Serpentine -bearing sediment, a rare sediment type that is formed and deposited in divergent, convergent, transform, and collisional plate -tectonic settings, carries important evidence of sediment provenance. Specific sources of serpentine -rich sediment display grain assemblages of distinct character that can be used to infer the serpentinization condition and sediment formation. This study reports quantitative and qualitative results on serpentine components in sandstones from Ocean Drilling Program Legs 149 (Iberia), 210 (Newfoundland), and 125 (Mariana and Izu-Bonin regions), and from serpentine -rich debris flows and arenitic breccias in deep -water successions in the Northern Apennine fold-thrust belt. We propose a textural scheme that offers a visual guidance for evaluating serpentinite grains that can be broadly adopted, is easily reproducible, and reduces user bias in determining compositional modes that allow comparison of serpentinite grain populations in arenites from different depositional environments, provenance, and associated tectonic settings. These data allow us to define a scheme for serpentine -dominated deposits that demonstrates the presence of two main groups of grain textures (pseudomorphic and non-pesudomorphic) with specific mineralogy and crystal shape as a function of temperature and pressure in the source rocks. The quantitative analysis of the serpentine -rich arenites and fine-grained sediments derived from forearc and rifted continental -margin settings shows that the studied samples are characterized by high percentages (c. $ 80%) of serpentine detritus and subordinate dense minerals and other lithic fragments, including basalt. In rifted continentalmargin settings, the prevalent textures in serpentinite sandstones consist of polygonal mesh, mesh -core, and hourglass that all belong to the pseudomorphic category, which preserves the pre -serpentine features and mineralogy. These textures are typically formed in low -temperature conditions (< 390 degrees C); lizardite is the most common mineral, along with minor chrysotile and, in rare cases, antigorite. In contrast, in forearc settings, serpentine -rich grain assemblages exhibit dominantly non-pseudomorphic, interlocking, and interpenetrating textures, dominantly composed of lizardite and recrystallization of lizardite by antigorite. Minor preserved ultramafic minerals related to dynamic recrystallization might be associated with the diapiric rise and protrusion of serpentine bodies. The Northern Apennines case study adopted to test this model indicates that the relationship of detrital serpentine texture to setting can be employed in provenance studies. Firstly, serpentine -bearing sediments derived from ophiolites deformed in fold-thrust belts have more variable serpentinite content, ranging from a few percent to < 10% for samples from deep marine environments, to typically c. 20 to # 50% for stream and beach samples. This compositional variation arises from mixing of sediments derived from deeper to shallower oceanic lithosphere (peridotites and serpentinites) with material from overlying volcanic rocks and sedimentary cover. The deep -water serpentine -rich sands of the Northern Apennines display variable compositions with intermediate characteristics. The source of the serpentine -bearing deposits is interpreted to be a residual oceanic lithosphere characterized by subcontinental mantle-lherzolite originated in the Middle-Late Jurassic by mantle delamination. The serpentinitedominated debris flows and sand beds contain serpentine grains that exhibit compositional and textural transitions from pseudomorphic to non-pseudomorphic categories, along with changes in mineralogy from lizardite to antigorite. Serpentinite with pseudomorphic texture is observed in the mantle section away from the deformed area. On the contrary, the presence of serpentine -rich arenites with dominant non-pseudomorphic textures suggests derivation from tectonized serpentine along fault scarps and or as products of serpentine diapirism. The detailed serpentinite texture scheme used to classify sand grains in this study includes pseudomorphic (often lizardite, minor crysotile) and non-pseudomorphic textures, with the latter attributed to temperature- and pressure -controlled recrystallization (often to antigorite) or shearing during or after serpentinization. For comparison of different detrital-serpentinite populations, a new ternary plot is proposed where counted parameters are grouped into three end members: undeformed, deformed, and recrystallized. This plot appears to discriminate different sources of detrital serpentine by tectonic setting (e.g., Iberia and Newfoundland margins vs. Mariana forearc) and shows the potential complexity of serpentinite sources in the Apennine basin example. Additional texturally based petrographic data sets are needed to determine the usefulness of this plot in provenance studies.

