Drift, evidently of Illinoian age, was deposited on St. Lawrence Island at the margin of an ice cap that covered the highlands of the Chukotka Peninsula of Siberia and spread far eastward on the continental shelf of northern Bering Sea. Underlying the drift on the northwestward part of the island are mollusk-bearing beds deposited during the Kotzebuan Transgression.

A comparison of mollusk faunas from St. Lawrence Island, Chukotka Peninsula, and Kotzebue Sound suggests that the present northward flow through Bering and Anadyr Straits was reversed during the Kotzebuan Transgression. Cold arctic water penetrated southward and southwestward bringing an arctic fauna to the Gulf of Anadyr. Warmer Pacific water probably entered eastern Bering Sea, passed eastward and northeastward around eastern and northern St. Lawrence Island, and then became entrained in the southward currents that passed through Anadyr Strait.

Vertical movements of the earth's surface related to postglacial rebound, the eustatic rise in sea level and the elastic deformation of the globe due to melting of late glacial ice sheets are calculated for simplified models of the earth. The movements of the ground are large and require a reevaluation of what is meant by eustatic sea level change. This is defined here as an ocean-wide average change in mean sea level and its measurement requires widely distributed observations weighted according to the areas of oceans they represent. Evidence of a postglacial (6000-0 years BP) relative rise in sea level comes largely from regions affected by ground subsidence related to adjacent upward postglacial rebound movements in deglaciated areas: evidence for a relative fall of sea level comes from coastlines well removed from areas of rebound and which have been affected by a rise of the continental areas through compensation for the eustatic load. It is concluded: (1) no substantial eustatic change of sea level in the past 6,000 years is required to explain postglacial sea levels: (2) in late glacial time the eustatic curve is probably more like the sea level curve of Texas and Mexico than that of the Atlantic seaboard of the United States: (3) that the information of past sea levels, when sufficiently widespread, can provide an important method of studying the deep mechanical structure of the earth.

A reexamination of the sequences of planktonic foraminifers and calcareous nannoplankton in the Plio-Pleistocene sediments beneath the Louisiana continental shelf has been undertaken in order to modernize correlation schemes that were established 10–20 y.a. As a consequence, it can be shown that (1) a new correlation of marine micropaleontological and continental glacial events is necessary; (2) the Gulf Coast faunal events can be reliably correlated with those in the type Italian Pleistocene section and in the deep-sea cores; (3) it is becoming increasingly evident that it is invalid to correlate the Plio-Pleistocene boundary, as defined by paleontology, with a climatically defined boundary.

Oxygen isotopic analysis and absolute dating of deep-sea cores show that temperatures as high as those of today occurred for only about 10% of the time during the past half million years. The shortness of the high temperature intervals (“hypsithermals”) suggests a precarious environmental balance, a condition which makes man's interference with the environment during the present hypsithermal extremely critical. This precarious balance must be stabilized if a new glaciation or total deglaciation is to be avoided.

Presently submerged Bahaman stalagmites can be used to date Pleistocene low sea level stands. Good precision was obtained using both 14C and 230Th-/234U-methods. The respective dates obtained were 21,900 ± 600 and 22,000 ± 350 YBP.

A decision appears imminent to define the lower boundary of the Holocene formally in terms of the European sequence, as comprising all or part of the interval between the end of the Bølling Interstade and the end of the Younger Dryas Stade (ca. 12,100–10,350 14C years BP). However, a lower boundary in this position can define the base of a European provincial stage only (the Flandrian). The interval contains no boundary suitable for global use, because temperature trends in many parts of the north polar and north temperate regions, including Europe, were then distorted by vast masses of melting ice inherited from Full-Glacial times. The last unquestionably worldwide major climatic event before the Hypsithermal Interval was the sharp cooling that has been inferred from glacier advances culminating about 14,500–14,000 14C years BP, and consequently the horizon at the transition from cooling to warming at the end of this episode should be defined as the base of the Holocene.

Nelson Bay Cave is located on the Robberg Peninsula (34°06′ S, 23°24′ E) at Plettenberg Bay, Cape Province, South Africa. Excavation of the Late Quaternary fill of the cave has provided a rich assemblage of mammalian remains dated between ca. 18,000 and 5000 radiocarbon years B.P. Identification and analysis of these remains has shown that important changes in the composition of the mammalian fauna took place first about 12,000 B.P. and again about 9000 B.P. The earlier change is especially clear-cut and is interpreted to reflect the disappearance of grassland from the area as well as the influence of rising sea level. Both faunal changes were accompanied by changes in associated artifactual materials and it is suggested that faunal and cultural changes were causally linked. The mammalian species dated between 18,000 and 12,000 B.P. include the latest recorded Sub-Saharan occurrences of some extinct taxa and indicate that terminal Pleistocene/Early Holocene megafaunal extinctions may have been more important in Southern Africa than has hitherto been thought.

