Jacek Puziewicz

Solid speciation and mobility of potentially toxic elements from natural and contaminated soils: A combined approach

The study area (Szklary Massif, SW Poland) comprises three sites of different soil provenance: (1) natural serpentine Cambisol, (2) anthroposol situated on waste dump and (3) cultivated Inceptisol developed on glacial tills next to the dump. Potentially toxic elements (PTE) have either lithogenic or anthropogenic origins in these sites. The chemical partitioning of Co, Cr, Cu, Ni, Pb and Zn among solid forms was determined by sequential extractions coupled with direct mineral identifications (SEM, electron microprobe analysis - EMPA, and XRD). Examination of solid residues after several extraction steps was conducted in order to discuss the indirect speciation obtained by the extraction method. Total concentrations of PTE having anthropogenic origin greatly exceed those of lithogenic origin. Mobility of studied PTE is variable in the different environments except for Cr which is always mostly found in residual fractions of extractions. Cu and Pb are more mobile than Cr and Co in all soils. Zn is more stable (Cu>Pb>Ni>Co>Zn>>Cr) in the serpentine soil and cultivated epipedon (Pb>Cu>Zn>Ni>Co>>Cr) than in the anthroposol (Zn>CuPb>Ni>Co>>Cr). PTE of lithogenic origin are generally less mobile than those from anthropogenic origin except Ni which is more mobile in the serpentine soil. Nonetheless, mineral forms of metals better determine their mobility than metal origin. Identification by direct methods of the PTE mineral form was not possible for metals present at low concentrations (Cu, Pb). However, direct mineralogical examinations of the solid residues of several extractions steps improved the assessment of the PTE solid speciation and mobility, particularly for Cr, Ni and Zn.

Lithospheric mantle beneath NE part of Bohemian Massif and its relation to overlying crust: new insights from Pilchowice xenolith suite, Sudetes, SW Poland

The Oligocene/Miocene basanite from Pilchowice (Sudetes Mts., SW Poland) carries numerous small xenoliths of mantle peridotite, mostly harzburgite. The Pilchowice xenolith suite is dominated by harzburgites and dunites containing olivine Fo 90.2–91.5 (group A). The peridotites of group B (olivine Fo 88.6–89.4), and C (olivine Fo 83.2–86.5) are subordinate. The peridotites suffered from significant melt extraction (20–30%) and were subsequently subjected to metasomatism. Three different trace element compositional patterns of group A clinopyroxene occur, which are typical of silicate melt, carbonatite melt and silicate–carbonatite melt metasomatism, whereas groups B and C were affected by silicate melt metasomatism only. The Pilchowice basanite occurs at the contact of Karkonosze–Izera Block and Kaczawa Complex, two major geological units of Sudetes. The Pilchowice xenolith suite documents underlying lithospheric mantle of composition and depletion degree similar to those described in the whole Lower Silesian mantle domain, which forms NE termination of Saxo–Thuringian zone of the European Variscan orogen. The crustal structure of the orogen is, therefore, not mirrored in the mantellic root.

Two-mica andalusite-bearing granite with no primary muscovite: constraints on the origin of post-magmatic muscovite in two-mica granites

Abstract The two-mica granite from Gęsiniec (Strzelin Granitic Massif, SW Poland) consists of quartz, K-feldspar, normally zoned plagioclase (30 ± 7 % An), subordinate biotite and muscovite and magmatic andalusite. Andalusite crystallised before the outer parts of plagioclase grains were formed. Biotite has constant Fe/(Fe + Mg) ratio of approximately 0.81. Five textural types of muscovite occur in the granite: (1) muscovite replacing andalusite, (2) embayed interstitial muscovite, (3) muscovite forming aggregates with biotite, (4) muscovite accompanying biotite and chlorite in microfissures and (5) fine muscovite forming fringes at the contact between larger muscovite plates and K-feldspar. They are commonly associated with albite. Crystallisation of muscovite started significantly below the granite solidus, mostly by the replacement of andalusite. Formation of muscovite continued during cooling of host rock. The growth of individual plates was initiated at different undercoolings and the plates whose crystallisation was frozen at different stages of growth occur. Those that were formed earlier are richer in titanium and iron relative to the later ones. As the rock contains no Ti and Fe saturating phases, the content of Ti and Mg in muscovite depends on their local availability. The homogeneous Fe/(Fe + Mg) ratio of biotite indicates that it was re-equilibrated at the post-magmatic stage.

