Pseudodifflugia horrida Pin. . Euglypha compressa Cart. . 1 Euglypha filifera Pén. • Euglypha al yeolata Duj 2 1 Euglypha laevis Pony 1 Assulina seminulum Ehrenbg. 21 Assulina muscorum Groff . • . 32 • Sphenoderia lenta Schlumb. • . . 2 Trinema enehelys (Ehrenbg.) Pén. 2 3 1 Trinema lineare Pén . 22 1 Cory thi on d ubiu m Tar 1 1 Cory thion pulchellum Pén. . • . 12 1 Cryptodifflugia sacculus Pén. . Ditrema flayum Arch. 1 .1 1 .1 Amphitroma wrightianum Arch 2 2 1 1'! A ni ph aroma ste n o s L om u m Nüssl. 1 113 1 1 2 , Clathrulina elegans Cienk. . . .
Itotatorien: olungalus Woh 2 1 1 Rotifer ciirinus Ehrenhg Cal I id i n a august icollis Murr. 1 2 russoola %el. I 11 I 1 Callidina bidens Gosse 1 I 1 N o to in ni a ta groonland ion Bergond. Diaselliza oxigua Cowie Diurella bidens Lucks 2 1 2 2 • 46 • (341)
Samples collected ai-id de- termined by Fr. STEINECKE See meaning of numbers below on trans- lation page 40
1 _1 1 12 3 14 5 6 17 I 8 9 110,11 Diurella collaris Rouss ‘2it Rat lulus longiseta Schrank . 1 Diplax bisulcata Lucks Diplax crassipes Lucks Oathypna ungulata Gosse . . . 9 Dis tyla Ilexilis Gosse 21 Monostyla lunaris Ehrenbg. . . 1. 1. Colurella colura Ehrenbg Ploesoma triacanthum (Bergcnd ) Voi,gt Ploesoma truncatum Lev.. . . Microdon clavus Ehrenbg 9 Gastrotrichen: Ohaetonotus macrochaetus Ze- Enka
It is a matter of course that the above material is as yet insuf-
ficient for establishing definite associations, even though index species
are easily recognizable for certain biocoenoses (cf. the works of STEIN-
ECKE on East Prussian bogs, those of SKADOWSKY and others on Russian bogs,
etc., in the bibliographic index of the present work).As regards the con-
jectured causes - above all the various ion concentrations and acidities
see the measurements of RUTTNER (BREHM & RUTTNER 1926, p. 349) and of
WEHRLE; also the papers enumerated in the list of literature in the
above-named works. • • 47 (3 41)
The compilation in the preceding pages is intended to serve only
for a comparison with the subfossil species found in the boring samples from
the eruptive complex of the Anterior Rotmoos.
Here, the peat samples proved to be throughout much poorer in micro-
organisms than the peat samples from the Zehlau in East Prussia.
In the Rotmoos too, just like in the Zehlau and other bogs investi-
gated in this respect, the frustules of diatoms have remained pre-
served merely in the upper layers of the Sphagnum peat, and even there only (342)
in exceptional cases. Apparently, as a rule , the colloidal silicic acid of
the valves is, after a certain time, dissolved by the humic acids of the • peaty water of the raised bogs. Exclusively those diatomic valves (predo- minantly Navicula subtilissima and Eunotia), cemented into the shells of the
Rhizopoda Amphitrema stenostomum, remain well recognizable in their out-
lines. This rhizopod, however, was detected in only three drill samples
of the Rotmoos peat, so that nothing can be reported on the diatoms
of most necrocoenoses.
In the individual boring samples Desmidiaceae were
distributed rather unequally: whereas at the bottom of the bog, in
the 'algal gyttjat , numerous species could be ascertained in a
rather fair preservation, the layers of Sphagnum peat were
almost deficient thereof . The Protococcales displayed a
similar deportment. 48 • (342) As to animal remains, Oribatides and crustaceans (particularly Chydo-
ridae) were not infrequent in certain places. In peat layers of differing
depths only just one cell wall of Rotatoria was dicovered, namely Callidina
angusticollis MURR. Up to this day the animal is found living in the shore mud
of the large pools as well as in the Tintenlacke of the Rotmoos; also in pools
of the Obersee bogs. After the decay of the oeganism, its carapace remains lying
unchanged in the peat; it has been observed by a great variety of authors in the
peat of raised bogs, but it has not been correctly recognised (it was designa-
ted as "raised-bog flasks," "flask-shaped shells," cf. RUDOLPH & FIRBAS 1924,
p. 34; furthermore, dissertation of Rob. FAHL, Breslau 1926). The animal is ty-
pical of deeper pools and hollows in raised bogs; hence its remains in the peat
are an indication that this peat was constituted of biocoenoses bearing this
character.
In the peat, quite strikingly, carapaces of shelled rhizopods were equal-
ly found only as isolated specimens. Against 30 species from the Zehlau peat,
only 11 species were observed in the Rotmoos peat. Apart from two Amphitrema
species, the others were just only species found regularly in any raised-bog
peat; naturally, among them also Ditrema flavum, which, in the literature deal-
ing with bogs, has roamed about ever so long as "raised-bog keglet" or even
as "Nephelis cocoon," until LAUTERBORN (in STARK 1924) and STEINECKE have re-
cognized it as a rhizopod.
For purposes of comparison, its recent occurrence in the Obersee and
pertinent quagmires is also noted in the following Tables(see pp.
344 to 349). • It results from the Tables that, starting withadepth of 400 cm, (343) 49 (343)
the association of micro-organisms is completely modified. The sediment demon-
strates that the lowermost layers must have been deposited by biocoenoses of
a radically different nature than the ones of the upper layers. Whereas the
younger part of the peat carries - almost exclusively - fossils that even to-
day exist in the raised bog, the remains of the oldest layers belong to species,
absent in parts of the Rotmoos investigated up to now. Therefore it is quite ,, 1 feasible to identify the necrocoenoses of the younger peat deposits by com-
paring them with conditions prevailing nowadays. Because, despite the scanty
occurrence of fossils in these layers, even today precisely the preserved spe-
cies are typical of individual biocoenoses.
In the species, however, from the depth gyttja comparisons are impos- 1 • sible with recent associations of the Rotmoos. For determining necrocoenoses *) of those depth layers, one can only refer the species found as fossils to the
deportment of their recent specific equivalents at other localities. It is a
matter of course that this is feasible only to a restricted degree and with
considerable caution; all the more because a number of yet unknown forms has
been discovered in the algal gyttja.
In the following we draw conclusions about the aspect of the long since
vanished biocoenoses from their fossil remains (see also F i g . 11 )
1 *) With this term we designate fossil biocoenoses. WASMUND has proposed the word ithanatocoenosesi for them, but now he wishes to distinguish between ordinary dead associations or tnecrocoenoses' (meaning remains of organisms preserved in their original environment) and dead associations, or tthana- tocoenoses,' where an actual process of burial has taken place, like shell and waste accumulations, castings (wool balls, feathers, bones, etc.) which he has investigated. In small basins of lakes and in bogs we mostly en- • counter only the first-named case. 50 • (343) Depth of 600 cm : varved clay of the last ice age; as much as devoid
of fossils (in the uppermost layer no pollen whatsoever, not Even when treated
with hydrochloric and hydrofluoric acids; mere scanty moss and chitin
remains . GAMS ).
Depth of 550 cm : interstadial algal gyttja; 35 species of Desmidiaceae,
1 Zygnemal, 6 Protococcales and 3 rhizopods were found in a mostly faultless
preservation. Not one of the algae is still alive today in the Anterior Rotmoos,
but an inconsiderable part exists in the quagmires and the open water of the
neighbouring Obersee. In bogs Arcella vulgaris is confined to flat-moor areas.
Centropyxis aculeata and Hyalosphenia elegans are index forms for transitional
and raised-bog Sphagna in the North German plain, but not in the Alpine area, (350) • where both of these species are not infrequent among inhabitants of small pools, particularly at high altitudes.
Concerning the dispersal of the Desmidiaceae that, apparently, no longer
exist in the Rotmoos and the Obersee, more abundant data can be found, above
all, in SCHMIDLE, in KURZ and in DUCELLIER (more literature about them, for ex-
ample, in DONAT 1927); it results therefrom that most of these species are
rather widespread in the Central Alps (e.g., the Utztal,Engadine and Wallis)
at altitudes of about 1900 - 2200 m; this tallies well with the result of the
pollen analysis, according to which, during the last interstadial, similar cli-
matic conditions as today must have prevailed in the Central Alps near the fo-
restlimits. This is confirmed not only by the algae, but by the lime-containing
sediment as well; also by the zoo-remains (chironomids, Pisidia, etc.), ac-
cording to which the basin of the Anterior Rotmoos was infilled at that time
with an open, neutral or alkaline water body (G A M S ). Amung the algae
51 • (344 8c 345) -- 11ohrung I. Rotmoos - itegent1nri. 11-1,en: occurrence Fossil micro-organisms Interslitc11 Spliag mintorf—p eat Rotrnoos hipperOberseo Lake mDxgzujaud_-- .110 Gywal - e Thdenlacke Schwingrasen loossilo Mihroorganisinen Depth Tie.tu Tide TieM e (1) = e a . (13estimmungen von ter. Steinecku) "n° f"e,„ . ..._ g . E e El E 5 ..c ,.,... 0 ... 0 ,Le g 0 (1+1). 4. ..., Sue C.) 5 § C 0 it) .0 C -S a)e Determined by 0 0 0 0 o o Me '5 e :ea' iS .,D`" Fr. STEINECKE o tO 0 u-J o Ir) tO P14:1 It) gri if> LO 10 IS: 0 _ rije GO co W • - . . _ 3111irozoen [ (2) (3) (4) ; 65_l (6) (7) (8) .(9) Rhizopoden: 1 Amelia vulgaris Ehrenbg. 1 1 1 Arcella artocrea Leidy I I 2 .1 1 '1 Cou tropyxis aculeata Ehrenbg 1 .1 1 2 llyalosphenia el egans Leidy 2 2 1 Phryganella nidulus Pén. ,1 Cryptodifflugia sacculus Pén. 1 Assulina seminulum Ehrenbg. 2 1 . 1 Trinenia lineare Pén 1 2 1• Ditreina flavum Archer 1 1 1 .1 •1 2 Amphitreina stenustom U III Niisslin 1 3 2 Amphitrema wrightianum Archer 2 9 1
ltotatorion: Callidinit angustico1lis Mori. 2 12 2 i\lonos1.y1;1 lunaris 1 0,11renbg. 1 •1 • Pluesoina triarantliuni (11ergend.) Voit . .1 Arthropoden: ,1. 2 Resit; von Insekleni) RPnlal-ns. Qf. i.nSe.cts.,2 1 nest° von Oribatiden2) ". 0.f .) 2 2 21 I It I + 1 + l i (ladoceren 5) 2 +
11111trophylen Schizuphyceen: Oscilla toria sp
Flagellaten: Phacus sp (?) • Peridinium cinetum (1\I in) Ehroubg. var. pa- lustre Lind
*) 1 At 5.6 and 5 m particularly Tanytar- (1) Quaking swards sids, at 5.6 m also a mandible of Sia- (2) In the lagg lis flavilatera.The old gyttja also con- (3) Marginal hollows tains Pisidia (GAMS). (4) Hummocks of the quagmires *) 2 It would seem especially Notaspis/Hy- (5) Hollows of the quagmires 3 drozetes (GANS). (6) Mud of the banks *) In particular Chyderideae. The samples (7) Hummocks from 160 and 200 cm additionally con- (8) Hollows tain, among others, Copepoda/Sperma- (9) Lake • tophora (CAMS). 52 • (346 & 347)
130111ms Iloltrung 13 • Recent 11ezeldesAlatreton:occurrence t - , ._. . Spliagnundurf p ea t Mud llygy t ja .1 III endatli- ale llyLlja'. Itohnuos üpperObmee „ . Lake Fossile N1 i k ruurgan isinun Depth 'Meru 'Piero Tielu c qi c I in ienlacke Schwingrasun (1) . . „ • , il, .0 al . . . . . (liestininuingen von I.' v. 5 Lei n oul3 e) -1) .4) ..,14' 4t,' id c
