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© 2012 Wiley Periodicals, Inc. Published online in Wiley Online Library (wileyonlinelibrary.com). DOI 10.1002/ert.21359 Social networks and technology are infiltrating every facet of our personal and work lives, and human resource professionals, senior leaders, and business executives are struggling to understand the full impact of this in the workplace. Some may feel that the explosion of social media and the technologies that support them pose a threat to productivity, security, and business culture. A recent study released in March 2012 from Harris Interactive and ESET reported that more than 81 percent of employees work using their personal mobile device, with an increasing number of them working virtually or as part of a results-oriented work environment or work-from-home program.1 Add that to the 340 million tweets posted via the microblogging social-networking site Twitter.com2 and the conversations of nearly 900 million Facebook users,3 and it’s easy to see why these new engagement platforms demand our attention. However, instead of seeing the explosion of social media, which use smartphones, tablets, and other mobile devices, as workplace liabilities, I propose that businesses embrace this new communication shift and new role of technology and learn how to use it in a way that advances business strategies and realizes business goals. GENERATIONAL FACTORS AND THE NEW WORKFORCE

Detailed analysis of over 1,000 subsurface Silurian palynology samples from 34 wells has allowed the development of a robust biostratigraphy based on acritarchs, chitinozoans and cryptospores for the Qusaiba Member of the Qalibah Formation, central Saudi Arabia. The new index fossils described herein augment the Arabian Plate Silurian chitinozoan zonation. The high-resolution biostratigraphic zonation consists of nine First Downhole Occurrences (FDOs) from the lower Telychian through Aeronian. In particular, three regionally recognizable palynologic horizons were identified within the lower part of the informally designated Mid-Qusaiba Sandstone (Angochitina hemeri Interval Zone), and above the FDO of Sphaerochitina solutidina. This high level of biostratigraphic resolution provides a framework for the integration of the sedimentology and calibration with global sea level curves, leading to a detailed understanding of the sequence stratigraphic evolution of this part of the Silurian in Saudi Arabia. Sedimentological core studies identify three Depositional Facies Associations (DFAs) within the Mid-Qusaiba Sandstone interval, including: (1) shelfal deposits (DFA-I) characterized by interbedded hummocky cross-stratified sandstones, graded siltstones and bioturbated mudstones; (2) turbiditic deposits (DFA-II); and (3) an association of heavily contorted and re-sedimented sandstones, siltstones and mudstones (DFA-III) that is considered representative of oversteepened slopes upon the Qusaiba shelf. Integration of the newly recognized palynostratigraphic horizons and the sedimentological data facilitates an understanding of the sequence stratigraphic evolution of the Mid-Qusaiba Sandstone interval and its immediate precursors. Thus a Maximum Flooding Surface (MFS) is identified from significant palynostratigraphic, as well as sedimentological evidence, and concurs with the MFS identified regionally with the Monograptus convolutus Graptolite Zone. Several mud-prone cyclothems downlap onto the MFS. Each of these is identified by its own palynostratigraphic marker: these mud-prone cyclothems represent the distal parts of a Highstand Systems Tract (HST). The end of the HST is marked by evidence of a major, episodic drop in relative sea level. Thus, a relationship is identified wherein successive palynostratigraphic marker horizons, newly identified in this study, are partially eroded by the introduction of sandy turbidites (DFA-II). These turbidites arise from storm-induced erosion of gully complexes in the upper submarine slopes that are present as topography upon the Qusaiba shelf. Each of the successive drops in sea level is separated from the next by a minor, subsequent sea level rise, which precludes further submarine erosion and turbidite deposition, and is instead evident in the widespread occurrence of shallow marine (shelfal) muds and sandy tempestites (DFA-I). The lowstand per se is considered to be represented by the most widespread distribution of the DFA-II turbidite deposits, and is associated with the youngest Mid-Qusaiba Sandstone marker horizon identified in this study, namely Rugosphaera agglomerata n.sp. The youngest unit of DFA-II lowstand turbidites is limited in its occurrence to the more proximal parts of the study area, and thus is considered to represent the onset of the succeeding Transgressive Systems Tract (TST). Of the biostratigraphic indices used for correlation within the Qusaiba Member, Rugosphaera agglomerata and Eupoikilofusa curvata are formally described and two additional important species, Fractoricoronula n.sp. and ?Oppilatala n.sp., are retained in open nomenclature.

