In the history of Western thought, the philosophical study of man has been part of the philosopher's pursuits from the time of the ancient Greeks. But after a lapse of over two thousand years, the study in this field remains not much developed and its achievements are far from satisfactory. Already in 1928, Max Scheler in his Man's Place in Nature pointed out the troubled condition of the philosophical study of man: “Man is more a problem to himself at the present time than ever before in all recorded history… We do not have a unified idea of man. The increasing multiplicity of the special sciences, valuable as they are, tend to hide man's nature more than reveal it.” In more recent times, Paul Ricoeur, although approaching the issue from a somewhat different perspective, nevertheless came to a similar conclusion. In his essay The Antinomy of Human Reality and the Problem of Philosophical Anthropology, he stated: “The sciences of man are dispersed into separate disciplines and literally do not know what they are talking about.” It seems to me that part of the explanation for this Situation lies in the way of thinking of Western learning, with its peculiar segmentation of fields of inquiry. During this century, some branches of human sciences, such as psychology, sociology, ethnology, political science, economics and psychoanalysis, have developed rapidly. They deal with the study of man from different angles, and have really accumulated a rich wealth of data. But what man is as such is still not clear. Unless we succeed in forming a comprehensive view of man as a whole, we will not be able to have a real insight into human nature and will be lost in a mass of disconnected and isolated data which seem to lack conceptual unity. We must recognize that the sciences of man in the contemporary Western world belong exclusively to the Western cultural tradition which originated in the early Greek civilization with its own concepts of values. They are entirely divorced from the other great cultures of the world, for instance, the Indian and Chinese cultures, which are as important as the Greek culture in the history of civilization. In order to reach a deeper understanding of man, it is perhaps necessary to make cross-cultural comparative studies. Therefore a short survey of the studies of man in ancient Chinese philosophy may not be superfluous. I would like to confine my survey to the early Chinese philosophers of the pre-Qin period, not only because it is almost impossible to deal with the entire history of Chinese philosophical ideas spanning over two thousand years in an article, but also because the ancient time is the most creative and most important period in the development of Chinese thought.

Alliances in the aristocracy of the Republic, that theme has engaged eager and assiduous study in the recent time. Not without the danger of exaggerations and schematism. In consequence, abundant controversy. Moreover, tedium ensues when the method is applied to periods devoid of testimony about persons who can be grasped as persons.

The rate of vapor-phase sorption of tetrahydrofuran (THF), tetrahydropyran (THP), and 1,4-dioxan (DIOX) onto a Wyoming montmorillonite saturated with Al3+ or Cr3+ has been studied by isothermal gravimetry in the temperature range 18° to 105°C using samples of different weights and grain-size distributions. The rate of sorption for all the cyclic ethers increased with decreasing sample and grain size, demonstrating that inter-, rather than intraparticle mass transfer was rate-determining. Optimization of the sample parameters (2 mg sample of <45-μm grain size, pretreated at 120°C yielded integral diffusion coefficients at 18°C of 0.5 × 10−14 m2/s for DIOX for the Cr3+-clay to 3.5 × 10−4 m2/s for THF for the Al3+-clay; however, no temperature or cationic dependence of the cyclic ether uptake was observed. In general, the rate of sorption of the cyclic ethers increased as THF ≥ THP > DIOX indicating that the sorption rate of THF and THP was dependent on concentration or that DIOX sorption was retarded by bidentate coordination to aluminum ions at the edges of the clay platelets.

Hydrothermal chlorite replaces igneous biotite in the Gold Hill, Utah, quartz monzonite. Chemical compositions of coexisting biotite and chlorite determined by electron microprobe and wet chemical methods were used to evaluate chemical mass transfer during the alteration process. The mole ratio Mg/(Mg + Fe) varies from 0.52 to 0.65 in the chlorite and from 0.51 to 0.60 in the parent biotite. The Mg content of the chlorite decreases systematically with increase in the volume percent replacement of biotite. Homogenization temperatures of fluid inclusions in nearby quartz microveinlets indicate that the chloritic alteration took place at approximately 200°C.

Textural relationships suggest that the alteration of biotite to chlorite is isovolumetric, but a comparison of mineral compositions and mineral assemblages with phase diagrams in which Al or volume are conserved among solid phases suggests that the chlorite compositions are best explained as a function of reaction progress in an Al-conservative system. The chlorite composition changes in response to changes in solution composition produced by the dissolution of successive small amounts of biotite. Representative mass balance for the alteration of all of the biotite to chlorite in 1 m3 of rock containing 336 moles of biotite indicates that 74 moles of Mg, 35 moles of Fe3+, 420 moles of H+, and 2 moles of Mn are added to the rock and that 311 moles of K, 54 moles of Fe2+, 76 moles of Ti, 53 moles of F, and 6 moles of Cl are lost to solution. The mass transfer for partially altered biotite is 11 to 188 moles of K, 2 to 46 moles of Ti, 2 to 44 moles of F, and 0.3 to 6 moles of Cl removed per cubic meter of rock and 1 to 26 moles of Fe3+ and 20 to 347 moles of H+ added. The mass transfer of Mg varies from 12 moles added to 32 moles removed per cubic meter of rock depending on mineral composition and extent of replacement.