Palaeozoic rocks in the Betic Cordillera are widespread in the Malaguide, Alpujarride and Nevado-Filabride complexes of its Internal Domain. The Malaguide stratigraphic successions record a deepening trend during the post-rift evolution of a divergent continental margin that was paleogeographically related to the Northern Paleotethys from the latest Ordovician to the Early Carboniferous. Since the Serpukhovian it evolved to a convergent margin with Culm-like synorogenic sedimentation. Also probably at that time most of the Nevado-Filabride and Alpujarride rocks were affected by a Variscan tectonometamorphic evolution that was followed by latest Variscan local granite emplacement at ca. 300-280 Ma.

This paper challenges the classical idea that the Val Marecchia Nappe, the highest of the north-eastern Apennines, is a nappe that originated from the External Ligurian Domain and consisting of Upper Cretaceous–Middle Eocene rocks, accreted to the Palaeo-Apenninic Chain in the Middle-Late Eocene due to the Ligurian tectonic phase. Its succession comprises a Middle-Late Jurassic ophiolitic substratum and its sedimentary cover of Late Jurassic to Early Miocene age. This succession is quite similar to those of the North-Calabrian and Parasicilide Units of the Southern Apennines and of many Maghrebian and Betic Flysch Domain Units, all originating from the Western Tethys and deformed since the Early Miocene. The Val Marecchia Nappe succession was likely deposited in an oceanic realm that differs from that of the Ligurian Domain and was located in a more external palaeogeographic position with respect to that of the Ligurian Domain. The oceanic realm of the Val Marecchia Nappe constituted the northwards extension of the Maghrebian Flysch Basin-Lucanian Ocean system.

The results of litho- and biostratigraphic studies of three sections measured in weakly metamorphosed Famennian carbonate successions of the Stilo Unit in the Serre Massif (Calabria, southern Italy), together with recently published stratigraphic data related to other Devonian carbonates from the same area, allow definition of three formations: Assi Formation, San Giovanni Formation, and Ponte Vina Formation. The Assi Formation consists of grey, slightly nodular limestones alternating with thin-bedded calcareous slates; the type section has recently been dated, by conodonts, as Early-Middle? Devonian. The San Giovanni Formation consists of reddish nodular limestones, rich in greyish matrix, and contains Famennian (Late Devonian) conodonts. The Ponte Vina Formation is mainly composed of metacarbonates recently dated as Late Devonian by means of conodonts. These new data suggest correlation with nearby domains belonging to the Sicilian Longi-Taormina Unit or other better-known Paleozoic sequences in the western Mediterranean area, such as the Alps and the Betic and Rifian chains, and indicate that the studied succession developed in a sedimentary basin along the northern Gondwana margin during the Devonian.

