Operculate cyclostome bryozoans (Eleidae) from the Bohemian Cretaceous

Eleidae (‘melicerititids’) are unusual cyclostome bryozoans possessing operculate zooids and mandibulate polymorphs (‘eleozooids’) resembling the avicularia of cheilostome bryozoans. Here we describe 13 eleid species from the Cenomanian-Turonian of the Bohemian Cretaceous basin in the Czech Republic. Three species of Meliceritites are new: Meliceritites kankensis, M. stillativa and M. upohlavyensis. Reptoforicula gen. nov. is introduced for free-walled eleids with multilamellar encrusting colonies, containing the type species Reptoforicula zbyslavensis sp. nov. and R. vodrazkai sp. nov. Type specimens of three species erroneously assigned to Eleidae are refigured and their true affinities discussed. This study underscores the value of eleozooids in distinguishing between otherwise closely similar eleid species. The Bohemian late Cenomanian-early Turonian eleid fauna is dominated by encrusting species, a pattern that is typical of nearshore localities and contrasts with offshore chalks where erect, vincularian species are more numerous.     

Systematics of Upper Cretaceous calloporid bryozoans with primitive spinose ovicells

The majority of fossil and Recent cheilostome bryozoans brood their larvae in ovicells. These double-walled, hood-like skeletal structures are thought to have arisen through modification of spines belonging to the zooid distal of the maternal zooid. Support for this hypothesis comes from the existence of ovicells constructed of multiple spines in a few Upper Cretaceous species belonging to two groups, microporids and cribrimorphs. Here we report the discovery of similar multispinose ovicells in a third group, calloporids, which are closely related to primitive cheilostomes that do not brood their larvae. The genus Distelopora Lang, 1915 from the Cenomanian ('Chalk Marl') of Cambridge is taken out of synonymy and shown to comprise the type species ( D. bipilata ) and two new species ( D. langi and D. spinifera ) of multiserial calloporids. Between 5 and 15 spine bases are arranged in a crescent on the gymnocyst of the zooid distal of each maternal (egg-producing) zooid in Distelopora . This indicates the presence of an ovicell formed by a cage of basally articulated spines. Similar ovicells represented by 18–19 spine bases occur in a uniserial calloporid from the German Campanian Allantopora krauseae Voigt and Schneemilch, 1986, which is made the type species of the new genus Unidistelopora . Another calloporid from the Cambridge Cenomanian has ovicells constructed by two claw-like, flattened, non-articulated and laterally juxtaposed spines. Described as Gilbertopora larwoodi gen. et sp. nov., this multiserial species provides a link between Distelopora and more typical cheilostome ovicells. The spines forming primitive ovicells provide a good example of exaptations, co-opted from their original function protecting the polypide of the distal zooid.     

Paleoecology of epizoans and borings on some Upper Cretaceous chalk oysters from the Gulf Coast

Analysis was made of a hard substrate fauna found on right valve interiors and exteriors of the epifaunal reclining oyster Pycnodonte mutabilis from the Maastrichtian (Navarroan) Saratoga Formation (southwestern Arkansas). Comparison of boring and encrustation patterns on both sides of valves indicates that a major portion of colonization on valve exteriors occurred while host oysters were alive. Paleoautecologic information derived from such valve exterior patterns includes evidence of rheotropic orientation by encrusting juvenile P. mutabilis and preferential location of Trypanites sp. borings in surficial shell grooves. Valve exteriors supported a hard substrate paleocommunity which had the following non-interactive progressive colonization sequence: (1) Trypanites sp. and P. mutabilis juveniles; (2) Entobia sp., serpulid worm tubes, and Bullopora sp.; and (3) cheilostome bryozoans. This sequence could have been caused by low seasonality and ranked success of colonizing encrusters and borers. Colonization of valve interiors generally differed from exteriors only in that many interiors were first colonized by the clionid sponge that created Entobia sp., which had already occupied the exterior, and which quickly bored through the valve to occupy the interior upon the host's death. □ Trace fossils, epizoans, borings, Gryphaeidae, palaeoecology, communities, colonization sequence, Late Cretaceous, Maastrichtian, Navarroan, Arkansas.     