Well over five thousand languages are known to exist or to have existed in the world, but hundreds of these are no longer living languages used by speakers and speech communities in their day-to-day activities and lives. Some of them lead a pseudolife as revered monuments of the past which still have some restricted and specialised roles to play today, such as Latin, Ancient Greek, Church Slavonic and others, but most of them are of interest and concern only to a small group of linguists, historians and some other experts who look at the past. Many languages have disappeared without being known to us in any great detail, with only some fragmentary materials in them - written or noted down by speakers or observers of them hundreds or even thousands of years ago - at our disposal to give us some idea as to what those languages were like. Others have disappeared without even that scanty information about their nature being available to us; only their names are known from historical records, or perhaps some remarks were written down by someone many years ago and were preserved over the ages to tell us something about some special features of such a language or such languages and who and what kind of people their speakers were. Many other languages, certainly a much larger number than the dead languages about which we know something, have disappeared without our knowing anything of or about them.

Raman and Fourier-transformed infrared spectra of natural trioctahedral chlorites of polytype IIb were obtained for a series of samples characterized by distinct Fe/(Fe + Mg) and Si/Al ratios ranging, respectively, from 0.04 to 0.94 and from 5.18 to 1.86. All samples were characterized by X-ray powder diffraction, and quantitative electron microprobe analysis. In the 3683-3610-cm−1 spectral range, the wave number of the OH-stretching band from the 2:1 layer (band I) decreased with an increase of iron content at constant Al(IV) content. The more intense bands II and III at about 3600 cm−1 and 3500 cm−1, were assigned to hydroxyl groups involved in hydrogen bonds: (SiSi)O... HO, with the hydrogen bonds being roughly perpendicular to the basal plane, and (SiAl)O... HO, respectively. At higher tetrahedral Al and octahedral Fe contents, spectra exhibited OH-bands II and III, respectively, at a lower frequency. Band III intensity increased and band II was enlarged for chlorites displaying higher Al(IV) contents.

In the 1300–1350-cm−1 spectral range, most infrared spectra displayed intense bands at 1090, 1050, 990, and 960 cm−1, which were assigned to T-O stretching of symmetry species Al and E1. The second type of bands observed both in Raman and infrared spectra were at about 650–800 cm−1; they were assigned to OH vibrations and were strongly dependent on the composition of the interlayer octahedral sheet, especially on the Fe content.

The earliest Chinese record of the maritime relations between India and China can be found in the “History of the Former Han Dynasty” (Chien Han-shu) which covers the period from B.C. 206 to A.D. 23. In its chapter (28b) on geography it is stated that ever since the time of the Emperor Wu (Wu Ti, B.C. 14087) the country called Huang-chih has sent tribute to the Chinese court, which in turn dispatched envoys to this remote country. Huang-chih has been identified by many scholars with Kāñcī (Conjeeveram) on the east coast of South India. It is recorded that there were chief interpreters belonging to the Yellow Gate (the office of eunuchs serving in the palace) who went to sea to buy bright pearls, opaque glasses and other rare articles, taking with them from China gold and various kinds of silk for exchange.

Even in scientific usage there are terms that we believe we understand and when we try to pinpoint what they refer to we notice that these terms do not have a precise meaning. This applies, in linguistics, to the term Indo-European. Mostly, when used as an adjective, it seems to apply to those languages that derive, hypothetically, from a disappeared idiom which some scholars for nearly two hundred years have been trying to reconstruct. Thus, it is said that Sanskrit, Greek and Latin are Indo-European languages. When this epithet is applied to French it causes surprise. From a comparative viewpoint, French is usually seen as a Romance language and only Romance languages taken together or, better said, Latin from which they derive, seem to merit the epithet. When used as a noun, “Indo-European” may designate the disappeared language itself. But serious scholars give it a precision in this case like commun in French, proto in English or Ur- in German. Does this imply that we may designate as Indo-European the sum of the individual languages of this family, whether they still exist or have disappeared? One may indeed take a chance and do it, but not without startling or even shocking one's public.

