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Research Article| February 01, 2013
Strong tectonic and weak climatic control on exhumation rates in the Venezuelan Andes
Mauricio A. Bermúdez;
Mauricio A. Bermúdez *
Laboratorios De Termocronología Y Geomatemáticas, Escuela De Geología, Minas Y Geofísica, Facultad De Ingeniería, Universidad Central De Venezuela, Caracas, Venezuela
Institut Des Sciences De La Terre (Isterre), Université Joseph Fourier, Centre National De La Recherche Scientifique (CNRS), BP 53, 38041 Grenoble Cedex 9, France
E-mail: mauricio.bermudez@ing.ucv.ve.
Peter A. van der Beek;
Peter A. van der Beek
Matthias Bernet
Lithosphere (2013) 5 (1): 3–16.
https://doi.org/10.1130/L212.1
Mauricio A. Bermúdez, Peter A. van der Beek, Matthias Bernet; Strong tectonic and weak climatic control on exhumation rates in the Venezuelan Andes. Lithosphere 2013;; 5 (1): 3–16. doi: https://doi.org/10.1130/L212.1
We studied the relationships among present-day relief, precipitation, stream power, seismic energy, seismic strain rate, and long-term exhumation rates for the Venezuelan Andes. Average long-term exhumation rates were determined for seven large catchments in the Venezuelan Andes from fission-track analysis of detrital apatite. A quantitative comparison between eight new detrital apatite fission-track (AFT) age distributions presented here and previously published bedrock AFT age patterns shows that detrital AFT ages can be used for predicting exhumation patterns across the mountain belt. Catchment-averaged exhumation rates estimated from the raw data range from 0.48 ± 0.02 km m.y.−1 to 0.80 ± 0.26 km m.y.−1 Accounting for variable sediment yield and assuming that short-term sediment production rates scale with long-term exhumation rates, these rates vary from 0.33 ± 0.07 km m.y.−1 to 0.48 ± 0.08 km m.y.−1 No variation in rates is observed between the northwestern and southeastern flanks of the mountain belt, despite a threefold increase in precipitation from the northwest to the southeast. Long-term exhumation rates are strongly correlated with relief in the different catchments, weak or negative correlations exist with precipitation data or present-day erosion indexes, while the correlation with seismic energy released by earthquakes is weak to moderate. This lack of correlation may be caused by the insufficient temporal range of the available precipitation and seismicity data, and the different time scales involved in the comparison. Long-term exhumation rates are, however, strongly correlated with seismic strain rates (which take the temporal earthquake magnitude-frequency scaling into account), suggesting that the moderate correlation with seismic energy is indeed related to the different time scales and that tectonic control on exhumation is significant. In contrast, given that precipitation patterns in the Venezuelan Andes should have been installed during Miocene times, we suggest that decoupling of relief and exhumation from present-day climate explains the lack of correlation between exhumation and precipitation.
The relative importance of tectonic and climatic control on relief development and exhumation in mountain belts remains strongly debated (e.g., Molnar and England, 1990; Burbank et al., 2003; Reiners et al., 2003; Strecker et al., 2009; Champagnac et al., 2012). Problems limiting our ability to discriminate between the driving forces for the development of topography and erosion include the limited temporal precision with which variations in exhumation rate, climate, and tectonics can be resolved and compared (e.g., Whipple, 2009), and the different temporal scales for which we have records of these processes (Burbank et al., 2003; Reiners et al., 2003; Vernon et al., 2009). While thermochronologic data record denudation on million-year time scales, seismicity (arguably a proxy for the intensity of at least brittle tectonics) and precipitation records (an admittedly reductionist climate descriptor) generally do not go back more than a few decades. Nevertheless, the comparison of spatial patterns of long-term exhumation rates and short-term seismicity and precipitation may provide some first-order insights into the processes driving exhumation, even in the absence of strong spatial correlations (Finlayson et al., 2002; Dadson et al., 2003; Koons, 2009; Vernon et al., 2009).
The Andes are important in the discussion on climate versus tectonic controls on topography and exhumation in mountain belts because of the obvious link between laterally varying topographic characteristics and climatic zonation (e.g., Montgomery et al., 2001; Lamb and Davis, 2003), as well as the strong asymmetry in orographic precipitation associated with this orogen (e.g., Bookhagen and Strecker, 2008). While many studies have concentrated on the southern and central Andes (e.g., Strecker et al., 2007; Farías et al., 2008; Thomson et al., 2010), attention has recently also focused on the Northern Andes. Mora et al. (2008), for instance, described strongly asymmetric deformation and exhumation patterns in the eastern Colombian Andes, which they linked to the strong NW-SE precipitation gradient across this part of the mountain belt. In contrast, Mora et al. (2009) and Parra et al. (2009) argued for a strong control of inherited crustal structure on spatio-temporal patterns of exhumation and relief production.
In this study, we present new detrital apatite fission-track (AFT) data from seven river catchments in the Venezuelan Andes, the northeasternmost extension of the Northern Andes. We compare the detrital AFT data to available bedrock AFT data of the Venezuelan Andes (Kohn et al., 1984; Bermúdez et al., 2010, 2011) in order to test whether they faithfully record exhumation in the catchments (e.g., Ruhl and Hodges, 2005; Brewer et al., 2006) and to spatially integrate the still relatively sparse in situ data. The objective of this study is to examine the relative controls of climate and tectonics on exhumation and relief development in the Venezuelan Andes. For this purpose, long-term exhumation rates derived from the detrital thermochronology data are compared to present-day relief, precipitation rates, seismic energy release, seismic strain rate, and short-term erosion potential predicted from the average stream power of individual drainages.
GEOLOGIC SETTING
The Venezuelan Andes were formed by oblique convergence between the continental Maracaibo block and the South American plate, driven by eastward movement of the Caribbean plate (Fig. 1A, inset; Case et al., 1990). The orogen is characterized by high seismicity and spatially variable exhumation since Miocene times, as recorded by AFT thermochronology data (Kohn et al., 1984; Bermúdez et al., 2010, 2011). The structure of the Venezuelan Andes is controlled by reactivated faults that delineate individual tectonic blocks. These faults were inherited from early Mesozoic rifting, and possibly from earlier orogenesis (Aleman and Ramos, 2000; Pindell and Kennan, 2001). Bermúdez et al. (2010) defined at least seven tectonic blocks with contrasting exhumation and cooling histories, separated by major strike-slip and thrust faults. The orogen is bounded by two seismically active thrust belts to the northwest and southeast (Colletta et al., 1997; Fig. 1B). The most important strike-slip fault systems are the right-lateral Boconó, Central-Sur Andino, and Caparo faults and the left-lateral Icotea, Valera, and Burbusay or Carache fault systems (Fig. 1A). The Boconó fault zone extends from the border with Colombia for more than 500 km to the northeast (Fig. 1A) and divides the Venezuelan Andes symmetrically in its central part into two separate chains; the Sierra La Culata to the northwest and the Sierra Nevada to the southeast are delimited by the NW fold-and-thrust belt to the north, and the Boconó fault to the south; and the Boconó fault, other tectonic block (Caparo, inBermúdez et al., 2010) and SE fold-and-thrust belt to the south, respectively (Fig. 1B). These two blocks cooled rapidly but diachronously during the late Miocene–Pliocene (Kohn et al., 1984; Bermúdez et al., 2011). In contrast, the Caparo tectonic block is delimited by the Boconó fault system and Central-Sur Andino–Caparo faults system, and the Trujillo tectonic block is delimited by the Boconó fault system, Valera fault system, and Burbusay fault (Fig. 1A), at the southwestern and northeastern ends of the Venezuelan Andes, respectively, and both experienced slow cooling from the late Oligocene to late Miocene onward (Bermúdez et al., 2010). Both these blocks are dominated by Paleozoic and Mesozoic sedimentary rocks, whereas Proterozoic to Paleozoic gneisses and granites are exposed in the core of the mountain belt, in the Sierra Nevada and Sierra La Culata ranges. This crystalline basement is covered by Cenozoic sedimentary rocks of the Maracaibo and Barinas foreland basins to the north and south, respectively (Fig. 1).
DETRITAL APATITE FISSION-TRACK THERMOCHRONOLOGY
Thermochronology of detrital minerals allows the quantification of cooling rates and exhumation processes in convergent mountain belts (e.g., Garver et al., 1999; Carter, 2007), providing a complementary record of the erosional history of a mountain belt with respect to local cooling paths deduced from in situ samples within the orogen (Brandon and Vance, 1992). Detrital thermochronology applied to modern river sediments provides a spatially integrated view of the exhumation history of an entire drainage basin, which may be the only way to characterize exhumation patterns for inaccessible areas.
Data Collection and Discrimination of Age Components
We collected samples for detrital AFT thermochronology from seven river catchments draining the Venezuelan Andes. The Coloncito, Tucaní, San Pedro, Agua Viva, and Mimbós Rivers drain the northern flank, the Chama and Chejendé Rivers drain the central range, and the Santo Domingo River drains the southern flank of this mountain belt (Fig. 2). Samples were collected along active river channel bars at all sites and prepared using standard techniques (cf. Bermúdez et al., 2010). We aimed at dating at least 100 grains per sample in order to attain statistically significant AFT age populations. This objective was attained for five out of eight samples (Table 1).
