Karl Krainer

Hydrology of Active Rock Glaciers: Examples from the Austrian Alps

Hydrological investigations of three active rock glaciers in the Austrian Alps (Reichenkar rock glacier in the western Stubai Alps, Kaiserberg rock glacier in the western Ötztal Alps, and Gößnitz rock glacier in the Schobergruppe) demonstrate that discharge is mainly controlled by the local weather conditions, the thermal properties of the debris layer, and the physical mechanisms that control the flow of meltwater through the rock glacier. Discharge of active rock glaciers is characterized by strong seasonal and diurnal variations. Water derived from snowmelt and summer thunderstorms is quickly released causing floods. Fair weather periods with intense melting of snow and ice cause pronounced diurnal variations in discharge. Water temperature of active rock glacier springs is constantly below 1°C during the whole melt season. Electrical conductivity of the water is low during high discharges due to high amounts of meltwater derived from snow/icemelt and/or precipitation, and high during cold weather periods and in autumn when discharge is very low and consists mainly of groundwater. The discharge pattern of active rock glaciers is similar to that of glaciers due to similar meltwater sources and flow paths. However, the average yearly mean specific discharge from active rock glaciers is significantly lower than that of glaciers.

Late Serpukhovian (Namurian A) microfacies and carbonate microfossils from the Carboniferous of Nötsch (Austria)

SummaryThe Carboniferous of Nötsch (Austria), divided into Erlachgraben, Badstub and Nötsch Formations, is composed of a thick sequence of dominantly siliciclastic deepsea sediments. Intercalated marly and silty limestones in the upper Erlachgraben Formation consist of bioclastic wackestones and algal wackestones/packstones which contain a diverse fossil assemblage of formainifers, algae and pseudo-algae. These microfossils are accurately described and documented, and three species of algae are established:Principia fluegeli n. sp.,Paraepimastopora noetschensis n. sp., andNanopora pseudofragilissima n. sp.Based on the occurrence of both important species of the foraminifers Lasiodiscoidea (Howchinia gibba andEolasiodiscus dilatatus), and also on the presence ofEndothyranopsis plana, of the lastEarlandia ex. gr.vulgaris and of the firstEostaffella exp gr.postmosquensis, the upper Erlachgraben Formation is dated as late Serpukhovian (goniatite biozone E 2 of the Namurian A; Arnsbergian stage, corresponding to the Zapaltyubinsky of the standard Russian sequence; foraminiferal biozones 18 or Cf 7 of Belgium, or Cf 16 of the Donbass).Compared to the Pyrenees and the Donbass region, the algal flora of the Carboniferous of Nötsch seems to be relatively endemic. Algae and foraminifers originally inhabited a shallow carbonate ramp and were transported and redeposited in a deep-water environment by gravity flows. The formainifers most probably migrated from the Donbass region along the shelf of a narrow seaway to Nötsch.

SMALLER FORAMINIFERS, CHARACTERISTIC ALGAE AND PSEUDO-ALGAE OF THE LATEST CARBONIFEROUS-EARLY PERMIAN RATTENDORF GROUP,CARNIC ALPS (AUSTRIA/ITALY)

Limestones of the latest Carboniferous-early Permian Rattendorf Group (Lower Pseudoschwagerina Limestone, Grenzland Formation and Upper Pseudoschwagerina Limestone) of the Carnic Alps (Austria/Italy) contain a rich and interesting assemblage of smaller foraminifers, algae and pseudo-algae. The foraminiferal assemblage of the Lower Pseudoschwagerina Limestone is identical to that of the Auernig Formation. The Grenzland Formation is characterized by the appearance of the genus Geinitzina and Pseudovermiporella, and the disappearance of Bradyinidae. The Upper Pseudoschwagerina Limestone contains the same species as the Grenzland Formation, but is characterized by the local appearance of Neoendothyra (?) and diverse species of Hemigordiidae and Nodosarioidea. The biostratigraphical value of diverse species of Hemigordius, iA renovidalinai sensu Baryshnikov = iNeohemigordiusi sensu Pinard & Mamet, Nodosinelloides , Protonodosaria and Geinitzina for the Asselian and early Sakmarian stages is briefly discussed. The systematical part contains some generic remarks on the Hemigordiidae and Nodosarioidea. Due to the porcelaneous wall, the microfossils Ellesmerellapermica (Pia) (= iGirvanellai subparallela Flugel & Flugel-Kahler) and Pseudovermiporella spp., which are generally interpreted as algae, are considered as attached miliolinid foraminifera. A new genus of problematical Chlorophyta, Homannisiphon, is established.