From mantle roots to surface eruptions: Cenozoic and Mesozoic continental basaltic magmatism

Basaltic volcanism is an important process in shaping large areas of the Earth’s surface, not only in continental extensional environments and at the ocean floor. This special issue contains a collection of fifteen papers that are dedicated to recent researches on various aspects of continental basaltic magmatism from its mantle roots via the ascent paths of the melt to the surface where different styles of volcanism take place erupting lavas or through explosive volcanism depositing various types of pyroclasts. Two of the fifteen were published earlier (Downes et al. 2015; Herrero-Hernandez et al. 2015). Continental basaltic volcanism also contributes to the total terrestrial sedimentary budget not only by its primary pyroclastic deposits but also their reworked varieties. Most of the papers result from presentations at the BASALT 2013 conference, which took place from April 18–24, 2013, in Gorlitz, Germany (Buchner et al. 2013). The conference was organized by the Senckenberg Museum of Natural History Gorlitz and co-organized by the International Association of Volcanology and Chemistry of the Earth´s Interior (IAVCEI)—particularly its Commission on Monogenetic Volcanism—and the “Sachsische Landesstiftung Natur und Umwelt” LaNU Academy). Since the conference was held in the heart of Europe in Germany with accompanied field excursions to Poland and the Czech Republic, many contributions are related to the Cenozoic Central European Volcanic Province (Fig. 1). However, there was also a variety of contributions about Mesozoic and Cenozoic basaltic rocks worldwide. This variety is reflected in this issue. The issue brings together studies on different aspects of basaltic magmatism. Thus, this volume contains petrological and geochemical studies spanning from studies of mantle peridotites to those on volcanic rocks as well as papers presenting geophysical data and interdisciplinary interpretation.

Clinopyroxene phenocrysts from the Księginki nephelinite(SW Poland)

Abstract The Eocene nephelinite from Księginki quarry (SW Poland) contains five types of clinopyroxene phenocrysts varying by texture and chemical composition. Type I phenocrysts are formed of Mg-rich (mg# = 0.93–0.88) homogenous cores, patchy mantle and zoned rims. Abundant type II is less magnesian (mg# = 0.65–0.88) and consists of spongy or spongy-patchy core surrounded by zoned rims, whilst in type III (mg# = 0.69–0.84), the cores are massive but patchy. The mg# of cores of type IV phenocrysts is slightly lower than that of type I (0.79–0.89), but its cores are either massive or patchy. Type V is very scarce and consist of relatively Mg-poor (mg# = 0.75–0.77) core enveloped by nonpatchy, sometimes zoned mantle and zoned outer rim. Chemical composition of type I and type IV cores suggests that they are xenocrysts introduced into the nephelinite from disintegrated peridotite and clinopyroxenitic xenoliths, respectively. Type V is also of xenocrystic nature, but its source rock was significantly more evolved than mantlederived ones. Types II and III are possibly cognates from the host nephelinite or a melt related to the nephelinite. All the types of phenocrysts suffered from disequilibrium with the nephelinitic (or proto-nephelinitic) melt or dissolution during adiabatic uplift. Linear variation in chemical composition of phenocrysts of Księginki nephelinite suggests its evolution because of fractional crystallisation, without significant influence of other differentiation processes.