The lower Omo basin, southern Ethiopia, preserves formations of sedimentary and pyroclastic rocks which span a substantial range of later Cenozoic time. These formations are often extraordinarily rich in vertebrate fossils and have also afforded a series of molluscan assemblages from contexts radiometrically dated by K/Ar or 14C. The late Cenozoic molluscan fauna has been previously ill-known in this part of Africa and these assemblages provide a broad faunal zonation for the northern sector of the Eastern Rift valley. The five principal assemblages are here treated as faunal groupings, rather than as formal faunal zones. Three groupings are recognized for the Pliocene/Pleistocene time range, one grouping for the later Pleistocene and one grouping for the subrecent and present.

The southeastern coast of South Africa's Cape Province underwent complex geomorphic evolution during the late Cenozoic, leaving a variety of erosional forms and a detailed, complementary record of distinctive sediments. The latter include several new lithostratigraphic units and paleosol horizons. An almost ubiquitous planation surface, the 200-m Coastal Platform, is associated with the fanglomeratic and deltaic Keurbooms Formation (late Tertiary?). A major sea level at +120 m truncated a laterite paleosol and was followed by accumulation of land rubble and littoral deposits to 101 m, constituting the Formosa Formation. Then follow sea level stages at +60, +30, and +15–20 m, as well as several generations of weathered eolianite, including the Brakkloof Formation with the deep superposed Brakkloof Soil. Beaches at +5–12 m, with thermophile mollusca and C14 dates of >40,000 yr mark the Swartkops horizon, probably of Eem interglacial age. Next are cryoclastic screes and cave deposits, and ultimately the podsolic Brenton Soil of the Würm Interpleniglacial. Transgressive eolianites and coastal dunes after 16,000 BP were interrupted by pedogenesis ca. 7500 BP and stabilized after 4200 BP when sea level reached +2.5 m. Geomorphic instability in stream valleys after 1000 BP was followed by man-induced activation of the coastal dunes, since the late 18th century. Environmental patterns accompanying this succession at various times included (1) semiarid pediplanation, (2) interior dune formation, and (3) intensive, cold-climate denudation, all under open vegetation in what is now closed, humid forest; by contrast, some of the more aberrant paleosols indicate warmer, perhumid conditions.

Pollen studies of the four European interglacial intervals indicate a strong similarity in vegetational sequence: a pretemperate phase (I) marks the late glacial, early temperate (II) and late temperate (III) phases mark the interglacial proper, and a posttemperate phase (IV) represents the beginning of the next cold period. A grossly similar record is now known for the last interglacial (Sangamon) of central and southeastern United States. The Holocene sequence in both Europe and America are completely typical of the interglacial sequence, although much more is known of the geographic variations.

Estimates for the duration of the interglacials range from 10,000 to more than 30,000 yr, according to counts of the annually laminated sediments (organic varves).

The Holocene has already run a course of at least 10,000 yr. If it is like earlier interglacials, it will end soon, giving way to gradually developing cold conditions, which may not lead to glacial maxima for tens of thousands of years.

A suite of four terraces in the upper Rio Henares drainage system (Rio Tajo basin) now provides a partial geomorphological link between the Middle Pleistocene, Lower Paleolithic archeological sites at Ambrona and Torralba (upper Ebro basin) and those in the vicinity of Madrid. The Campiña and Low Terrace features are shown by radiocarbon dating to be of Holocene and Würm ages, respectively, while the Middle and High Terraces are best designated as being Middle and Lower Pleistocene ages, respectively. Stratigraphic relationships between the upper and lower Rio Henares segments need to be established.

A “glacial cycle” is defined as a major global climatic oscillation of the order of 105 yr, developed within an “ice age” sensu lato which may last 106–107 yr and which recurs at widely spaced intervals in geologic time (ca. 2 × 108 yr). The ice age situation thus only persists during 5–10% of all geologic time and is preconditioned by geotectonics and not by extraterrestrial controls.

The repetitive nature of the glacial cycle is demonstrated by independent records from (a) glacigenic, ice-melt deposits, i.e., tills and fluvioglacial terrace accumulations; (b) eolian by-products, i.e., loess; (c) marine terraces and beach deposits, eustasy inversely reflecting the ice volumes; and (d) deep-sea deposits, biologically and lithologically reflecting the climatic events. Only the marine section offers a continuous, uninterrupted record. Different chronometric techniques confirm a major cycle of the order of 105 yr (eight repetitions in the last 700,000 yr), but there are multiple types of modulation, in part related to self-accelerating feedback, either negative (retardation) or positive, leading to acceleration.