1-/e s in id ia cue n : 1'0111111u erassi II.SIIII 11 111 13u Lly. .1 3 2 1 Fe iiI u in Ill inut ni Mall's) Cl. 3 1i11j11111 iliilyiiiiiiarliiilii Emiiti. 33 •1 2 I) o cliii u iii undulalum . . . . . ' Tcuiiiuuuioiu.s winut us Do 13y. , • . 2 I , 2 .12 Cus iii n ri u iii Ito! ry 1 is NIonegli. V. ge in inilei ti 1 114;10 Nurikl role Italfs i:iisuiiiiitiiti 1. relin 1 11 in 2 Iiiill (:us ni a ri 11111 cii tIll hi I a Ilre, ■ 2 ! I I IL 2 • Ces iii a riuin lu veil wipe I Ill u Iii Lund. • I) ; felilt • IIU bun lira. 1 Cosinarium grit 3 I. Id ill lia tu in Nordst. Ces in a ri u in gra it a tu in v. su hgra 1 feli I
For meanings of (1) to (9) see translation page 51
• 53 (348 & 349)
ltotmoœ Itelirling 11 _ Recent Rezen Les Auftreten: occurrence Sphagnuniturf iet - — ------peat mudDygyttja Tids mil Itotmoos ;!;:£97; Itpp rObursee ',ski 1'ossile Mikroorganisinen Depth Tido Tide Tide 2-- —61---rie) ----'I-7—'1n tented«) to •2) 9:5 0 141 Schwir easel' (1 ) (Bestimmungen von Fr. S tel n cc k to 0) tn 0 5 •ci , 5 cd6. e C) a u 0) 06.0 ..bC till 4 eyEl I ,g Ë I eE g_, e. -•,- e ....,cu •m o o o o 0 0 Ci) g a See o o 0 • 0.) o 0 0 5 c4,21 cl o o v) Cl ( '0 Q) cl Cl ..I' trà I te — 11.) C.) •-•1 I rn CD cy) t/2 al Cosmarium Gretac nova sp. (s. S. 354) . . . 1. q(2) 11 2 ,1 ( 3 )1(4) reld Ç,5 )1(6) i, Cosin a rium ini p ressul uni 1111I'v 1 (8) f (9) 2 !! raft= iss ng Cosin a riu in laeve Itabh. Il . I fehlt Cus in a ri u in n î t id U I u In 11e Nul fehlt 1 Cos in ariu in luicrosphinr Lu in Nordst I fetal, Cosmarium ornaturn Raifs 1 fehlt C.osmarium obliquum Nordst. • 1 Cos in arium or thostichu ru Lund. • 11 fella Cosmarium pseudogra na tam Nordst 2 fehit Cosmarium pseudopyramidatum Lund. f. ■ 3 i fehlt minor Nordst Cos m arium punctulatum Bréb. 2 fehlt Cos in ariu ru rectangular° Grun 21 fehlt Co s in a riu in re it j fo rm e 1..talfs • fehlt Co s 1H a ri U UI S I) pro t u itt i du in Nordst . 1 :I fehlt Cos su aritim s u b lu in itt u tu Nordst. var. K 1 ebsii (Ualw.) W. et U. S. West • 2 fehlt Cosninrium suhiiii fo vine NurdsL. 1 j fehlt Cosm a ri (I in tu ni ida in Lund. 2 fehlt Cos niariu m '1' iir pi n I i Bréb. forma 1 fehlt Cos in a ri u in `I' u rp I ii I i var. ex i III I u in W. (d. O. S. 2 fete ; Cos in a ri u iii le Luau plitha lin ii iii liib 2 fetal Cos merit' In I. IiitiIt I um Arch 11 / reul Cosni a rium un a tu iii Curda var. ere n ula- 2 um (Nupg.) Wit.l.r. lulilt as tru in a f f i lie Italfs fehll i Eu:0.03.11111 d III)iilili Naeg. f. glacial(' nova f, 2 full u la Hutted-1qm 11:411 \\i ntr.) ItoY • • • • 2 :1 fehlt A r th rodusin us v01111•11V0rMIIS \V. ut ti, S. West fuhlt Sta u ras train bicurne llauptfl. . . . . 11 Pohl" Stain:1'0.nm) b o route W. et G. S. West . 11 bull 8 IlL uras tnt ta h ra eh ia L ut iii Italfs var. sa b fossile 455) 11UVa var. (s. S. 11 fehlt taurastru In gracile ltalfs 2 1 fohlt urastru la hi a [I fold Lii Delp. forma . . . tu 2 fohlt Stu u ras tru in paradox um Meyen. 1 Staprastrum p Lerosperinum Lund 2 fehlt
For meanings of (1) to (9) see • translation page 51 54 • (3 50)
some species indicate open water, especially the Staurastrum species with their
partly rather long suspensive processes; of these Staurastrum manfeldtii (even
though just in the var. planctonicum) is today characteristic of the Untersee
plankton, whereas Staurastrum gracile occurs among theplankton of the Obersee.
The various Pediastrum and Scenedesmus species in their turn indicate
that the entire association must have lived in an open water body. From among
these organisms Pediastrum integrum f. granulatum and Scenedesmus acutus are
still living today among the plankton of the neighbouring Obersee. Cladocera
carapaces too and perhaps also Mougeotia suggest open water.
Consequently, the association has been deposited by a small Alpine lake.
Depth of 550 to 450 cm : the stadial clay-gyttja is almost devoid of • fossils. As to mosses, this depth contains Sphagna from the subsecundum group, prepanocladus cf. revolvens and Calliergon stramineum. And the occurrence of
Pediastrum integrum shows that open water continues to be present. On the other
hand, the finds of Phacus and Arcella vulgaris make it seem probable that no
larger raised bog existed as yet. Alpine small pool.
Depth of 400 cm : a different association makes its appearance. Pedia-
strum angulosum as a new occurrence here and the very numerous Cladocera cara-
paces admit of concluding that much open water is still on hand. Apart there-
from, however, Sphagnum leaves are found in abundance and, moreover, for the (351)
first time sphagnophilic raised-bog forms: the rhizopod Ditrema flavum and,
chiefly, the stenotope rotator of raised-bog pools Callidina angusticollis. Be-
side these animais there are algae, still living at present in the pools of the
Rotmoos (Penium crassiusculum, Penium minutum) next to Eurastrum affine, likewise • sphagnophilic, which, however, seems to have become extinct at the station. 55 • (351)
The previous pool forms have disappeared and according thereto, the water has
adopted a dystrophic character. Accordingly, the puddle of the Alpine 2asture
begins to develop into a provisionally still large swampy pond.
Depth of 350 cm : once again there is a new association in the gyttja,
which, due to the masses of Abies pollen has a fimmenitelike character; nearly
all of the components of this association are still alive today in the Rotmoos.
Among the rhizopods, Amphitrema stenostomum, a form of the hollows, is remark-
able; it cements into its shells the valves of the diatom Navicula subtilissima,
itself an inhabitant of the hollows. From among the Desmidiaceae too, we meet
preeminently species from the shore zone of today's Tintenlacke, like Penium
crassiusculum, P. minutum, P. didymocarpum, Docidium undulatum, Tetmemorus mi- • nutus and Cosmarium cucurbita. Some of the algae of this peat layer are in such a fair state of preservation that, in them, remains of chloroplasts (Tetmemorus
minutus) and bodies of the contents ,like oil drops (Cylindrocystis brebissonii,
Cosmarium cucurbita),are still detectable.
Again, the Cladocera indicate open water, in likeness to Pediastrum an-
gulosum, found abundantly. The water character of this necrocoenosis is still
determinable as peat water of a raised bog, due to the presence of the plank-
tonic alga Coelastrum conglomeratum (STEINECKE 1924, p.342), described from a
bog of Hanover and from East Prussian pools.
Thus the association displays entirely the aspect of the present-day
Tintenlacke, except for Pediastrum angulosum, which I no longer encountered in
the Rotmoos as, in a general way, it seems to prefer warmer water.
Simultaneously with the Atlantic Abies maximum, a lively growth has • started of Sphagna palustria; the lake has become a raised-bog pond. The 56 (351) 11) micro-organisms among the Sphagna of the pond margin are the same as
we find them today.
Depth from 300 to 20 cm : the total stratigraphic succession is formed
by very wet raised-bog peat, with a lot of Scheuchzeria and Carex limosa; it (352)
displays rather few remains of micro-organisms. All of them are present-day in-
habitants of the raised bog and, predominantly, organisms of the hollows. The
Sphagnum cover of the quaking carpet has a great number of hollows.
Due to the small amount of organic remains, the necrocoenoses of the
individual beds can be determined only with reservations. With a certain measure
of assurance, one might describe them as follows :
Depth of 230 cm : the rhizopod Amphitrema, the rotifer Callidina, as
well as the alga Zygogonium ericetorum; they would indicate a large pool. • Depth of 200 cm : the observed remains could point to a raised bog (among others, Calliergon stramineum and Scheuchzeria).
Depth of 160 cm : a striking amount of forms as found in large hollows
(Cladocera, Callidina angusticollis, Peridinium cinctum, Coelastrum conglome-
ratum, Penium minutum), so that a conclusion of much open domed-bog water im-
poses itself.
Depth of 100 cm : Sphagnum cf. recurvum along with forms of the hollows.
Depth of 50 cm : peat of Sphagnum magellanicum, with organisms of
hillocks and hollows.
It would seem premature to draw conclusions from these fragmentary find-
ings concerning the developmental history of the Rotmoos and its eruption.
As regards the rich algal flora of the interstadial and warmth-period
gyttja, we refer the reader to what was said about the Rehberg Bog (p. 322) and, • furthermore, to the partly rather similar findings in the Scandinavian bogs 57 (352)
(LAGERHEIM, BORGE, HOLMBOE and others); of North Germany (STEINECKE, DONAT,
KOPPE & KOLUMBE, and others); of Bohemia (RUDOLPH); of den (STARK, who lists
from the lacustrine Cretaceous of bogs near the Lake of Constance a particu-
larly great number of species); of Württemberg (BERTSCH) and Switzerland (NEU-
WEILER, FRCH & SCHRUTER, BRUTSCHY). The concordance between the Cosmaria of
the Rotmoos gyttja and the finds of STARK is rather considerable. Even the
statement of STARK that "Cosmarium granatum frequently appears in numerous spe-
cimens in the field of vision of the microscope" is valid in the same manner
for the algal gyttja of the Rotmoos.
Our knowledge, however, about the thermal requirements and the total
dispersal of the individual species, several of which (e.g., Cosmarium arctoum,
C. crenatum and C. undulatum var. minutum = C. alpinum) seem to be of an Arctic/ • Alpine character, is, at this point, far too insufficient for the purpose of (354) utilizing the findings forafloristic and climatic history (GAMS ).
REMARKS CONCERNING A FEW FOSSIL ALGAE (see F i g • 10 )
A few forms, not described until now, were found in the algal gyttja.
In cases where the divergences as against known species are but inconsiderable,
I refrain from conferring names on them; as it is, the diversity of forms espe-
cially among the Cosmaria and Staurastra is anyhow very great. Since in fossil
species merely the cell walls are present, I also abstain from giving precise
diagnoses and refer the reader to the figures.
Pediastrum angulosum (EHRENBG.) MENEGH. Under this specific name I list
a Pediastrum which would approximately correspond to the var. impeditum RAC.,
but could just as well be designated as P. boryanum var. rugulosum G.S. WEST. 58 • (353 )
•
F i g . 10 . Algae from the gyttja of the Rehberg Bog and the Anterior Rotmoos. Magnification x 750. Original by F.STEINECKE Staurastrum hicorno Hauptfl. forma. Sefton- und Scheitelansicht. *) 2, S I, a ur as tr u m b rac Ilia t um ltalfs forma sub fossil() nov a f. Soi ten- uncl Scheitelansicht. 8, .Muas tram clubium Naeg. forma glaciale nova I. Cosmarium Tur pin ii forma, Vorder- mid Sclioitelansiclit.**) 5. To traedron minimuM (A . Ru.) 11 ansg. 5. Cosmarium WU; tau nova sp. Vorder- und Scheitelansielit. 7 . Cos m ail um Lumidu in Lund, forma. \Tardily- und
*) Seiten- & Scheitelansicht = lateral and top view **) Vorder- & Scheitelansicht = front and top view • 59 (354)
The differences between the two Pediastra are anyhow flot of a fundamental na-
ture. Cells 10-20 p broad, coenobia 80-150 p large.
Tetraedron minimum (A. BR.) HANSG. F i g • 5 . The small alga, frequent
particularly in the gyttja of the Rehberg Saddle Bog is placed within this
group because, apparently, it represents one form of this widespread plant.
Similar forms with terminal points and a punctate membrane have been described.
Since, however, the cell content is lacking, the alga could be just as well
grouped with the genus Arthrodesmus of the Desmidiaceae, or also the genus
Staurastrum. Except for its size, the observed alga resembles in particular and
rather precisely the St. Clepsydra NORDST. var. sibiricum (BORGE) WEST & G.S.
