bluuebunny/crossref_metadata_2025_split huggingface dataset:
Liptinite macerals in Singrauli coals, India: their characterization and assessment
Authors: Misra Basant K. , Singh B.D. 
Published: September 2022

The record of liptinite macerals in Indian Permian coals has been uniformly quite low under normal reflected light. In fact, high inherent clastic minerals intimately associated with liptinite macerals in these coals tends to mask them, at times, completely, obstructing identification and for this reason they are considered to be poor in liptinite content. Petrographic investigations carried out on Early Permian Turra coal seam and Late Permian Jhingurdah coal seam of Singrauli Coalfield, under blue light excitation, recorded appreciably high amounts of liptinite macerals (13-57% on mineral matter-free basis) as against maximum up to 19 per cent (m.m.f basis) under normal reflected light. The liptinite macerals in these coals are formed chiefly by sporinite (7-40%) and liptodetrinite (1-16%). Cutinite, suberinite, resinite, alginate, exsudatinite and fluorinate are the other macerals of liptinite group together occurring in only subordinate amounts.
The coals of the Turra seam associated with Barakar Formation have relatively higher liptinite content than that of the Jhingurdah seam of Raniganj Formation. Such high concentration of sporinite has not been reported so far from the Indian Permian coals. The increase in liptinite/sporinite content coincides with increase in mineral matter content in many instances, i.e., dull bands normally have high liptinite content. The sporinite concentration in dull coal bands of the Permian coal seams mark the presence of semi-cannel or cannel coal bands.
39th Sir Albert Charles Seward Memorial Lecture: Climate changes over space and time: their repercussions on the flora and vegetation
Authors: Meher-Homji V.M. 
Published: September 2022

The changes in the climatic types from region to region over the vast expanses of the Indian sub-continent have been examined in terms of quantum of rainfall and distribution of rainy pattern: length of the dry period and season(s) of occurrence of rains. The interyearly variability introduces a further dimension in the diversity of the climate types. The vegetation pattern generated by the climatic diversity is briefly reviewed. Of particular interest is the transition from the tropical type of climate in India to the Mediterranean type further westwards.
As to the climate changes through the geological ages, the impressive record of megafossils collected by the scientists of the Birbal Sahni Institute has yielded valuable evidence of the vicissitudes. For the Quaternary period, palynology has played a key role in reconstructing the climate-vegetational history. A criticism may not be out of place. Many of the reconstructions refer to climate change only in terms of rainfall amount ignoring the distributional pattern (number of dry months, season of occurrence of rains). Sometimes the botanical markers selected are not fidel indicators of climate. In the much acclaimed and frequently cited palaeopalynological study of Gurdip Sing et al., (1974), the taxa selected like Artemisia, Maytenus, Mimosa, Oldenlandia, Cyperus, Syzygium cumini are not very fidel indicators of a humid phase. If the climate of the Thar had changed to humid type in true sense of the term, the pollen of the forest species of the Aravallis should have turned up in the profile of the Sambhar Lake.
In other cases, palynologists in their enthusiasm attribute even man-induced change in the vegetation to climate. The meticulous study of Caratini et al (1991) brings out a distinct change from forest vegetation to savannah type in the Western Ghats 3,500 years B.P., which incidentally pinpoints the beginning of the anthropic activity with burning of vegetation promoting the growth of grass-savanna. In yet other cases, the change in vegetation appears likely due to shifts in the course of river rather than fluctuations in rainfall (Jolly & Bonnefille, 1992).
A hypothesis has been suggested as to how the species responded or adjusted phenologically to the drift over a vast latitudinal span from 30° S to 30° N. it has also been pointed out that major deforestation can bring about a climate change in disrupting the normal rainy pattern decreasing the number of rainy days and drastically altering the micro-climates. The physical mechanisms involved have been enumerated.
Vegetation mapping has provided clues for the areas to be protected on priority basis for conservation of biodiversity and for permitting the migration of species through these protected corridors in the wake of climatic change: from the cooler’s zones to the warmer and from wetter to the drier. The need for study of populations in plant taxonomy has been stresses for assessing finer changes in climate.
Distribution, evolution and extinction of global early Carboniferous flora
Authors: Chandra Shaila , Keqin Sun 
Published: September 2022