Cenozoic ultramafic intrusive rocks in upper mantle beneath SW Poland

Goldschmidt Conference Abstracts 2009 Spring residence times: Role in weathering rates F.A.L. P ACHECO 1 AND C.H. V AN DER W EIJDEN 2 Department of Geology and Centre for Chemistry, UTAD, Vila Real, Portugal (fpacheco@utad.pt) Utrecht University, The Netherlands (chvdw@geo.uu.nl) Estimation of plagioclase (Pl) weathering rates (W Pl = ([Pl]/t)×(Q/A Pl )) at the watershed scale of springs requires the prior evaluation of a number of parameters which include the mole fractions of Pl ([Pl]) and their fracture surface areas (A Pl ), the residence times of springs (t) and their annual discharge (Q). An atempt to relate the weathering of plagioclase to mixtures rich in halloysite and to quantify the W Pl for a number of very small spring watersheds from the Vila Pouca de Aguiar region (VPA, North of Portugal) is documented in [1]. In this paper we take a step further by focusing our attention on adjusting the previously used advective flow equation and introducing hydraulic turnovers for the assessment of t. Now, the advective flow equation (t = (n e /K)(F 2 /D h )) replaces the average watershed depth (D) by the average depth of the saturated aquifer (D h ), whereas hydraulic turnovers assign t = V h n e /Q. V h is the saturated volume of the aquifer characterized by an effective porosity n e and a hydraulic conductivity K, and F is the average lateral path from the recharge area to the spring site. The evaluation of n e , K, F and Q has been addressed by [1]. The D h of the VPA springs could be related to their isotopic composition ( 87 Sr/ 86 Sr) and to annual precipitation (P): D h = [( 87 Sr/ 86 Sr) spring – ( 87 Sr/ 86 Sr) rain ] / (5.62×10 –7 P – 4.66×10 –4 ). The corresponding V h ’s were determined from the total watershed volumes (V) as calculated by a terrain modeling software: V h = V×(D h /D). The plagioclase log rates (Figure 1) are: –12.4±1.8 (adjusted flow equation) and –13.5±1.1 (turnover times). Relative to the former results, there is a decrease in the average log rates, by 0.2 in the first case and 1.4 in se second case. Number of cases Methane oxidation rates by AMS M. P ACK 1 *, M. H EINTZ 2 , W.S. R EEBUR G H 1 , S.E. T RUMBORE 1 , D.L. V ALENTINE 2 AND X. X U 1 University of California Irvine, Irvine, CA 92697 (*correspondence: mpack@uci.edu) University of California Santa Barbara, Santa Barbara, CA 93106 (mbheintz@umail.ucsb.edu, valentine@geol.ucsb.edu) In the marine environment methane (CH 4 ) oxidation consumes up to 84% of the CH 4 produced and mitigates the release of CH 4 , a potent green house gas, to the atmosphere [1]. The microbialy mediated process is an important sink in the global CH 4 budget, yet it remains poorly quantified because only a small number of direct oxidation rate measurements are available. Traditional oxidation rate measurements use regulated levels of radiotracers ( 14 C- and 3 H-CH 4 ) in conjunction with scintillation counting and come with certain limitations: safety and contamination factors restrict the measurements to isotope vans, and radioisotope use may not be permitted in foreign venues and may complicate shipping. We have developed a rate measurement that utilizes non- regulated levels of 14 C-CH 4 tracer (<50nCi/g) [2] in conjunction with accelerator mass spectrometry (AMS). The high sensitivity of AMS allows for a 10 3 reduction in tracer activity which relaxes complications with tracer shipping, handling and waste disposal. Together with ease of performance, this method could provide a larger sample throughput and therefore a better quantification of the marine CH 4 oxidation sink. Further, it allows for easy quantification of the fraction of CH 4 taken up in microbial biomass as well as the fraction oxidized, thereby providing important information about the activity of methanotrophs in the ocean. Our rate measurements compared to 3 H-CH 4 rate measurements on water from the same Niskin bottles are generally consistent. The two measurements are similar when ambient rates are high, but diverge when rates are low. [1] Reeburgh (2007) Chem. Rev. 107, 486-513. [2] Vogel (2000) Nucl. Instrum. Methods Phys. Res. B 172, 885-891. Turnover times Flow equation Times A983 Log (W Pl ) Figure 1: Log rates of plagioclase. [1] Pacheco F.A.L., Van der Weijden C.H. (2008). Geochimica et Cosmochimica Acta, v. 72, no. 17, Page A715.