WEST (WEST, Monograph, Pl. 122, Fig. 10).
Euastrum dubium NAEG. forma glaciale nova f. F i g . 3 . In the ar-
rangement of the tubercles it diverges from the species; length 26 p, width 18 p.
Cosmarium granatum BRÉB. Found preeminently in a form possessing an own
specific name as C. pseudogranatum NORDST. Some few specimens in the var. sub-
granatum NORDST., a form approximating the C. impressulum ELFV.
Cosmarium gretaenova sp.Fig. 6 • The well-characte-
rized, undoubtedly new species approximates C. radiosum WOLLE. Cell halves
with ten radially disposed rows of granules, which diminish in size from the
lateral margin towards the centre. Length 26 p, breadth 22 p, thickness 12 p.
Cosmarium tumidum LUND. forma. F i g . 7 . Length 32 p, breadth 22 p,
thickness 15 p.
Cosmarium turpinii BRÉB. forma. F i g . 4 . Is remarkable by tu- (355)
bercle arrangement and small size; length 40 p, breadth 26 p, thickness 20 p. • Staurastrum bicorne HAUPTFL. forma [Chief floristic forma ?1. F i g . 1 . 60 (355)
It diverges from the typus in the arrangement of the tubercles on the mem-
brane. With processes, length 55 p, breadth 70 p.
Staurastrum brachiatum RALF'S forma subfossile nova forma. F i g • 2 .
The form somewhat approximates the illustration of the species in WEST (P1.141,
Fig. 2). With processes, 25 p long and broad.
GENERAL RESULTS AND FUNDAMENTAL CONS IDERATIONS
e) The age and velocity of formation of the Lunz deposits
For a comprehension of all the processes of sedimentation and bog
formation it is indispensable to introduce a chronology, be it initially even
just relative. Accordingly, as long as over 30 years ago, Albert HEIN & BRUCK- • NER have tried to determine the interval of time elapsed since the glacial re- cession from the Alpine lakes and they arrived at the figure of 13,000 to
16,000 years. Aside from upon morphometric data, these computations were based
merely on the amounts of present-day sedimentations, which GUTZINGER too has
measured in the Lunz Untersee with the aid of mud chests. He ascertained a
yearly mud deposit averaging 1 mm per year.
But - as was already established by GUITZINGER - sedimentation varies
to such an extent in different parts of a lake as well as in different yearly
seasons, while, moreover, there are such serious objections to the method of
mud chests that, in this manner, no incontestable chronology can be worked
out. Likewise, the numerous attempts to determine their age from the massive-
ness of peat strata have failed throughout.
It has long since been commonly admitted in Fennoscandian Quaternary • research that a 61 • (355)
safe chronology can only be obtained through correlations with datable moraines,
shorelines, etc., on the one hand and, on the other, with the aid of archaeolo-
gical discoveries. Outside of Scandinavia the best-known geochronological inve-
stigations are those undertaken by DE GEERS, but it must not remain unmentioned
that especially his most recent expositions (YMER 1925) regarding correlations
of moraines and shorelines have also met with a strong and justified opposi- (356)
-Lion on the part of his compatriots MUNTHE, THOMASSON and others, as well as of
Norwegian, Danish and Finnish Quaternary investigators.
Still, the countings of yearly stratifications by Swedish and Finnish
geochronologists (LIDÉN,SANDEGREN, SAURAMO and others) have established with an
adequate amount of certainty that the great Fennoscandian terminal moraines have • been formed approxinately 11,000 years ago, the last post-glacial moraines about 9,300 years ago; the latter preceded the fini-glacial climatic improvement and
the bipartition of the inland ice in Jâmtland (that had taken place around
6,900 B. C.). The great Fennoscandian terminal moraines correspond rather cer-
tainly to the Gschnitz moraines, the last Fennoscandian post-glacial moraines
to the Daun moraines of the Alpine glaciers (PENCK & BRUCKNER, RUDOLPH & FIRBAS,
BAYER and others). They are flot - as I myself still assumed in 1923 by follow-
ing SCHREIBER as well as SCHULZ - younger than the climatic improvement, but
Preboreal. Likewise, as revealed by the latest investigations of LUNDQVIST as
well as THOMASSON, the Ancylus Period of the Baltic Sea is also Preboreal,
instead of Boreal, as was erroneously assumed up to now.
Unfortunately, the precise emplacement of the stadial moraines has not
as yet been established in the Lunz area. The multiple ring of moraines between • the Untersee and Lunz is generally interpreted as young terminal moraines. 62 • (356) PENCK supposed that, at that time, the snow limit in the Seebach Valley was
lying a 1150 m. Larger moraines are present in the Ybbs Valley at an altitude
of 650 m in the Langau; in the Seebach Valley they correspond to those of the
Wagnerfeld and the Sgge. In both cases they are very probably lake moraines
("Bühl" in a wider sense). I believe to have recognized the Gschnitz moraines
of the Ybbs Valley with a fair certainty in the tremendous moraine masses at the
Oisklause - altitude about 1000 to 1100 m - near the uppermost reaches of the
Ybbs; these moraine masses, strange to say, are not marked in the geological
map. The corresponding moraines in the Seebach Valley must be searched for at
the Ellmauer, below the Obersee where, anyhow, they are buried in the talus
pilesof the declivity. As to the Daun moraines, one can expect them only above
the Obersee and Rotmos.
• Consequently, in case these evaluations are correct, the possibility
exists that older stadial and interstatial deposits can be found in the Unter-
see than in the Obersee. Here at the Untersee the formation of the varved clays,
the greatest drilled massiveness of which amounts up to now to 2.85 m, has be-
gun with the retreat of the glacier from the inner young moraines, whereas it (357)
is most probable that this occurred at the Obersee only subsequent to the re-
cession of the Gschnitz moraines; and in both cases this has lasted until the
definite retreat of the glacier from the respective lake. At the Untersee this
time interval amounts to at least 300 years.
Now, since n o moraine material rests on top of the interstadial gyttja only of the Obersee and the Rotmoos but, instead,/clay and fine sand, which must
have been washed down from the head of a glacier at a greater height, the latter,
apparently, cannot be any other than the one of the Daun stage and, gl› 63 • (357) accordingly, the interstadial ascertained at both places is the Gschnitz/Daun
interstadial, which, conform to the dating as described above, must have ex-
isted 7,500 to 9,500 years ago.
A comparison of the pollen diagrams from the Obersee and Rotmoos with
those obtained thus far from the Untersee and Rehberg Bog ( F i g . 11 , p.359)
evidences that in the latter as well no older fossil-carrying strata have been
disclosed. Consequently, the entire period between the lake moraines up to the
end of the Gschnitz stage is represented in the varved clays and the 10-15 cm
thick iron-sulfide clay on top of the latter, plus the then following, about
40-cm thick unstratified clay. It does not appear unlikely that the strong iron-
sulfide precipitate in Horizon I, which reappears in a very similar layering in
the Walchensee [Lake of Walcheni (personal communication by F. HEIM), is organo-
• genic and represents the Bühl/Gschnitz interstadial; judging by the very scanty
fir and willow pollen, apparently originating from a greeter distance, The Bühl/ 1 Gschnitz interstadial must have had an absolutely Arctic climate *) .
The then following interstadial where, for the first time, appear birch
and hazel, plus soon thereafter also spruce, is doubtlessly the same as that of
the Obersee, so that, accordingly, Horizons II of both the Untersee and Obersee
scale are synchronous and fall into the ninth millennium B.C.The interstadial
fossil forms in the Untersee, Rehberg Bog and Rotmos are distinguished by a
particular abundance in algae.
1 *) In the Lünersee [Lake of Leni of the Rhaetikon that lies at an altitude of 1940 m merely the warmth-period strata are developed as a similar iron- sulfide gyttja. More details concerning this in: Verh. Verein. f: Limnol. 4 (Rom) [Proc. Assoc. f. Limnology (Roma).1- NOTE provided while paper • was in the press. 64 (357)
It is still impossible for the time being to indicate to whichever of
the periods in the development of the Baltic Sea this interstadial corresponds,
because the time intervals of the Preboreal, differentiated by MUNTHE & SUNDE-
LIN, most recently by THOMASSON, have not been correlated as yet with the geo-
chronologically dated moraines.
It is, in contrast, very probable that Horizons III in the Untersee (358)
and Rehberg Bog, Horizon IV in the Obersee plus Rotmoos, indicate the beginning
of the post-glacial warmth period, and this not only between each
other, but that they are also synchronous with the beginning of the of the warmth
period at the Baltic Sea (Period VIII on Gotland by VON POST, the Echino-Ice Sea
by THOMASSON; but the bipartition of the DE GEER around 6,900 B.C. is apparent- • ly somewhat younger). The subdivision of the warmth period in the Lunz area is rendered diffi-
cult mainly by the fact that not even from a wider environment any Archaean
findings have been brought to light and that none such can be expected. There-
fore we depend on correlations with the archaeologically datable bore-log
profiles from Krain and Bohemia; particularly so from the northern Alpine fore-
land - Salzburg into Switzerland.
FIRBAS (1923) assumes that beech and fir begin to spread in Krain at the
end of the Preboreal, right after the appearance of the oak/mixed-forest and the
alder; the same occurred at the transition from the Boreal to the Atlanticum
in the northeastern Alps and the greatest part of the Alpine foreland, whereas,
in Bohemia, it took place only in the mid Atlantic period. Near Lunz too the
above-named trees invariably appear together, as will be seen in the following, • namely, only just a little later than in Krain and earlier than in the other 65 • (358) bogs thus far investigated in the Eastern Alps.
Among the most striking phenomena of the older warmth period, alike in
the Alps and their foreland, the secondary mountain chains and the Baltic area,
are, on the one hand, a very pronounced hazel peak, on the other the intersec-
ting points of the fir and spruce curves. It goes without saying that one cannot
presume these two horizons having been simultaneous everywhere, as evidenced al-
ready by the fact that this point of intersection lies at the Untersee, in Salz-
burg and the eastern part of Upper Bavaria shortly above the hazel maximum,
whereas, at the Obersee, somewhat below it. Moreover, this state of affairs is
complicated by the fir curve comprising the combined total of both the Pinus
silvestris and the P. montana pollen, even though and naturally the two species
behave rather differently (cf. STARK 1927). Nevertheless, Pinus montana, still
growing today at the Obersee and Rotmoos, has not been pushed back here by spruce
and fir forests later than at the Untersee where, quite undoubtedly, P.silve-
stris was also strongly represented. At the Baltic Sea as well as in Bohemia
and South Germany the first hazel apex, apart from which in places and rather (360)
frequently another yet stronger one was developed, is interpreted as Boreal and,
up to now, there is no reason to date it differently near Lunz, even though it
might have occurred later at the Obersee than at the Untersee.
Thus, provisionally and in agreement with my South German colleagues,
I designate the time from the first appearance of the oak/mixed-forest (III at
the Untersee, IV at the Obbersee) up to the point of intersection of the fir
and spruce curves at the Untersee as Boreal. At the beginning of this period
the then present lakes at the Rehberg and in the Anterior Rotmoos develop their • deltaic sequences. • • •
10 ZO 30 140 50 60 70 80 90% I 1i. te,, Pinus —Larix --Pic ea —..—Abies Betula C orylus--e—Eichenmischw aid —0---111nus Fagus
VI
V
EC
UnterseeDc Obersee 1 Vorderes Rotnaoos Lower Lake Dc Upper Lake I Anterior Rotmoos
.1 1 1 t 1 1 1
F i g . 11 • Pollen diagrams from late-glacial (interstadial and stadial) plus early post-glacial lake profiles 66 • (360) The same as nearly everywhere else the boundary line between the Atlan-
ticum and the Subboreal is very indefinite. In all of the Alpine foreland as
well as on the Alpine pastures and in Bohemia it has been-ascertained that still and spruce in the late Neolithic, hence the early Subboreal, oak/mixed-forest/dominated ,
whereas the beech did not gain preponderance before the bronze age. It would
seem that the first fir peaks are Atlantic everywhere but, in contrast, I regard
the point of intersection of the fir and beech curves at the Untersee (VII) and
also the first beech climax already as Subboreal; by all appearances, however,
the first beech climax has not been simultaneous at the Rehberg Saddle plus Ober-
see with the same climax at the Untersee (as to the history of immigration of
the beech and its present-day dispersion, cf. Chapter h). The findings in the
bogs at the Untersee (p. 314) and on the Rehberg Saddle, both of which evidence
• that they had a low-water interval or a drought between Horizons VIII and IX (at
the Rehberg it occurred already prior to the heech peak of that place) agree
with the above assertions.