The uniform Lepidodendropsis flora of the Early Carboniferous is uniformly and widely distributed in the Cathaysia, Laurasia, Kazakhstania and Gondwana continents. This is characterized by Lepidodendropsis, Sublepidodendron, Archaeosigillaria, Archaeocalamites, Sphenopteridium, Cardiopteridium, Rhodeopteridium, Rhacopteris, Triphyllopteris and Adiantites, etc. the global climatic differentiation was not very obvious during the Early Carboniferous, therefore, all Early Carboniferous plant assemblages belonged to the same phytogeographic province. It is known that some typical genera of the Lepidodendropsis flora of the Early Carboniferous, such as Lepidodendropsis, Lepidosigillaria and Archaeosigillaria are recorded from the Lower Devonian in Libya, Africa (Lejal-Nicol, 1975) and some elements of this flora are also recorded from the Late Devonian in China and other parts of the world. It is considered that this Lepidodendropsis flora gradually started appearing in the Early Devonian, began to diversify in the Late Devonian and reached its maximum development in the Early Carboniferous. The flora tended to decline in the Late Early Carboniferous and resulted in its extinction in the end of the Early Carboniferous.
Although some plant elements in Cathaysia, Euramerica, Angara and Gondwana had already appeared in the Early Carboniferous, especially in the late Early Carboniferous, the occurrence of the new taxa was regarded as a result of gradually increasing climatic differentiation and plant evolution. During the transition period from the Early Carboniferous to the Late Carboniferous, the differentiations of climatic conditions, tectonic movements, continental positions, oceanic currents and glaciation were quite obvious, resulting in the extinction of numerous typical elements of the Early Carboniferous flora and the appearance of some forerunners of the Late Carboniferous floras in the world. The Cathaysia, Euramerica, Angara and Gondwana floras derived from the identical Lepidodendropsis flora of the Early Carboniferous, but developed and flourished in different environmental conditions.
Terminal Proterozoic-Cambrian sequences in India: a review with special reference to Precambrian-Cambrian Boundary
Authors: Kumar Gopendra , Shanker Ravi , Mathur V.K. , Maithy P.K. , Bhattacharya S.K. , Jain R.K. 
Published: September 2022

The Terminal Proterozoic marine sequences, grading into Cambrian, are present in the Krol Basin (Lesser Himalaya), the Kashmir, Spiti-Zanskar and Kumaun Basins (Higher Himalaya) and in Marwar Basin (western India). These sequences postdate a major tectono-thermal event associated with Cadomian Orogeny and rest on eroded older successions which include well-dated Malani Igneous Suite (Malani Rhyolite 745 ±10 Ma; Siwana Granite 731± 14 Ma) in Western India and over the Salkhala Group with granites (745 ± 50 Ma) or the Simla Group in the Himalaya. This cycle of sedimentation terminated with Pan-African Orogeny in Late Cambrian. These sequences are dominantly siliciclastic in basins in Higher Himalaya while those in Krol Basin and Marwar Basin show development of thick carbonate-evaporite facies with or without phosphorite. From the Upper Vindhyan and Bhima Groups in central and south India, respectively a Chuaria-Tawuia Assemblage along with sphaeromorphida Acritarch of Early Neoproterozoic age has been recorded. The δ13C values range from +1.3 to +4.0 ‰ PDB and that of δ 18O from -5 to -9‰ PDB. These are, thus, not considered part of this sequence. In absence of age-determinating biota and radiometric dates from the basal part of the succession, the lower boundary of the Terminal Proterozoic cannot be delineated and dated. However, a significant depletion in values may be taken to mark the lower boundary.
The upper boundary of the Terminal Proterozoic (Precambrian-Cambrian Boundary) cannot be demarcated in terms of GSSP due to the absence of trace fossils of Zone-1 (Harlaneilla podolika Zone) and Zone-II (Phycodes pedum Zone) in carbonate facies in Krol Basin and poor documentation of siliciclastic facies in Kashmir and Spiti-Zanskar Basins. The trace fossils correlative with ichnozone-III occur in all sections in the Himalayas and are useful for regional and global correlations. However, a significant depletion in δ13C values has been recorded in the carbonate facies of the Krol Basin between the horizons yielding Ediacaran and small shelly fossils of Meishucunian Zone-I. This has also been recorded in the Marwar Basin below the Phosphorite Bed. This depletion may be correlated with that recorded from the Precambrian-Cambrian transition in Siberian Platform, Anti Atlas Mountains, Morocco, China, etc. It may be taken into consideration to define and mark the boundary in the absence of trace fossils.
Ultrastructure of the sporoderm in megaspores of some Indian Selaginellas
Authors: Bajpai Usha 
Published: September 2022