Two samples of quartz-rich sandstones collected in the Numidian Flysch of Southern Apennines (Italy) have been studied to highlight the provenance of detritus using radiometric dating by LA-ICP-MS of detrital zircons and to compare the obtained ages with those of the Betic and Maghrebian Chains. The provenance of quartzose detritus from European or African Plates is still debated in these Chains, accordingly the ages of the detrital zircons can contribute significantly to discriminate the origin of the quartzose supply.The U-Pb zircon ages (n = 47) vary from 3047 +/- 13 Ma (Mesoarchean) to 516 +/- 19 Ma (Cambrian). The predominance of Paleo-Proteozoic ages (2500-1600 Ma) and the lack of Hercynian and Alpine ones suggest a provenance of the Numidian supply from North-African cratonic areas during the early-middle Langhian, when the Numidian successions of Southern Apennines were deposited. In addition, a cluster of ages at 773 +/- 24 Ma and 668 +/- 12 Ma in one sample and at 664 +/- 17 Ma in the other sample, calculated on zircon domains with magmatic zoning, testify to an important contribution from Neo-proterozoic "granitic" rocks widely outcropping in the North-African Craton.The age data on detrital zircons from Numidian sandstones in Southern Apennines overlap those found in the Numidian sandstones widespread in the Betic Cordillera and in the Maghrebian Chain from south Spain to Sicily. This suggests that the entire depositional zone in which Numidian Flysch deposited, was fed from a southerly source represented by the African Craton where Archean, Proterozoic and Cambrian rocks widely crop out from the Atlantic coast to the Hoggar and Tibesti Massifs. Finally, it must be outlined that a Meso-Archean zircon age (3047 Ma) has been found in the Numidian Flysch of the Southern Apennines whereas in the Numidian Flysch of the Maghrebian Chain, zircons older than Paleo-proterozoic (1840 Ma) have not yet been found. (C) 2015 Elsevier B.V. All rights reserved.

The Numidian Flysch shows constant lithological features from the strait of Gibraltar to central Italy. It is characterized by quartzarenites showing grains of monocrystalline, rounded and frosted quartz, and by kaolinitic mudstones. This research has pointed out that in the southern Apennines 1) the Numidian Flysch was deposited exclusively in the Campania-Lucania carbonate platform and in the Lagonegro-Molise basin, both located on the Apulian continental margin, and never is present in tectonic units originated from the oceanic area located west of that margin; 2) in the axial zone of the Lagonegro basin it stratigraphically follows a formation consisting of varicoloured clays (Argille Varicolori Auct.); 3) its age is limited to the early-middle Langhian, that is to say, it begins to sediment about 7 million years later than in the Maghrebian chain and deposited for a time span limited to 1–1.5 Ma. The thickness of the Numidian Flysch gradually decreases towards the north from about 600–1,000 meters to a few tens of meters and in some of the northeastern outcrops it is represented only by some layers of quartzarenites. This is accompanied by a decrease in size of the particles becoming more and more finer. In addition, northwards and frequently in the same section, a lower mineralogical and textural maturity (from quartzarenites to litharenites, and presence of abundant matrix, sub-angular, polycrystalline and deformed quartz grains) is well recognizable. In the Campania-Lucania carbonate platform the Numidian Flysch evolves to pelagic marly-clayey deposits, followed by mineralogically immature turbidite sandstones of Serravallian age. In the Lagonegro basin the Numidian Flysch replaces Cretaceous-lower Miocene turbidite deposits, consisting of limestones and red marls, on the western side of the basin, variegated clays in the axial zone and calcareous turbidites or variegated clays in the eastern side. Since the late Langhian, it evolves to pelagic sediments followed by lower Tortonian immature turbidite sandstones. In the successions of the Molise basin the Numidian Flysch is interbedded in a succession consisting of calcareous turbidites and pelagic limestones and marls, reaching the Messinian. The lithological features and the age of the Numidian Flysch in central-southern Apennines, therefore, point out an evolution different from that of the Numidian Flysch of the Maghrebian chain. During the early Miocene, a paleogeographic barrier or other unknown obstacles prevent Numidian sands from reaching the south-Apenninic domains. In the early Langhian, the disappearance of these obstacles allows sands to reach the deep basins located on the Apulian margin. In the late Langhian the Numidian sedimentation is canceled and replaced by mainly pelagic sediments, which will evolve to foredeep deposits in the Serravallian-Messinian time span. In addition, the significant presence of feldspathic and lithic grains testifies a double detrital supply: polycyclic quartzose sands and kaolinitic mudstones from the African craton and metamorphic and plutonic grains from the Hercynian or older rocks of the internal units of the southern Apennines. The Numidian Flysch of the southern Apennines allows to assign the tectonic units in which is present to the Campania-Lucania carbonate platform or to different zones of the Lagonegro-Molise basin and therefore is of great importance in the reconstruction of both the Mesozoic-Cenozoic paleogeography and a tectono-sedimentary evolution very difficult to decipher, given the convergence of sedimentary facies in the Apenninic deep basins since Cretaceous to Miocene, the presence of several tectonic phases and of out of sequence and back-thrusts.