Since, in its turn, the formation of shaking bogs in the Obersee (pp.
325 and 329) renders such a low-water period presumable, the disturbed Horizon
IX must also be essentially Subboreal; in such a case, however, we have to
reckon with later rebeddings and in-washes of the gyttja, so that these local
phenomena are of no significance for the over-all chronology.
The second beech climax, recognizable in both the quagmires of the
Obersee and the Sphagnum peat of the Anterior Rotmoos, is, in contrast, already
Subatlantic, just as in South Bavaria; the same is valid for the resumed rise
of the spruce and fir curves at the Untersee (IX). • Similar slides as have been brought about by the gravel in-wash between 67 • (360) Horizons V and VI in the Untersee bore-log profile Fa and also in disturbed
Horizon IX in the Obersee have already occurred previously (see Fig. 8 E )and
might equally be ascertainable for most recent times, as has been done by NIP-
KOW at the Lake of Zurich and by F. HEIM at the Walchensee (the latter investi- (361)
gation, however, still lacks a precise time determination). LUNDQVIST has al-
ready shown that such disturbances can make the evaluation of individual lake
borings or sounding samples entirely illusive, in case such borings and sound-
ings are not connected through line profiles.
Subsequent to having thus and with the aid of guide horizons gained not
only a relative but, with certain reservations, an absolute chronology, we can
now turn to the question of the rate of sedimentation during
the individual time intervals. At first, however, I shall describe the result
• of similar but quite more circumstantial investigations by LUNDQVIST in Swedish
lakes (1925, p. 112); it is entirely concordant with that of my own research:
"It is made clear by the bore profiles to what a high degree the mecha-
nical factors, in other words the exposure, influence the increment [in sedi-
mentationi. The same kind of sediment may, in one place, increase with a rela-
tive rapidity, while, in a directly adjacent one, it may grow very slowly. . .
It is a general rule that lime and clay sediments as well as algal gyttja form
relatively speedily. The same holds true for the littoral coarse-detrital gytt-
jas.Fine-detrital gyttjas, however, grow considerably slower, the same as pro-
fundal coarse-detritus gyttjas. But it has to be regarded as a principal rule
that all sediments form relatively rapidly up to the point of the sedimentation
limit, when the increment ceases." • LUNDQVIST does not provide numerical evidence for these statements, but 68 • (361) it is given by his drawings of bore-log profiles. To render a comparison possible
with LUNDQVIST's findings, 1 indicate in the following table the approxi-
mate position of his three principal guide horizons, from which the approximate
quantities of sedimentation can be computed. The indicated thicknesses of the
sediment are the thus far observed maximum amounts from relatively undisturbed
bore profiles (deposits of debris and drift material excluded).
Hence, according to this very crude calculation, the rate of sedimenta-
tion per year amounts in the Pre- Boreal to about 0.15 - 0.5 mm, during the Bo-
real 0.5 to 1 nuat and, starting with the warmth period, 1 to 2 mm, which values
agree rather nicely with those that GUTZINGER has measured in the Untersee.
Assuming that these values are also true for suspended matter and that
there are no gaps in the sedimentation as well as no particular wash-ins, it can
be expected that suspended matter in the Untersee would attain a thickness of (364)
sedimentation amounting to about 14 m.
But it should be emphasized once more that these figures can in no way
be regarded as constant magnitudes for determined lakes and time periods. Chief-
ly and at the outset, higher values have to be expected at borings along the
shoreline with its considerable drift material.
LUNDQVIST's result to the effect that fine-detrital gyttja is forming
relatively slowly seems contradicted by the fact that, in the southern basin
of the Obersee (cf. F i g . 7 ), a fine-detrital gyttja has been deposited; it
was accumulated in its major part during the warmth period and attained a thick-
ness of up to 7 m and more. But here we have to reckon with a subsurface inflow
of these soft plastic masses into the basin; in the following Chapter we shall • return to the subject. Maybe even an 'upward flow,' or more correctly,
69 (362) UNTERSEE & REHBERG SWAMP
Maximum amounts of Years Guide horizons and events sedimentation total thick- per ness 1000 yrs. 1900 Introduction of Elodea shore erosion,artificial deforestation 1000 IX. Resumed rise of spruce & fir curves, reforestation of Rehberg swamp 0 Rise of lake level, ruin of forest on Rehb erg swamp e Lwa 3 in elm, 1
- 1000 Afforestation of Rehberg swanp VIII. Beech climax - 2000 Bog formation at Steinbauer summit } etwa 2 ni etwa 1;f2 ii - 3000 VII. Point of intersection between spruce and fir curves
- 4000 Inanigration of Spongilla lacustris } etwa 1 1/2 ni etwa 1 ii in the Untersee - 5000 VI. Intersection point of fir with 1, etwa 1 ni etwa 2 g; .1 . spruce & pine curve •••••••1 6000 V. Hazel climax,delta facies of Rehberg 1. } eLwa .1 ni IV. First appearance of pine & beech,Fon- eLwa I a tinalis in the Untersee IA m III.First appear. of oak/mixed-forest } - 7000 i Impoverishment of total biotic existence during Daun Stage
- 8000 1 m etwn Interstadial gyttja with many algae, im- migration of zooplankton II. Immigration of hazel, birch, spruce Cvclotella distinguenda - 9000 Clay of Gschnitz Stage 40 em etwa 3 fe
10-15 em - 10,000- Iron sulphide clay etwa Iû a . etwa 3 ni Varved clay of lake moraines
* etwa = approxiMately • 70 (363)
• T OBERSEE and ROTMOOS Scandinavian chronology Amounts of sediment. I Lund- Jahre ' Guide horizons and events thick/per V. POSt Blytt- clvist 1925 Sernmuler jiess 12'9 years Introduction ofof ElodeElodea yrs. 1900 1 Erosion of quagmires Forming of inundation belt 1000
Bog bursts of Rotmoos lv Suballant. Younger Sphagnum peat in 0 Rotmoos eroded Uplift of quagmires II X. Second beech climax III —1000 Spongilla in the Obersee Rapid delta formation and eutro- phization of Obersee — 2000 '1/41 Growth of the Rotmoos Subboreal h IX. Disturbed horizon in the — 3000 Obersee III i VIII. First beech climax j. IV etwa etwa — 11000 III 3/4 in V VII. First Abies apex Atlantiscli — 5000 / VI. First spruce apex
1 V. Hazel peak etwa II VI — 6000 • Intersection fir & spruce % m m Boreal curves °twit etwa Delta formation of Rotmoos lake j. 30 cm 25 cm Xl VII 4 First Daphnia longispina — 7000 d III. Clay bands ; reappear- ance of spruce In fraboreal Disappearance of spruce & —8000 deciduous trees 1 Interstadial gyttja with 30 cm 15 cm Tanytarsus & spruce VIII q II. First occurrence of Hazel and birch Subarktisch I. First occurrence of — 9000 1 fir pollen IX Varved clays of Gschnitz Stage Arldisch — 10 000
* etwa = approximately • 71 • (364)
a whirling-up of the reddish, fine-sandy depth gyttja from the bog hollow has
taken place, since this gyttja has been found several times in the disturbed
horizon of the northern transverse profile at a depth of but 4 m, whereas,
normally (cf. map drawn according to GUTZINGER, F i g . 6 , p. 324), it is en-
countered only below a depth of 5 m.
For the history of lakes and bogs the speed of sedimentation is not of
so great an importance, as ascribed to it by geologists in many cases. There-
fore, from the above computation, I do not wish to draw any other conclusions
but the one I arrived at from experiences in other contexts, namely: for micro-
stratigraphic purposes, samples have to be taken regularly at shorter intervals
in older sediments than in younger ones. If, from the latter, a sample is ana- • lysed for pollen every 25 cm, it is imperative to take and investigate samples from Every 15 cm if similar time lapses should be comprehended for the fir
period; for Subarctic strata, this should be done every 5 - 10 cm as, long since,
it has been the practise among Swedish sedimentary stratigraphists.
f) Deltaic deposits, formation of quaking bogs, and shore erosion
It has been rEvealed both at the Untersee and the Obersee that a notable
progression of the "delta-facies vegetation" does no longer take place nowadays
and that, much rather, the lake water is the erosive factor, particularly also
at the bog margins. This result contradicts the current mode of viewing the mat-
ter by geologists, geographers and botanists as a continually progressing "ma- (365)
turing" and "filling up by plant growth" of stagnant water bodies due to "delta-
facies vegetation." Therefore, we have to investigate whether the phenomena as-
• certained at the Lunz Lakes represent exceptions or whether, in other places 72 (365)
as well, they are encountered as regular processes.
Already years ago (1923, p. 39), I have shown in the example of the Oster
Lakes that the "delta-facies vegetation" (Phragmiteta, Cariceta, Cladieta, etc.)
must not necessarily represent outposts, but may just as well be rear-guards
at recessions o f shore - banks. As early as in 1909 and with a particular emphasis
in his last works, L. VON POST has pointed to the regional types of deltaic se-
quences, which, on the one hand, are determined by the physiology of the lake
(the "types of lakes"), on the other hand, by the climate; these relationships
have thus far remained as much as unheeded in Central Europe. VON POST calls
special attention to the fact that, during the Subboreal, a land vegetation, for
instance, a swamp forest, frequently followed inuitediately upon gyttja, without
a broader "zone of deltaic formations' intervening. And a particular group of
pertinent delta-facies phenomena, that of quaking-bog developments, has not as
yet found the recognition it deserves, either in VON POST's or in SANDEGREN's
and LUNDQVIST's works. Therefore, I use the findings established in the Lunz
Lakes as an inducement to deal with this deficiency at least to some extent.
The prevailing opinion concerning the formation of swinging or swaying
swards - (in Bajuvarian [ancient TBavarian'i called 1Wampen0 in Alamanic 'sway-
ing grounds;' in Low German 1 1(àhpen, FledderT; in Dutch idrijftillen, onland;'
in English 'quaking or shaking bog;T in Swedish Igungfly; 1 in Russian Tsplawi-
na, plawa;' in Hungarian 'Up') - has perhaps been most clearly stated by the
Dutch geologist STARING 1853: "The quaking swards . . . are among some of the
general means possessed by nature to form bogs in deep water." From among the
numerous modern handbooks, also expressing the opinion that the quagmires "push • themselves forward across deeper water," we may name just the 'Bodenkunde' 73 (365)
[Soil sciencel by RAMANN (Third Edition, p. 182) and the Russian 'Moorkunden 1
p. 18); also SUKATSCHOW (Third Edition, [Swamp sciencesl by DOKTUROWSKIJ (1922, ing pp. 27-30). The latter contrasts the "cover-/-over with vegetative growth (na-
rostanie) with the usual choking-up with plant growth or bogging-up (zarostanie)
and remarks quite rightly that very little is known about the actual processes
involved here.
That conditions are not as simple as often represented has been shown
for the first time by KLINGE 1890 who has pointed to the influence of prevail- (366)
ing wind orientations which, on the one hand, encourage, on the other hand,
hinder the emergence of deltaic formations. Thereafter, FeH,by following the
studies of HEER and based on his own observations, has investigated the mode of • formation of the floating islands at the Barchet Lake in Canton Thurgau; accord- ing to him, these islands can take their origin either from forward-expanding
vegetative covers, from the separation of quagmire fragments (either by man or
through frost) and, furthermore, through a "vertical rupture due to an uplift",
caused by "dissimilar imbibitions of differing peat layers piled one on top of
the other."In this context FeHroints to the "Schwimmendes Land von Waakhusen"
[the 'Floating land of Waakhusen'l near Bremen and the Flottegar of Ilmola in
Finland (G. ANDERSON). Furthermore, the "Flotteholm" [floating island] of the
Ralângen near Linkeiping was added to these examples; it has been known since the
17th century and was described by 6BERG and others. FRUH & SCHRUTER (1904,p.54)
divide the proper quaking bogs as follows: on the one hand the succedan-
e o u s [Lat. succedaneus = successive] ones, which grow progressively from
the shore into the open water; this has been frequently described (but only ra- 411 rely observed as yet); on the other hand, the simultaneous ones 74 (366)
ones upon drained peat or mud surfaces: "Upon a drained peat surface (water-
rich peaty mud) a turf grows up by wind dissemination and gradually mats to-
gether into a dense cover; by subsequently infiltrating water the bottom layer
thereof is soaked and the turf is transformed into a quaking sward." The authors
ascribe this mode of origin only to a Rhynchosporetum swaying bog.