Because apatites in detrital samples are derived from different sources with variable bedrock ages within a drainage area, the grain-age distribution may contain several grain-age components (Brandon and Vance, 1992; Garver et al., 1999). Different methods have been proposed for deconstructing a fission-track grain age distribution into its age components, the most popular of which has become the binomial peak-fitting method (e.g., Galbraith and Green, 1990; Brandon 1992, 1996). Here, we use this method (as described by Stewart and Brandon, 2004) to decompose the grain-age distributions of our modern river samples. Resulting age peaks are reported in Table 1 and Figure 2. All samples except from the Tucaní catchment record a late Miocene (6–10 Ma) age peak, and all except those from the northwesternmost catchments (Agua Viva and Chejendé) also record a Miocene–Pliocene (2.5–6 Ma) age peak. Although all samples contain older (15–35 Ma) single-grain ages, only the Santo Domingo, Agua Viva, Tucaní, and Chama catchments record an older (early–middle Miocene; 14–25 Ma) age peak. The late Miocene age population is dominant (57%–100%) in most samples, except for the Santo Domingo and Coloncito catchments, where the younger (Miocene–Pliocene) age population is larger. In the Tucaní sample, 90% of the grains are grouped in a 5.9 ± 0.7 Ma age peak. The Chejendé River is a tributary of the Agua Viva and drains part of its catchment (Fig. 2); for this reason, we merged the detrital data for the corresponding samples (0507 and 0807) and applied the decomposition of the grain-age distribution as done previously. The resulting age peaks are very similar to those from the Agua Viva sample alone (Table 1).
Access to the southern flank of the Venezuelan Andes is difficult, and our data set contains only one river draining to the south. The Santo Domingo River sample shows a similar grain-age distribution and peak ages as the rivers that drain to the north (Table 1; Fig. 2), although the component ages are slightly older than corresponding age peaks in the other samples.
Although binomial peak fitting provides a convenient means of analyzing detrital thermochronology data, it may mask similarities in age structure between different samples. In order to analyze this, we use the Kolmogorov-Smirnov and Kuiper tests (Conover, 1980) to quantitatively compare the detrital age probability density functions (PDF) for the seven catchments (cf. supplementary material, Figure S1 and Table S11). These comparisons indicate that, at a 95% confidence level, the samples from four catchments located in the central part of the Venezuelan Andes (Chama, Tucaní, Santo Domingo, and San Pedro) yield a similar detrital age distribution, while the age distributions of the other samples are significantly different from each other.
Comparison of Detrital and Bedrock AFT Ages
Previous studies have shown that detrital thermochronology faithfully records source-area exhumation in a number of different settings (e.g., Bernet et al., 2004; Ruhl and Hodges, 2005; Brewer et al., 2006). Here, we compare our detrital AFT grain-age distributions of an individual drainage to previously published bedrock AFT ages. We analyze the Chama catchment, because it is the only one within the Venezuelan Andes for which sufficient in situ data (Kohn et al., 1984; Bermúdez et al., 2011) are currently available to derive a reliable bedrock age map.
Several authors (Stock et al., 2006; Vermeesch, 2007; McPhillips and Brandon, 2010) have developed quantitative methods for comparing bedrock and detrital age patterns. We adopted the approach described by Vermeesch (2007), randomly sampling a number of ages equal to the number of single-grain ages in the detrital sample from the interpolated bedrock age map. This method has the advantage that it takes into account Poisson-distributed measurement uncertainties. We sampled the bedrock age distribution and constructed the predicted age probability-density function (PDF) and cumulative-density function (CDF) 1000 times (Fig. 3A). We then used the Kolmogorov-Smirnov (K-S) (Conover, 1980) and Kuiper equality tests (Ruhl and Hodges, 2005) to compare the predicted AFT CDFs and PDFs with the detrital AFT data. Additional simulations (5000; 10,000) do not change the statistical results of our comparison. The resulting average p-values show that the inferred bedrock age distribution is significantly different from the detrital age distribution at the 95% confidence level; all simulations fail the Kuiper test, and the vast majority also fail the K-S test.
There are several possible reasons for this discrepancy. First, we do not take into account potential variations in apatite content for different lithologies in the catchment, whereas this may strongly influence the detrital age distribution (e.g., Tranel et al., 2011). However, (1) we have no information on the relative apatite abundance in different rock types of the Venezuelan Andes, and (2) the sampled Chama catchment is mainly underlain by relatively homogeneous Precambrian basement rocks (see Chama River in Fig. 1A).
Another possibility is that the catchment is not currently eroding at a uniform rate, which is an inherent assumption when randomly picking ages from the interpolated bedrock age distribution. It is relatively simple to weight the bedrock age distribution according to a model of inferred present-day erosion rates (Vermeesch, 2007; McPhillips and Brandon, 2010). Here, we assume that the short-term erosion rates in the catchment are coupled to the long-term exhumation rates, which can be estimated from the AFT ages using a simple one-dimensional (1-D) thermal model (cf. next section). We thus resampled the interpolated bedrock age distribution, letting the probability of sampling any particular age be determined by the long-term exhumation rate associated with that age, relative to the average long-term exhumation rate of the catchment. The resulting predicted CDFs/PDFs compare very favorably to the observed detrital AFT age distribution (Fig. 3B); both the K-S and Kuiper tests suggest the two distributions are similar at the 95% confidence level.
We conclude from these comparisons that the detrital AFT age distributions provide a reliable estimate of in situ bedrock ages in the sampled catchments when weighted by their associated long-term exhumation rates, implying that the apatite yield of the catchment (as recorded by our detrital samples) is controlled by the long-term exhumation rates.
Long-Term Exhumation Rates
The detrital age distributions can be used to provide predictions of average long-term exhumation rates of individual drainages, which can be compared to potential tectonic or climatic control parameters. We employed a simple 1-D steady-state thermal model developed by Brandon et al. (1998; see also Ehlers, 2005; Reiners and Brandon, 2006) to convert detrital AFT ages to exhumation rates. Because this model does not take either transient thermal effects (e.g., Rahl et al., 2007) or the three-dimensional (3-D) effects of topography (e.g., Whipp et al., 2009) into account, predicted exhumation rates should be considered as first-order estimates. Parameters used for these calculations are a surface temperature of 25 °C, layer thickness to constant temperature of 40 km, thermal diffusivity of 25 km2 m.y.−1, heat production of 10 °C m.y.−1, and a temperature at the base of the layer of 700 °C (for details, see Bermúdez et al., 2011). The last two values were constrained by inverse modeling of age-elevation relationships in the central Venezuelan Andes (Bermúdez et al., 2011) and imply a pre-exhumation surface geothermal gradient close to 25 °C km−1. The model iteratively calculates an exhumation rate (ɛ), cooling rate, closure temperature (Tc), and closure depth (zc) from the AFT ages, using the Dodson (1973) equation to solve for the closure temperature of the AFT thermochronometer and a steady-state thermal structure to relate this to the closure depth.
For each detrital sample, we used this procedure to translate single-grain ages into exhumation rates, which we then combined to predict a catchment-wide average long-term exhumation (ɛT) rate as:
where ɛj is the exhumation rate inferred for grain j, and N is the total number of grains in the detrital sample. In order to include the expected effect that rapidly exhuming areas of a catchment will contribute more sediment (and thus more datable apatite grains), as indicated by the comparison of bedrock and detrital age distributions in the previous section, we also calculated a weighted long-term catchment-averaged exhumation rate (ɛT)w:
Results are reported in Table 2. Catchment-averaged exhumation rates vary between 0.48 ± 0.02 km m.y.−1 for the Santo Domingo catchment and 0.80 ± 0.26 km m.y.−1 for the Mimbós catchment. As expected, weighted-average rates are lower, and all weighted long-term exhumation rates in the central Venezuelan Andes overlap within error, varying between 0.33 ± 0.07 km m.y.−1 (Agua Viva–Chejendé) and 0.48 ± 0.08 (Coloncito) km m.y.−1 The northeastern Agua Viva–Chejendé catchment shows the lowest long-term exhumation rates (<0.35 km m.y.−1). The central Chama and Santo Domingo catchments show intermediate rates (0.35–0.40 km m.y.−1), and the catchments located on the northwestern flank of the range show the highest exhumation rates (>0.40 km m.y.−1). In the following discussion, we will focus on the weighted-average catchment exhumation rates, which we consider to be the most reliable estimates.
POTENTIAL CONTROLLING PARAMETERS
In order to explore the potential topographic, tectonic, or climatic controls on the exhumation rates determined herein, we derive quantitative measures for these controls (relief, precipitation, seismicity, and stream power) in the following sections.
Elevation and Relief
The Venezuelan Andes rise from sea level at Lake Maracaibo, to the north of the mountain belt, to close to 5000 m elevation at Pico Bolívar in the Sierra Nevada block (Figs. 1 and 4A). This part of the Andes most probably emerged as an orographic barrier at ca. 8 Ma (Hoorn et al., 1995; Bermúdez et al., 2011). The central Sierra Nevada and Sierra la Culata ranges (Fig. 1B) include more than 60 peaks with elevations of 4300 m and above (Fig. 4A). These highest parts of the Venezuelan Andes were glaciated during the Quaternary. Moraines of the Last Glacial Maximum are encountered at 3400–3600 m elevation (Schubert, 1984), with older moraines occurring at elevations several hundred meters lower. The mean elevation of the range is significantly lower to the northeast and southwest, varying between 1160 and 1695 m (Bermúdez et al., 2010).
