On August 27, 1992, the General Motors (GM) auto plant in Van Nuys closed after a half-century serving the Northeast San Fernando Valley. Its closure undercut the livelihoods of auto workers like Raymond Álvarez and his father Ramón. Today, the father and son duo look at “The Plant,” an outdoor shopping mall, and wonder whether the In-N-Out fast-food restaurant or T-Mobile store marks where they once stood on the assembly line. The departure of the GM plant and other long-standing manufacturing firms propelled the area into economic distress as Los Angeles was reeling from another crisis, the 1992 Uprising. In the wake of these events, elected officials clamored to revitalize the city. Six years later, “revitalization” came in the form of the shopping center, The Plant. By tracing the historical trajectory of one shuttered auto plant, from factory to shopping mall, this article demonstrates how neoliberal ideology gained legitimacy over the last several decades.

It follows from the temporal nature of mind—the main concern of this essay—that mind functions are not localized in brain space.“ Time is extendedness, probably of the mind itself”, concludes Saint Augustine in Book XI of his Confessions (26.33), and, in our days, this extendedness can be made visible through an oscilloscopic “line” or trace of slow potentials. These graded, additive (not all-or-none) autorhythmic and seemingly self-generating potentials are primary events recorded at synapses. Autorhythmic brain structures (Zabara, 1973) appear to be the source of time frames, while a change in time frames (as reflected in the EEG) leads to synchronization and desynchronization of brain structures respectively. Synchronization forms a homogeneous time domain, such as obtained during rhythmic exercises, chanting, listening to music and mental processes that are the hallmark of religious practices (Rogers, 1973). Desynchronization of brain structures on the other hand marks a functional independence of neuronal elements with each element available for separate channels of data processing, for example, during hallucinogenic drug-induced central sympathetic arousal, that is, a waking dream state (Fischer, 1979).

Our thinking is still the captive of the dichotomy “national/ international.” The reaction to nationalism takes the form of an abstract internationalism, and reaction to internationalism leads to the rebirth of nationalism. However, this dichotomy was only true (and that relatively) in 19th century Europe, or at the latest, at the beginning of the twentieth century, when subnational cultures seemed on the way to disappearing, and everything European was considered “universal” (two hypotheses that the facts prove to be untrue). As H. Frey observes, “Today, the decline or decadence of the West is part of the contemporary view of the world, like the electron or the dinosaur.” The linear outline of progress, with Europe at the head, did not withstand the test of the First World War. The year 1918 marked the beginning of the end of Europeanism. Since then, we have begun to speak of “areas of civilization” (Splengler), “civilizations” (Toynbee), “cultural coalitions” (Lévi-Strauss). The existence of “areas of civilization” (regions) is commonly admitted today; it has entered journalistic language and even the structure of regional commissions and agencies of the United Nations (Europe, Near East, Southern Asia, South-east Asia, and the Far East). New communities have inserted themselves between nations and humanity. What do they represent? Are they something unique, or are they divided into a certain number of types in opposition to each other because of some characteristic? And in what way have they modified our view of universal history?

Terms of address are the words we use when we speak to someone. The circumstances in which they are used are the same everywhere: when we call to someone; when we meet someone; when we want to attract someone's attention; when we speak to one person in a group—to ask a question or to give an order; at the beginning of a discourse; on an envelope; and at the beginning of a letter. Nevertheless, it depends on a particular society whether the use of these terms, in a given circumstance, is necessary or not. In Chinese, for example, when one meets someone he knows, he is not obliged to call him by name, title or any other term. The most normal attitude is to ask a question about what he is doing, a question whose objective depends on the circumstances and whose form depends on the degree of familiarity one has with the person addressed.

An unusual vanadium chlorite precipitated during the formation of a vanadium-uranium ore deposit in the Henry Basin, southeastern Utah. The ore deposit formed by reduction and precipitation of U and V in the presence of organic matter at the interface between a stagnant brine and overlying, circulating meteoric water. Some samples of the vanadium chlorite (heated before analysis) contain ≥ 10% V2O5. In fresh samples, most of the vanadium is in the trivalent oxidation state. X-ray powder diffraction data suggest that Fe and V are concentrated preferentially in the interlayer hydroxide sheets of the chlorite. A d(060) value of 1.52 Å indicates that the chlorite probably has a dioctahedral structure which is distended by the presence of octahedral Fe and V. The vanadium ore zone is flanked by peripheral zones containing perfectly ordered chlorite/smectite. This chlorite/smectite contains much less V than the pure chlorite. This chlorite may have formed by the progressive precipitation of vanadium-rich interlayer hydroxide sheets in the mixed-layer chlorite/smectite in the most reducing portion of the ore zone. The pure chlorite is a IIb polytype, which, for nonvanadiferous analogs, is ordinarily found in high-temperature environments; however, no evidence exists to show that these rocks have ever been exposed to elevated temperatures. In fact, the presence of unreacted smectite in a potassium-rich setting and the low vitrinite reflectance of coalified plant debris indicate a low-temperature history for these sediments.