POTONIE (1911, pp. 225-238) also deals in detail with the succedaneous
mode of formation of the quagmires and the floating islands; but in addition he
names an example of the simultaneous mode, namely the Drausen Lake in the Vistu-
la/Nogat Delta (cf. TOEPPEN, CONWENTZ & BERTRAM); he remarks in this connection:
"The described phenomenon is by no means rare; I have observed it myself fre-
quently enough, among other places in the area of the Stettin Haff." • In the Netherlands, SCHIERBECK (1917) distinguishes primary and secondary quaking bogs, the latter ones consisting of detached lowland-moor fragments.
VAN BAREN (1924, p. 935) undertakes a further division by distinguishing: (1) the
actual "drijftillen," constituted of centripetally growing reed beds, at most
m thick and, nowadays, in their majority "physiologically dead." (2) More
massive reed beds, for which he proposes the Dutch name tonland.' (3) Part
pieces of shaking bogs, separated either by man, by breaking-up ice or sudden
water-level fluctuations, and thus set in motion. (4) Floating islands proper (367)
which, in Holland, are nearly absent. (5) Lowland-moor islands having been
left behind at peat-cutting due to their abundance in wood content.
We are not going to enlarge here upon the reed quagmires, described re-
peatedly from the Netherlands, the Vistula/Nogat Delta and also particularly
from Hungary and Russia; in contrast, we shall confine ourselves to the moss- • rich, especially Sphagnum- rich,quaking swards of the boggy lakes and 75 (367)
investigate the question whether these are more frequently 'succedane-
o u s', hence growing out progressively into constantly open water, or 's i -
multaneous,' meaning that they have taken their origin throughasub-
sequent uplift from an at least temporarily drained substratum. FRUIT has written
in 1904 that "from most localities, the mode of origin is unknown," and this is
still valid today, as was remarked also by SUKATSCHOW.
As to Alpine lakes, I know quaking bogs I have examined myself, which
can be compared with those of the Obersee, namely: the quagmires of the Hechten
Lake, at a distance of only 11 km in Steiermark; an investigation of its vege-
tation is expected from H. ZUMPFE; from the Lungau (the Seetal and Dürneck
Lakes, studied now by F. VIERHAPPER); from the Schwarsee near Kitzbühel; from • the Upper Engadine (e.g. Statzer Lake); from the Reusstal (Arniberg, cf. GAMS & NORDHAGEN 1923, p. 117; the islands floating there in the dammed-up lake, con-
stituted of peat lumps detached during the Subboreal from the drained horizon,
correspond entirely to the Flyttegar or Flottegar of Ilmola and the Flottholm
of the RalAngen); from the Wallis (for instance Lac de Champex; no stratigra-
phic investigations, however, are available therefrom as yet).
But stratigraphic studies are much more numerous from the moraine land-
scapes of the Lower Alps, thus in Upper Bavaria (e.g., the moraine lakes of
theChiem region, the Stein and Kasten Lakes, Osterseon Lake near Kirschau,
Oster Lakes, Ess Lake near Starnberg, cf. GAMS & NORDHAGEN, pp. 36-43, PAUL &
RUOFF 1927); Upper Swabia (cf. GAMS & NORDHAGEN, pp. 144-156, STAUDACHER 1924),
and Northern Switzerland (e.g. Barchet Lake in Canton Thurgau, already described
by HEER and Fell ; I too have visited this lake and have found that its quaking • bogs much resemble those of the Obersee and Hechten Lake; the Andelfinger Lakes, 76 (367)
the Pfà:ffiker and Katzen Lakes, the Lützel and Seeweid Lakes near Hombrechti- the kon, cf. FRUH & SCHRUTER, also WALDVOGEL, as well as/work expected soon by
MESSIKOMMER on the PfSffiker Lake).
Here we may lay stress just onto two relatively lime-poor, but none the
less absolutely eutrophic swamp lakes, distinguished by the fossil occurrence
of T ra p a c ea e: the Lützel Lake in Canton Zurich and the Feder Lake in (368)
Upper Swabia. WALDVOGEL (1900, p. 299) writes about theLützel Lake:
"RAMANN explains the origin of floating bogs: 'Parts of the shoots and
roots of the marginal plants extend freely into the water; they may deposit
humous substances amidst each other and, finally, form a floating peat cover.'
I could accept this explanation without much ado for phenomena in Lützel Lake, • if it were flot Carex stricta that occupies the marginal zone of the floating bases. C. stricta is in the habit of conquering exclusively firm substrata.
"Our islands did probably originate as a consequence of the great fluc-
tuations in the surface levels of the lake. These fluctuations may amount to as
much as 1.5 m and are brought about by the use of water power. The outlet was
lowered beneath its natural depth; through a construction of traps the water
can be dammed up and discharged to a certain limit.
"Sometimes in the past, conditions prevailed most certainly where the
differences in the water gauge were not considerable, be it that water power
was not or only insignificantly called for, be it that moisture conditions re-
mained in a state to prevent a considerable water decrease even in the summer.
Thus the Carex vegetation had the possibility to gain footholds upon the or-
ganic deposits at the marginal zone of the lake and to push forward. If, there- • after, a sudden and strong decline of the water occurred, the great mass, in 77 (368)
like measure as the water decreased, pressed upon the soft substratum, compres-
sed it, or squeezed it out into the lake, which rapidly acquired a depth of
2 - 3 m. That part of the matted vegetative sward that rested upon a more solid
substratum could not participate in the depression, and a rupture was bound to
take place. When the high water returned, the whole mass, matted together through
the cohesive network of shoots and roots,was lifted upward, had lost its sub-
stratum and slid out into the lake as an island."
It seems, the only correction one should make in this representation
by WALDVOGEL would be that, in the Lützel Lake as well, the deltaic sequences
did most certainly not appear during a period of continuous high water, but
during continuous low-water times. For the rest, WALDVOGEL has clearly recog-
nized the simultaneous mode of formation of these quagmires, which much re-
• semble those of the Obersee.
As to the history of the Feder Lake, Head Forester STAUDACHER has been
able to trace its development very precisely with the aid of soundings and ni-
vellations; he succeeded therein due to the assistance of the stone-age and (369)
Hallstadt period settlements of that region. STAUDACHER arrived at the result
that the formation of quaking bogs had taken place with an exceptional rapidity
during the Subboreal, because the brown-moss/sedge marsh (nearly entirely
exempt of reeds) pushed itself forward right on top of the gyttja of the boggy
lake, strongly eutrophic already at that time; this movement, however, had come
to a complete standstill from the Hallstadt period up to the time of the arti-
ficial level lowerings of the 18th and 19th centuries. It was only during the
Hallstadt period that a true reed belt developed, forming simultaneously a pro- • tection against shore erosion: "Whatsoever has become delta formation at the 78 (369)
Feder Lake, will remain Delta formation" (STAUDACHER). At this lake the forma-
tion of the quagmires was particularly expedited by the fact that, due to the
pressure of the marsh, the gyttja flowed lakeward, thus exposing new and new
shore zones to being grown-over, until this process was interrupted for a long
time by the Subatlantic deterioration of the climate. In the described case of
the Feder Lake simultaneous quaking-bog formation has been demonstrated and
dated with a particular certainty.
C.A. WEBER has already observed similar movements of the gyttja in North
German marshy lakes. I want to point here with emphasis to the connection between
the formation of quaking swards and the presence of an abundant and mobile
gyttja, which circumstance very probably holds true not only for the Lunz Ober-
see, but for most of the enumerated marshy lakes. Namely, in said cases (perhaps
• with the exception of the artificial Arniberg Lake) it is not a question of
oligotrophic or dystrophic water bodies, but of more or less mesotrophic to
eutrophic marshy lakes with a marked formation of fine-detrital gyttja, corresp-
onding essentially to the "forest-humus and herb-humus" lakes, also the "humus-
mud lakes," as described by KOPPE & UTERMUHL; in contrast thereto, quagmire for-
mation is much rarer and occurs scarcely ever to a similar degree in, for ex -
ample, the oligotrophic Lobelia and Isoetes lakes. This fact of the marshy
quaking bogs being bound to a high plankton and mud production is comprehensible
only, when the formation of the swaying carpets is essentially simultaneous and
not succedaneous.
I also know very similar phenomena from a few interglacial bore profiles,
e. g., that of Wildhaus in the Toggenburg, described by me in 1918 in con- • junction with Arnold HEIM. 79 (369)
Regarding more distant regions, we may just only mention a few strati-
graphically investigated examples from Sweden and Russia. The formation of quak-
ing bogs, as described by SANDEGREN from the southern shore of the Hornborga (370)
Lake, has begun therein only subsequent to the artificial lowering of the sur-
face level during the 70-ies of the past century; it corresponds entirely to
the processes that occurred subsequent to the surface lowering of the Feder
Lake resorted to in the same century. Due to the climatically conditioned level-
lowering during the Subboreal, rapid deltaic formations also took place at the
Hornborga Lake, but thereafter they were interrupted for a long time. Like the
Feder Lake, the Hornborga Lake possesses an abundant bird life and a eutrophic
plankton gyttja. • As early as in 1909, L. VON POST described a Subboreal formation of Sphagnum quaking mats directly upon detrital gyttja from the Uja marsh
near Ngrke; since that time this "Subboreal type of delta formation" has also
been found in other Swedish regions.
As to Russian boggy lakes, those of Kossino near Moscow have been inve-
stigated most thoroughly by KUDEJASCHOW. They too are mesotrophic humus-mud
lakes. The transverse profile laid through the Heiliger See [Holy Lake] shows
very clearly a Subboreal quaking-bog formation, sloping steeply towards the
lake and likewise revealing traces of erosion; thus it appears as completely
analogous to the Lunz Obersee and the Swedish Uja Marsh. Apparently, similar
conditions like at the Obersee prevail also, for instance, at the Waldai Lake,
investigated by LASTOTSCHKIN and others; but thus far that lake has not been
investigated stratigraphically. • In one of the largest Lithuanian marshes, that of Schuwinta, a lake 80 • (370) exists, hemmed in by huge quaking bogs; in 1926 I was able to determine that
it is also mesotrophic and develops an abundant gyttja.
The dystrophic raised-bog water bodies display an entirely different de-
portment; thus the bog-pools of the Baltic marshes, where floating covers of
Sphagnum cuspidatum, Cophalozia fluitans and Drepanocladus fluitans may well be
formed, but nowhere develop into quaking bogs of a more considerable size.
These examples may suffice to show that the simultaneous formation of - quaking bogs, mentioned both by FRUH and by POTONIÉ as a rare exception, is in
no way infrequent, but absolutely the rule, at least in the mesotrophic humus-
mud lakes. I do not intend to say with this assertion that the succedaneous quag-
mire formation does not occur at all. Except for the just mentioned dystrophic • domed-bog water bodies, they may also be found in eutrophic, reed-belt fringed water bodies, but this fact is still in need of a stratigraphic confirmation.
Incidentally, the designations ?simultaneous' and 'succedaneous' should better (371)
be avoided, since the 'simultaneous? build-up of the quaking sward does not
either proceed abruptly, but may develop by stages.
It could be regarded as a striking fact that the most intensive bog for-
mations at the Untersee and Obersee fall precisely into the Subboreal; but in
a climate with exceptionally abundant precipitations (today 1700 min yearly at
the Untersee, considerably more at the Obersee), this is not to be wondered at.
The same condition seems to likewise prevail in many other Alpine marshes.