Megaspores of six species of the genus Selaginello were studied under light microscope and Scanning Electron Microscope. In general, the sporoderm of all the species investigated shows a tuberculate sculpture, intervening areas have fine reticulum. The sporopollenin units could also be examined in some megaspores by fracturing the spore wall.
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Palynology in stratigraphy of lesser Himalayan sedimentary sequences from Arunachal Pradesh, India
Authors: Srivastava Suresh C. , Bhattacharya A.P. 
Published: September 2022

Arunachal Pradesh has a distinct geological setup and significant data have been generated during the last decade both from Permian as well as Tertiary sediments. The palynoflora investigated from Lesser Himalayan Permian sediments of Arunachal Pradesh has been differentiated into five palynozones 1. Plicalipollenites stigmatus 2. Callumispora gretensis 3. Crucisaccites indicus 4. Pselldoreticulatispora baraknrensis and 5. Primuspollenites + Rhizomaspora: the oldest being Palynozone I (Rilu Member, Rangit Formation) representing Late Asselian whilc Palynozones 2-5 (Garu Formation) represent Early Sakmarian to Early Artinskian age.
The palynoassemblages recorded from Tertiary sediments in Arunachal Pradesh largely show the overwhelming presence of angiosperm pollen. viz. Lakiapollis. Neocouperipollis, Arecipites, Pellicieroipollis and Ctenolophonidites. Pteridophytic spores. viz., Todisporites. Cyathidites. Striatriletes and Crassoretitriletes shows similar age connotations. Broadly two distinct palynozones have been differentiatcd. viz., Lakiapollis ovatus and Striatriletes susannae assemblage zones. At some sections presence of dinoflagellate and acritarch indicate marine influence during Early Tertiary.
Permian spores also occur in reworked state within Early Tertiary sediments. Palynological investigations carried out along the thrust suggest that some thrust slices of Tertiary rocks arc wedged deep within the Permian outcrops. These evidences indicate severe post depositional tectonic effect in these regions. Palynological evidences along with faunal evidences. Wherever possible, have been summarised to decipher the stratigraphic resolutions, palaeogeography and palaeoenvironment of the region.
Similar Tree Ring pattern in the Gymnosperm woods from Late Permian of Antarctica and India
Authors: Bera Subir , Banerjee Manju 
Published: September 2022

Tree rings revealed in a newly described gymnosperm wood Araucarioxylon ghoshii sp. nov. from Raniganj Formation, Raniganj Coal field, India are similar to the tree rings described in the in situ gymnosperm fossil woods from the Late Permian of Antarctica.
The rings of the fossil woods from Antarctica and India have higher proportion of early woods compared to little amount of late wood. Characteristic zigzag pattern of early wood tracheids formed due to collapsing and crushing of tracheid files and false rings occur in the woods recorded from two distant areas. The characters suggest occurrence of rapidly growing young forest in both the continents during Late Permian. Quantitative analysis of growth rings in A. ghoshii reveals a CSDM curve with right skewedness +19% suggesting its possible evergreen nature with small to moderate leaf retention time.
Long term monitoring of air-borne pollen and fungal spores and their allergenic significance
Authors: Khandelwal Asha 
Published: September 2022