Relief was calculated as the maximum elevation difference within a variable radius, between 1 and 15 km, for every pixel in the digital elevation model (e.g., Montgomery and Brandon, 2002). There is a power-law relationship between average relief of the different catchments and the radius at which it was calculated, with scaling exponents around 0.5–0.6, characteristic for low-latitude mountain belts (Champagnac et al., 2012). The present-day relief of the Venezuelan Andes for a 5 km radius is shown in Figure 4A. Highest relief values of close to 3500 m are found along the central Chama River valley, which follows the Boconó fault. Other areas of high relief are located on the northwestern and southeastern flanks of the mountain belt. Relief is much lower within the central Sierra Nevada and Sierra la Culata ranges and in the Caparo and Trujillo blocks in the southwest and northeast of the Venezuelan Andes (Figs. 1 and 4A). The former are characterized by extensive low-relief summit surfaces that show widespread evidence for glacial beveling through cirque retreat (e.g., Mitchell and Montgomery, 2006; Foster et al., 2008), whereas the latter show subdued relief at lower mean elevations with widespread soil mantling of slopes.
The topography of the Venezuelan Andes generates a well-developed orographic precipitation pattern. Moist air masses from equatorial South America in the south need to rise in order to cross the Venezuelan Andes to the north, causing heavy precipitation on its southern flank, whereas the center and northern flank of the belt are more arid. It has been proposed that the present-day precipitation and drainage system of the Venezuelan Andes started developing at ca. 8 Ma, in response to tectonically driven surface uplift (Hoorn et al., 1995; Bermúdez et al., 2011). We used precipitation data from 30 meteorological stations in and around the Venezuelan Andes to elaborate a mean annual precipitation map for the past 20 yr. Although these measurements do not record snowfall as accurately as rainfall, the vast majority of precipitation is rainfall in the low-latitude Venezuelan Andes. The database was compiled from different sources: (1) National Oceanic and Atmospheric Administration (NOAA) World Temperature- Precipitation data set (2011); (2) published data (Stansell et al., 2006; Naranjo and Duque, 2004); (3) bioclimatic net stations of Mérida (http://www.cecalc.ula.ve/redbc/colecciones/colecciones_datos.html); and (4) data provided by Gerard Kopp (2007, personal commun.) of the Institute for Meteorology and Climate Research, University of Karlsruhe (Germany) for the Mérida Atmospheric Research Station at Pico Espejo (MARS). The present-day precipitation map shown in Figure 4B was compiled from these data using nearest-neighbor interpolation (Arya et al., 1998), and it highlights the strong precipitation gradient between the northern and southern flanks of the Venezuelan Andes, with precipitation ranging from 1.6 to 3.4 m yr−1 on the southern flank as opposed to 0.09–1.1 m yr−1 on the northern flank. A particular feature is the arid patch that expands into the orogen between El Vigía and Mérida: Hot dry winds from the north exploit the Chama River valley to penetrate deep into the orogen, generating a unique arid climate in this area (Fig. 4B). A remotely sensed (Tropical Rainfall Measuring Mission [TRMM], NASA) precipitation data set synthesized by Bookhagen and Strecker (2008) shows overall similar patterns, both qualitatively and quantitatively.
Seismicity
Historical and instrumental seismicity in the Venezuelan Andes is strongly concentrated along the Boconó fault system. Smaller seismic events are scattered within a band of several tens of kilometers width adjacent to this fault zone, indicating that many of the fault branches are also active (Fig. 5A). However, most of the seismicity occurs along the main trace of the fault at an average depth of ∼15 km. Larger seismic events tend to occur at greater depth to the northwest (Lake Maracaibo basin) and southeast (Barinas basin) of the surface trace of the Boconó fault, reaching more than 40 km depth (Dewey, 1972; Niu et al., 2007). A seismic zone of intermediate depth (∼160 km) occurs toward the southwestern boundary of the Venezuelan Andes and continues below the Eastern Cordillera of Colombia. This significant concentration of events is known as the Bucaramanga seismic nest (Schneider et al., 1987) and occurs within the subducted Caribbean slab below northern South America (van der Hilst and Mann, 1994). More scattered, but relatively high-magnitude (M > 5) earthquakes are associated with the north-south–oriented Icotea, Valera, and Burbusay fault systems to the north of the Venezuelan Andes (Fig. 5A).
Focal mechanisms suggest predominantly right-lateral faulting along the Boconó fault, left-lateral faulting along the north-south–trending faults to the north of the Venezuelan Andes, and orthogonal thrusting along the northwest and southeast foreland fold-and-thrust belts (Colmenares and Zoback, 2003; Corredor, 2003; Cortés and Angelier, 2005). These focal mechanisms indicate a compressional stress regime with σ1 oriented approximately WNW-ESE across the central Venezuelan Andes, evolving toward a strike-slip regime with a NW-SE–directed σ1 axis to the northeast. Studies of active tectonic landforms in the Venezuelan Andes, together with regional tectonic reconstructions, suggest that the current tectonic regime was installed during Pliocene–Quaternary times (Backé et al., 2006; Egbue and Kellogg, 2010).
In order to quantify the effects of seismicity across the Venezuelan Andes, we compiled a seismicity record over the past century (from January 1911 to January 2011), using data available from the digital library of the Geophysics Laboratory of Universidad de Los Andes, Mérida (http://lgula.ciens.ula.ve/), and data provided by the Fundación Venezolana de Insvestigaciones Sismológicas (FUNVISIS; http://www.funvisis.gob.ve). The data were filtered using two criteria: (1) epicenters of earthquakes located between latitudes 72.25°W and 70.00°W and longitudes 7.75°N and 10.00°N; (2) only data with reported local magnitudes Ml were considered. Figure 5A shows a summary of earthquakes that occurred in the Venezuelan Andes during the past century. We calculated the released seismic energy (Se) from the local magnitudes using the classical expression of Gutenberg and Richter (1954):
The values of the parameters a and b were estimated by a least-squares fit of cumulative magnitude-frequency relationships constructed from subsamples of the seismic database for each catchment in 0.5° × 0.5° cells and are equivalent to the intersect and slope, respectively, of the Gutenberg-Richter relationship (Gutenberg and Richter, 1954). Released seismic energy values were summed within circles with radius of 25 km around the epicenter of each earthquake. Figure 5B shows the resulting map of seismic energy obtained from this procedure. The rate of seismic energy release is highest in the central Venezuelan Andes (Chama catchment) and decreases toward the northeast and southwest. However, the calculated pattern is strongly affected by the Ml > 5 earthquakes that occurred on the Burbusay, Valera, and Icotea fault systems.
The record of seismic energy release spans only 100 yr, which is significantly shorter than the return period of major earthquakes in the Venezuelan Andes (300 yr for M > 7 earthquakes; Audemard, 1997). Consequently, the pattern of released seismic energy may be locally underestimated. However, the seismicity records brittle deformation of the upper crust; the spatial distribution and frequency of earthquakes are intuitively related to the rate of brittle deformation (e.g., Holt et al., 2000). Thus, we can use the compiled seismic database to estimate the present-day distribution of brittle strain rate and extrapolate the total amount of seismic strain over time scales longer than the observation interval, using the observed earthquake magnitude-frequency (Gutenberg-Richter) relationship. To achieve this, we used the method described by Braun et al. (2009) and calculated seismic/brittle strain rate as:
in which the parameters a and b are defined and calculated as explained already; Mmax is the maximum observed magnitude; μ is elastic shear modulus; and ΔV is the volume of the crust (that is, the moving 0.5° × 0.5° cell area multiplied by depth of the maximum-magnitude earthquake) in which the earthquakes were observed over a period of time Δt (in this case, Δt = 100 yr). The depth of the maximum-magnitude earthquakes (33–163 km) generally exceeds the depth of the brittle-ductile transition (∼15–20 km). Because we used the seismic strain rate as a proxy for brittle deformation, we recalculated seismic strain rates using only earthquakes with hypocentral depths less than 20 km. However, we did not find any significant differences between the two approaches. The maximum-magnitude bin used in the least-squares fit always had at least one earthquake in it. Cells with a correlation coefficient r2 < 0.95 (mostly due to an incomplete catalogue) were not considered. In order to check the robustness of the results, we tested the effect of removing the minimum- and maximum-magnitude bins on the a and b values and the effect of forcing b to be exactly 1, but neither caused the seismic strain rate to change significantly.
Figure 5C shows the resulting map of seismic/brittle strain rate from subsamples (sliding 0.5° × 0.5° cells) of the seismic database for the Venezuelan Andes. The resulting seismic strain-rate map (Fig. 5C) shows maximum deformation occurring in the central and northwest Venezuelan Andes, with a second maximum occurring to the south of the mountain belt in the area of the 21 December 2001, Mw = 5.6 earthquake. Seismic strain rates vary between ∼10−17 s−1 at the northeastern (Agua Viva–Chejendé catchment) and southwestern extremities of the belt, the latter influencing average seismic strain rates in the Chama catchment, and ∼10−15 s−1 in the center of the belt (Mimbós, San Pedro, and Coloncito catchments).
Short-Term Erosion Potential
The long-term exhumation rates estimated from detrital AFT ages can be compared to model predictions of the intensity of short-term erosion using the erosion-index approach of Finlayson et al. (2002). The erosion index (EI) can be calculated in different ways as a function of stream power, which is the rate of potential energy expenditure by flowing water and has been used extensively in studies of erosion, sediment transport, and geomorphology as a measure of the erosive power of rivers and streams (Wilson and Gallant, 2000; Wobus et al., 2006). The analysis is based on a prediction of bedrock incision rate as a function of stream power (Finlayson et al., 2002; Tucker and Whipple, 2002):