Late- and Post-Variscan Sediments of the Eastern and Southern Alps

In the Southern and Eastern Alps late- to post-Variscan sedimentation processes started during the Late Carboniferous (Late Moscovian/Cantabrian). The sediments of the Carboniferous sequence of Notsch and Veitsch, which are also briefly discussed, are interpreted as “synorogenic sediments”.

Flow velocities of active rock glaciers in the Austrian Alps

Abstract. High surface flow velocities of up to 3 m a–1 were measured near the front of three active rock glaciers in the western Stubai Alps (Rei‐chenkar) and Ötztal Alps (Kaiserberg and Ölgrube) in Tyrol (Austria) using differential GPS technology. Flow velocities have increased since about 1990. The highest velocities were recorded in 2003 and 2004, but showed a slight decrease in 2005. At the Reichenkar rock glacier, flow rates are constant throughout the year, indicating that meltwater has no significant influence on the flow mechanism. At Ölgrube rock glacier, flow velocities vary seasonally with considerably higher velocities during the melt season. Meltwater is likely to influence the flow of Ölgrube rock glacier as evident by several springs near the base of the steep front. Because the high surface velocities cannot be explained by internal deformation alone on Reichenkar rock glacier, we assume that horizontal deformation must also occur along a well defined shear zone within a water‐saturated, fine‐grained layer at the base of the frozen body. The increased surface flow velocities since about 1990 are probably caused by slightly increased ice temperature and greater amounts of meltwater discharge during the summer, a product of global warming.

Sedimentology, microfacies and stratigraphic distribution of foraminifers of the lower “Pseudoschwagerina” Limestone (Rattendorf Group, late carboniferous), carnic alps (Austria/Italy)

KurzfassungDer Untere „Pseudoschwagerinen“kalk (Rattendorfer Schichtgruppe) ist aus einer zyklischen Abfolge fossilführender, flachmariner Kalke mit geringmächtigen Einschaltungen klastischer Sedimente aufgebaut. Im Schulterkofel-Profil sind drei Zyklen ausgebildet. Die klastischen Einschaltungen an der Basis aller drei Zyklen entstanden während relativer Meeresspiegeltiefstände, während der nachfolgenden Transgression wurden gebankte fossilführende Kalke und massige Algenmounds abgelagert. Gebankte Kalke mit Kieselknauern und Mergelzwischenlagen werden als Sedimente gedeutet, die während relativer Meeresspiegelhochstände in Wassertiefen von einigen Zehnermetern abgelagert wurden. Innerhalb des Unteren „Pseudoschwagerinen“ kalkes treten in verschiedenen stratigraphischen Niveaus, insbesondere an der Basis und am Top von klastischen Einschaltungen, Kalkbänke auf, in denen Fusuliniden angereichert sind. Taphonomische Merkmale und die Zusammensetzung der Fusulinidenfaunen sprechen gegen eine Aufarbeitung, bzw. Transport durch Strömungen. Sie deuten vielmehr darauf hin, daß es sich um parauthochthone Vergesellschaftungen handelt, die während Perioden mit geringem Sedimenteintrag angereichert wurden. Biostratigraphisch wird der untere Teil des Unteren „Pseudoschwagerinen“ kalkes (Zyklus 1) mitRuzhen-zevites ferganensis ohne Vertreter der GattungDaixina (Bosbytauella) noch in diesokensis-Zone eingestuft. Der Großteil des Unteren „Pseudoschwagerinen“ kalkes (oberster Teil von Zyklus 1 bis Zyklus 3) wird in diebosbytauensis-robusta-Zone gestellt. Für die Karbon/Perm-Grenze kann aus biostratigraphischer Sicht nur ein Intervall zwischen dem obersten Anteil des Zyklus 3 (Schwagerina versabilis-Rugosofusulina arianica) und tektonisch isolierten Kalkbänken aus der darauffolgenden, überwiegend klastisch entwickelten Grenzland-Formation (Sphaeroschwagerina-Pseudoschwagerina = mittleres Assel) angegeben werden. In den Karnischen Alpen liegt die Karbon/Perm-Grenze somit unmittelbar unterhalb der Basis oder innerhalb der untersten, klastisch entwickelten Grenzland-Formation.AbstractThe Lower “Pseudoschwagerina” Limestone (Rattendorf Group) is a cyclic sequence composed of fossiliferous, shallow marine limestones and thin clastic beds. In the Schulterkofel section three depositional cycles are well developed. Clastic intervals at the base of all depositional cycles formed during relative sea-level lowstands, during transgression well bedded fossiliferous limestones and massive algal mounds were deposited. Bedded cherty limestones with marl intercalations are interpreted as deposits formed during relative sea-level highstands with water depths of some tens of meters. In the Lower “Pseudoschwagerina” Limestone (LPL) fusulinid rich limestone beds occur in different stratigraphic levels, particularly at the base and on top of clastic intervals. Taphonomic features and composition of fusulinid assemblages indicate that reworking and even redistribution of fusulinids play a subordinate role. They are considered as parauthochthonous assemblages, accumulated during periods of low sediment input. Based on fusulinid biostratigraphy, the lower part of the LPL (depositional sequence 1) is correlated with thesokensis Zone, because of the occurrence ofRuzhenzevites ferganensis without species of the genusDaixina (Bosbytauella). The main part of the LPL (uppermost part of depositional sequence 1 to sequence 3) belongs to thebosbytauensis-robusta Zone. For the Carboniferous/Permian (C/P) boundary only an interval can be estimated between the upper part of sequence 3 (Schwagerina versabilis-Rugosofusulina arianica) and tectonically isolated limestone beds of the overlying, predominantly clastic Grenzland Formation (Sphaeroschwagerina-Pseudoschwagerina = middle Asselian). In the Carnic Alps the C/P boundary lies therefore immediately below the base or within the lowermost clastic Grenzland Formation.