The qualitative and quantitative analyses of aerospora at Birbal Sahni Institute of Palaeobotany are assessed for the biogenic pollutants of Lucknow atmosphere. The Impaction method was employed for preparing annual pollen and spore calendars over six years (1969-1970, 1970-1971, 1971-1972, 1983-84, 1984-1985, 1985-1986). As many as 61 types of pollen grains and 27 types of fungal spores have been encountered. The maximum numbers of pollen grains were recorded in the year 1985-86 (24383) and minimum in the year 1969-70 (13005), whilst the maximum number of fungal spores encountered were in 1971-72 (22604) and minimum in the year 1969-70 (12771).
It has been visualized that long term pollen/spore monitoring at a particular site provides a strong base for the prediction of aeroallergens as a warning towards the allergenic disorders. The well recognised allergenic pollen and spore of Lucknow area include Argemone mexicana, Amaranthus spinosus, Cannabis sativa, Chenopodium album, Prosopis juliflora, Cyperus rotundus, Ricinus communis, Xanthium strumarium and many species of Aspergillus.
Occurrence of the Genus Pachypteris in the Triassic of India
Authors: Pal Pankaj K. , Basu Moumita 
Published: September 2022

The leaf genus Pachypteris Brongniart occurs commonly in Mesozoic rocks throughout the world. In India, the genus has hitherto been known only from the Lower Cretaceous strata of Rajmahal, Jabalpur, Bhuj and Pariwar formations. However, a few specimens collected from the Janar River beds of Tiki Formation, in their gross features and cuticular details, evidently represent a new species of the genus. The species, named as Pachypteris hirsuta sp. nov., in addition to its obvious hypostomatic lamina, is characterized by the presence of polygonal trichome bases. Each trichome base is surrounded by a ring of radially elongated cells.
From Janar River beds, species of Lepidopteris, Dicroidium, Xylopteris, Sphenobaiera and Baiera have been described earlier. Pachypteris is a further addition to this assemblage. On the basis of faunal and floral remains, Tiki Formation has been dated as Upper Triassic. Occurrence of Pachypteris is hereby recorded for the first time from Indian Triassic strata.
Pennsylvanian megaspores from northeastern border of the Paraná Basin, Brazil: Correlation with Indian Gondwana megaspores
Authors: Mune Sandra Eiko , Tewari Rajni , Bernardes-de-Oliveira Mary E.C. 
Published: September 2022

Analysis of sediments from Campinas and Monte Mor, municipalities of the State of São Paulo, Brazil, has revealed the presence of new megaspores in addition to the known taxa. Trilete, alete, azonate and gulate dis persed fossil megaspores were recorded from the lower and middle levels of the Itararé Group from the northeastern border of the Paraná Basin (Lower Pennsylvanian) of Campinas municipality (Upper Bashkirian-Lower Moscovian) and of Monte Mor municipality (Kazimovian). Twenty-four species of megaspores recovered from one or both of these localities have been systematically analyzed and the synonymy of four previously described megaspores has been discussed.
The present study of megaspores from Campinas reveals the presence of the taxa Banksisporites dijkstrae, B. endosporitiferus, B. utkalensis, Biharisporites spinosus, Bokarosporites psilatus, B. rotundus, Duosporites perversus, Duosporites sp. a, Lagenicula horrida, Lagenicula sp., L. nudus, L. rugosus, Lagenoisporites cf. L. hispanicus and Lagenoisporites. sp. The megaspores from Monte Mor includes the taxa Bokarosporites rotundus, Duosporites sp. b, Lagenoisporites nudus, L rugosus and L. cf. L. hispanicus. The taxa Bokarosporites rotundus, B. psilatus, Banksisporites utkalensis, B. endosporitiferus, B. dijkstrae and Biharisporites spinosus are also known from the Permian of India. Banksisporites tenuis previously detected in Campinas and Monte Mor localities is also a species which is shared with India. The presence of these taxa in the Pennsylvanian of the Paraná Basin, Brazil indicates their appearance in the Carboniferous. While all of them persisted up to the Permian, some like Biharisporites spinosus, Banksisporites tenuis and B. utkalensis extend up to Triassic and Early Cretaceous as well. The presence of these megaspores both in India and in Brazil indicates the occurrence of common ancestral heterosporous early land plants. An attempt has been made to inte rpret the palaeogeographic distribution pattern of some of the megaspores which appeared earlier in Brazil as compared to India, suggesting the floral migration from Brazil towards India.
Insect herbivory in Gondwana plants
Authors: Srivastava Rashmi , Srivastava A.K. 
Published: September 2022