where e is the local incision rate, A is upstream drainage area (used as a proxy of discharge), S is local slope, and m, n, and k are constants. The parameter k is mainly related to bedrock erodibility. Given the similar geologic and geographic conditions of the studied catchments and the lack of information on relative erodibility of the different lithologies outcropping in the Venezuelan Andes, we take k to be uniform throughout the study area. Setting k to unity, the predicted erosion index becomes:
Spatial variations in precipitation P can be incorporated into the prediction of EI in order to study their influence on spatial variability of the erosion potential:
where (Ap) is the pixel area, P is the local precipitation, and the summation sign implies summing along the flow-lines within the catchment in order to calculate the flow accumulation. We term EIp the precipitation-modulated erosion index.
Different m and n values can be employed in Equations 6 and 7, depending on the control of river incision rates by total stream power, stream power per unit channel width, or shear stress (Finlayson et al., 2002; Tucker and Whipple, 2002). In the case where incision is controlled by total stream power (TSP), m = n = 1. For incision controlled by stream power per unit channel width (USP), m = 1/2 and n = 1. If incision is controlled by fluvial shear stress power (SSP), m = 1/3 and n = 2/3.
Logarithmic erosion index maps for the Venezuelan Andes predicted by the six possible models (TSP, USP, and SSP for uniform or spatially variable precipitation) are shown in Figure 6. These maps emphasize distinct zones of high erosion potential associated with the steepest terrain and largest discharge of the main rivers. If uniform precipitation is considered, the most important zones of high erosion potential of the Venezuelan Andes are located in the central Chama and Santo Domingo valleys, with secondary regions of high erosion potential on both the northern and southern flanks. Consequently, under this assumption, the Chama and Santo Domingo Rivers, together with the small catchments (Tucaní, San Pedro, and Mimbós) on the northwest flank of the orogen, have high relative erosion indexes (whether considering TSP, USP, or SSP), with the peripheral Coloncito and Agua Viva–Chejendé River catchments showing lower erosion indexes (Table 2).
When the precipitation data are incorporated in the erosion index predictions, the results differ significantly because of the strong orographic effect (Fig. 4B), with maximum erosion potential shifting to the southeastern flank of the mountain belt (Fig. 6). In particular, the predicted high relative erosion index in the central Chama River valley disappears when precipitation is taken into account, due to the pronounced aridity of this valley. Consequently, the southeast-draining Santo Domingo catchment is predicted to have the highest relative erosion index (whether considering TSP, USP, or SSP), followed by the Chama River catchment. Incorporating spatially variable precipitation lowers the relative erosion index values for the small northwestern Tucaní, San Pedro, and Mimbós catchments, which become indistinguishable from those for the peripheral Agua Viva–Chejendé and Coloncito catchments (Table 2).
DISCUSSION: RELATIONSHIPS AMONG TECTONICS, CLIMATE, AND EROSION IN THE VENEZUELAN ANDES
Whether long-term exhumation rates in mountain belts are controlled to first order by tectonic or climatic factors remains a matter of debate. Some authors have argued for strong coupling between long-term exhumation and precipitation, for instance, for the Central Andes (Montgomery et al., 2001) and Washington Cascades (Reiners et al., 2003), while others have argued for decoupling between long-term exhumation and precipitation, such as in the central Himalaya (Burbank et al., 2003) or in the European Alps (Vernon et al., 2009). Recently, Mora et al. (2008) argued for coupling between precipitation and exhumation rates in the Eastern Cordillera of Colombia, which is contiguous to the Venezuelan Andes. Can long-term exhumation rates in the Venezuelan Andes be correlated to present-day precipitation rates? If they are uncorrelated with precipitation, what could be the controlling factor driving exhumation? The underlying question is, how strongly are tectonic and climatic processes coupled and on what time scales? Table 2 summarizes our observations on long-term exhumation, predicted short-term erosion potential, and potential controlling factors for the seven studied catchments in the Venezuelan Andes. The challenge lies in comparing exhumation rates over several millions of years, derived from detrital AFT ages, with present-day precipitation or seismicity data that were collected over the past 100 yr or less.
In order to gain insight into the potential controls on erosion and exhumation rates in the Venezuelan Andes, we calculated Pearsonian correlation coefficients between each of the measures reported in Table 2. Table 3 summarizes the results of this analysis. Given that we compare all variables for seven catchments, correlations are statistically significant (at a 95% confidence level) for a Pearson correlation coefficient r ≥ 0.7.
Figure 7 shows how long-term exhumation rates in the Venezuelan Andes correlate with different potential control parameters (present-day relief, precipitation, seismic energy release, seismic strain rate, and stream power). A first observation is the very strong positive correlation (r = 0.92) between long-term exhumation rates and 5-km radius relief, implying that the present-day relief of the Venezuelan Andes is adapted to the long-term exhumation rates. The correlation we find here is much stronger than that reported, for instance, in the European Alps (Wittmann et al., 2007; Vernon et al., 2009) or in the San Bernardino Mountains of California (Binnie et al., 2007). The reason for this is probably the comparably lower exhumation rates and relief in the Venezuelan Andes, so that bedrock landsliding on threshold slopes, which tends to decouple relief and exhumation rates (Montgomery and Brandon, 2002), is less important with respect to these other mountain belts. In effect, large proportions of slopes close to the threshold for landsliding are only encountered in the central Sierra Nevada and Sierra la Culata blocks of the Venezuelan Andes (Bermúdez et al., 2010).
In contrast, long-term exhumation rates appear to be decoupled from present-day precipitation rates; they appear even (weakly) negatively correlated with present-day precipitation (i.e., highest exhumation rates occur on the dry northwest flank of the orogen). Also, whereas short-term erosion indexes (EI) are not correlated to long-term exhumation rates for any of the three models (i.e., TSP, SSP, or USP), the correlations become even weaker or negative when spatially variable precipitation rates are taken into account in the calculation of these measures (EIp). The lack of correlations suggests that the present-day precipitation pattern does not strongly control long-term exhumation rates in the Venezuelan Andes, in contrast to what has been inferred for the contiguous Eastern Cordillera of Colombia (Mora et al., 2008). However, two caveats need to be recalled before concluding from these data that climate and exhumation are decoupled in the Venezuelan Andes: (1) the relatively limited spatial extent of our sampled catchments, for which the wet southern flank is clearly under-represented, and (2) the time scale problem mentioned previously. Considering the first, it is clear that our data set would benefit from inclusion of additional remote south-flank catchments. As for the problem of comparing measurements on strongly varying time scales, whereas we obviously acknowledge that we cannot readily extrapolate the present-day precipitation measurements several million years into the past, we do note that (1) the Neogene sedimentary record of northern South America suggests that the topographic relief of the Venezuelan Andes, and therefore its associated orographic imprint, has been in place since late Miocene times (Hoorn et al., 1995; Díaz de Gamero, 1996); and (2) Quaternary glaciations, which may strongly modify erosion patterns in some mountain belts (e.g., Burbank et al., 2003; Gabet et al., 2008; Vernon et al., 2009), have been relatively limited in the Venezuelan Andes (Schubert, 1984; Stansell et al., 2006). It has been suggested, both in the Andes and elsewhere (e.g., Bookhagen et al., 2005; Abbühl et al., 2010), that spatial patterns of erosion are strongly influenced by the occurrence of extreme events, leading to decoupling between patterns of erosion and present-day average climate. This could be the case in the Venezuelan Andes, but sufficient resolution in the regional climate record to address this question is currently lacking.
In order to assess potential tectonic controls on long-term exhumation rates, we used cumulative seismic energy release and seismic strain rate as proxies for tectonic forcing (Tables 2 and 3). We estimated the cumulative seismic energy released within the different catchments in two different ways: by averaging the values of Figure 5B within each catchment, or by simply summing the seismic energy released by each earthquake within the catchment boundaries and normalizing by catchment area. The difference between the two methods is the extent to which earthquakes occurring outside the catchment boundaries are taken into account.
The inferred seismic energy release correlates weakly to moderately with either catchment-averaged exhumation rate or 5-km-radius relief, with r values varying between 0.41 and 0.64 (Table 3). As noted previously, the pattern of seismic energy release is strongly controlled by large (Ml > 5) strike-slip earthquakes located outside the Venezuelan Andes, which contribute significantly to accumulated seismic energy in the low-exhumation Agua Viva–Chejendé catchment, for instance. The seismic energy release only integrates a century of data and, similar to the precipitation records, may therefore not be directly comparable to long-term exhumation rates and relief. However, there is very little correlation either between measures of seismic energy release and stream-power–based erosion indexes, suggesting that short-term erosion rates (if these are correctly predicted by the stream-power models) are decoupled from seismic energy release.
In contrast to the pattern of released seismic energy, the inferred seismic strain rate correlates very strongly with both catchment-averaged exhumation rates (r = 0.81) and 15-km-radius relief (r = 0.85). Catchments on the northwest flank of the orogen that show the largest seismic strain rates (Mimbós, San Pedro, Coloncito; ∼10−15 s−1) are also characterized by the highest relief (>1650 m) and exhumation rates (>0.4 km m.y.−1). In contrast, the northwestern Agua Viva–Chejendé catchment, which has the lowest relief and exhumation rates, also shows very low seismic strain rates (2.5 × 10−17 s−1).