International audience; The QUSAIBA-1 shallow core drilled in NW Saudi Arabia penetrated the Qalibah, Sarah and Qasim formations. The Silurian graptolites and chitinozoans from the Qusaiba Member of the Qalibah Formation have been investigated previously. The present study focuses on the Upper Ordovician part of the core hole. A total of 39 core samples from the glacio-marine Sarah Formation and from the upper part of the Qasim Formation were processed for chitinozoans. Part of the sample set yielded abundant and well-preserved specimens associated with graptolite remains, scolecodonts, acritarchs and cryptospores. Other samples from glacially related sediments contained only a few fragmented chitinozoan vesicles of early Late Ordovician species suggesting reworking. Four different chitinozoan assemblages are identified. The youngest one is restricted to two samples located very close to the gamma ray peak and to the highest evidence of glacial sediments. This assemblage is dominated by Cyathochitina species including C. caputoi, associated with subordinate numbers of Ancyrochitina, Euconochitina and Belonechitina species. This assemblage does not contain the classical Late Ordovician chitinozoan taxa and an early Rhuddanian age is considered possible. The underlying interval is less productive and sometimes virtually barren. This interval yields a second assemblage mainly composed of broken specimens of Tanuchitina, Cyathochitina, and Euconochitina. Most of these forms seem reworked, probably through glacial erosion. The composition changes drastically in the older core samples where abundant Armoricochitina nigerica and Ancyrochitina species are associated with e.g., Euconochitina lepta, Calpichitina lenticularis, Acanthochitina barbata and Desmochitina minor. This constitutes the third recovered chitinozoan assemblage. In addition to the classical components, new species have been observed. This assemblage occurs in pre-glacial strata and is assigned to the late Katian (Ashgill). The oldest processed sample contains Belonechitina, Hercochitina, Conochitina and Euconochitina species. This fourth assemblage, however, lacks A. nigerica and suggests an older age assignment (e.g., late Caradoc of the British chronostratigraphy).

International audience; A total of 58 core samples from three shallow core holes (Qusaiba-1, Baq'a-3 and Baq'a-4) penetrating the Qalibah Formation in Central Saudi Arabia have been investigated. The core samples are grey-greenish hemipelagic shale or silty-shale and yield very well-preserved and abundant Early Silurian chitinozoans. Most of the recorded chitinozoan assemblages are highly diverse and include several new taxa coexisting with well-known species. Five chitinozoan biozones ranging from the Aeronian to the Telychian, and considered of regional value at the scale of Northern Gondwana regions, are identified. From the oldest to the youngest they are the: Conochitina alargada, Angochitina hemeri, Angochitina maclurei, Tanuchitina obtusa and Euconochitina silurica biozones. The three older regional biozones have been already reported in Saudi Arabia (Paris et al. 1995) whereas the two youngest ones are documented for the first time in the Arabian Peninsula. Their eponymous index species were described from the subsurface of the Algerian Sahara. Several sub-biozones of at least local application are also defined. The fairly closely spaced and regular sampling permits the total range of several highly diagnostic forms to be better constrained and thus the interval of uncertainty between biozones is reduced. Beside abundant chitinozoans and acritarchs, sporadic occurrences of scolecodonts and of eurypterid cuticle fragments are also noted in the organic residues. The presence of eurypterids suggests a shallowing trend in the sedimentary record, which is consistent with the distribution of the graptolites sicula and/or rhabdosomes. Indeed, the graptolites are frequent through the Qusaiba Member, except in the youngest examined samples where shallower environments like those in the Sharawra Member begin. Recently, Zalasiewicz et al. (2007) studied in detail the range of the graptolites in the three shallow cores. These graptolite data provide independent chronostratigraphical control refining previous age assignments. The alargada and the hemeri chitinozoan biozones correspond to the mid-Aeronian convolutus graptolite biozone whereas the maclurei chitinozoan biozone extends through the early Telychian guerichi and turriculatus graptolite biozones. The obtusa and the silurica chitinozoan biozones occur in an interval devoid of graptolites are referred to the mid-late Telychian as they do not contain yet typical Sheinwoodian species.