Within any given cycle there is an Interglacial, Anaglacial, Pleniglacial and Kataglacial phase, characteristics of which are repeated on a small scale in minor cycles. Their timing is variable in a latitudinal sense, apparently steered by radiation changes that first affect the tropics.

Interglacials are defined in their classical stratotype areas of NW Europe, by sedimentary sequences characterized by the pollen of deciduous forests, pointing to climates at least as warm as those of the present time. The present cycle began ca. 10,000 YBP, with the start of the Holocene epoch, and the contemporary warm phase is seen as a typical interglacial stage. Such warm peaks characteristically last about 10,000 yr. Symptoms of the expected ensuing glaciation range from a global fall in temperature since mid Holocene, to tropical desiccation (growth of deserts) and high latitude retreat of tree lines.

Four new radiocarbon dates of elevated strandlines in tectonically active areas of eastern Indonesia and East Malaysia indicate average rates of uplift that range between 4.5 and 9 mm annually during the past 24,000 yr. These values are at least three times higher than former estimates from eastern Indonesia. Another radiocarbon date from the south arm of Sulawesi—also tectonically mobile—indicates a rate of uplift of 1.4–2.5 mm per year which corresponds with earlier determinations. This particular case, however, suggests that the sample was probably located close to a north-south axis about which southern Sulawesi was tilted during the Quaternary.

In the Langkawi islands, West Malaysia, one of the regionally ubiquitous shorelines at about 2 m above sea level was dated at 2590 ± 100 yr BP which corresponds with Fairbridge's (1961) Abrolhos Submergence.

The distribution of planktonic foraminifera has been studied in 28 piston cores of Late Pleistocene age from the western Gulf of Mexico. Detailed correlation between the cores has been made possible by a high degree of similarity of frequency changes within several species; by coiling direction changes within Globorotalia truncatulinoides; by a datum level representing the near extinction of Globorotalia menardii flexuosa, and Globorotaloides hexagona at the end of the last interglacial; by three distinct volcanic ash horizons, and by calcium carbonate dissolution effects at distinct intervals. Almost all species demonstrate distinct frequency oscillations that are correlatable between cores. A high proportion of these are clearly related to paleoclimatic oscillations and reflect rapidly changing water-mass conditions within the Gulf of Mexico during the latest Pleistocene. No interval appears to have been represented by stable environmental conditions. Causes of frequency changes within several other species are not clearly related to inferred paleoenvironmental changes. High similarity of faunas exists at all times between the northwest and southwest Gulf of Mexico, reflecting similarity of water-mass conditions over a wide latitudinal range. High sedimentation rates, which average between 10 cm/1000 years and 30 cm/1000 years, have enabled a detailed paleoclimatic curve to be established for the last 200,000 years. Three interglacials and two glacials are recognized. Distinct foraminiferal assemblages have enabled definition of 18 zones most of which are related to paleoclimatic changes. Most intense coolings occurred at the end of the penultimate glaciation (zone W) and during the middle of the Wisconsin glaciation (zone Y).

The Gulf of Mexico curve is somewhat similar to those of other regions based on O18/O16 ratios, except that, despite close control, no intense cooling is apparent near the end of the last glaciation. The most sensitive warm water indicators are the G. menardii complex and Pulleniatina obliquiloculata; the most sensitive cooler water forms are Globorotalia inflata, and Globigerina falconensis. Several species have intermediate temperature tolerances. Much climatic information is lost when only the G. menardii complex is utilized in climatic studies, because these forms are essentially absent during glacial episodes. The most distinct faunal change associated with the Holocene warming does not coincide with the Z-Y boundary defined by the first consistent occurrence of G. menardii but occurs slightly earlier during the latest Wisconsin. The X zone, based on the consistent occurrence of the G. menardii group is of shorter duration in Gulf of Mexico cores than in cores from the central Caribbean Sea and the equatorial Atlantic Ocean.

Three major volcanic ash horizons coincide with climatic coolings; almost immediately preceding the last interglacial (135,000 years B.P.); towards the end of the last interglacial (end of zone X; 90–95,000 years B.P.), and in the earliest part of the last glaciation (75,000 years B.P.). A drastic reduction of G. menardii flexuosa and G. hexagona coincides with the middle ash horizon.

Quaternary occurrences of voles of the genus Phenacomys south of the North American continental glaciation range in age from Kansan through early Recent times and are mapped from twenty fossil localities. Phenacomys cannot be used as an index fossil, but makes a good climatic indicator because of its modern boreal affinities. It is largely confined to the present day Canadian and Hudsonian Life Zones of North America.

