New Quaternary Mammalian Faunas and Cave Deposits in the Zhoukoudian Area, Beijing

The Boiano Basin is one of the largest Quaternary intermontane basins of the central‐southern Apennines within one of the most tectonically active areas of the Mediterranean region. In order to reconstruct its entire Quaternary stratigraphic, tectonic, and palaeoenvironment evolution, lithofacies and palaeomagnetic analyses have been performed on a 900 m‐deep borehole (CP1) drilled in the southwestern sector of the basin. The Quaternary succession consists of an alternating of alluvial fan and fluvial–marshy deposits for a total thickness of 240 m, unconformably laying on Lower Miocene deposits of the Sannio Unit, thrusted on upper Miocene deposits of the Molise Flysch. In addition, the stratigraphic study and facies distribution of 29 intermediate and shallow wells drilled in the basin, allowing us to define the thickness and lithofacies variations of the Quaternary sedimentary units inside the entire Boiano Basin in the sector of Campochiaro alluvial fan. Our results demonstrate that the Boiano Basin infilling started during the late Early Pleistocene (c. 1.1 Ma) and developed with variation in lithofacies distribution and thickness. The first depositional unit (Early Pleistocene–early Middle Pleistocene in age) was palustrine and fluvial–marshy, the second (Middle Pleistocene in age) was characterized by the occurrence of the first cycle of alluvial fan deposition, the third (late Middle Pleistocene in age) was newly palustrine and fluvial marshy and, finally, the fourth recorded two cycles of alluvial fan deposition (late Middle Pleistocene and Late Pleistocene in age, respectively), interspersed by short periods of palustrinity, tephra layers deposition, and palaeosols development. The study allows the hypothesizing that the Quaternary infilling was accommodated within a graben (or semigraben) structure, affected mainly by extensional fault systems localized in the inner part of the basin and secondly by fault systems bounding the basin.

Ungulates from Atapuerca TD6

The Middle and Late Pleistocene mammalian faunas of Japan are described with new opinions on their succession and relation to the continental faunas. Although fossil materials assignable to early Middle Pleistocene are seemingly scarce in Japan, the fauna of that time is considered to have been transitional between the Early and Middle Pleistocene ones. On the other hand, fossil records which are younger than early Middle Pleistocene are abundant from the mainlands of Japan; viz. the Honshu-Shikoku-Kyushu area.In the middle Middle Pleistocene, the fauna of this area contained a considerable number of taxa which are extant today in the area (about 50%). It was also characterized by a high proportion of endemic species and the predominance of temperate forest elements. From this time to the late Middle Pleistocene, several species disappeared from the fauna; at the same time, immigrants from the continent were scarce. The faunal characters of the late Middle Pleistocene were basically identical with those of the preceding time.In the early Late Pleistocene, no mammal seems to have immigrated from the neighboring continent, and faunal composition was almost consistent with that of the late Middle Pleistocene. The elements of that fauna still persisted in the late Late Pleistocene, apart from the extinction of a few forms. In addition to the fact mentioned above, immigration from the northern part of the continent was recognized in the late Late Pleistocene, although it was restricted to a few large herbivore forms and to a short time duration.The introduction of the continental faunas to the mainlands of Japan during Middle and Late Pleistocene times was not so remarkable as previously inferred. Therefore it becomes doubtful that the faunas of the area were drastically replaced by the immigration of the Choukoutien, Wanhsien and Loess faunas of China during those times.

The current study focuses on the emblematic Myopus/Lemmus species complex (tribe Lemmini) in the European Pleistocene fossil record. The members of the two genera occupy distinct ecological niches and have different external appearances, but they are remarkably similar in their dental morphology, so that they were commonly thought of as undistinguishable in the fossil record. Thus, more or less all European Lemmini fossils have been assigned to the genus Lemmus. In the Early Pleistocene site of Schernfeld (Germany), the species Lemmus kowalskii had been described. It was thought by some authors that all Lemmini from Early to late Middle Pleistocene belong to this species.In the current study, we investigated Lemmini molar morphology from Western and Central European sites including Schernfeld (Early Pleistocene), Sackdillinger Höhle (Sackdilling Cave), and Koněprusy C718 (both early Middle Pleistocene), as well as other fossil localities with fewer specimens, formerly assigned to Lemmus kowalskii. Using an extensive modern referential material of Lemmus and Myopus, this study proposes to re-evaluate taxonomic status of the Middle and Early Pleistocene Lemmini. This modern referential also allows a better understanding of the morphology of Lemmus kowalskii specimens and its variability.Our results highlight the very high variation within fossil populations, as well as significant statistical differences between populations of the Early and Middle Pleistocene localities. A large part of these fossil specimens is firmly identified as Myopus sp., including the L. kowalskii holotype. Our identifications demonstrate that in most Early and Middle Pleistocene sites considered in this study, both genera (Lemmus and Myopus) are present. Possible interpretations and consequences for current view of lemming history are discussed, as well as some of the paleoecological and paleoenvironmental implications.