Symbiosis between gastropods and bryozoans in the late Ordovician of Cumbria, England

Five examples of symbiosis between gastropods and trepostome bryozoans are described from the Ashgill (late Ordovician) of Cumbria (England). The gastropods are invariably found associated with the bryozoans. whereas the bryozoans may be free-living. Encrustation is considered to have taken place, in most cases, on mature, living gastropod shells, resulting in the trepostome utilizing the shell as a surrogate basal disc. Three specimens show encrustation on an empty gastropod shell, causing the trepostome to develop a basal disc similar to non-encrusting forms. The bryozoan colony probably benefited from the symbiotic relationship by increased water flow over the colony, caused by gastropod locomotion, whereas the gastropod was afforded protection from predators. The new species Spiroecus nidhoeggi. Diplotrypa hvergelmi and Monotrypa fontinalis are described.     

Algal borings and framboidal pyrite in Upper Ordovician brachiopods

Algal borings in the shells of the articulate brachiopods Plaesiomys subquadrata (Hall) and Hebertella sinuata (Hall) from the Richmond Formation of Ohio are empty, or partially to entirely filled with pyrite. The pyrite occurs as single framboids and other crystal forms, or in chains filling the bores. The borings provide some insight into the early diagenetic history of the Richmond sediments near Cincinnati. Pyritization probably occurred within a few years, only a short distance (a few centimeters) below the sediment surface through the activities of sulfur-reducing bacteria. Pyrite precipitated around a nucleus such as a bacterium or algal cell, or developed within an organic structure such as an algal cell or organic membrane.     

Late Campanian to late Maastrichtian bryozoans encrusting on belemnite rostra from the Aktolagay Plateau in western Kazakhstan

Twenty species belonging to fifteen genera of cyclostome and cheilostome bryozoans encrusting belemnite rostra are described from the late Campanian to Maastrichtian of the Aktolagay Plateau, in western Kazakhstan. Due to the moderate to poor preservation of the material, only four cheilostome species are identified down to the species level: Wilbertopora? besoktiensis (Voigt, 1967), ‘Aechmellina’ stenostoma Voigt, 1930, and two new species, ‘Aechmellina’ viskovae and Cheethamia aktolagayensis. All remaining species are left in open nomenclature. Type material of Wilbertopora? besoktiensis from the early Maastrichtian of the Mangyshlak Peninsula in Kazakhstan, has been re-examined. Palaeobiogeographical and implications are discussed. Cheilostomes slightly dominated over cyclostomes in the Aktolagay Plateau fauna encrusting on belemnites in terms of diversity. The dominant colony forms observed were spots and sheets.     

Rare bryozoans (Stenolaemata) with bilateral colonies from the Jurassic and Cretaceous of the East European Platform

New bryozoans characterized by a bilateral vertical colonies colonies—Cardioecia refuga sp. nov. (Tubuliporida), Elea lyapini sp. nov., E. troshkovensis sp. nov., and E. taylori sp. nov. (Melicerititida) from Middle Jurassic (Middle Callovian) of the Moscow region (Russia), and Biforicula legitima sp. nov. (Melicerititida) from the Upper Cretaceous (Lower Campanian) of the Southern Donets Basin (Ukraine)—are described. All species described in this paper belong to genera that have been recorded for the first time in the East European Platform. Some morphological structures in the colonies of these bryozoans and some distinctive features of the order Melicerititida that emphasize the difference of this order from bryozoans of other orders of the class Stenolaemata are examined.     

Tentacle structure in freshwater bryozoans

Tentacles are the main food‐gathering organs of bryozoans. The most common design is a hollow tube of extracellular matrix (ECM), covered with ten columns of epithelial cells on the outside, and a coelothelium on the inside. Nerves follow the ECM, going between the bases of some epidermal cells. The tentacle musculature includes two bundles formed by myoepithelial cells of the coelothelium. The tentacles of freshwater (phylactolaemate) bryozoans, however, differ somewhat in structure from those of marine bryozoans. Here, we describe the tentacles of three species of phylactolaemates, comparing them to gymnolaemates and stenolaemates. Phylactolaemate tentacles tend to be longer, and with more voluminous coeloms. The composition of the frontal cell row and the number of frontal nerves is variable in freshwater bryozoans, but constant in marine groups. Abfrontal cells form a continuous row in Phylactolaemata, but occur intermittently in other two classes. Phylactolaemata lack the microvillar cuticle reported in Gymnolaemata. Abfrontal sensory tufts are always composed of pairs of mono‐ and/or biciliated cells. This arrangement differs from individual abfrontal ciliary cells of other bryozoans: monociliated in Stenolaemata and monociliated and multiciliated ones in Gymnolaemata. In all three groups, however, ciliated abfrontal cells probably serve as mechanoreceptors. We confirm previously described phylactolemate traits: an unusual arrangement of two‐layered coelothelium lining the lateral sides of the tentacle and oral slits in the intertentacular membrane. As previously reported, tentacle movements involved in feeding differ between bryozoan groups, with phylactolaemates tending to have slower movements than both gymnolaemates and stenolaemates, and a narrower behavioral repertoire than gymnolaemates. The morphological and ultrastructural differences between the freshwater species we studied and marine bryozoans may be related to these functional differences. Muscle organization, tentacle and coelom size, and degree of confluence between tentacle and lophophore coeloms probably account for much of the observed behavioral variability.     