Our data thus suggest that active tectonic deformation of the Venezuelan Andes provides a much stronger control on long-term exhumation rates throughout the orogen than the pattern weighted by precipitations. They also suggest that the widely used stream-power–based erosion potential does not adequately model erosion rates throughout the mountain belt. The reason for this may be that the simple stream-power expression does not take into account the effects of sediment flux, stochasticity of discharge, and incision thresholds (e.g., Whipple, 2004; Lague, 2010). We have previously suggested an overall tectonic control on relief and exhumation rates in the Venezuelan Andes because the orogen can be divided into fault-bounded blocks that each have their characteristic relief and exhumation history (Bermúdez et al., 2010), as also observed in other obliquely convergent mountain belts (e.g., Spotila et al., 2007). It would be interesting to map out erosion rates throughout the Venezuelan Andes using cosmogenic nuclides in stream sediments in order to analyze whether the same patterns emerge on shorter time scales.
Detrital AFT analysis of modern river sediment provides an efficient tool for studying long-term exhumation rates in complex areas with difficult access, such as the Venezuelan Andes. We have shown that the technique efficiently records average catchment-wide long-term exhumation rates when compared to in situ samples. The detrital AFT ages of seven major catchments of the Venezuelan Andes reproduce and extrapolate the exhumation patterns reported by Bermúdez et al. (2010, 2011) and can thus be used to infer exhumation rates in areas where in situ data are absent. Our results suggest that using weighted average exhumation rates, in order to include the effect of higher sediment yields in rapidly exhuming areas of a catchment, improves both the fit to observed detrital age distributions and the correlations with potential control parameters.
Catchment-averaged long-term exhumation rates in the Venezuelan Andes are fairly constant at 0.31–0.48 km m.y.−1 Rates are higher (>0.4 km m.y.−1) on the northwestern flank of the mountain belt (Mimbós, San Pedro, Tucani, and Coloncito Rivers), whereas they are lowest (0.31 km m.y.−1) in the northeastern Agua Viva–Chejendé catchment. The large Chama and Santo Domingo catchments draining the central Venezuelan Andes show intermediate rates of 0.37–0.38 km m.y.−1 Average exhumation rates correlate very well with relief of the catchments as well as with seismic strain rates, but correlations with both stream-power–based predictions of short-term erosion potential and precipitation are weak or negative.
The lack of correlation between long-term exhumation rates and relief, on the one hand, and precipitation, on the other, suggests that either precipitation is not the main controlling factor driving exhumation and relief development in the Venezuelan Andes, or that the short-term record of present-day precipitation is not representative of long-term average values. Alternatively, erosion may be effectively controlled by extreme climate events that are not captured by the record. A moderate correlation with seismic energy release indicates that the 100 yr seismic record does not fully capture the current deformation, because of the long recurrence time of large seismic events. However, we show that calculating the seismic strain rate and its extrapolation over geologic time is feasible and allows us to study relationships among long-term exhumation rate, relief, and tectonics. Our study suggests that the climatic control on exhumation rates in the active orogens of northern South America may have been overstated. Climatic variations appear to only have a second-order control on relief, erosion, and long-term exhumation rates, as has been suggested elsewhere (e.g., Riebe et al., 2001a, 2001b; Kirchner et al., 2001).
This study was supported by the Consejo de Desarrollo Científico y Humanístico (CDCH) de la Universidad Central de Venezuela (UCV), project number PI 08-00-6219-2006 and ECOS-Nord project V08U01. We thank engineers Juan Flores and Antonio León for support during field work. We acknowledge Gerhard Kopp of the Institute for Meteorology and Climate Research, University of Karlsruhe, Germany, for providing the meteorological data from the Mérida Atmospheric Research Station for Pico Espejo (MARS). María Elena Naranjo of the Universidad de Los Andes (ULA) provided precipitation data of the following stations: Páramo de Mucuchies, Páramo Pico El Aguila, Los Plantíos, Mucubají, Valle Grande, and Tabay. FUNVISIS (Fundación Venezolana de Investigaciones Sismológicas) provided access to the seismicity data. Finally, we thank Jean Braun and Christoph Glotzbach for discussion and assistance during the writing of this manuscript, and Bodo Bookhagen and an anonymous reviewer for constructive comments.
1GSA Data Repository Item 2012271, Fig S1: comparison among cumulative density functions (CDF) of single-grain ages for all the catchments; Table S1: Results of Kolmogorov-Smirnov equality test for the CDF's, is available at www.geosociety.org/pubs/ft2012.htm, or on request from editing@geosociety.org, Documents Secretary, GSA, P.O. Box 9140, Boulder, CO 80301-9140, USA.
© 2013 Geological Society of America
(A) Geologic and structural map of the Venezuelan Andes, modified from Case et al. (1990), Audemard et al. (2000), and Bermúdez et al. (2010, 2011). Major fault systems are indicated (IFS—Icotea; BFS—Boconó; CSAFS—Central-Sur Andino; CFS—Caparo; VFS—Valera; and BurF—Burbusay). Tectonic blocks across the text: Sierra Nevada, Sierra La Culata, Caparo, and Trujillo are delimited by Boconó fault system and SE thrust; NW thrust and Boconó fault system; Boconó fault system, Central-Sur Andino fault system–Caparo fault system; and Boconó fault system, Valera fault system, and Burbusay fault, respectively. (B) Simplified structural cross section of central Venezuelan Andes (modified from Colletta et al., 1997). SLC—Sierra La Culata, SN—Sierra Nevada de Mérida. MB—Maracaibo Basin.
Shaded 90-m-resolution digital elevation model of the Venezuelan Andes (Jarvis et al., 2008) with location of bedrock apatite fission-track (AFT) ages (white circles) and detrital samples (star symbols). Thick dark-gray polygons indicate catchment boundaries. Histograms show distribution of detrital AFT ages for the different samples (note logarithmic age scale); the grain-age distributions were decomposed into peak age components using binomial peak fitting (Stewart and Brandon, 2004). Peak ages (P1, P2, P3) are indicated, with the number of grains (percentage in parentheses) that constitute each population.
Comparison of measured (continuous black line; dashed lines indicate 95% confidence limits) and predicted bedrock (gray lines indicate 1000 random samples) cumulative density age functions (CDFs) for the Chama catchment; inset shows probability-density functions (PDF) for comparison. (A) A comparison for random (unweighted) sampling of bedrock age distribution. (B) Results for a weighted age distribution, where the probability of sampling a particular bedrock age is a function of the associated long-term exhumation rate relative to the average exhumation rate (see text for discussion). Numbers show average Kolmogorov-Smirnov (KS) and Kuiper (KT) statistics, with associated p values, which test the null hypothesis (H0—the distributions are indistinguishable). The number of simulations that fail the KS and KT test at a significance level p = 0.05 is also indicated.
(A) A 5-km-radius relief across the Venezuelan Andes, draped over a shaded relief image. Peaks over 4300 m elevation in the central part of the range are indicated by triangles. Mean relief for each analyzed catchment is summarized in Table 2. (B) Average precipitation pattern (m yr−1) across the Venezuelan Andes, compiled from various databases (see text for details), is overlain on shaded relief image of topography.
(A) Major active faults systems (modified from Audemard et al., 2000) and seismicity database compiled for the period 1911–2011 from digital libraries at Universidad de Los Andes (http://lgula.ciens.ula.ve/) and FUNVISIS (http://www.funvisis.org.ve). (B) Cumulative seismic energy released, calculated from the earthquake database. Individual earthquakes with M > 5 occurring outside the Venezuelan Andes are indicated (1—31 December 1993, 9.65°N, 70.70°W, Mw = 5.4; 2—21 December 2001, 8.17°N, 70.96°W, Mw = 5.6; 3—03 January 2006, 9.89°N, 71.92°W, Mw = 5.0; 4—04 August 2006, 9.97°N, 70.65°W, Mw = 5.2; 5—29 December 1995, 9.75°N, 70.26°W, Mw = 5.3; 6—12 February 1998, 9.14°N, 70.23°W, Mw = 5.6). (C) Seismic strain rate as predicted from the distribution and magnitude of earthquakes and the maximum earthquake magnitude Mmax, of each catchment using a 0.5° × 0.5° binning of the data (see text for explanation).
Ten-kilometer-radius average logarithmic stream power index maps across the Venezuelan Andes. Left columns (A, C, and E) take spatially variable precipitation into account (stream power calculated following Eq. 7); right columns (B, D, F) assume spatially constant precipitation (stream power calculated following Eq. 6). (A–B) Total stream power (TSP; m = n = 1 in Eq. 6 and Eq. 7). (C–D) Unit stream power (USP; m = 0.5; n = 1). (E–F) Shear stress power (SSP; m = 0.33; n = 0.67).
Correlation plots for: (A) 5-km-radius relief, (B) present-day precipitation, (C) seismic energy release, (D) seismic strain rate, (E) total stream power (uniform precipitation) and (F) total stream power (spatially variable precipitation), all versus exhumation rate. Released seismic energy was calculated from the map of cumulative seismic energy release within 25-km-radius windows around each earthquake (Fig. 3B). Seismic strain rate was calculated only for catchments with more than 10 earthquakes following Equation 4 in the text. For all correlations, r is the correlation coefficient calculated for a least-squares regression line without considering error bars, and rw is the correlation coefficient calculated for the Williamson (1968) regression line.
DETRITAL APATITE FISSION-TRACK DATA FROM MODERN RIVER SAMPLES IN THE VENEZUELAN ANDES
MEASURES OF LONG-TERM EXHUMATION RATE AND POTENTIAL CONTROL PARAMETERS FOR EACH CATCHMENT
PEARSONIAN CORRELATION COEFFICIENTS BETWEEN MEASURES OF TABLE 2 FOR ALL CATCHMENTS