Early and Middle Pleistocene of North America

The present paper treats of the results of a detailed geomorphological investigation carried out along the lower course of the Vltava, and in the wide environment of the Labe, up stream from its confluence with the Vltava between Mělník and Roudnice n. L. Characteristic features of the morphology of the area under investigation are erosion-denudation phenomena on the one hand, and accumulation phenomena on the other. Erosion-denudation phenomena are represented by structural denudation plateaus occuring especially on the right bank of the Labe, and developed at several different levels. Their approximate age may be determined by their relation to the development and the genesis of the valley of the Labe, and especially, to the terraces. The oldest structural denudation plateaus occuring at a height of 325 m date from Later Tertiary (Pliocene), others are of Quarternary age (predominantly Early Pleistocene, rarely Middle Pleistocene, only exceptionally Late Pleistocene). In the north-eastern part of the mapped area, structural and tectonic conditions of cretaceous rocks played an important part in the origin of pictoresque sandstone cities as well as in the development of deeply incised canyons, which most often, follow the course of fissures and faults in the cretaceous sediments. The place of confluence of two main Bohemian rivers - the Labe and the Vltava - in the area between Říp and Mělník was shifted several times in the Quarternary. The most effectual influence upon the intricate development of water streams in this area exercised the basalt hill Říp nowadays situated in the middle of accumulations of Eearly Pleistocene terraces. The terrace material had been deposited mostly by the Vltava after it had left in the Algonkian its close valley before Kralupy n. V. Besides its petrological composition, this terrace material differs strikingly with its coarser grain from that deposited by the Labe. The uppermost river sands and gravels at northern foot of Říp and on the Sovice hill (at a height of 278 m-130 m above the surface of the Labe) most probably date from the Latest Neogene (Pliocene). Pleistocene terraces have developed here at all levels. A detailed study enabled us to determine in this area a terrace system different from the one on the Vltava (compiled by Q. Záruba 1942). Seven large Pleistocene terrace accumulations were distinguished which is less than Q. Záruba had distinguished on the Vltava. From these terrace accumulations we have excluded levels formed by lateral river erosion. In this way 15 terrace levels could be determined on the whole. From a comparison with the longitudinal profile drawn by Q. Záruba, becomes evident that his terraces Ib and II a form a single terrace accumulation (our terrace III), just as terraces IIIa and IIIb (our terrace V) and terraces IVa and IVb (our terrace VII). The Eolian accumulation in the area under investigation was composed of loess cover and loess drifts mostly of Middle and Late Pleistocene age, and of sedimented sands which form sand dunes mostly of west-eastern direction reaching in places the height of 5-6 m. They were blown here in Würm from river deposits. Periglacial processes resulted in ice-wedges and solifluction which asserted itself most strikingly at the foot of the basalt hill Říp where it formed a continuous solifluction cover of Early and Middle Pleistocene age strewn with boulders mixed with cretaceous debris and Eolian sediments. Periglacial processes together with the Eolian activity caused the asymmetrical development of some valleys (the best example is the valley of the brook Čepel in the place where it heads from south to north). The river network in this area passed through an intricate development, especially in the place of the confluence of the Vltava and the Labe. Changes of similar kind can best be traced on enlarged surfaces of terraces. In the Earliest Pleistocene at the time of terrace I, the Vltava skirted the eastern foot of Říp and devided into two branches at the