A revision of field data and new biostratigraphic analyses have highlighted that the lowest part of the Poggio Carnaio Sandstone Fm consists of greyish marls, formerly attributed to the Antognola Marl Fm, and that calcareous nannofossil assemblages from these marls as well as from the overlying turbiditic sandstones are characterized by some taxa first occurring in Tortonian. Moreover, the occurrence of Discoaster cf. berggrenii could suggest an age not older than late Tortonian for the studied succession. The Poggio Carnaio Sandstone Fm, therefore, from its base is not older than Tortonian and constitutes a thrust-top basin unconformable succession, deposited on sub-ligurian units.

This paper explores the dark side of institutionalisation of trust research. More in particular, it signals two major perils: the risk for trust to be just another managerial fad and the difficulty for the research on trust conducted within the management science field to have an impact on other fields such as marketing and economics. A quick empirical test shows that while the first peril seems to be not that relevant, the risk of isolation and limited impact is a serious one. The paper suggests how to consider and avoid these perils, in order to strengthen the contribution research on trust makes towards better practice, and in order to conquer more legitimate space and recognition within institutionalised research.

Ophiolite-derived debrites, microbreccias and olistoliths are interbedded in the Monte Morello and Argille Varicolori Formations of the Val Marecchia Nappe, constituting the highest tectonic unit of the north-eastern Apennines and usually considered as having originated from the External Ligurian Domain. The ophiolite-derived clastic rocks were supplied exclusively by an oceanic sequence, consisting of peridotite, gabbro, basalt, radiolarite, pelagic limestone and shale. They are interbedded within a succession made up of fine-grained carbonate and siliciclastic turbidites, and of pelagic claystones. Petrographic and sedimentological features of the ophiolite-derived breccia and sandstone units testify to an intrabasinal source area for these clastic rocks rather than an extrabasinal origin from subaerially exposed oceanic crust, forming the inner flank of the basin, as previously suggested. Due to their Oligocene-earliest Miocene age, the deposits in which debrites and olistoliths occur, are related to Early Neo-Alpine tectonic events that caused reactivation and/or inversion of old normal/transform faults. Unstable fault escarpments provided a preferential path for submarine landslide and turbidite emplacement. Debrites, microbreccias and olistoliths, therefore, were added to the basin fill of fine-grained turbidite and pelagic deposits. This study suggests that the Val Marecchia Nappe succession was deposited on an oceanic substratum. Stratigraphy and age of the succession of this nappe can be well framed only in the evolution of the Sub-ligurian Domain, whereas they conflict with the interpretation of the Val Marecchia Nappe as a nappe originated from the External Ligurian Domain, as suggested previously by most authors. This interpretation also requires an oceanic substratum for the Sub-ligurian Domain, i.e. the existence of an oceanic belt external to the Ligurian Domain, which was deformed only in the Early Miocene. The Sub-ligurian Domain, therefore, would be an eastern branch of the Central Tethys and would represent the extension in the Northern Apennines of the Maghrebian-Lucanian oceanic realm, as recognized in the Betic Cordillera, Maghrebian Chain and Southern Apennines. (C) 2013 Elsevier B.V. All rights reserved.