At both Lunz Lakes,a Subatlantic erosion follows
upon the Subboreal marsh formations; due to the prolonged floods of 1926, yet
promnted at the Obersee by the artificial damming-up, this erosion had particu- • larly drastic effects (see PLATES II and III ). Not only lumps of the 81 • (371) quaking bogs were torn off and drifted away in likeness to WALDVOGEL's descrip-
tion of the Lützel Lake, but even parts of the Caricetum peat were carried off
within the inundation belt. Merely in some places Carex goodenowii and inflata
could withstand these attacks and, in the process, they assumed in many cases
similar shapes as Carex elata stricta = hudsoni) of theZsombék Marshes, or
like the C. juncella of the lake shores in Lapland ( PLATE II ). LUNDQVIST has
shown that erosive phenomena play a great role in the Zsombék Marshes and even
that the characteristic growing shape of the above C. juncella ("declivity
cleft" in FRUIT & SCHRUTER) can be interpreted as an outright adaptation to period-
ical flood erosions; he has demonstrated this in particular for lestermyren
[Mgster Marshl on Gotland. According to him (1919, p. 170), "the Carex stricta • association is the most capable of resistance to erosion and is even encour- aged by the latter."
g) The growth of bogs and bog eruptions
Now, erosive phenomena are in no way restricted to flat and transitional
bogs. It has been shown particularly by OSVALD that the erosion of raised bogs
increases rapidly from the continental towards the oceanic bogs; it is nearly
entirely lacking in the continental silvan raised bogs and is strongest in those
that are no longer domed at all, namely the "terrain-covering" (OSVALD 1925) or
"soligenous" (VON POST 1926) marshes of the Atlantic coastal areas. The bog erup-
tions, long since known from the British Isles, synoptically dealt with by
KLINGE 1891 and by FleH 1897, represent merely a special group of these Atlan-
tic erosive phenomena. Flei describes 25 bog-bursts from Ireland, two from Eng- • land, one each from Scotland, Oldenburg, the Island of Dag, plus two from the 82 • (372) Falkland Islands. Near Riga and Reval I could myself observe that the steep
peripheral declivities of the raised bogs at the Baltic eastern coast display
very marked erosive phenomena. C.A. WEBER (1924) describes a second case of a
bog eruption from northwestern Germany; for us it is of a particular importance
because it is the first one to be precisely investigated stratigraphically and,
moreover, it is a fossil bog-burst: in the Subatlantic period it has filled up
the megalithic tomb of Hammah, just subsequent to its having served for a later
burial during the iron age.
Fell knows only one report from the Alpine area that concerns the quaking
bogs of the Zellertal in Upper Bavaria; it is by RATZEL (Jahrbuch des Deutsch-
OsteereiŒhl‘enAlpenvereins [Yearbook of the Germano-Austrian Alpine Assoc.] 1886, • p. 411): there, subsequent to a considerable soaking, "at the occasion of an ac- cidental injury, simply by piercing the grassy turf covering the peat with the
alpenstock, that peat is riven apart and causes the water to squirt up into a
great height."(Similar phenomena may also be observed in the not as yet erupted
bogs of the Posterior Rotmoos). According to FRUH, bog eruptions represent "soil
masses in a movement of sliding, hence rather 'slipping' than eruptions," and
they are bound to occur in areas of a strongly oceanic climate. In his opinion,
bursts in the Lower Alps are kept in check foremost by the "Cyperaceae and Grami-
neae that interlace the whole mass together vertically," and also due to the
fact that most bogs have been developed in troughs.
As was already mentioned, several circumstances participate in bringing
about the eruptions in the Lunz Rotmoos: apart from the great humidity and the in a somewhat inclined position emplacement of the Rotmoos/on top of a marked karst-limestone topography, caulked-
up only in places byeacial clay, there is, furthermore, the insignificant 83 • (372) consolidation of the marshy cover (lack of Calluna and Trichophorum caespito-
sum, scarcity of Eriophorum vaginatum); finally and in particular the damage
caused by the large game that wallows here.
But even the nonerupted bogs in the string of the Rotmoos quagmires are
all of them dead; this is already proved by the abundant presence of Molinia 1 and the absence of normal generative complexes *) . Considering the great humi-
dity (the yearly total of precipitations may amount to far more than 2 m
according to measurements obtained up to now at the Obersee Hut), this might
seem rather striking, but it becomes comprehensible when we contemplate the growth
of Alpine bogs in general.
Namely, it is revealed that by far the greatest number of Alpine (373)
raised bogs are dead, or at least, are no longer noticeably growing. It would
• seem that SCHREIBER was the first author to fact. While, however, point to this
he ascribes the forest growth in most of the Lower Alpine bogs to the dryness
of our modern climate - in many cases this holds true - one must, in contrast,
hold the too considerable humidity and too low temperature responsible for the
fact that, in bogs, erosion predominates over growth. FIRBAS 1926 has given a
more detailed description of the erosive phenomena in the High Alpine bogs of
the Vorarlberg; ; he points out quite correctly that the Alpine bogs above the
present forest limit, covered with Trichophoretum caespitosi and Nardetum, are
dead throughout and in a state of erosion. All of them have been formed at a
period when they were positioned in the spruce and fir stage, hence a warmer
time interval than the present one. 1 *) I prefer this expression to the somewhat ambiguous "regenerative complex," commonly used in Sweden. - Compare, by the way, p. 387, at the bottom; • translation p. 102. 84
(373 )
Now, the Rotmoos of Lunz lies not only below the forest limit but even
below the beech limit; none the less it seems situated already above the stage
of optimum marshy growth. The most luscious Sphagneta of the area are found at
an altitude of 600 - 1000 m above sea level, like in the major part of the nor-
thern Alps and the Jura in general; in the Central Alps they lie at altitudes
of about 1000 - 1500 m, which is the zone of maximum air humidity and nebulosi-
ty. Thus the 'Rotmoos, 1 at an altitude of mere 680 m at Weichselboden (near the
Hochschwab, 15 km SSE of the Lunz Rotmoos) is still engaged in the most vi-
gorous growth; it possesses typical generative, forest-hollow and bog-pool com-
plexes, quite similar to those of the Baltic marshes, whereas the Lunz Rotmoos,
at an altitude of 1124 m, does no longer seem to offer optimum conditions for • a bog increment. (In this connection one has to differentiate between bog growth and growth of the individual Sphagna; several species of the latter climb in
the Central Alps as far as beyond the tree limit).
Similar phenomena can be detected all through the Alps. I have visited
a great number of marshes in Lower Austria, the Steiermark and South Tyrol, up
into Western Switzerland; thereafter all around the Baltic Sea, and I can report
on the result that not only the Alpine bogs above the forest limit, but also
those Subalpine bogs situated in the knee-wood region (dwarf mountain-fir) or
larch/Pinus cembra stage are, with quite rare exceptions,dead and ina
state of erosion. Wherever Subalpine bogs still grow at present,
thus at the Dürrneck Lake in the Lungau, at the Lake of Staz (Stazersee) in
Upper Engadine and at Lac de Champex in the Wallis, this is caused much rather (374)
by edaphic and locally climatic factors than by regionally climatic conditions, • But the factor that restrains the growth of Alpine bogs is not - if 85 (374)
exceptions are disregarded - a too low, but too high a humidity, and the eros-
ion one observes nearly everywhere is brought about by said humidity. Also,
I already know quiteanumber of localities with true phenomena ofoutflo w.
I might remark at once that the latter display the closest interrelationship
with the solifluction (cf., for instance, B. KREBS 1925), which,
as is known, is not nearly as widespread in the Alps as in Northern Europe,
even though it is in no way rare. Therefore I do not hesitate to speak at bog
eruptions of "creeping-soil terrasses."
Thus far I have observed the most beautiful outflow phenomena of this
kind at the Lasaberg [Lasa Mountaini near the Salzburg/Steiermark boundary;
there, a raised bog,lying at the forest limit and an altitude of about 1900 m, • had erupted and caused the formation of a splendid complex of stringed-up marsh-forest hollows parallel to the declivity curves of the bog and bearing
a very northern character. BREIDLER already had gathered here Sphagnum lind-
bergii, so frequently found in the northern marsh-forest hollows and so ex-
tremely rare in the Alps. I have seen a similar occurrence at the Mdele above
Dornbirn in the Vorarlberg.
Somewhat less impressive are the terraces of creeping wet soil, grown
over with Trichophorum caespitosum (among other species, together with the
northern Thalicum alpinum) at the Seiseralp in the Dolomites, plus similar oc-
currences in the Engadine, Avers, the northern Tessin and the Wallis. Erup-
tions resembling those of the Rotmoos and at the Lasaberg are reported to me
from the Latten mountain chain (H. PAUL) and from the Bernese Oberland(W.HUHN).
The erosive phenomena observed by FIRBAS on the Bieler Hele [Suintait of Biel] in the Vorarlberg • /belong also in this group. According to facts established both by him and myself, 86 • (374) it is very likely that by far the majority of the Alpine bogs have grown within
the limits of the interglacial interval and especially during the Subboreal
fir/spruce forest stage.
But this is not all: the mentioned happenings are not confined to the
Alps. OSTER, RUDOLPH AND FIRBAS have observed similar phenomena at the bogs of
the Riesengebirgskamm [crest of the Riesengebirgel, and it seems that exactly
the same is valid for the Subarctic and Arctic marshy areas. As early as in
1867 GEIKIE has explained the Scotch landscapes of peat mounds as caused by
water erosion, and KIHLMAN too ascribes the origin of the Lapland peat-mounds (375)
(in Russion 'bugort, in Laplandish tpalsat') to the erosion by the permafrost
ground. Near Abisko in Torne-Leppmark I have seen myself that the pals bogs are
dead and in the process of considerable erosion.
• Likewise, the Atlantic Rhacomitrium lanuginosum marshes, widely distri-
buted at the Norwegian West Coast, on the British Isles and on the Farel.ers, are
for a great part fossil formations, rather dominated by erosion than yet growing.
I have also seen myself that the nowadays predominant Rhacomitrium lanuginosum
on, for example, the bogs of And er in Vesteraalen (cf. OSVALD 1925) constitutes
just merely the uppermost peat layers of said bogs. The Atlantic Molinia, Tricho-
phorum and Nardus bogs are just as dead as the Alpine ones. Cf. in this con-
nection ERDTMAN 1927 and, furthermore, AUER 1927 (Supplement p. 387).
It would take us too far afield to give detailed descriptions of all
the said effects caused by water and wind erosion, by regelation and solifluc-
tion, and to prove them by quoting the very extensive Russian,Fennoscandian
and British literatures plus my own observations. Since, however, these phena- • mena, so significant for the entire developmental history of the vegetation, 87 (375)
have thus far aroused too scant an attention not only in the Alpine but also
in the Scandinavian descriptions of plant life, I wish to point to their ex-
tensive regional occurrence with great emphasis in order to incite other wor-
kers,so they may undertake more precise investigations on the subject.
Accordingly, we arrive at the principal result, namely: the raised bogs
cannot continue an unlimited growth, when precipitations are increasing, while
temperatures decrease, but that, subsequent to a maximum reached already in the
lower coniferous-forest stage, their increment diminishes again and soon is no
longer able to keep in step with the erosion. All of the more massive peat de-
posits above todayls Alpine and Arctic forest line are in their greatest part
fossil formations.
• h) On the silvan and climatic history of the Eastern Alps
The expositions that still follow here are continuations as well as
supplements to the descriptions by FIRBAS; in most of the questions I am in
full agreement with him.
Up to now, foremost the silvan and climatic histories of the late glacial
and the oldest post-glacial are insufficiently known, not only in the Alps but
also in northern and eastern Europe. My expositions of 1923 (GAMS & NORDHAGEN) (376)
concerning them are now obsolete in many points. I have said on several oc-
casions - (a few critics like BAYER have overlooked it) - that the view long
since defended by PENCK & BRUCKNER, RUDOLPH & FIRBAS, namely that both the
Gschnitz and the Daun stages are Preboreal, is correct. But FIRBAS has not suc-
ceeded thus far to ascertain incontestable stadial and interstadial fossil-bear- • ing deposits, while believing that such a proof can certainly become possible 88 (376)
(1926, p. 570); I trust, however, to have provided this proof in my fore-
going explanations.
In this context, the result of the Lunz bore-profiles is as follows:
from the Second Wuerm maximum to the Gschnitz stage a high-Alpine or Arctic
climate was dominant uninterruptedly; it did no longer permit an unbroken tree
growth even on the nunatacs projecting from the glaciers. Since BERTSCH & STARK
have shown that, subsequent to the Wuerm maximum, Pinus montana had been the
prevalent tree species for a long time in the by far warmer area of Lake Con- out stance and was crowded/therefrom but slowly by the silvan fir, it is easily
comprehensible that the region of the Lunz Lakes was at that time already situ-
ated in the Alpine stage. The isolated but all of them well-preserved pollen
grains of Pinus and Salix I found in the oldest deposits of the Untersee might
• have originated quite well from individual shrubs upon the nunatacs or from
the extra-moraine area.
Despite the fact that during the Bühl/Gschnitz interstadial the glaciers
in the Lunz area had retreated to a height beyond today's Gschnitz moraines,
this period has not either left behind any other organogenic formations but the
iron-sulphide clay of the Untersee (p. 310 and Figs. 2 and 3 ). This seems
to me most easily imaginable under the assumption of a supremely cold continen-
tal climate, the same as has been regarded as prevailing in the case of the
faunas of the older Magdalenian.