time of accumulation of terrace II. The western branch headed from Velvary northwards, the eastern branch followed the western brim of the Horní Beřkovice Plateau and the northern side of the Krabčice Plateau towards the Labe which it joined most probably east of Libkovice p. Ř. At the time of origin of terrase III, the Vltava headed from Veltrusy towards north-north-west to Roudnice n. L., and farther towards north-west to the Lower Ohře. Its second branch most probably flew along the eastern side of Říp. The river Vltava shifted its stream permanently at the time of terrace IV. This terrace follows the lower course of the Vltava and the Labe along its present valley. At the time of terrace V the river started forming a large meander north-west of Cítov. At that time also the Roudnice meanders started developing (and have kept on doing so up to the present), as indicated by B. Zahálka (1946). B. Zahálka presumes the main cause is the hill Sovice built of rocks hardened with basalt. The Cítov meander was abandoned by the river as early as in the erosion phase between terrace V and VI. Simultaneously with the origin of terrace VI the basalt Jenišovice hill was exhumed. The largest part of the Labe stream flew through the tectonic depression of Mělník, the side stream most probably through its present valley. At the time of terrace VII, the Vltava skirted on all sides the foot of the Jenišovice hill with the remains of the plateau of terrace VI. At the time following the origin of the terrace level VIIb, the Vltava was captured by the Labe in the place of their present confluence under Mělník, whereas before that the place of their confluence had been constantly moving up-stream. At the time of terrace VI both rivers most probably joined somewhere in the vicinity of Dolní Beřkovice. The most important factor for the development of relief in the area under investigation was the erosion and accumulation activity of rivers, which gave rise to terrace levels. In our opinion - based upon studies carried out in this area - during the deepening of the valley, after the accumulation of the terrace sediments, the river started cutting down into its own deposits, and forming - through lateral erosion - lower levels on the gradually narrowing valley floor. Through a further intense deepening, the river cut through its own sediments and their substratum down to the comparatively narrow floor of a more or less outstanding depression in the valley bottom, and is consequently the lowest place of the next terrace. In the period of accumulation, the river deposited first of all its sand-gravel load in this depression; upwards, valleys widened to the detriment of the deposits of higher-situated terraces and the cretaceous substratum. The upper layer of the terrace sediments was deposited as high as the level of the accumulation surface of the terrace. Processes of accumulation and lateral erosion participate in the origin of terraces. The main erosion phase of the development of the valley dates from the time succeeding the deposition of terrace IV, and from the time of the origin of Middle Pleistocene terraces, at which time valleys of main rivers and their tributaries were deepened. Valleys (mostly dry) and valley depresions, dividing plateaus of Middle and Early Pleistocene terraces in the area of the Říp plateau, originated already in Earlier Pleistocene and acquired their present form in Middle Pleistocene. In Later Pleistocene numerous short valley depressions were deepened no more. There are mostly fossil phenomena formed in periglacial climate in conection with the erosion phases of the main streams. The oldest network of valleys dating from as early as Younger Tertiary occurs on the right bank of the Labe in the Jizera Plateau and Polomené Hills. Practically no changes in the course of valleys took place in Pleistocene, they kept just on cutting down most intensively. The youngest erosion processes manifested themselves in the deepening both of valleys and valley depressions, and in the formation of deep gorges.