Reactions of Sr, La, and Nd (the latter two elements simulating Am and Cm) with potential backfill minerals for radioactive waste storage and with repository wall rocks, such as shale, were investigated under simulated repository conditions of 200° and 300°C for 12 weeks under a confining pressure of 30 MPa. The solid and solution reaction products were characterized to determine the nature and extent of reaction. Chlorite, illite, kaolinite, montmorillonite, mordenite, and clinoptilolite and four shales removed as much as 61.2 and 98.5% of the added SrCl2 and Sr(OH)2 from solution, respectively, by ion exchange and/or by forming new strontium compounds such as SrAl2Si2O8, Sr2MgSi2O7, SrCO3 (strontianite), and SrAl2Si4O12·2H2O (Sr-wairakite). The formation of these sparingly soluble Sr phases by the reaction of the soluble Sr compounds with such backfill materials indicates that the backfill may serve as a barrier during the thermal period of the waste in the life of a repository. These same minerals and shales removed as much as 99.99% of the added La or Nd from solution at 300°C by forming new phases such as LaOHCO3, NdOHCO3, and possibly La or Nd oxides and hydroxides. Zeolites reacted with La and Nd to form smectite. Thus, if La and Nd truly simulate the reactivity of Am and Cm, properly designed backfills can serve as a barrier to the migration of transuranic elements of nuclear wastes.

It is a high honor to be invited to give this first Brindley Memorial Lecture. I view it as taking the first step on a ladder, to be followed by suceeeding talks that climb higher to the pinnacle that George Brindley erected for us in clay mineralogy. If George were with us, he would be sitting on the front row, as usual, keeping the speakers and audience "honest" in our deliberations. In turn, I would be privileged to ask him personally to enlighten us with his valued opinion on the many questions I will be asking in this talk.

Zeolites and associated minerals occur in a tholeiitic basaltic pillow lava sequence that makes up part of the Eocene Siletz River Volcanics in the central Coast Range, Oregon. Regional zoning of zeolite assemblages is not apparent; the zeolites formed in joints, fractures, and interstices, although most occur in central cavities of basalt pillows. The zeolites and associated minerals identified, in general order of paragenetic sequence, are smectite, pyrite, calcite (small spheres), thomsonite, natrolite, analcime, scolecite, mesolite, stilbite, heulandite, apophyllite, chabazite, mordenite, calcite (scalenohedra and twinned rhombohedra), laumontite, and amethystine quartz. Common three-mineral assemblages are: natrolite-analcime-stilbite, stilbite-heulandite-chabazite, stilbite-apophyllite-chabazite, and natrolite-mesolite-laumontite.

Alteration of basaltic glass, which was initially abundant, appears to have been an important factor in formation of the zeolites. Isotopic data suggest that zeolitization occurred during a low-temperature (60°–70°C) submarine hydrothermal event, or by reactions of cold (∼10°C) meteoric water with basalt over a long time. The occurrence of different mineral assemblages in cavities of adjacent basalt pillows indicates that these minerals crystallized in closed systems that were isolated as fractures and joints were sealed by deposition of smectite and early zeolites. Although the total chemical composition of the mineral assemblages in cavities is similar, different mineral species formed because of the sensitivity of zeolite minerals to slight variations in physical and chemical conditions within individual cavities.

To understand the genetic relationship between hisingerite material in the joints of an overlying grey basalt and nontronite and Fe-rich saponite in the joints and matrix of a more deuterically altered, underlying green basalt, the hisingerite material was treated in a series of hydrothermal experiments. No well-ordered clay mineral was produced at temperatures <340°C, although extended treatment for 445 days and at 110°C or 42 days at 180°C resulted in the formation of materials that gave broad, weak, basal X-ray powder diffraction (XRD) reflections characteristic of 2:1 phyllosilicates. Hematite did not form at 110°C, but it did form at 180°C in 1- and 6-week runs. Treatments at 340°C in Pt, Ag-Pd, and Au containers resulted in mixtures of Fe-rich saponite + hematite, but the same starting material treated at 340°C in stainless steel yielded, in addition, some chlorite, probably due to the more reducing conditions in the stainless steel container. Treatment of the unaltered grey basalt at 340°C and 50 MPa for 10 days resulted in complete alteration of olivine (and probably glass) to a trioctahedral smectite.

The Fe-rich saponite produced by the hydrothermal treatment of the hisingerite material has a composition and XRD pattern similar to the Fe-rich saponite found in the green basalt and an XRD pattern similar to that produced by the hydrothermal treatment of the grey basalt; thus these clays may have had a similar origin. The compositions and XRD patterns of these clays are not similar, however, to those of the nontronite in the joints of the green basalt. The nontronite probably formed during a subsequent low-temperature alteration.