Authigenic, well-crystallized kaolinite and dickite occur within sulfide mineral deposits (mine-size to hand-specimen size occurrences) of the Mississippi Valley type in Arkansas, Kansas, Missouri, Iowa, Wisconsin, Illinois, and Indiana. Fluid inclusions in these rocks indicate temperatures of formation as high as 140°C. These authigenic kaolin-group minerals are probable geologic indicators of a regional thermal event. Such elevated temperatures are probably the result of heated waters derived from deeply buried sedimentary or tectonic basins, of passage of the region over a hot spot, or of an episode of thinning of the crustal plate in the mid-continent region.

Inspired by Columbus, Spaniards set out on an adventurous voyage of the circumnavigation of the globe and, to their surprise, encountered a new continent.

This is the essential fact. There were no preliminaries, no previous knowledge, but an abrupt and unexpected meeting between a handful of men who represented the mentality of Spain at the end of the 15th century and an immense geographical panorama that slowly and continuously unfolded, populated by beings for whom there was not even a name and who represented native cultures in different stages of devopment with no previous contact with Europeans, almost diametrically opposed in values, concepts and mentalities to what the transatlantic navigators represented and brought with them.

Classification and identification criteria of maximum-degree-of-order (MDO) polytypes of homo- and meso-octahedral micas based on the distribution of the intensities of 20l (13l) and 02l reflections are proposed. Calculated | F(20l) |2 and | F(02l) |2 values for single crystals of micas with different compositions are given for one-, two-, and three-layer polytypes. Transmission powder diffractometry is proposed as a suitable method for the identification of the different groups of mica polytypes from polycrystalline specimens. Calculated powder patterns and the characteristic properties of the diffraction patterns of random and highly oriented aggregates are employed for identification purposes. The individual MDO polytypes are designated by generalized Ramsdell symbols which also contain information about their position in the classification system.

Yucca Mountain is being studied as a potential site in southern Nevada for an underground, high-level nuclear waste repository. A major consideration for selecting this site is the presence of abundant zeolites in Miocene ash-flow tuffs underlying the region. Beneath Yucca Mountain four diagenetic mineral zones have been recognized that become progressively less hydrous with depth.

Zone I, the shallowest zone, is 375–584 m thick in the central part of Yucca Mountain, but 170 m thick to the north. Zone I contains vitric tuffs that consist of unaltered volcanic glass and minor smectite, opal, heulandite, and Ca-rich clinoptilolite. Zone II thins south to north from 700 to 480 m and is characterized by complete replacement of volcanic glass by clinoptilolite with and without mordenite, and by lesser amounts of opal, K-feldspar, quartz, and smectite. Zone III thins south to north from 400 to 98 m thick and consists of analcime, K-feldspar, quartz, and minor calcite and smectite. Heulandite occurs locally at the top of zone III in the eastern part of Yucca Mountain. Zone IV occurs in the deepest structural levels of the volcanic pile and is characterized by albite, K-feldspar, quartz, and minor calcite and smectite.

Clinoptilolite and heulandites in zone I have uniform Ca-rich compositions (60–90 mole % Ca) and Si:Al ratios that are mainly between 4.0 and 4.6. In contrast, clinoptilolites deeper in the volcanic sequence have highly variable compositions that vary vertically and laterally. Deeper clinoptilolites in the eastern part of Yucca Mountain are calcic-potassic and tend to become more calcium-rich with depth. Clinoptilolites at equivalent stratigraphic levels on the western side of Yucca Mountain have sodic-potassic compositions and tend to become more sodium-rich with depth. Despite their differences in exchangeable cation compositions these two deeper compositional suites have similar Si:Al ratios, generally between 4.4 and 5.0. Analcimes have nearly pure end-member compositions, typical of these minerals formed by diagenetic alteration of siliceous volcanic glass; however, K-feldspars are Si-rich compared to the ideal feldspar formula.

Bulk-rock contents of Si, Na, K, Ca, and Mg of zeolitic tuffs generally differ significantly from stratigraphically equivalent vitric tuffs, suggesting that zeolite diagenesis took place in an open chemical system. Both the whole rock and the clinoptilolite are relatively rich in Ca and Mg in the eastern part of Yucca Mountain and rich in Na in the western part. The Ca- and Mg-rich compositions of the zeolitized tuffs in the eastern part of Yucca Mountain may be due to cation exchange by the sorptive minerals with ground water partially derived from underlying Paleozoic carbonate aquifers.

Diagenetic zones become thinner and occur at stratigraphically higher levels from south to north across Yucca Mountain, probably due to a higher geothermal gradient in the northern part of the area. The diagenetic zones were established when the geothermal gradient was greater than it is today, probably during the thermal event associated with the development of the Timber Mountain-Oasis Valley caldera complex north of Yucca Mountain.