Putative sensory structures in marine bryozoans

Abstract. SEM studies of 21 species of marine bryozoans demonstrated that the abfrontal side of the tentacles bears a row of mono- or multiciliated cells, which are presumably sensory. In stenolaemates, the abfrontal cells, as well as the cells at the tentacle tips and the laterofrontal cells, are monociliated. In the 17 gymnolaemate species studied, each tentacle tip bears at least 3 multiciliated cells, each with a tuft of 5–7 stiff cilia of various lengths. On the abfrontal tentacle surface, mono- and multiciliated cells alternate, but all species studied have multiciliated cells at the base and the tip of each tentacle. In live animals, single cilia perform occasional flicks, whereas the tufts of 7–15 cilia on the multiciliated cells are immotile. Length and number of abfrontal cilia vary between species. Two types of multiciliated, putative sensory organs were found on the introvert of some gymnolaemates. One has an apical knob surrounded by a ring of cilia; the other has an apical tuft of cilia. The ultrastructure of the sensory cells of tentacles and introvert was studied in Rhamphostomella ovata . Our observations on both fixed and living material all suggest that these cells are primitive mechanoreceptors. The few species lacking ciliary structures on the introvert have long proximal ciliary tufts on the abfrontal tentacle surface.     

Palynofloristical investigation on the late Cretaceous and Paleocene of China

As late cretaceous and Paleocene was an important stage in the evolution of angiosperms, so studies on flora of this periiod are of great significance. In recent years many palynological data of late Cretaceous and Paleocene have been recorded from different parts of China, especially the Southeastern China. An attempt is made here to allow deductions regarding the problem of existence of some palynological provinces during this period in China. Three provinces may be divided as follows. I. The wet subtropical and warm-temperate palynofioristical province of northeastern China. During late Cretaceous, this palynoflora was marked by occurrence of Aquilapollenites, Mancieorpus, Fibrapollis and Wodehouseia. Aquilapollenites amplus, A. crassus, A. megaprojeetus, A. asper, A. affenatus A. alatus, Mancieorpus andaensis, FiburapaUis mirifieus and Wodehouseia oeulata ...... are noted. Besides these eharacteriestic elements, there are many species of Proteaeiites and some species of Beaupreaidites, Loranthacites, Quereoidites, Salixipollenites, Gothanipollis, Plicapollis, Utmoideipites, Cranwellia, Alnipollenites and Trieolporopollenites. Gymnosperms pollen comprise Abietineaepollenites, Pinuspollenites, Cedripites, Taxodiaceaepollenites and Araueariacites. Sehizaeoisporites are very rich in species and numbers. Polypodiaceoisporites, Osmundacidites and Cyathidites are rarely Maud. Paleocene palynoflora is characterized by scantiness or absence of Aquilapollenites and Wodehouseia. Paraalnipollenites eonfusus, P. orthoeostatus, BetulaepoUenites pli eoides and some species of Myricipites, Comptonia and Momipites are predominant. These pollen may be related to Betulaceae, Juglandaceae and Myricaseae. Taxodiaceaepollenites, Cedripites and Podoearpidites are commen, It reflects that during late Cretaceous the flora was wet and subtropical, but in Paleocene, it turned to be wet and warm-temperate. According to the abundanee of Aquilapollenites and Wodehouseia, this palynoflora may belong to the Eastern AsianWestern North American Paly-nofioristical Province. II. Arid subtropical palynofioristieal province of South China. During late-Cretaceous this palynofiora comprises Morinopollenites Wang & Zhao (M. normalis, M. minor, M. polyprojeetus, M. rhombiformis) and Janhangpollis Wang & Zhao (J. radiatus, J. arciformis, J. sayaxngensis, J. ringes, J. mikros). Besides this, species of Proteacidites, Beaupreaidites, Myoporumpollenites, Crassimarginpollenites, Cranwellia, Magnolipollis, Rutaceoipollenites, Ilexpollenites, Symplocospollenites, Nyssapollenites, Palmaepollenites and Chenopodipollis were recorded. Classopollis, Exessipollenites and Rugubivesieulites were abundant in this assemblage. Aquilapollenites is rarely recorded, except along the coast region of eastern China. In paleocene some species of Nanlingpollis Sun & He, Pentapollenites jiangsiensis, Tricolporopollenites rombicus and Sapotaceoidaepollenitess trieoloporatus are recorded, but Morinopollenites and Janhanpollis were unknown. Ulmoideipites, Ulmipollenites, Ephedripites and some verrucate spores (Pterisispora) were very abundant. According to the feature of the pouch assemblages, the flora of South China during that time was of arid subtropical in nature. It seems to be nothing to do with other palynofloristical provinces in the world. III. Arid subtropical palynofloristical province of Northwestern China. Palynofiora of this period has been recorded from a few localities throughout this area. Normapolles group (Atlantopollis, Pseudoatlantopollis, Chaonopollenites, BasopoUis and ExtratriporopoUenites), Proteacigites microverrucatus, Eehitriporites magnus and Triatriapollenites echinatus were present. Besides that, Beaupreaidites, Rutaceoipollenites, Lonicerapollis and Engelhardtioipollenits were also occurred. In gymnosperms Ephedripites and some disaccate pollen were abundant. The percentage of Normapolles is increasing from east to west, while Proteaeidites is decreasing. In Paleocene Nudopollis and Trudopollis of Normapolles group were present, while Proteacidites 8issappeared. The palynoflora of this province was of an arid and subtropical in nature, which is somewhat in connection with the European-Eastern American Palynofloristical Province by the presence of Normapolles.     