Sandstone petrography and mudstone mineralogy and geochemistry of Triassic mudstones and sandstones from continental redbeds of the Malaguide Complex (Betic Cordillera, southern Spain) provide useful information on provenance, palaeoclimate and geodynamics during the early stages of the Pangea break-up, and on their diagenetic evolution. The sandstones are quartzarenites to sub-litharenites, with minor lithic fragments and rare feldspars. The mudstone samples show a PAAS like elemental distribution. The samples likely record recycling processes from their metasedimentary basement rocks that significantly affected the weathering indices, and monitors cumulative effects, including a first cycle of weathering at the source rocks. Sandstone composition and chemical–mineralogical features of mudstones record a provenance derived from continental block and recycled orogen that were weathered under warm and episodically wet climate. Source areas were located towards the east of the present-day Malaguide outcrops, and were formed by fairly silicic rock types, made up mainly of Palaezoic metasedimentary rocks, similar to those of the Paleozoic underlying series, with subordinate contributions from magmatic–metamorphic sources, and a rare supply from mafic metavolcanic rocks. Clay-mineral distribution of mudstones is dominated by illite and illite/smectite mixed-layer that result from differences in provenance, weathering, and burial/temperature history. Illite crystallinity values, illitization of kaolinite, occurrence of typical authigenic minerals and apatite fission-track studies, coupled with a subsidence analysis of the whole Malaguide succession suggest burial depths of at least 4–6 km with temperatures of 140–160 °C, typical of the burial diagenetic stage, and confirm the Middle Miocene exhumation of the Betic Internal Domain tectonic stack topped by the Malaguide Complex.

In this study, we report the results of litho- and biostratigraphic analyses made in the mildly metamorphosed Paleozoic succession of the Longi-Taormina Unit (Peloritanian Mountains, southern Italy), which up to now is poorly known. Three main formations based on their litho- and biostratigraphy have been defined and proposed for the first time (from base to top): Castelmola Formation, Lower Pizzo Leo Formation, and Upper Pizzo Leo Formation. The first two formations, composed mostly of marine fine-grained siliciclastic rocks, host Upper Ordovician calc-alkaline and Silurian alkaline volcanites, respectively. The upper formation is made up primarily of Silurian-Devonian pelagic metacarbonates which have released conodonts from Ludlow and Lochkovian (delta Zone) to Emsian (kitabicus, excavatus, and nothoperbonus-inversus zones) as well as Emsian dacryoconarids. These findings are relevant as they are the oldest ever found in this sector of the Alpine Chain, and they have enabled the best and most accurate dating made until now. The studied Paleozoic succession proved to be an important key-site to better understand facies evolution to neighboring domains like, in particular, the Calabrian Stilo Unit or other better-known Paleozoic sequences around the western Mediterranean, like those outcropping in the Alps or in the Betic and Rifian chains.

In the Peloritani Mountains (NE Sicily), the Favoscuro west section (near Pizzo Leo, between Floresta and Roccella Valdemone, Messina Province) cross-cuts the Variscan basement of the Longi-Taormina Unit. This section, in the less deformed part, shows a mildly metamorphosed continuous 50-m-thick Palaeozoic succession of metamarls and calc-schists with a bed of nodular metalimestones occurring at the base and of calc-schists at the top. The basal bed yielded a conodont fauna consisting of several fragments of Pa elements of Ancoradella cf. A. ploeckensis Walliser, 1964 (Ludlow, Ancoradella ploeckensis - Polygnathoides siluricus zones). The topmost bed yielded one fragment of a Pa element of Polygnatus cf P. Idtabicus Yolkin, Weddige, Izokh & Erina, 1994 (early Emsian, Polygnathus kitabicus Polygnathus excavatus zones). This conodont fauna, although not well preserved due to greenschist facies metamorphism and deformation, for the first time enables the recognition of upper Silurian and Lower Devonian rocks in the Peloritani Mountains. The Favoscuro west section studied herein is of important stratigraphic significance as it encompasses the Silurian/Devonian boundary

The Palaeozoic successions of the Longi-Taormina Unit (Peloritani Mountains, north-eastern Sicily) are formed mainly by slightly metamorphosed siliciclastic sequences, containing Upper Ordovician acidic rocks and undated alkaline volcanic layers at different stratigraphic heights. These Palaeozoic successions are locally capped by fossiliferous calcareous beds. A detailed biostratigraphic study on conodonts yielded by these carbonates has revealed an Upper Silurian-Lower Devonian age for this interval. These new biostratigraphic data are very useful as they indicate that some of the undated alkaline volcanic layers, being overlain by Upper Silurian-Lower Devonian conodont-bearing metalimestones, are surely related to volcanism not younger than the Late Silurian-Early Devonian and presumably Silurian in age.