These observations are an extension of those of a friend, the late Mircea Eliade, who more than once dealt with the problem of time. Philosophers have long been interested in this problem, which obviously concerns all of us. The nature of Eliade's preoccupations obliged him, but aside from that, we sense that the subject was close to his heart and that what he called “the terror of history” was a fundamental problem for him. He spoke of it at length in Le Sacré et le profane, in Le Mythe de l’éternel retour, in Images et symboles. His approach was that of a moralist and philosopher, but we know that this distinguished scholar was in reality an encyclopedist.

“There is not, nor has there ever been, ideology,” write Deleuze and Guatter. This sybiiline aphorism is surely true: an ideology is never more than rationalizing and justifying behavior, which convinces no one but the already convinced and amuses or bores the others. It is thus a small thing in comparison with the random wandering of thought throughout history and the arbitrariness of cultures, “nurtures: “ since Nietzsche, or a certain aspect of Nietzsche, taught us to be in despair of the Truth, we can no longer impute this wandering and this arbitrariness to the distortion of who knows what natural light by ideology.

A complete conversion series for mica/smectites was found in a hydrothermal alteration envelope around Kuroko-type ore deposits at the Shinzan area, Akita Prefecture, Northeast Japan. The minerals are an alteration product of volcanic glass of Miocene age and are commonly associated with zeolites and silica minerals. Degrees of ordering of interstratification of the minerals change discontinuously from Reichweite g = 0 (100–55% expandable layers) to g = 1 (45–20% expandable layers), and from g = 1 to g = 2 (<20% expandable layers). This pattern of conversion differs from the behavior of mica/smectites during burial diagenesis which undergo a continuous change in ordering type, and from the behavior of rectorite which displays a constant expandability and ordering (45–55%) over a wide range of conditions. Differences between these minerals were also found in the relationships between expandability and total layer charge, and between expandability and number of non-exchangeable interlayer cations. In mica/smectites from the Shinzan area, chemical changes in the interlayers and tetrahedral and octahedral sites are consistent with a reaction in which K-enrichment and K-fixation in the interlayers are controlled by an increase in negative layer charge. This conversion occurred in response to a steep geothermal gradient and migrating hydrothermal solutions.

Bis-ethyl 2-hexylphosphoric acid (di-2 EHPA) dissolved in decane is chemisorbed on kaolinite and montmorillonite dispersed in an acidic aqueous solution. The adsorption results in the formation of complexes with the surface cations of the clays. The adsorption isotherms are of the Langmuir type and reveal a limiting value of adsorption on H+-kaolinite of 12.2 mg/g, comparable to that measured in the absence of water. For H+-montmorillonite, however, the limiting value in the presence of acid is somewhat less (20.6 mg/g vs. 23.8 mg/g). Di-2 EHPA does not react with the magnesium cations available at the surface. The isotherm is “stepped” and suggests the presence of adsorption sites with distinctly differentiated energies. The sites of di-2 EHPA adsorption can be masked by treating the two clay minerals with polyphosphate anions. Thus, with pyro- and tripolyphosphate anions, di-2 EHPA uptake in acidic medium is very low. Adsorbed di-2 EHPA can be recovered by treating the clays with fluoride, hydroxyl, and dihydrogenphosphate anions. Dihydrogenphosphate anions lead, however, to a state of equilibrium between the organic and inorganic phosphate anions adsorbed.

The Cs selectivity of several natural zeolitic tuffs and synthetic zeolites was measured. Phillipsite-rich tuffs from California and Nevada exchanged 13.5 and 23.7%, respectively, of the Cs present in simulated alkaline defense waste containing 0.00025 M CsCl in 5.5 M NaCl-NaOH solution from the Savannah River Plant, Aiken, South Carolina; whereas mordenite-rich tuffs from Arizona and Nevada exchanged less than 12.7%. The immobilization or fixation of Cs in phillipsite unlike other zeolites can be achieved by heating the zeolite at 600°C for 4 hr in air and collapsing the silicate (aluminate) tetrahedral rings around the Cs ions to produce a Cs-feldspar-type phase. Treatment of the Cs-exchanged phillipsite-rich tuff at 800° to 1000°C resulted in pollucite, CsAlSi2O6, which also “locks in” the Cs ions in its structure. The fixation of Cs exchanged in phillipsite can also be achieved by the formation of pollucite upon hydrothermal treatment at 300°C and 30 MPa pressure within 12 hr. These results suggest that phillipsite-rich tuffs are good candidates for Cs immobilization by heat treatment at low temperatures after they have been used as sorbents in waste decontamination.