Inferring larval type in fossil bryozoans

Pachut, J.F. & Fisherkeller, P. 2010: Inferring larval type in fossil bryozoans. Lethaia, Vol. 43, pp. 396–410. Larval type in extinct organisms might be recognizable because larvae of living marine invertebrates are approximately of the same size as the initial post‐larval organism. Two larval types typically occur. Planktotrophic larvae feed on other members of the plankton, potentially prolonging their larval existence and producing broad geographic distributions. Conversely, lecithotrophic larvae feed on yolk supplied by the fertilized egg, often settle quickly after release, and display more restricted distributions. However, some lecithotrophic bryozoans undergo embryonic fission forming multiple, small, polyembryonic larvae. The relationship between post‐larval size and larval type was evaluated in bryozoans by comparing the size of the ancestrula, the founding individual of a colony, to the sizes of extant planktotrophic, lecithotrophic and polyembryonic lecithotrophic larvae and ancestrulae. The sizes of larvae and ancestrulae in extant lecithotrophic and planktotrophic cheilostome (gymnolaemate) species are statistically the same. They are, however, statistically larger than the polyembryonic larvae of extant cyclostomes (stenolaemates). In turn, the sizes of cyclostome larvae are indistinguishable from the ancestrulae of extant and fossil cyclostomes, the ancestrulae of other fossil stenolaemate species measured from the literature, and the ancestrulae of three of four genera from North American Cincinnatian strata. Ancestrulae of a fourth genus, Dekayia, are the same size as cyclostome ancestrulae but are statistically smaller than the ancestrulae of other stenolaemates. With few exceptions, stenolaemates have statistically smaller larvae and ancestrulae than both lecithotrophic and planktotrophic cheilostomes. We infer that the sizes of fossil ancestrulae permit the discrimination of taxa that had polyembryonic lecithotrophic larvae from those possessing other larval types. This inference is strengthened, in several cases, by the co‐occurrence of brood chambers (gynozooecia) and restricted palaeobiogeographic distributions. The presence of cyclostomes in Early Ordovician strata suggests that polyembryony may have been acquired during the initial radiation of Class Stenolaemata. Polyembryony appears to be a monophyletic trait, but confirmation requires the demonstration that species of several stenolaemate suborders lacking skeletally expressed brood chambers possessed polyembryonic larvae. □Ancestrulae, evolution, fossil bryozoans, gynozooecia, larvae.     