text:
Q: How to send UDP messages to each machine in LAN I want to send Udp message to each machine in LAN by not using broadcast. so, my code like this:
int sock = socket(AF_INET, SOCK_DGRAM, 0);

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Only about first 20 machines (192.168.1.2 ~ 192.168.1.20) could receive the message, most of other machines could not receive it.
I try to send to 20 machines, then sleep(5), then send to the other 20 machines, and so on. but this way is useless.

A: By definition, UDP is stateless, and does not guarantee delivery. From https://en.wikipedia.org/wiki/User_Datagram_Protocol

There is no guarantee of delivery, ordering, or duplicate protection.

So, you've observed that some of your UDP packets weren't delivered. That's perfectly fine, since UDP packet delivery is not guaranteed.

redpajama_set_name: RedPajamaStackExchange


California will not require eighth-graders to take algebra – a transfer that is line with the Frequent Core standards being adopted by most states, but that will leave college students unprepared for college. Berliner, David C. 2009. Poverty and Potential: Out-of-School Elements and School Success. Boulder and Tempe, AZ: Education and the Public Interest Heart, and Education Policy Analysis Unit. (accessed October 12, 2013). Maturity is a character trait one has to come back to on their own. To grasp when maturity is not warranted, in order that the kid can have some fun, is just as necessary as to when being mature at time when warranted or wanted.
Listed below are some approaches recognized by research as more effective: Democratic educational approaches are in; indoctrination out. I not too long ago attended a workshop put on by a special education advocacy group. The workshop was supposed to introduce us particular ed dad and mom to the best way to navigate the 'major shifts in implementing common core requirements.'. Preece, J. (2004). Grownup education and poverty discount: a world precedence. Papers presented at Botswana Conference, College of Botswana. Pp. 407.
Folks can study at their very own tempo without any strict regulations; there aren't any class schedule and fixed timings and assignments. Solely the standard of work is evaluated, not the speed or the appearance of the student. Even, individuals can interact online and discuss with the scholars, students, researchers, subject-matter consultants and professors for any sort of question or issues.
Behaviorally talking, the problem introduced to the staff of learners will trigger them to regulate to the stimuli and foster a change in conduct thus producing learning. Cognitively the members of the crew will use reflective techniques to seek the advice of and provide a solution. As to the list you supplied, I have to reconcile that with my different sources, however I can let you know I excluded most of the line gadgets as they weren't direct help to the public; a lot was for providing infrastructure.
I provided college students alternatives to carry small-group discussions with their web site classmates on the assigned readings from the supplementary text for the course, Worlds of Distinction (Stoller & Gibson, 1997). This text provides a collection of short articles, in addition to poetry and prose that focus on diversity within the getting old experience of individuals, households, and racial and ethnic groups. Pupil participation in such small group discussions was excellent. The teams faxed their comments to me and got credit for participation. A solo scholar at a site may ship his or her feedback in the same manner. I typically tied these student feedback into subsequent lectures.


Reports of people seeing Angels come from all over the world. Some with events of unexplained happenings in times of tragedy that disappear into the ether. Do Angels exist? In my opinion, yes. They comfort us in times of sorrow, they lead us away from danger, they give us signs, they rejoice with us.
We connect with Angels through prayer. Prayer is one of the most beautiful things we can do in the world. It takes us to a place of surrender, serenity, and grace. It is where we spiritually talk one on one with Jesus and send him gratitude for His many blessings, including sending his Angels to protect us, our family, friends, and surroundings. Jesus has never failed me, even in times when things turned out differently than expected. Prayer is like that, we receive for our highest good, not for our highest want.
Angels work in union with Jesus to assist us in our highest purpose in life. I am humbled by their presence and deeply grateful for their guidance. Think of Angels as guides sent from Jesus who protect and support you while also loving, comforting and celebrating life with you.
Angels beckon us to the beauty of life as they call out to us. My Mom always taught me to say hello to everyone I meet with a smile because they could be an Angel in disguise or sent by an Angel to give us messages and I am delighted by the conversations I have in life. Sometimes they lead back to memories of my childhood, to things I have been reading about, to places that would interest me, to leading me on a journey in life. The timing of Angelic synchronicity is divine and unmistakable. While you may question it, I have found the most comforting way is to have faith and learn from it.
All we need to be is open in life to the many possibilities. Divine fate reaches beyond our exterior and touches our soul to raise our energy to that of Spirit giving the purest of love that heals us. If you have never felt their love, I encourage you to open yourself to receive it. While we don't always see the miracles being created in life, we sometimes get a glimpse of them, even if in the corner of our eye or in our dreams. I always welcome them as I quiet my mind and meditate on their love to hear their words and write as they guide me.
Angels are everywhere. A choir of Angels singing in the cemetery on the other side of a mound that no one saw or heard other than a child, to being lifted by something under the water while falling in the ocean jumping ice clampers in the harbor, to a shower of rose petals along a path, to cherubs visiting prior to a baby physically entering the world.
Signs of Angels, especially in nature are all around us. We need only stop and see them as Angels guide us to them. Animals are also one of the purest connections with our soul. Deer, for instance, bring warnings and greetings in life when we need a visual representation. Simply watch and pay attention to understand the message.
Prayers are always heard, you just need to say them. He has compassion for us, you need only be open to receiving it. Pray and be grateful to Him for sending His Angels to call upon us. For He is always with us, all the days of our lives. God bless and blessed be, in Him, with Him, through Him, as His Angels unite hand in hand and glorify Him for our greatest good. Amen.
Would it be possible to share articles from your website on my own website at www.twinflames1313.com?


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text:
Virgin Road – Die Henkerin und ihre Art zu leben (japanisch ) ist eine Light-Novel- und Mangareihe von Mato Sato, welche in den Gattungen Dark Fantasy, Yuri, Isekai und Action zu verorten ist.

Der Roman startete im Juli 2019 im Magazin GA Bunko des Verlages SB Creative mit Illustrationen von Nilitsu. Die Reihe brachte bisher (Stand: 17. Juni 2022) sieben Bände hervor. Im Juni 2020 startete Mato Sato einen Manga-Ableger mit Zeichnungen von Ryō Mitsuya, der beim Verlag Square Enix im Magazin Young Gangan erscheint. Die Mangareihe brachte (Stand: 17. Juni 2022) drei Bände hervor, die im Tankōbon-Format erschienen. Sowohl die Light Novel als auch der Manga wurden von Yen Press für eine Veröffentlichung außerhalb Japans in englischer Sprache lizenziert. Im deutschsprachigen Raum erscheinen die Roman- und Mangareihe beim Verleger Altraverse.

Im Jahr 2021 wurde die Produktion einer Anime-Fernsehserie angekündigt, die im April 2022 im japanischen Fernsehen startete. Die Geschichte verfolgt die Priesterin Menou und die aus einer anderen Welt beschworenen Akari Tokitō auf deren gemeinsamer Reise um einen Weg zu finden, Akari zu töten.

Zusammenfassung

Ausgangslage
Vor langer Zeit kamen Menschen, die Verlorenen aus einer fremden Welt namens Japan in die Hiesege. Jeder dieser Menschen verfügt über eine besonders starke Fähigkeit, die als "Pures Konzept" bekannt sind. Dadurch, dass diese Menschen aus Japan in diese Welt kommen – unter anderem durch rituelle Beschwörungen – wurde diese von der Kultur der Beschworenen beeinflusst. Für lange Zeit florierte die Zivilisation. Allerdings stellte sich heraus, dass die Verlorenen die Kontrolle über ihre übermenschliche Fähigkeiten verlieren, je öfter sie diese einsetzen und die Welt dadurch ins Verderben stürzen können.

Bis in die Gegenwart existieren vier legendäre Desaster, die als Human Error bekannt sind: Das Salzschwert, welches den gesamten westlichen Kontinent in eine riesige Salzwüste verwandelte, das Pandæmonium – ein undurchdringlicher, sich niemals auflösender Nebel am südlichen Archipel aus dem regelmäßig Monster strömen – die mechanische Zivilisation, die den gesamten Osten kontrolliert und Starhusk, welches den nördlichen Kontinent zum schweben brachte.

Um zukünftige Katastrophen zu verhindern, wurde das Beschwören von Andersweltern verboten und unter Strafe gestellt. Die Faust, eine Auswahl von Priesterinnen und Priestern der Kirche, überwacht, dass die Regeln nicht gebrochen werden. Unter diesen Priestern befinden sich auch so genannte Executioner, die über magische Fähigkeiten verfügen und im Geheimen Attentate auf Anderswelter verüben, die in der Welt auftauchen.

Handlung
Menou ist eine erfahrene Assassine im Auftrag der Kirche, die als Executioner bekannt sind. Ihre Aufgabe besteht darin, die in ihre Welt beschworenen Menschen, so genannte Verlorene zu neutralisieren, bevor diese zu einer Gefahr für die Zivilisation werden. Denn die Verlorenen haben übernatürliche Fähigkeiten, die als Pures Konzept bezeichnet werden, welche bei übermäßiger Anwendung außer Kontrolle geraten und die Welt ins Verderben stürzen können. Als Menou eines Tages von dem König beschworenen Mitsuki erfährt, dass der Adel eine weitere Person, ein Mädchen, in diese Welt gerufen hat, sendet diese ihre Assistentin Momo zum Schloss, um Informationen zu sammeln.