The Gschnitz/Daun interstadial following thereafter must already have
been considerably milder. It is likely that at that time open woods of silvan
firs and birches were growing around the Untersee, soon enough joined by immi- • grating hazel as well as also spruce. Even the hazel pollen found by BERTSCH 89 (376)
in the Subarctic moss-layer of the Schussenquelle [spring of the Schussen River]
and seemingly belonging to the late Magdalenian might be of an equivalent age.
The hazel pollen discovered in the interstadial of the Rotmoos may well have (377)
been blown upward from lower regions; in contrast, the spruce had reached at
least the Obersee, where its pollen amounts to 15%. Consequently, the upper
spruce limit has been lying during the last interstadial at most 500 m below
the one of today which averages from 1550 to 1600 m.
Herelwish to especially stress the occurrence of alder pol len
in the interstadial of the Rotmoos; on account of its inconsiderable amount (2%)
it may possibly also originate from quite a distance away, while none the less
proving that an alder (probably Alnus viridis) was already growing at that time
in the area. Namely, FIRBAS (1926, p. 582) particularly emphasizes the absence
• of positive alder remains in the late glacial deposits of the northeastern and
the Lower Alps he has investigated himself, jointly with BERTSCH & STARK. Even
if FIRBAS's doubts concerning SCHMIDLE's report on alder roots in the varved
clays of Lake Constance may be justified, I can nevertheless not quite agree with
his conclusion that the Alpine alder appeared only later in our regions due to
climatic conditions.
I am able to adduce on this point yet another find, for which I am in-
debted to Privy Councillor PENCK.
I received from him samples ofawashed-in clay from the Karwen-
del Val ley in the Tyrol, which, according to PENCK, had been deposited
immediately subsequent to the formation of the Gschnitz moraines, hence it ori-
ginates from the same interstadial. Except for six species of land and morass • snails, (Hyalina nitens MICH., Vitrina elongata DRAP., Patula ruderata STUDER, 90 (377)
Carychium minimum MULL., Cochlicopa lubrica MULL. and Limnaea truncatula MULL.),
I found therein a forest-moss (Drepanocladus uncinatus [HEDW.1 WARNST.), leaf
remains of grasses of one Potentilla and one Vaccinium (probably the bilberry
[myrtillusl), spruce needles and the catkin rachis of an alder which, in its
turn, also confirms the presence of Alnus in this interstadial spruce/fir stage.
It is possible that, in those times, the alder had advanced from the Southern
Alps only just to the upper Inn Valley and Ybbs Valley, but not to the true
Alpine border, in likeness to so many southern immigrants that, even in later
times, did not spread further.
The question which beds of the interstadial formations, as described
from the area of the Baltic Sea (Alleri;d, southern Scandinavia, Masuria, out- • skirts of St. Petersburg, etc.), most of which have not as yet been ranged be- tween definite moraine echelons, would correspond to one another and the Alpine
strata, has not been fully investigated thus far; also, the partly interstadial
and partly likewise very algae-abundant "glacial clays" of the Lower Alps (cf. (378)
GAMS & NORDHAGEN, BERTSCH & STARK) cannot as yet be correlated in each case. It
is remarkable that many of the algae found in the Lunz interstadial seem to
have disappeared ever since, whereas, in contrast, others as well as also the
planktonic crayfish Bosmina coregoni in the Untersee, Daphnia longispina in the
Obersee, the chrysopid Sialis in the Rotmoos plus other organisms have uninter-
ruptedly existed since the interstadial.
It becomes comprehensible that, by the Daun advance, the spruce has been
driven out from the Obersee but not from the Untersee, if, by agreeing with
PENCK & BRUCKNER, one assumes for that time a depression of the [climaticl bound- • aries by around 300 - 400 m (in the Gschnitz stage by 600 m) below today's limits.
Height of Meteorlog. Stations above sea level 91 le der Stationen• über dem Mee ■ \ 20 d 0 (378) e .1 1 "mforest limit •o W / , t , 1800 P /5 ee hc■ f4e. e- cb , / o. t,2 e, Inn gc f •La cite hç f ci'r 11Neuhaus ouha us ' 'I I ",à;t •GHaam' in' ._„> o:c-. ---i --i1 1600 o u) . u-,.... 1 -,.> IFi chi t engebiet*.engebiet* se00 w ô L--. .i. 1 I ï I Fi ch t 0.0 • ■•-i 44 —.'CS0 . i •Josefsberg . /i (0 4-J . .._.__Ï L9 i • t 1 r.r. Itolio 1 I Iensto enst0 in i i 1400 P c0 —' ; ' cl) 4J -•-', '5 • WiWi dal dipe pe 5 I, •Galm We Ccrc hhsel se 1 bbatIc_ pz1 1300 › ' ,I '''r'-= '''' CO P-1 MI .g, .,-1 so . 1 \ 1 2o0 ›, 0 —..«, / ,it'a — • Gu sswerk • Bigire ra 1pae. ..., .--„ ro..„ - • CO Wo.idiketan. I • LInazel.- .7f.11 I P 'Lîr=- .711 mlarch area •71) rbrhell. 1"=7:-..,.... ›-1 100 400 500. WO 700 800 goo 1000 _ *=Eichenmischwaldgebiet = oak/mixed forest area; **=Buchengebiet = beech area; ***=Fichtengebiet = spruce area; all other names = Meteorolog. Stations
F i g . 12 . Hyohypsogram of the Ybbs-, Erlaf- and Salza- [river] region.
During the Daun stage, the Obersee was situated in the knee-wood phase, the
Untersee in the fir/larch/spruce phase. It would be most interesting to ascer-
tain the dispersional history in the Alps of the larch with a greater pre-
cision. Up to now this has not been achieved because larch pollen is so diffi-
cult to diagnose; in like manner I have not, up to now, investigated the sepa-
ration of the Pinus silvestris and Pinus montana pollen by variation stati-
stics (cf. STARK 1927).
In order to clearly explain the significance of the Preboreal and warmth- modifications interval forest/, I must intercalate a few words about the present-day altitu-
dinal gradations. In the Ybbs Valley, like most anywhere, the oceanic character
of the climate decreases very rapidly inward towards the Alps, which is illu-
strated best of all in the above diagram of precipitations (hyohypsogram, cf. (379)
GAMS 1923); it also evidences how closely the silvan stages are bounded by de-
finite climatic conditions. Unfortunately, up to now we possess not more than • 15 years of observations from our more restricted area of investigation; 92 (379)
according thereto we can compute for the Untersee (Seehof Station) an average
amount of about 1700 mm of precipitations, for the Obersee about 2250 HMI.
Now, the normal altitudinal gradations, both in this our area and in
other mountainous regions as well, suffer all kinds of complication s:
firstly, at the transition from the oceanic climate of the Alpine periphery -
( the tinsubrian climateqthat of northern Italyi), where the beech mounts as
high as to the forest limit or the knee-wood area - to the median spruce climate,
it may happen that the peaks are considerably more 'oceanic' than the valleys,
so that already for this reason - as shown in the diagram - an upper beech phase
may develop above the spruce phase. This is indeed a fact at the Scheibling-
stein and the erenleitenkogel, where the beech, like in Insubria, climbs up to • 1530 m and even into the dwarf mountain-fir area. Secondly, a reversal of the normal altitudinal stages is brought about
by an inversion of the temperature, which is very nicely observable just in
the Seebach Valley, as well as in the basin of the Obersee as that of the Unter-
see. On several of the Obersee islands and on the Rotmoos grows a lot of knee-
pine, which will not be free from snow earlier than the actual knee-fir stage.
Above the knee-pine there is a spruce belt, still higher a beech belt, on top
of which we have another spruce belt, and only thereafter follows the knee-fir
belt proper.
In the third place, a similar inversion is also simulated by edaphic
conditions in that instead of the "climatic climax forest" - due to the ad-
verse character of the soil - appears a "subclimax" (in the sense of America),
which actually belongs to other stages of vegetation. Upon the meagre soils of • the principal Dolomite parts,spruce, pine and beech have become acclimated only 93 • (379) in a very restricted way, so that less demanding conifers are found here, where-
as, in other places, the latter have long since been crowded out by the above-
named tree species. These unassuming conifers are found especially on the steep
declivities, while, on the lower southern slopes, we have thin fir forests
with Corylus, Amelanchier, Erica and very peculiar Molinieta; on the northern
slopes woods of larch & spruce and in the ravines oftentimes knee-firs with
Erica, Rhododendron, Dryas and Carex-firma associations, as are encountered other-
wise not before the Subalpine stage of stunted dwarf mountain-fir and further
upward. I have stated in the Bulletin de la Murithienne (1927) that these cases (380)
are perfectly analogous to what K. TROLL explains as lowland-terrasses heaths
in his work of 1926.
In the fourth place, it is man himself and the livestock and game he
• protects who very considerably displace the forest boundaries.
All of these complications observable nowadays and partly already des-
cribed by KERNER, NEVOLE and others, even though not sufficiently explained, must
also reflect upon the developmental history of the forests, which, in this pa-
per, cannot be sketched but very briefly. A detailed, cartographically supple-
mented description of the entire vegetation will follow later on.
The interglacial-interval deelcpment is absolutely analogous to what
has been ascertained in other places of the Eastern Alps and its foreland.
C f • FIRBAS, PAUL & RUOFF; also my report in the Zeitschrift für Gletscher-
kunde [Review of Glaciology]). One has do differentiate:
A fir period, the last Boreal part of which may be designated as
fir/hazel time. To ascribe to this period a particular continental climate is • indeed unnecessary because firs and larches still thrive today in the oceanic 94 • (380) climate of Lunz and Gaming, once they find adequate edaphic conditions, namely
such that exclude a competition.
A spruce/fir period, where, apart from the hazel, the species of the
oak/mixed-forest likewise occur (in our area they are predominantly linden and
elm;)up to now, regrettably, I was unable to ascertain anything in regard to the
former dispersion of Acer platanoides, Sorbus aria, Evonymus latifolius, Ilex,
etc., previously more markedly represented than today; and finally - probably
from the beginning of the bronze age - the actual beech/fir period.
Here I may just call attention to some local particularities and di-
vergences from a development as ascertained regularly in other areas.
Fir and beech appear relatively very early in the Boreal, prior to the • hazel maximum and shortly subsequent to the species of the oak/mixed-forest; this fact is easily explainable by immigrations from the southeastern Alps. The
early and vigorous spreading of these species will have been facilitated by the
relatively high oceanic character of the surrounding mountains, whereas in the
valleys, especially on the principal Dolomite, the conifers of the preceding
fir period could, in many cases, hold their own. The fir forests of those
places with their juniper and hazel undergrowth can be regarded as outright
relicts from the fir/hazel time and the lower knee-fir region with its Subal-
pine flora as a remainder of the Subarctic knee-wood period, both of them (381)
brouglit about by local conditions of soil and climate.
It would seem that, in greater quantities, the fir will always have co-
lonized the foggiest stations, which would explain the great variety in its
quantitative occurrences in deposits that are probably synchronous. And in • the littoral lacustrine deposits we must, moreover, reckon with local in-washes 95 (381)
of spruce and fir pollen, so that, here, the deciduous trees are most like-
ly under-represented in the pollen diagrams.
The elevation of the forest limit during the interstadial interval, as
ascertained by FIRBAS for the Tauern Mountains and the Vorarlberg, cannot be
proved directly in the beddings of the Lunz area because no stratigraphically
utilizable bore-profiles can be found above today's forest limit.
Nowadays, the peak of the Dürrenstein projects about 50 m above the knee-
fir stage. The possibility that this peak might have been artificially cleared
of forest growth is contradicted by the fact that spruce and knee-wood suffer
extremely under snow pressure and wind grinding at their highest growth limits,
so that, there, appear purely Alpine plant associations like Polytricheta sex-
angularis. If, in the well-documented opinion of F1RBAS one has to reckon with
• an interglacial-interval elevation of the forest limit by at least 300 m, then
the 1877 m high Dürrenstin peak and the 1892 m high Oetscher peak have also
been lying within the spruce stage. And actually, upon the Dürrenstein peak, I
was able to still find strongly eroded remains of forest humus, containing
dwarf-pine wood. Today, the normal spruce limit is already at 1550 - 1600 m,
and 1 have seen the highest crippled spruce at around 1700 m on the southern
slope of the Dürrenstein. This former afforestation of the peaks explains their
relative poverty in Alpine plants, most of which still grow at the named relict
stations in the valleys, from where a renewed colonization could have taken
place. SERNANDER has already presumed similar conditions for the North Swed-
ish "IdejNllen" [secondary mountain peaksl.