Everybody knows nowadays that the degree of development is measured according to a certain number of criteria, of which the most important one, and initially the only one. was the Gross National Product (or G.N.P.) of each country, related to the number of inhabitants. The arbitrarily-settled line some twenty years ago between the rich and the poor or, as called at that time, the “underdeveloped”, was based at the level of 1000 U. S. dollars per capita. The expression was badly accepted by those it described, because development confers a dignity which cannot be refused to anybody. That is why the following euphemism appeared: “developing countries”, as promising as it is little compromising. Later on, this exclusively economical criterion was moderated by several additives, linked to social structure, to the rate of elimination of illiteracy, and even to cultural factors.

The mineralogy of the clay fraction was studied for soils and saprolite on two Blue Ridge Front mountain slopes. The clay fraction contained the weathering products of primary minerals in the mica gneiss and schist parent rocks. Gibbsite is most abundant in the saprolite and residual soil horizons, where only chemical weathering has been operable. In colluvial soil horizons, where both physical and chemical weathering have occurred, the clay fraction consists largely of comminuted primary phyllosilicates —muscovite, chlorite, and possibly biotite—and their weathering products: vermiculite, interstratified biotite/vermiculite (B/V), and kaolinite. The clay-size chlorite contains Fe2+ as indicated by Mössbauer spectroscopy, and is more resistant to weathering than biotite. The vermiculite and B/V, both weathering products of biotite, contain Fe3+. Vermiculite in colluvial soils and, especially, surface horizons is weakly hydroxy-interlayered. The kaolinite in the clay fraction resulted at least partly from the comminution of kaolinized biotite in coarser fractions.

The hematite content ranged from 0 to 8% of the clay fraction and strongly correlates (r =.95) with dry clay redness, as measured by the redness rating: RR = (10 - YR hue) × (chroma) ÷ (value). The hematite is largely a product of the weathering of almandine; thus, the soil redness is dependent on the amount of almandine in the parent materials and its degree of weathering in the soils. Goethite (13–22% of the clay fraction) imparts a yellow-brown hue to soils derived from almandine-free parent rocks. The release of Fe in relatively low concentrations during the weathering of Fe-bearing primary minerals, particularly biotite, appears to have promoted the formation of goethite.

13C and 29Si nuclear magnetic resonance spectroscopy with magic-angle spinning bas been used to study the short-range ordering and bonding in the structures of intercalates of kaolinite with formamide, hydrazine, dimethyl sulfoxide (DMSO), and pyridine-N-oxide (PNO). The 29Si chemical shift indicated decreasing levels of bonding interaction between the silicate layer and the intercalate in the order: kaolinite: formamide (δ) = -91.9, ppm relative to tetramethylsilane), kaolinite: hydrazine (-92.0), kaolinite: DMSO (-93.1). The 29Si signal of the kaolinite:PNO intercalate (-92.1) was unexpectedly deshielded, possibly due to the aromatic nature of PNO. The degree of three-dimensional ordering of the structures was inferred from the 29Si signal width, with the kaolinite: DMSO intercalate displaying the greatest ordering and kaolinite: hydrazine the least. 13C resonances of intercalating organic molecules were shifted downfield by as much as 3 ppm in response to increased hydrogen bonding after intercalation, and in the kaolinite: DMSO intercalate the two methyl-carbon chemical environments were non-equivalent (δ = 43.7 and 42.5).

The oxidation of As(III) to As(V) by K-birnessite was examined at different temperatures, pHs, and birnessite/As(III) ratios. Experiments ranged in duration from 5 to 64 hr, and solution and solid products were determined at several intervals. All experiments showed that the reaction produced large amounts of K+ to solution and very little Mn2+. As(V) was released to solution and incorporated into the K-birnessite. The oxidation was initially rapid and then slowed. The oxidation of As(III) was probably facilitated initially by autocatalytic Mn-As(V) reactions occurring mostly in the interlayer, in which large amounts of As(V) and K+ could be easily released to solution. The reaction also slowed when interlayer Mn was exhausted by forming Mn-As(V) complexes. Mn(IV) could only be acquired from the octahedral sheets of the birnessite. The two-stage reaction process proposed here depended on the layered structure of birnessite, the specific surface, and presence of exchangeable cations in K-birnessite.

Joseph Alois Schumpeter (1883-1950) stands among the intellectual giants of the twentieth century, especially in the field of economics; in his long and varied impact on the profession, he is second only to Maynard Keynes. He was a pragmatist in his economic philosophy, an “objective scientific investigator with no particular axe to grind” (Newman, et al., 746). His encyclopedic History of Economic Analysis, edited after his death by his wife and published in 1954, is a monument to his gigantic and versatile achievements; and it remains the locus classicus of almost all works in this area.