Rhyncholites and conchorhynchs as calcified jaw elements in some late Cretaceous ammonites

Conspicuous calcareous coverings are present in the anterior region of 17 fossil jaws from late Cretaceous rocks of Hokkaido (Japan) and Sakhalin (U.S.S.R.). The jaws were preserved in calcareous nodules either in situ in body chambers of ammonites or in close association with identifiable ammonite conch remains. From the morphologic similarity between in situ and isolated jaws, they may be attributed to Tetragonites glabrus, Gaudryceras tenuiliratum, G. denseplicatum, G. sp., and Neophylloceras subramosum. The jaw apparatus of these species is composed of two three-dimensional black walls of carbonate apatite, which might be a diagenetic replacement of chitinous material. The calcareous coverings in both upper and lower jaws closely resemble those of upper (rhyncholite) and lower (conchorhynch) jaws of modern Nautilus as well as rhyncholite and conchorhynch fossils in their gross morphology, microstructure, and chemical composition. Calcified remains of cephalopod jaws known as rhyncholites and conchorhynchs have been reported from late Paleozoic to Recent. The present discovery of ammonoid rhyncholites and conchorhynchs suggests that at least some previously known late Paleozoic and Mesozoic counterparts belong to the Ammonoidea. The essential similarity of jaw elements of some Late Cretaceous ammonites and modern Nautilus gives reliable information on the feeding habits of the former. The sharp and thick ammonoid rhyncholites and conchorhynchs may have had a special function for cutting up food, similar to those of Nautilus.     

The role of modern and fossil cyanobacterial borings in bioerosion and bathymetry

Measurements on modern coral reefs at Lee Stocking Island (Bahamas) illustrate that boring cyanobacteria species make a major contribution to microboring bioerosion rates. Borings attributed to cyanobacteria also occur in fossil environments. Bioerosional studies on Permian and Triassic reefs show similar intensities to those observed on modern equivalents. The importance of borings assigned to cyanobacterial activity is even more apparent in paleobathymetry. Comparison of the bathymétrie ranges known from modern and fossil microborings demonstrates a preference of boring cyanobacteria for shallow marine environments. Furthermore, some traces are linked to distinct portions of the shallow euphotic zone. They significantly contribute to characterize typical microboring assemblages, which are used for paleodepth reconstructions. In contrast to these stenobathic species, one cyanobacterial species turned out to be eurybathic. It has been recorded as deep as the dysphotic zone but may even extend to the aphotic zone.     

Environmental change drove macroevolution in cupuladriid bryozoans

Most macroevolutionary events are correlated with changes in the environment, but more rigorous evidence of cause and effect has been elusive. We compiled a 10 Myr record of origination and extinction, changes in mode of reproduction, morphologies and abundances of cupuladriid bryozoan species, spanning the time when primary productivity collapsed in the southwestern Caribbean as the Isthmus of Panama closed. The dominant mode of reproduction shifted dramatically from clonal to aclonal, due in part to a pulse of origination followed by extinction that was strongly selective in favour of aclonal species. Modern-day studies predict reduced clonality in increasingly oligotrophic conditions, thereby providing a mechanistic explanation supporting the hypothesis that the collapse in primary productivity was the cause of turnover. However, whereas originations were synchronous with changing environments, extinctions lagged 1–2 Myr. Extinct species failed to become more robust and reduce their rate of cloning when the new environmental conditions arose, and subsequently saw progressive reductions in abundance towards their delayed demise. Environmental change is therefore established as the root cause of macroevolutionary turnover despite the lag between origination and extinction.     

Paraboloid colony bases in Paleozoic stenolaemate bryozoans

Dendroid stenolaemate bryozoan colonies with paraboloid bases developed initially in the same manner as stenolaemate colonies with broadly encrusting bases. Their unique shape is related to the narrowly cylindrical shape of the encrusted surface (algal stipe?) and to radially differentiated rates of growth from the point of colony origin. The colony shape is interpreted as an adaptation to unconsolidated substrates in relatively quiet though not necessarily deep water.     