Von dieser erfährt Menou, dass der Junge die Wahrheit gesagt und der König tatsächlich eine weitere Person in diese Welt gerufen hat. Menou macht sich auf den Weg Weg zum Schloss und versucht dort dem Mädchen, Akari Tokitō, unter einem Vorwand zur Flucht zu verhelfen. In einem unachtsamen Moment des Mädchens, wird diese von Menou scheinbar heimtückisch ermordet. Jedoch muss Menou feststellen, dass ein Attentat auf das Mädchen nicht ausreicht, um sie zu töten. Denn ihr pures Konzept der Zeit sorgt dafür, dass sie diese trotz ihres Todes zurückdrehen kann. Menou schlägt Akari vor, unter dem fälschlichen Vorwand einen Weg zu finden, um sie wieder in ihre eigene Welt zu bringen, eine Reise anzutreten. Tatsächlich aber sucht Menou nach einer Möglichkeit, Akari umzubringen, bevor diese die Kontrolle über ihre Fähigkeit verliert und die Welt ins Ünglück stürzt.

Charaktere

 Eine junge Priesterin, die auf das Jagen und Ermorden von Verlorenen ausgebildet wurde. Sie ist sich im klaren, dass die meisten Verlorenen unschuldig sind und keine Fehler begangen haben. Ihre Ausbildung schreibt allerdings vor, dass Verlorene ermordet werden müssen, da sie eines Tages von ihrer Fähigkeit korrumpiert werden und dadurch die Welt ins Verderbnis stürzen. Bevor Menou auf Akari, eine Verlorene, trifft, hat sie immer wieder den Traum, sie in Japan getroffen zu haben. Nun agiert Menou unweigerlich als Eskort für Akari und sucht nebenbei nach einem Weg, sie zu ermorden. Als Kind überlebte Menou ein Unglück, bei dem ihre Heimat durch das Salzschwert in eine Salzwüste verwandelt wurde. Dieser Vorfall führte dazu, dass ihre Seele durch das Trauma "gebleicht" und so zu einer "emotionslosen Schale" wurde. Zu diesem Zeitpunkt wurde Menou von der Priesterin Flare gefunden und von ihr ausgebildet. Als Executioner hat Menou völlige Kontrolle über ihr Ether und trägt vorwiegend ein Messer zum Töten bei sich.

 Eine Oberschülerin, die von König Grisarika aus Japan in Menous Welt gerufen wurde. Ihr Pures Konzept der Time erlaubt es ihr jegliche Elemente der Zeit zu kontrollieren, einschließlich das instinktive Zurückdrehen der Zeit, um sich wiederzubeleben, sobald sie stirbt. Zu Beginn wirkt Akari tollpatisch und hohlköpfig, aber auch freundlich und zutraulich, was dazu führte, dass Akari Menou bei ihrer ersten Begegnung schnell vertraute, da sie glaubte, dass das Aufeinandertreffen mit ihr Schicksal gewesen sei. In Wahrheit jedoch hat Akari unter Kosten ihrer Erinnerung, was lediglich ein Gefühl des Déjà-vus hinterlässt, die Zeit bereits mehrfach auf Anfang gestellt um Menou vor ihrem Tod zu retten. Sie kennt Menous wahre Absicht und schwört, sich nur von ihr töten zu lassen. Akari ist in Menou verliebt.

 Wie Menou ist Momo eine Priesterin und zudem ihre Gehilfen, die Menou bei ihren Missionen durch Informationsbeschaffung, das Vorbereiten von Tarnung und im Kampf unterstützt. Sie hegt seit jeher Gefühle für Menou, da sie seit der Kindheit miteinander eng befreundet sind. Das zeigt sich unter anderem daran, dass Momo die Haarbänder, die sie einst von ihr geschenkt bekam, wie einen Schatz behütet. Sie beginnt Eifersucht auf Akari zu entwickeln, als Momo erkennt, dass Menou und Akari sich näher kommen. Wie Menou hat auch Momo völlige Kontrolle über ihre Magie und führt als Waffe eine Sägekette mit sich.

 Die Kriegerprinzessin von Grisarika. Sie ist voreilig und mutig, weswegen sie anstatt ihrer Rolle als Adel und ihren höfischen Aufgaben nachzukommen, lieber nach starken und ebenbürtigen Kontrahenten sucht. Sie kämpft mit einem Großschwert, welches mit Feuermagie ausgestattet wurde.

 Eine legendäre Priesterin, die durch ihr unglaubliches magisches Können und der Anzahl an niedergestreckten Verlorenen von sich reden gemacht hat. Nachdem sie die junge Menou von einem Verlorenen rettet, nimmt Flare diese als ihre Auszubildende bei sich auf.

 Eine Erzbischöfin der Kirche und Menous direkte Vorgesetzte. Sie erteilt Menou die Aufgabe, Akari in die Stadt Garm zu eskortieren, um diese dort zu exekutieren. In Wahrheit jedoch will Orwell sich Akaris Pures Konzept zunutze machen, um die Zeit für sie zurückzudrehen. Orwell ließ zuvor junge Mädchen entführen und deren Lebenskraft aussaugen, um diese auf sich selbst zu übertragen.

 Ein japanischer Oberschüler, der in Menous Welt beschworen wurde. Von Mitsuki erfährt Menou, dass neben ihm eine weitere Person beschworen wurde. Sein Pures Konzept [Null] erlaubt es ihm alles und jeden auszulöschen. Er wird von Menou ermordet, bevor er seine neu gefundene Kraft missbrauchen kann.

 Die Tochter des Grafen Libelle, der über die gleichnamige Hafenstadt regierte, und einer Verlorenen. Da sie nicht die Kräfte ihrer Mutter geerbt hat wurde sie von anderen Menschen verschmäht, was dazu führte, dass Manon sich das Leben nehmen wollte. Heute befiehlt sie über eine Organisation, die sich The Fourth nennt und von sich behauptet, eine eigene emanzipierte gesellschaftliche Klasse zu sein. Während sie sich in der Öffentlichkeit als naiv und sanftmütig zeigt, hat sie eine Neigung zu sadistischen Morden. Privat ist sie die "Große Schwesterfigur" für Pandæmonium, aus dessen Blut sie eine gefährliche Droge produziert. Sie stirbt, als sie sich als Opfer anbietet, um Pandæmonium zu befreien, wird aber von dieser später wiederbelebt.

 Eine der vier so genannten Human Errors, heraufbeschworene Menschen, die die Kontrolle über ihr Pures Konzept verloren und die Welt ins Verderben stürzten. Obwohl sie vor mehreren hundert Jahren beschworen wurde, besitzt sie den Körper eines zehnjährigen Mädchens. Ihr Pures Konzept [Chaos] erlaubt es ihr nach belieben Monster zu erschaffen und zu kontrollieren. Da sie von ihrem Puren Konzept vollständig korrumpiert wurde, agiert sie wie ein Kleinkind ohne eigenen Willen. Sie ist in einem niemals auflösenden Nebel gefangen und wurde durch Manon Libelle eigenes Opfer kurzfristig befreit.

Medien

Light Novel
Mato Sato startete die Light-Novelreihe im Jahr 2019. Die Illustrationen werden von Nilitsu gezeichnet. Der Verlag SB Creative veröffentlichte diesen in seinem Magazin GA Bunko und erhielt später eine eigenständige Printveröffentlichung unter dem Verlag. Bis zum 17. Juni 2022 wurden bereits sieben Bände der Romanreihe in Japan veröffentlicht. Im September des Jahres 2020 kündigte der US-amerikanische Verleger Yen Press an, den Roman für eine englischsprachige Veröffentlichung lizenziert zu haben.

Eine deutschsprachige Veröffentlichung erscheint beim Verleger Altraverse.

Manga
Am 5. Juni 2020 startete Mato Sato basierend auf seiner Romanreihe einen Manga-Ableger, der von Ryō Mitsuya gezeichnet und im Young-Gangan-Magazin des Verlages Square Enix erscheint. Bis zum 17. Juni 2022 wurden drei Bände der Mangareihe im Tankōbon-Format herausgebracht. Im März des Jahres 2022 gab Yen Press bekannt, den Manga außerhalb Japans in englischer Sprache zu veröffentlichen.

Altraverse, welcher sich die Rechte an einer deutschsprachigen Veröffentlichung der Romanreihe sichern konnte, gab bekannt, sich ebenfalls die Rechte an der Manga-Umsetzung gesichert zu haben.

Anime-Fernsehserie
Auf dem GA Fest 2021, welches als Livestream-Event ausgetragen wurde, wurde angekündigt, dass die Romanreihe eine Umsetzung als Anime-Fernsehserie erhalten werde. Zu der Enthüllung wurden bereits die Sprecherinnen der beiden Hauptcharaktere Menou und Akari bekannt gegeben. So leihen Iori Saeki der Priesterin Menou und Moeka Kishimoto der Oberschülerin Akari ihre Stimmen. Im Juli 2021 wurde das Kernproduktionsteam der Öffentlichkeit vorgestellt. Die Anime-Fernsehserie entstand im Animationsstudio J.C.Staff unter der Regie von Yoshiki Kawasaki. Das Drehbuch stammt aus der Feder von Shōgo Yasukawa. Das Charakterdesign wurde von Keiko Tamaki basierend auf den Illustrationen von Nilitsu entworfen. Michiru komponierte die Serienmusik. Als Produzenten fungierten Egg Firm und SB Creative.

Das Lied im Vorspann heißt Paper Bouquet und wurde von Project Mili interpretiert. Der Abspanntitel, Touka Serenade, wurde von der Sängerin ChouCho eingesungen. Die zwölf Episoden umfassende Animeserie lief vom 1. April bis zum 17. Juni 2022 auf Tokyo MX, BS11 und AT-X im japanischen Fernsehen. International wurde der Anime von Sentai Filmworks lizenziert und exklusive auf HiDive im Simulcast mit englischsprachigen Untertiteln gezeigt, darunter auch in Deutschland.