Status-based affiliation represents a valuable resource in economic exchange. However, affiliation strategies introduce a status ordering paradox: whereas higher status actors seek to maintain status hierarchies, lower status actors strive to affiliate with more prestigious actors. In this paper, using original data on the network of social and professional ties among 72 hotel managers clustered in an Italian hotel district, we develop a theory of status-seeking behavior that involves the exchange of status for valued resources.

In the Beni lssef Massif, nearly 30 km west of Chefchaouen (Morocco), the thickest post-nappe succession within the Rifian sector of the Maghrebian Chain seals the tectonic contact between the Intrarifian External Tanger and Loukkos Units, related to the Rifian External Domain. This succession is very important for the reconstruction of the deformation timing of the Rifian Maghrebids. The age of its base, in fact, is an important constraint for defining an upper boundary to the stacking of both the Intrarifian and Maghrebian Flysch Basin Units, because clasts fed by the Melloussa and Numidian Flysch Nappes are abundant in the conglomerate layers. Field and biostratigraphic analyses pointed out the presence of a Lower Beni Issef Fm, unconformable on the Intrarifian External Tanger and Loukkos Units, and an Upper Beni lssef Fm, unconformable on both the Intrarifian Units and the Lower Beni lssef Fm. The Lower Beni Issef Fm, 150 m thick, consists of lenticular conglomerates with huge blocks in a marly-clayey matrix, followed by marls and minor sandstones. It deposited in a siliciclastic platform, shows a fining upward trend and is affected by metre- to hectometre-sized, locally reversed, folds. Samples collected 45-50 m above the base of the formation resulted not older than late Tortonian in age, but an older age for the base of the formation cannot be excluded. The Upper Beni lssef Fm, up to 550 m thick, starts with coarse conglomerates followed by medium- to coarse-grained well-bedded sandstones and by grey-blue marls and mudrocks. It indicates deposition in a channelized marine delta, with evolution towards pro-delta pelites, and shows sub-horizontal or gently dipping beds towards the east. Biostratigraphic data indicate a probable Messinian age for this formation. The composition of the arenites of both Lower Beni lssef and Upper Beni Issef Fms is quartzolithic and all samples show a notable content of monocrystalline well-rounded quartz and sedimentary lithic fragments. Detrital modes, all falling in the Quartzose Recycled and Transitional Recycled fields, suggest a provenance from recycling of sedimentary successions, easily recognizable in the Flysch Basin and External Units, mainly the Numidian Nappe sandstones. A Tortonian age of the Lower Beni lssef Fm would agree with the Late Serravallian age of the uppermost beds of the External Tanger Unit and indicate that the most probable age for the stacking of the lntrarifian Units falls in the Late Serravallian-Middle Tortonian time span. The Lower Beni Issef Fm was involved in a compressive tectonic phase testified by north-south striking folds. Later, probably during Messinian, the Upper Beni Issef Fm deposited in a younger intramontane basin, resting on both the Intrarifian Units and the Lower Beni Issef Fm. Successively, the Upper Beni Issef Fm was passively transported piggyback on top of the fold and thrust belt during later tectonic evolution of the Rifian Maghrebids. This tectonic evolution results quite similar to that recognized in the Tellian and Sicilian Maghrebids and also in the southern Apennines. (C) 2010 Academie des sciences. Published by Elsevier Masson SAS. All rights reserved.