Plant–insect interaction is dominant in the extant flora and it is estimated that more than one million species of insects directly or indirectly survive on plants. In comparison, such association is limited in extinct flora, mainly due to problem in identifying structural features associated with the insect wronged plant fossils. Concerted efforts and comparative structures observed in extant flora have unfolded the mystery of insect herbivory in fossil plants. The study has helped to understand the feeding pattern and evolutionary features of insects during different time intervals and provide significant evidence to comprehend the co–evolution of plant and insect in the geologic past. Herbivorous insect wings discovered from different Gondwana successions of India belong to families and genera of Homoptera, Heteroptera, Mecoptera, Coleoptera and Blattoidea. The remains of Coleoptera and Mecoptera in all probability represent the earliest record in fossil flora. Insect herbivory is well recognized in Indian flora in the form of insect galls, chewing and eaten marks of leaf margin, disfigurement of lamina, egg–like pouches, trailing marks, mining activity, etc. The available records demonstrate the presence of well-knit coalition of insect–plant interaction in Indian Gondwana successions.
Diverse type of insect herbivory recovered in the Gondwana flora of India implies that insects used the plants for various purposes such as feeding, shelter and laying eggs for their development/ survival and the process has thus helped in the development and evolution of insects in consortium with plants.
Behavioural studies on the pollen grains of Pinus roxburghii collected from Lucknow, India- A report
Authors: Dixit Pooja , Saxena Gauri , Kumar Dinesh , Singh Lav 
Published: September 2022

We have long recognized that natural climatic shifts influence the development of plants on earth. These slow temperature fluctuations have resulted in either the extinction or evolution of various species. A careful study of the comparative morphology of the living and fossil type suggests that the modern coniferous families originated independently from a group of extinct conifers called the transition conifers by Florin. The conifers reached their climax in the mid–Mesozoic times and have been on the decline ever since. Pinaceae is one such family whose pollen grains have been located as long back as in the Gondwana flora and have demonstrated morphological variations since then due to climatic changes.
Pinus is the most dominating genus of the family Pinaceae in gymnosperms. Pine grains are large due to their sacs or bladders, which make them one of the easiest pollen grains to identify. They are rich in non–enzymatic anti–oxidants, like provitamin A, B complex, C, D and E plus a host of minerals and amino acids. Apparently pine pollen is also a great defense against radioactive caesium that is appearing in dairy and other foods in the U.S.
The present study examines the changes occurring in one of the most sensitive phases of plant development in the living genus of Pinus, i.e. the behaviour of pollen, found to be dependent on number of genetic or environmental factors. The major environmental factors contributing to this abnormal behaviour include light intensity and quality, temperature and moisture and level of pollutants in atmosphere.
During present study, the Pinus cones were collected from five experimental areas of Lucknow that exhibited different level of deformities probably due to different levels of environmental stress or other genetic reasons. The clusters were unique in having deformed cones on the side facing the road while they were near normal on the side away from road indicating that the area around the roadside being more polluted and may be playing a detrimental role in cone morphology. Pollen of normal cones were bilateral, analept, usually bisaccate, spherical, slightly elliptical with verrucate corpus and sacci having pila, normal average size being 60μ–65μ including sacci and sacci attached almost full width of corpus, exine thick in proximal part of reticuloid corpus. While pollen grains of abnormal cones show abnormalities in their size, shape, size and number of wings, size and shape of corpus and development of pollen tube within microsporangium. The abnormalities were observed using scanning electron microscopic studies and its percentage was calculated using a light microscope.