Anthracoporella mounds in the Late Carboniferous Auernig Group, Carnic Alps (Austria)

SummaryA heretofore undocumented example of skeletal mounds formed by the dasycladacean algaAnthracoporella spectabilis is described from mixed carbonate-clastic cycles (Auernig cyclothems) of the Late Carboniferous (Gzhelian) Auernig Group of the central Carnic Alps in southern Austria.The massive mound facies forms biostromal reef mounds that are up to several m thick and extend laterally over more than 100 m. The mound facies is developed in the middle of bedded limestones, which are up to 16 m thick. These limestones formed during relative sea-level highstands when clastic influx was near zero.The mound facies is characterized by well developed baffler and binder guilds and does not show any horizontal or vertical zonation. Within the massive mound faciesAnthracoporella is frequently found in growth position forming bafflestones and wackestones composed of abundantAnthracoporella skeletons which toppled in situ or drifted slightly.Anthracoporella grew in such profusion that it dominated the available sea bottom living space, forming ‘algal meadows’ which acted as efficient sediment producers and bafflers. BecauseAnthracoporella could not provide a substantial reef framework, and could not withstand high water turbulence, the biostromal skeletal mounds accumulated in shallow, quiet water below the active wave base in water depths less than 30 m.The massive mound facies is under- and overlain by, and laterally grades into bedded, fossiliferous limestones of the intermound facies, composed mainly of different types of wackestones and packstones. Individual beds containAnthracoporella andArchaeolithophyllum missouriense in growth position, forming “micromounds’.Two stages of mound formation are recognized: (1) the stabilization stage when bioclastic wackestones accumulated, and (2) the skeletal mound stage when the sea-bottom was colonized byAnthracoporella and other members of the baffler and binder guilds, formingAnthracoporella bafflestones and wackestones of the mound facies.A slight drop in sea-level led to the termination of the mound growth and accumulation of organic debris, particularly calcareous algae, fusulinids, crinoids and bryozoans, forming well bedded limestones, which overlie the mound facies

Funsulinid assemblages and facies of the Bombaso Fm. and basal meledis Fm. (Moscovian-Kasimovian) in the central Carnic Alps (Austria/Italy)