The more considerable representation of the thermophilic deciduous trees • like hazel, elm and linden in the Boreal and Atlantic parts of the Obersee and 96 • (381) Rotmoos bore-profiles is another indication testifying in favour of an eleva-
tion of the forest limits. The 'stalked or suimuer oak! [Quercus pedunculata],
of which the last outposts are found today near the village of Lunz and the
Langau at an altitude of about 600 to 650 m, was scarcely ever of a more numer-
ous representation, but hazel and linden were ( as also the !pointed maple!
[Acer platanoidesi. Today, both of the latter stop already at the "Gamsstall" (382)
[Chamois shed] below the Obersee. During the interglacial interval both of them
were most probably growing at the /Buxbartmauer' [Goatsbeard Wall] above the
Rotmos and at the TJEgermauer! [Huntsmen Walli above the Obersee, where even
today isolated ash and montane elms are present.
The alder stands (Alnus incana) too around the Lunz Untersee go as far
back as into the Boreal. With their Brachypodieta silvatici they form the natural
• station for the bulbous plants Leucojum vernum and Narcissus radiiflorus, so
frequent today in the lush Alpine mountain meadows around the Untersee. Perhaps
it is from the latter that originates the pollen of an Iridacea, found in Ho-
rizon V (hazel period). The narcisses as well as Primula vulgaris (.= acaulis)
Daphne laureola, Evonymus latifolius and Ilex aquifolium , which reach the
Grubberg [Grub Mountaini and the Untersee only as last outposts, belong to the
Subatlantic or Western Mediterrean floral element, having attained - all of
them - their widest dispersion during the Atlantic part of the interglacial
interval. Perhaps even the rather numerous bastards of thermophilic plants
around the Untersee (for instance from the genera Crataegus and Rubus) are
also just relicts of that interglacial interval.
Naturally, fluctuations in the amount of rainfalls are scarcely noti- • ceable in the silvan aspect of an area rich in precipitations on the whole. 97 • (382)
In other localities too, the Subboreal for instance is mostly but feebly marked
in the pollen diagrams; and a cardinal mutation in the silvan aspect, namely
the vigorous and intolerant spreading of the beech, takes place regularly long
before the contact between the Subboreal and the Subatlantic.
But in contrast, both the Boreal and, in particular, the Subboreal
droughts express themselves rather distinctly in the fluctuations of the lacu-
strine surface levels. During the Boreal, delta formations occur in the fore-
lakes of the Rehberg (p. 322) and in the Anterior Rotmoos ; during the Sub-
boreal, both the Untersee (p. 314) and the Obersee (p. 329) must, on an aver-
age, have had lower low-water, or longer-lasting low-water periods than to-
day. At that time, the Obersee might have had no outlet as much as year after
year. During snow-melting, however, it too will certainly have had high-wa-
• ter times, which would have caused the bogs in their growing stages to be per-
iodically lifted up from their substrata, but the inundations of those periods
can searely have had the intensity and duration they display today.
The planned description proper of the vegetation will offer an occas- (383)
ion to enlarge upon the numerous and far-reaching modifications caused by man
in the course of the past century. Up to the completion of that work, there
will probably be sufficient metereological data from the new Meteorological
Station Seehof, so that, with their aid, it will be possible to numerically
characterize not only today's climate but also that of past periods.
0000000 • 98 (383)
LITERATURE
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;37, lhiue , J Obe• (len Einflu13 (lor miLlieren WindriehLung auf dus Verwiteliseq der Englas Bol, J (((b. 11, .1890. ;13. -- Elbooda 14, 1891 i(oppe, (I. J. 1(elumbe. Cher (lie 'û/1'( l, und subfossile Flora des Sand' Icatener àleores Rhin. lier, Deuts011. Ges, 44, 1926. u robs, ;,;,, liodenformun ill den 'pen. Definers Uttogr. Zeitsehr. 31, 1925. iCtul ejne u . 4V., Osnowye inomenLy isLorii Kossinskiell osjor. .111h 'biol. Station i(ossino 1, Moshad 192/I . • • 100 (385)
2. 11:aulrjase1iow, Z Ur Owsc.hich le der Seen. Verh. till. Ver. Limnol. 3,1927. 4.3 • :Kurz, À. Grundri13 ohm Algenflora des appenzellischen Mittel- und Vorder- lancles. Jahrb. St. Gall. Naturw. Ges. 58, 1922. 44, Lagerheim, Om lamningar af Rhizopoder, Ilelimier och Tiniinnider i Sveriges och FMlands lakustrina kvartâraflagringar. Geol. Füren. Fôrh. 23, 1901. 45. « Lastotschklu, D. A. u. a., Pribreshnyje soobschtschestwa Waldalskowo osera. Sapiski goss. hydrolog. Inst. 1, Leningrad 192G. Lenz, Fr., Gbironorniden und Seetypenlehro. Die NaLurwissenschaften 13, 1925. Ijungqvist, 3. 1.,.\regetationshilder fri'm iN11istermyr. Svensk Rot. Tldskr, ta,
48. LCSVYy, Ji., G. 'Laszlo 11, a., Die Geomorphologic des 11alalonseos und sciner Umgebung. Result. d, wiss. Md. d. lialalonsees, Wien 1915, 49, Idit1e1n5i1or, J., Nlannskripi. Ubor die Lunzer Dosmidinceenflora. 50. Lundqvist, U.; Utvecklingshistoriska insj5sLudier i Sydsvcrig,c. Svor. Geol. tinders. Arshok 18, 1925.. 51. thoden zur Unlersuchung der kliit.wieklungsgesehiehto der Soon, Abdor- haldens Mandl). d. bol, AybeiLsmethoden. Lie!. 173, 1925. 52. — Sj5arna Trainmen, Vaxjüsjiin och.Südra Bergundasjiin. Skrifter Siidra Fiskeriftiren. 1025. 53. Die Bodenablagerungen der Seell. Die Hinnengow;issor 2, Slut tgar1.1927 (konnte in Text Mat mehr hornet:sic -1We worden). ri 4, MIrhael, 1Z., Dio Vorglolsoherung dor Lassing•Alpon. Bor. V e r. Geogr. Univ. Wien 16, 1801. 55. Naumann, Einar, Undersi3kningku iivor rytoplankton och under don palagiska regionen fersiggimude gyttje-och dybildningar inom vissa syd- och tnellan- svenska urbergsvallen. K. Sv. Votensk.-Alcad. 'Mandl. 55, 1917, 55, Nov:Jr., J., Vegetatiimsverhnitnisse clos Oetseher- und Dürronsteingebieles in Niederüsterreich. Abh. Zoo'. hot, (les. Wien:3, 1905. 57. Nipkow„ Fr., Vorhinfige Mitteilungen iiher Untersuchungen des Schlamm- absaLzes im Hydrologie 1, 1920. 58. t) haï' dasVorhallen der Skelelto plunk Usehor Kieselalgon i I n gosollichinten Tiefenschlanun des Zurich- und 13aldeggersees. Ebenda 4, 1927. 50. blierg, V., H. Sieger, E. Svedmark u. O. À. Lindval1, Flottho linen i sjün lla- le.mgen. Geol. FOren, FOrli, 1(3, 1894. 00. Osvald, ii., Die Vegetation des Hochmoores Komosse. Sv, Vâxtsoc. }Tamil. 1, 1923. 61. Zur Vegetation der owanischen Hoc:moor° in Norwegen. Ehenda 7, 1925. 52, Die liochmoortypen Eu•opas. Sehrô1er'estsc1ur., Zürich 1925. 118. Paul, u. S. Ruoff., Pollenstatistische und stratigraphische i\foorunler- suchungen jill stidlichen Bayern, I, Bor. Hayer. But.. Ges. 19, 1927. 64. .l'Cl1C1C t., u, E. Brilehner, Die I\ lpen lin HiszeilalCor, Leipzig 1901- 1909. 65. von Post, L., Stratigraphische Studien 11 I >ii einige Torfmooro i I I Narke, Geol. F5ren. Feirh. 31, 1009. GG, -- (mil Ulnae u. liedo), Gotlands Geologi. Sver. Cool. tinders. Arsb. 331, 1025. 101, (386)
67. von Post, L. (lui L ( ranlund), Sùdra Sveriges Tory LiIlgangar. Ebenda 335, 1926. 1;8. -- Einige Aurgaben der regionalen Moodorsehung. Ebencla 337, 1926. 69. Potonié, IL, Die rezenten Kaustobiolithe 11. Die Humusbildungen, Abh. Pron 9. Geol. Land esanst. 1911, 70. Romani', E., Bodoni:uncle, 3. Ault, Perlin 1911. 71. Rudolph, IC, tilltersueliongen uher don Ait [b b0hinischer Moore 1, Abh. zool. bol. Des, 9, 1917, 72, u. F., Die Hoehmoore des Erzgebirges, lieih. Bol. Contralbl. 41, 192'1, 73. Pollenanaly Uccle UntorstiehlIng subalpiner Moore des If iesengebirges. lier. Deutsch, ties. 44, 1926. 74. liiister, P., Die subalpinen Moore des it ieseng,ebirgskannues. Der Kultur- Lech n ker, 1922. 75. Sandegren, 11., llornborgasjUn. Sver. Geol. Unders. Avh, 14, 1916. 76. ---- itagunchdrakiens postglaeiala utvecklingshistoria enlig,t den sub[ossila ' [brans vilinosbürd. Ebenda 12, 2, Ault 1924. • 77. Schierbeek, A., De studio der veeuen. K. Nederl. Aardr. Gen. 2 , S. 34, 1917. 78. - Fen on ander over drijftillen. Handel. 16. Nede.d. Niihau.- on Gel-lush. Gongres, 1917. 79. 8(111111(11e, lieitrage 7,111' alpinen Algon[lora. 1. Algen nus don ()daintier Alpen. Osten.. hot. Zeitsehr. 45-46, '1895-1896. 80. Sehreiber, H., Vergletscherung und Moorbildung in Salzburg mit Hinweiselt au!' dits Moorvorkommen und das naeheiszeilliche Klima in Europa. Verlag d. Deuischiist. Moorvor. Staab, .1911-1912, • Si. Skadowsky, S. N., (ber die al:Luella Healttion der Sulfwasserpecken und ihro biologische lledeulung. Verh. Vet., Dinmol, 3, 1926. 82. Staring, W. C.11., De veenen in Nederland, Verh, Comm, geol. kaart v. Netter!. 1, Haarlem .1853. 83. Stark, P,, Die Moore des badisehen 13odenseogebiels. Per. nat. Ces. Freiburg . 1925—'1927, 84. Ober die Zugelnirigkeit des Kieferpollens in den Versehiedenolf 'mitten der Bodunsceitioere Bor. Deutsch. lin!, (10ii, 45, 1927. 85. Staudneher, W., Die Verlandungsstudien dos oborschwahlelion Ft:don-woo. N. Jahrh, 1'. Mineral, 50, 1924. 86. Steinecke, Fr,, Die hoschallen Wurzelliitiler des Zehlaubruches, Sehr, Phys.- bkon. Ges, Ktinigsberg, 1915, — Die Algen des Zoldaubruches. Ebenda 1916. 88, -- Die notatorien und Gastrotrichen dos Zehlaubruehes, Ebenda 19'17. 89. --- Die Rotarienfauna von Oslpreuffen. Ebenda 1924. . . 90, -- Die Algen des 13eluia nana-Moors bei Non-Linum, Pot, Arehiy, 5, 1924 (S. 342). 91. -- Leitformen und Leillossilien des Zehlaubruches. Die Bedeutung der l'os- silen Mikroorganismen the Erkenntnis der Nekvozbnosen aines Moors. Rhonda 19, 1927. 92, Strihn, IC M., Norwegian mountain Algae. Ski'. Norsk° Vid.-Akad. Oslo, 1926. • 93. Suliatschow, W. Nr., Bolota Usw, 3. Anti., Leningrad 1926, - • 102 (387)
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SUPPLEMENT
To page 330 : The line profiles laid in October 1927 through the
Posterior Rotmoos have revealed that there, like at the Obersee, the Sphagnum
peat rests directly upon gyttja and continues likewise underneath the flat-bog
peat and the creek. Hence the high bogs, regarded initially as independent,
represent just only erosional remnants of Subboreal raised bogs that had oc-
cupied the entire breadth of the valley.
To page 375 : My opinion, as expressed in respect to the Arctic swamps,
is fully confirmed through AUER, V.: Investigations regarding the forest li-
mit and the peat soils in Lapland. - Comm. Inst. quaest. forest.Finl. 12, 1927.
0000000 let
OVER