Quaternary sediments in the Binh Tri Thien coastal zone are diverse in both material composition and development history. From land to sea, there are 4 structural regions: i) marginal plain region; ii) Coastal lagoon region; iii) Coastal sand dunes region; and iv) Monocline coastal subsidence region. In the vertical direction, all four regions have five sedimentary cycles as follows: a) Early Pleistocene (Q11); b) Early middle Pleistocene (Q12a); c) Late middle Pleistocene (Q12b); d) Early late Pleistocene (Q13a); e) Late late Pleistocene (Q13b-Q2). Four structural zones are characterized by different lithofacies complexes: 1) In the lowstand systems tract (LST) at the beginning of each cycle in all 4 structural zones, the SmaLST facies complex is present; 2) In the transgressive systems tract (TST), there are the following lithofacies complexes: a) region I: MsbTST; b) region II: MlgTST; c) region III: SmTST; d) region IV: Msam,mTST; 3) In the highstand systems tract (HST) there are the following facies complexes: a) Region I: (MsabHST); b) Region II: MslgHST; c) Region III: SmvHST; d) Region IV: SmmHST. The difference in sedimentary facies in the transgressive and highstand systems tract depends on the differentiation of four geological structure regions.

Discovery of Enhydrictis (Mustelidae, Carnivora, Mammalia) cranium in Puwan, Dalian, Northeast China demonstrates repeated intracontinental migration during the Pleistocene

Since the oldest known Acheulean lithic techno-typological features in Europe were reported at the site of Barranc de la Boella (Tarragona, Spain), continuous fieldwork has been conducted there in archeological deposits of the late Early Pleistocene age (0.99–0.78 Ma). As a result, excavations in two of the three open-air localities have significantly expanded the collection of lithic and faunal remains, allowing us to make progress in the interpretation of the hominin behaviors in an open-air fluvial-deltaic sedimentary environment. This includes examples of cumulative palimpsests, such as those found at the locality of La Mina, in which hominins only had a minimal role as modifying agents, as well as the extraordinary mammoth butchery site recorded at the Pit 1 locality. The aim of this paper is to present a comprehensive update of the collection of large shaped tools and to assess its significance in the framework of the earliest occurrence of the Acheulean in Europe. This cultural entity is increasingly well-documented for the early Middle Pleistocene, but very little is known about its presence in Europe before the Brunhes–Matuyama boundary. Large shaped tools appear in the three localities explored in the Unit II of Barranc de la Boella, including choppers (unifacial and bifacial) and standard Acheulean forms, such as picks, knives, and cleaver-like forms. Techno-typological and morphometrical analyses revealed a basic heavy-duty component obtained through simple shaping sequences coupled with significantly more elaborate tools produced on various large blanks (cobbles, slabs, or flakes). The complete bifacial and bilateral shapings have yet to be documented, but the present specific tool assemblage attests to the Early Acheulean technological threshold. Hence, the archaeological data from Barranc de la Boella provide insights into the first appearance of the Acheulean technology in Europe and add critical information to the debate on the technological variability of the Early Pleistocene hominin occupation of the continent. The results of this study revealed a technological assemblage unique in the known late Early Pleistocene archeological record from Europe, different from the rest of ancient Acheulean sites in this continent, which are dated at the Middle Pleistocene. This lends support to the hypothesis that Barranc de la Boella may represent a previously unrecognized Early Acheulean dispersion out of Africa connected to its first evidence at the gates of Eurasia, potentially moving over the northern Mediterranean coastal road to reach Western Europe.

On the basis of the results of former studies by the present authors five main groups of bears are recognized: Ursus gr. minimus - thibetanus (black bears), Ursus gr. etruscus (etruscan bears), Ursus gr. arctos (brown bears), Ursus gr. deningei - spelaeus (cave bears) and Ursus gr. maritimus (white bears). Black bears seem to have disappeared from Europe during the Late Pliocene, immigrated again at the beginning of the Middle Pleistocene, and definitively died out in Europe at the beginning of the Late Pleistocene. Etruscan bears occur more or less contemporaneously in the southern areas of Europe and Asia during the Late Pliocene. The Asian branch apparently became extinct at the end of this period, while the European stock survived, giving rise to more advanced representatives during the Early Pleistocene. Brown bears seem to have originated in Asia. This group dispersed widely in holoarctic areas diversifying into a great number of varieties. They reached Europe presumably at the very end of the Early Pleistocene. The arrival of brown bears in Europe is a crucial event, which approximately coincides with the great faunal turnover which marks the Early-Middle Pleistocene transition. Brown bears replaced the etruscan bears, typical of the Villafranchian faunal assemblages, and gave rise to the cave bear line. Cave bears were very successful in Europe during the Middle and Late Pleistocene and disappeared at the end of the last glaciation or even at the very beginning of the Holocene. White bears presumably originated from northern Eurasian brown bear populations during the Late Pleistocene.

A reappraisal of the Early to Middle Pleistocene Italian Bovidae

The Early and early Middle Pleistocene context of human occupation and lowland glaciation in Britain and northern Europe

Pleistocene mammals of Mediterranean islands

Hominin distribution and density patterns in Pleistocene China: Climatic influences

Geomorphic context of two acheulian sites in semi-arid peninsular India: Inferring palaeoenvironment and chronology