Canonical correlation analysis provides a means of reconstructing quantitative time series of past climatic variables during the last 15,000 years from fossil pollen spectra collected at three sites in the northern Midwest. This multivariate statistical technique was applied to a spatial array of modern pollen and climatic data in order to derive a set of mathematical transfer functions. These transform the fossil pollen spectra directly into quantitative estimates of past climatic values. The basic sequence of climatic events that is reconstructed is in general agreement with previous studies of postglacial climates in the Midwest, but quantitative estimates for certain of the variables, e.g., temperature and precipitation, are given for the first time.

Fossil pollen from three cores collected from lakes in Wisconsin and Minnesota allow a preliminary reconstruction of past east-west and north-south gradients of the climatic variables. Because changes in the circulation patterns in midlatitudes are the principal mechanism causing fluctuations in temperature and precipitation, past records of the atmospheric circulation are reconstructed along with records of temperature and rainfall. The time series derived show that the most pronounced climatic change indicated in Wisconsin and Minnesota occurred at the end of the Pleistocene (the beginning of the Holocene). This change is particularly evident in the climatic variables related to temperature, which rose ca. 3.3°C. A decrease in snowfall also occurred.

During the Holocene, the most marked change appears in the results from Kirchner Marsh, where the amount of dry western air began to increase and the precipitation to decrease about 9500 B.P. A reversal of these changes occurred about 5000 B.P. In contrast, relatively little change occurred among the reconstructed values from Wisconsin; a marked east-west precipitation gradient, therefore, developed in this region of the Midwest from 9500 to 5000 B.P.

The Mosbeck Site is in the southern part of the Lake Agassiz basin in northwestern Minnesota. The stratigraphic section at the site consists of seven lithologic units, which are from bottom to top (A) unsorted, pebbly, sandy, silty clay, (B) coarse gravel, (C) silty sand, (D) peat, (E) fine sand, (F) interbedded sand and gravel, and (G) unbedded dirty gravel. The lower few centimeters of unit E are unoxidized and contain black spruce and tamarack driftwood, which has been radiocarbon dated at 9940 ± 160 BP (I-3880). Units C-E contain numerous, well-preserved insect and mollusk remains. These fossils have been compared with modern species, and at least 76 insect and 15 mollusk taxa are present. Assuming that their ecological tolerances have changed little in the past 10,000 years, they provide valuable information about the environment of Lake Agassiz. Few of the insects are now found in the region, indicating that the environment has changed. With few exceptions the species present indicate that the climate and vegetation at the time were similar to the present-day climate and vegetation of southeastern Manitoba.

The lithology and faunal contents of the sediment are interpreted as follows. Unit A is Late Wisconsinan glacial sediment. Unit B is a lag concentrate formed by wave action during a regressive phase of Lake Agassiz. Unit C is the sediment of a small body of water that formed when the level of Lake Agassiz had dropped below the site. The banks were covered with a spruce forest. Open water gave way to swampy conditions, and unit D was formed. Both units C and D were deposited during the low-water Moorhead Phase of Lake Agassiz. Units E and F are shoreline sediment deposited as the lake level rose, drowning the vegetation. Unit G is modern ditch spoil.

A series of radiocarbon determinations have been carried out of lacustrine deposits contained in three playa basins, namely at Sambhar, Didwana and Lunkaransar, in Rajasthan, in conjunction with stratigraphical and palynological investigations. It is revealed that the lake deposits, which overlie thick beds of sand at each site, date back from early Holocene times (ca. 10,000 B.P.).

The authors present the radiocarbon evidence together with an outline of the stratigraphy of the deposits, and attempt to reconstruct the sedimentary sequence in the three basins since the beginning of the lacustrine phase. The significance of the more or less synchronous development in all the three playa basins is discussed with reference to postglacial climatic oscillations in northwest India.

Much of Baffin Island is close to the modern glaciation limit and climatic changes within the last decade are already being reflected in snow cover extent. Statistical analysis of glacierized and ice-free corries indicates that changes in direct solar radiation due to astronomical factors are inadequate to account for glacierization of those at present ice-free. These and other sources of evidence demonstrate the need for augmented winter snowfall in order to increase the extent of glacierization. The pattern of glacial history in this area is for maximum ice extent during the early glacial phase (>68,000, <137,000 BP), followed by a reduction in ice volume during the cold pleniglacial (>24,000, < 68,000 BP) and then a limited late glacial advance (the Cockburn Stade, ca. 8,000 BP) due to increased precipitation. The Barnes Ice Cap did not disappear in the Holocene as it did in the last interglacial. The area is highly suitable for long-term monitoring of climatic change and glacial response.