SummaryThe Bombaso Formation and basal Meledis Formation in the central Carnic Alps near Straniger Alm and Zollnersee (Austria/Italy) unconformably overlie the folded Variscan basement and consist of shallow marine clastic and carbonate sediments which are arranged to form two fining and deepening upward sequences. Particularly limestones and even breccias of the Bombaso Formation yielded a rich fusulinid fauna composed of 34 species which are attributed to the following zones:Quasifusulinoides quasifusulinoides-Protriticites ovatus; Protriticites pseudomontiparus, andMontiparus montiparus.Breccias of the Bombaso Formation west of Straniger Alm contain the oldest fusulinid fauna of the Carnic Alps, belonging to theQuasifusulinoides quasifusulinoides —Protriticites ovatus zone. The fauna is composed ofQuasifusulinoides quasifusulinoides, Q. fallax, Q. intermedius, Protriticites cf.ovoides, andPr. ovatus. This assemblage is most similar to that of the Peskovskaya Formation of the Myachkovian Horizon in the Moscow Basin indicating uppermost Moscovian age. Limestones from depositional sequence 1 at Zollnersee also contain fusulinids of the uppermost Moscovian which are characterized by a more diverse assemblage:Schubertella donetzica, Fusiella lancetiformis, Beedeina ulitinensis, B. consobrina, B. nytvica, B. siviniensis, Quasifusulinoides pakhrensis, Q. fallax, Q. kljasmicus, Q. quasifusulinoides, Fusulinella rara, andProtriticites ovatus. Limestones and calcareous sandstones-siltstones of the basal Meledis Formation of depositional sequence 2 near Zollnersee and at Cima Val di Puartis are characterized by fusulinids of theProtriticites pseudomontiparus zone (Protriticites globulus, Pr. pseudomontiparus, Pr. sphaericus, Pr. rotundatus, Pr. ovoides, Pr. lamellosus, andPraeobsoletes burkemensis) and byMontiparus paramontiparus zone (Praeobsoletes pauper, P. burkemensis, Obsoletes timanicus, O. obsoletes, Montiparus paramontiparus, M. umbonoplicatus, M. montiparus, M. likharevi, M. rhombiformis andM. priscus) indicating lower to middle Kasimovian age (Krevyakinskian and Khamovnicheskian Horizons of the Russian Platform).

SMALLER FORAMINIFERS OF THE UPPER CARBONIFEROUS AUERNIG GROUP, CARNIC ALPS (AUSTRIA/ITALY)

The micropaleontological components, particularly smaller foraminifers, from limestonesof theUpper Carboniferous Auernig Group (Carnic Alps, Austria/Italy) are described. Most of the taxa have been previously recorded from North America, Arctica and Russia (Urals, Donbass). The biostratigraphical value of Pseudovidalina , Nodosinelloides , Tezaquina and Vervilleina for the Oembourgian stage is recognized. The systematical part is principally devoted to generic discussion concerning Hemidiscus and Eolasiodiscus ; Palaeobigenerina , Deckerella , Cribrogenerina and Climacammina ; Ammovertella , Calcivertella and Calcitornella ; Spireitlina and Pseudopaleospiroplectammina ; Pseudovidalina and Raphconilia : Vervilleina and Tezaquina ; and Nodosinelloides , Protonodosaria and Nodosaria .

The schulterkofel section in the Carnic Alps, Austria: Implications for the carboniferous-permian boundary

SummaryThe upper part of the LowerPseudoschwagerina Limestone (Rattendorf Group), outcropping on the northwestern flank of Schulterkofel Mountain, Carnic Alps (Austria) is described with special emphasis on fusulinid microfossils and facies. This fusulinid-rich section offers an ideal opportunity for biostratigraphy in defining the Permo-Carboniferous boundary in this region.The LowerPseudoschwagerina Limestone is composed of shallow-marine limestones with intercalated thin siltstone and sandstone beds.Fusulinid limestones are represented by two types of wackestones, both containing large quantities of smaller foraminifers. Fusulinid grainstones are rare. Limestones rich in fusulinids were found only within the bedded limestone facies in beds both below and especially above siliciclastic intercalations. This may indicate that the best living conditions for fusulinids existed immediately before and especially after the climax of a regressive phase (sea-level lowstand). The fusulinid limestones were deposited within a protected, shallow-marine shelf environment with normal salinity.Pseudoschwagerinid fusulinids appear in the upper part of the LowerPseudoschwagerina Limestone, in samples SK 107d (undeterminable species) and SK 108, i.e. between 92 m and 93 m above the base of the section within a bedded limestone immediately above the uppermost clastic intercalation.The fusulinid fauna is represented by about 30 species belonging to only a few genera. Species ofTriticites andRugosofusulina dominate, whereas those ofDaixina, Rugosochusenella andPseudofusulina are rare. A characteristic feature of the fauna is the strong similarity with fusulinid faunas described from Russia as well as from Middle and East Asia. Some of the described fusulinids are new for the Carnic Alps.The first appearance ofPseudoschwagerina andOccidentoschwagerina (Occidentoschwagerina alpina Zone) in the upper part of the LowerPseudoschwagerina Limestone in the Schulterkofel section defines the position of the Carboniferous-Permian boundary.