Planktonic foraminiferal succession in late Cretaceous to early Palaeocene strata in Meghalaya, India

A roughly 10.5-m-thick succession within the Langpar Formation of the Um Sohryngkew River section, Meghalaya, India, constrained by the last occurrence of Globotruncanita stuarti and the first occurrence of Parasubbotina pseudobulloides , spans the K/T (Cretaceous–Tertiary) transition. The unit is divisible into three parts with the lower consisting of shaly limestone, weakly calcareous shale and silty shale with coal streaks. The middle part is dominated by calcareous shale with mud flakes, coprolites, burrows and pyrite nodules, followed by alternating limestone and marlite at the top. Planktonic foraminifera are rare to frequent within the unit. Based on the distribution of zonal indices, seven successive planktonic foraminiferal zones are recognized from across the K/T boundary. From base to top, these are CF4, CF3, CF2 and CF1 in the upper Maastrichtian part and Zone P0, Zone Pα and Subzone P1a in the lower Danian part. The biozones indicate that the section is biostratigraphically continuous across the K/T boundary. A similar foraminiferal succession and K/T transition is observed in the Langpar of the Cherrapunji-Mahadeo road section at a distance of over 5km. These K/T outcrops from Meghalaya provide the first record of a continuous K/T sequence in the Indian subcontinent with respect to planktonic foraminifera.     

Recent borings in limestone cobbles from Marloes Bay, southwest Wales

Limestone clasts from the beach at Marloes Sands, southwest Wales, contain slender, straight to sinuous borings cross-cut by younger, clavate borings. The former were probably produced by sipunculids or polychaetes; the latter preserve shells of the boring bivalve Gastrochaena dubia (Pennant). Unusually, the calcareous linings of the clavate bivalve borings extend into many of the slender worm borings. Such linings are considered part of the hard parts of the producing bivalve, but the chance association of the two morphologies of borings has led to the lining becoming intimately associated with both of them. The modified linings of the bivalve borings have a similar morphology to the crypt of certain clavagellid bivalves, perhaps presenting an analogue for the morphology of a pre-clavagellid, boring ancestor.     

Evolution of larval size in cyclostome bryozoans

Cyclostomes are the only order of stenolaemate bryozoans living today. The non-feeding larvae of modern cyclostomes metamorphose on settlement to produce a calcified dome-shaped protoecium. Protoecial diameter provides a proxy for larval size. The sparse data available on living cyclostomes suggests that protoecial diameter is about one-and-a-half times greater than larval width. Here we use protoecial diameter to estimate larval sizes in fossil and Recent cyclostome species. A total of 233 protoecia were measured, 143 from Recent cyclostomes and 90 from fossil cyclostomes, of which 84 came from the Jurassic. Protoecial diameter ranged from 82.5 to 690 μm, with 89% of protoecia having diameters between 100 and 300 μm. A comparison of 30 Jurassic with 51 Recent taxa of tubuliporine cyclostomes showed a significant difference in size frequency. Although the Recent taxa have a larger size range (83–465 μm) than the Jurassic taxa (125–249 μm), Recent species have a lower mode (125–150 μm) than the Jurassic species (175–200 μm). Most Jurassic cyclostomes may therefore have had larger larvae than their extant relatives. Reduction in larval size may be a component of the previously hypothesized reduction in overall body size resulting from competitive displacement by cheilostome bryozoans.     

Palaeoanellus dimorphus gen. et sp. nov. (Deuteromycotina): a Cretaceous predatory fungus

In habitats where nitrogen is the limiting factor, carnivorous fungi gain an advantage by preying on nematodes and other microorganisms. These fungi are abundant in modern terrestrial ecosystems, but they are not predestined for preservation as fossils. Conclusions on their evolutionary history are therefore mainly based on molecular studies that are generally limited to those taxa that have survived until today. Here we present a fossil dimorphic fungus that was found in Late Albian amber from southwestern France. This fungus possessed unicellular hyphal rings as trapping devices and formed blastospores from which a yeast stage developed. The fossil probably represents an anamorph of an ascomycete and is described as Palaeoanellus dimorphus gen. et sp. nov. Because predatory fungi with regular yeast stages are not known from modern ecosystems, the fungus is assumed to not be related to any Recent carnivorous fungus and to belong to an extinct lineage of carnivorous fungi. The inclusions represent the only record of fossil fungi that developed trapping devices, so far. The fungus lived c. 100 million years ago in a limnetic-terrestrial microhabitat, and it was a part of a highly diverse biocenosis at the forest floor of a Cretaceous coastal amber forest.