La conservazione viva dell'esistente. Storia, progetto e restauro nell'opera di Josef Wiedemann

La tesi analizza, nel quadro del secondo dopoguerra, quattro casi studio scelti tra le opere di ricostruzione dell’architetto Josef Wiedemann (1910-2001) nel centro di Monaco di Baviera: Odeon (1951-1952), Alte Akademie (1951-1955), Siegestor (1956-1958) e Glyptothek (1961-1972). L’architetto si occupa di opere simbolo della città di Monaco, affrontando la loro ricostruzione come un tema fondante per la storia e l’identità del popolo bavarese, ma soprattutto come un’occasione per definire un metodo d’intervento sulle rovine della guerra. Il suo lavoro è caratterizzato infatti per la ricerca costante di una sintesi tra interesse per la conservazione dell’antico e apertura al nuovo; ispirandosi all’insegnamento del maestro Hans Döllgast, Wiedemann traccia una nuova originale strada per l’intervento sull’antico, segnata da una profonda capacità tecnico-progettuale e dall'attenzione alle nuove esigenze a cui deve rispondere un’architettura contemporanea. Partendo dai suoi scritti e dalle sue opere, si può rilevare un percorso coerente che, partendo dalla conoscenza della storia dell'edificio, ripercorrendone l’evoluzione dallo stato che potremmo definire “originario” allo stato di rovina, giunge a produrre nel progetto realizzato una sintesi tra il passato e il futuro. L'architetto, nella visione di Wiedemann, è chiamato a un compito di grande responsabilità: conoscere per progettare (o ri-progettare) un edificio che porta impressi su di sé i segni della propria storia. Nel metodo che viene messo progressivamente a punto operando nel corpo vivo dei monumenti feriti dalla guerra, è percepibile fino a distinguerlo chiaramente l’interesse e l’influenza del dibattito italiano sul restauro. La conservazione “viva” dell'esistente, così come viene definita da Wiedemann stesso, si declina in modo diverso per ogni caso particolare, approdando a risultati differenti tra loro, ma che hanno in comune alcuni principi fondamentali: conoscere, ricordare, conservare e innovare.

Detrital Zircon Evidence for Mixing of Mazatzal Province Age Detritus With Yavapai Age (ca. 1700-1740 Ma) and Older Detritus in the ca. 1650 Ma Mazatzal Province of Central New Mexico, USA

Preliminary detrital zircon age distributions from Mazatzal crustal province quartzite and schist exposed in the Manzano Mountains and Pedernal Hills of central New Mexico are consistent with a mixture of detritus from Mazatzal age (ca. 1650 Ma), Yavapai age (ca. 1720 Ma.), and older sources. A quartzite sample from the Blue Springs Formation in the Manzano Mountains yielding 67 concordant grain analyses shows two dominant age peaks of 1737 Ma and 1791 Ma with a minimum peak age of 1652 Ma. Quartzite and micaceous quartzite samples from near Pedernal Peak give unimodal peak ages of ca. 1695 Ma and 1738 Ma with minimum detrital zircon ages of ca. 1625 Ma and 1680 Ma, respectively. A schist sample from the southern exposures of the Pedernal Hills area gives a unimodal peak age of 1680 Ma with a minimum age of ca. 1635 Ma. Minor amounts of older detritus (>1800 Ma) possibly reflect Trans-Hudson, Wyoming, Mojave Province, and older Archean sources and aid in locating potential source terrains for these detrital zircon. The Blue Springs Formation metarhyolite from near the top of the Proterozoic section in the Manzano Mountains yields 71 concordant grains that show a preliminary U-Pb zircon crystallization age of 1621 ¿ 5 Ma, which provides a minimum age constraint for deposition in the Manzano Mountains. Normalized probability plots from this study are similar to previously reported age distributions in the Burro and San Andres Mountains in southern New Mexico and suggest that Yavapai Province age detritus was deposited and intermingled with Mazatzal Province age detritus across much of the Mazatzal crustal province in New Mexico. This data shows that the tectonic evolution of southwestern Laurentia is associated with multiple orogenic events. Regional metamorphism and deformation in the area must postdate the Mazatzal Orogeny and ca. 1610 Ma ¿ 1620 Ma rhyolite crystallization and is attributed to the Mesoproterozoic ca. 1400 ¿ 1480 Ma Picuris Orogeny.

Radiocarbon analysis in an Alpine ice core: Record of anthropogenic and biogenic contributions to carbonaceous Radiocarbon analysis in an Alpine ice core: Record of anthropogenic and biogenic contributions to carbonaceous aerosols in the past (1650-1940)

Long-term concentration records of carbonaceous particles (CP) are of increasing interest in climate research due to their not yet completely understood effects on climate. Nevertheless, only poor data on their concentrations and sources before the 20th century are available. We present a first long-term record of organic carbon (OC) and elemental carbon (EC) concentrations – the two main fractions of CP – along with the corresponding fraction of modern carbon (fM) derived from radiocarbon (14C) analysis in ice. This allows a distinction and quantification of natural (biogenic) and anthropogenic (fossil) sources in the past. CP were extracted from an ice archive, with resulting carbon quantities in the microgram range. Analysis of 14C by accelerator mass spectrometry (AMS) was therefore highly demanding. We analysed 33 samples of 0.4 to 1 kg ice from a 150.5 m long ice core retrieved at Fiescherhorn glacier in December 2002 (46°33'3.2" N, 08°04'0.4" E; 3900 m a.s.l.). Samples were taken from bedrock up to the firn/ice transition, covering the time period 1650–1940 and thus the transition from the pre-industrial to the industrial era. Before ~1850, OC was approaching a purely biogenic origin with a mean concentration of 24 μg kg−1 and a standard deviation of 7 μg kg−1. In 1940, OC concentration was about a factor of 3 higher than this biogenic background, almost half of it originating from anthropogenic sources, i.e. from combustion of fossil fuels. The biogenic EC concentration was nearly constant over the examined time period with 6 μg kg−1 and a standard deviation of 1 μg kg−1. In 1940, the additional anthropogenic input of atmospheric EC was about 50 μg kg−1.