Zwischenzeitlich wurde angekündigt, dass die Animeserie eine englischsprachige Synchronisation und eine spätere Disc-Veröffentlichung im englischsprachigen Raum erhält.

Synchronisation

Rezeption
Die Romanreihe wurde mit dem Hauptpreis des GA-Bunko-Awards bedacht und erhielt aufgrundessen eine Umsetzung als Anime-Fernsehserie.

Die erste Episode des Anime wurde von mehreren Redakteuren des Onlineportals Anime News Network besprochen und erhielt überwiegend positive Resonanz. Gelobt wurde unter anderem die Balance zwischen den Charakteren, die Herangehensweise an das Isekai-Genre – so wird die Geschichte nicht aus dem Gesichtspunkt eines Beschworenen, sondern aus einer weltlichen Bewohnerin erzählt – sowie das Aufgreifen sämtlicher Klischees, die das Genre hervorgebracht hat. Lediglich Rebecca Silverman bewertete die erste Folge mittelmäßig. Sie schrieb, dass das Konzept zwar erfrischend, aber nichts neues sei und nennt das Werk Goodbye Otherworld, See You Tomorrow von Kazamidori als Vergleichsreferenz heran. Auch Momo, ein Charakter aus der Serie, die sie als "räuberische Lesbe" und ihr Verhalten wurden von ihr kritisch bewertet.

Weblinks
 Offizielle Homepage der Anime-Fernsehserie (japanisch)
 Eintrag zur Romanreihe in der Enzyklopädie von Anime News Network
 Eintrag zur Anime-Fernsehserie in der Enzyklopädie von Anime News Network (englisch)
 Eintrag in der Internet Movie Database (englisch)
 Eintrag zur Anime-Fernsehserie bei AniSearch

Einzelnachweise

Light-Novel-Zyklus
Manga (Werk)
Literatur (Japanisch)
Literatur (21. Jahrhundert)
Fantasyliteratur
Drama
Anime-Fernsehserie
Fernsehserie der 2020er Jahre
Fantasy-Fernsehserie

redpajama_set_name: RedPajamaWikipedia


text:
Twin Cities Daily Planet (https://www.tcdailyplanet.net/movies-tom-cruises-valkyrie-rides-slow-and-low/)
MOVIES | Tom Cruise's "Valkyrie" rides slow and low
By Jim Brunzell III (TC Daily Planet) | December 23, 2008
Valkyrie, the much-hyped and heavily advertised Tom Cruise action vehicle, opens on Christmas Day. After some reshoots were done last June, and after no fewer than four different release dates were announced—at one point, release was even going to be delayed until February 2009—everyone can now witness this amazing story told with lifeless imprecision.
Cruise's character, Colonel Claus von Stauffenberg, was an important figure in German history who led a failed assassination attempt against Hitler called "Operation Valkyrie" in 1944, but director Bryan Singer (The Usual Suspects, X-Men, Superman Returns) has turned Valkyrie from what could have been a captivating suspense thriller into a boring high school history class film strip.
valkyrie, a movie directed by bryan singer. opens december 25 at theaters across the twin cities. for information, see moviefone.com.
In a terrific opening action sequence, shot by Singer's regular cinematographer Newton Thomas Sigel, we see how Stauffenberg lost his eye, hand, and a few of his fingers on the remaining hand; shortly after Stauffenberg's recovery, Valkyrie dives into the assassination plot, with the events unfolding at a lethargic pace. Many unnecessary characters show up and contribute little or nothing to the plot (veteran actor Kenneth Branagh appears and then disappears for almost 90 minutes, only to show up in the woods for no apparent reason), and the tone of the film is all wrong. While there should have been suspense during a crucial bomb-planting scene, the event seemed as mundane as grabbing a newspaper; an unimportant phone call, on the other hand, is edited as though someone's life were in the balance.
The film does provide some unintentional laughs, including scenes of Stauffenberg using his newly minted glass eye as a prop. Carrying it around in a metal box, he takes it out and puts it in as he pleases. In a very contrived scene, he also uses it as an ice cube to get someone's attention. That eye gimmick was used to better effect in a far superior Cruise film, Minority Report.
Cruise is an actor capable of portraying rebels with a cause, but he stands out as the only American in an otherwise all-European cast. Why not cast a relatively unknown British or German actor to play Stauffenberg instead of slapping an eye patch on Maverick? Imagine if a young Shia LeBouf had been cast in place of Daniel Radcliffe in the Harry Potter series, with Jonathan Lipnicki playing Ron and Emma Roberts instead of Emma Watson as Hermione. If that sounds laughable, the same can be said about Cruise playing a German resistance officer. The only difference is that instead of a magic wand, he has a glass eye.
Jim Brunzell III (djguamwins@yahoo.com) writes on film for the Daily Planet and hosts KFAI's Movie Talk.
Jay Gabler

redpajama_set_name: RedPajamaCommonCrawl


The Hair Design School-E Greensboro offers 6-degree programs. Student-to-faculty ratio is 13:1. 1 high safety campus. 5.7% are women, and 94.3% are men. The average annual total cost of attendance at The Hair Design School-E Greensboro is 12253$, that is at the level of national average. 46% of full-time The Hair Design School-E Greensboro students completed their education in 150 percent of time: graduation rate is at the level of national average. Average salary after attending is $16,400, so if you studied 2 years, you'll get your funds back in less than 2 years.
Download The Hair Design School-E Greensboro Whitepaper!
Download the PDF with FULL information about the The Hair Design School-E Greensboro from opened government trustful sources - right now!
The The Hair Design School-E Greensboro is a private and academic-year institution, so it's net price represents an average of all programs and includes only undergraduates who first enrolled in the fall term and receive Title IV aid. The total cost of attendance depends on whether undergraduates live on campus, off campus (not with family), or off campus (with family).
Depending on the federal state, or institutional grant and available, The Hair Design School-E Greensboro students in your income bracket may pay more of less than the overall average costs.
The estimated cost of the Cosmetology, Barber/Styling, and Nail Instructor (the 2d largest program, lasting 6 months) is $5,150 per year and $61,800 in total.
139 of The Hair Design School-E Greensboro undergraduate students were awarded with some type of financial aid, it's 72 percents of all undergraduate students. This makes The Hair Design School-E Greensboro number 152 in the amount of financial aid awarded to students among all educational institutions in North Carolina.
Students at The Hair Design School-E Greensboro awarded 5 types of loans or aids, the biggest percent of students received a federal grant aid.
Here are the learning opportunities available in The Hair Design School-E Greensboro.
The Hair Design School-E Greensboro graduation rate is below the national average.
46% of full-time students enrolled for the first time to The Hair Design School-E Greensboro completed the education program and got a degree in 150 percent of the expected time of completion.
The student-to-faculty ratio at The Hair Design School-E Greensboro is 13:1, that means that for every 13 students the institution has one professor, lecturer or specialist with a degree in education. Lower student-to-faculty ratio is better - it means that professors can dedicate more time and attention to each student.
In The Hair Design School-E Greensboro the biggest percent of students are enrolled in on-campus courses.
Here are the students enrolled exclusively in distance education courses at The Hair Design School-E Greensboro and grouped by their location. Distance education courses are the most popular for students located in not reported location.
The campus located by 2001 E Wendover Ave address in Greensboro, North Carolina.
The Hair Design School - E. Greensboro in comparison of all branches in the US. It is calculated as the average percent of crimes yearly by five years of data for every campus, based on an overall number of students studying there. The branch is a part of The Hair Design School-E Greensboro with 2.13% of maximum crimes a year. The most often crimes detected on The Hair Design School - E. Greensboro are robbery, burglary, and motor vehicle theft.
The Hair Design School-E Greensboro offers 6 programs in total: 3 are for less than 1-year certificate programs and 3 are 1-year, but less than-2-year certificate programs.
This is one of the lowest number of programs in comparison with other 196 universities in North Carolina state. The Hair Design School-E Greensboro is one of the few institutions in North Carolina that offers a less than 1-year certificate program.
The Hair Design School-E Greensboro provides coursework for undergraduate students оnly.
In 2014-2015 academic year estimated full-time equivalent undergraduate enrollment was 114 students with 102912 сontact hours for 12-month instructional activity period.
I got my hair done here while visiting from CT and it was such a great job done by the student and the teachers so professional. On my next visit to Greensboro I will be getting my hair done at the school again and my nails also.
Rude people and the staff is racist, avoid if you don't enjoy humiliation.
Love this place at night good people friendly environment..
I will never go back here again. Went about two weeks ago to get hair relaxed and cut. I needed a change and I figured this place would be good. Not the case. I had to wait about 30 minutes before I was seen which I am ok with because it was near New Year's eve and I figured they would be busy. I get to my stylist and she acts like doing my hair is last thing she wants to do. I ask her questions about how I can get my hair to grow she kinda just says "time" and kept talking to someone else. Yes, the people doing your hair are students, but I expected more professionalism. Then the girl shadowing her, my stylist told her she didn't bother interacting with the customers much and that she did not like doing hair. My stylist kept going to other people's stations talking to them and halfway ignoring me it felt at times. I gave it two stars instead of one for the fact that the instructors were extremely nice and helpful in suggestions for me. The student stylists I saw were not acting professional and my stylist, I definitely did not get a professional vibe from her. I will not be returning here to get my hair done, but I do thank the two instructors, the one up front and the lady with the long hair who were both very kind and helpful.


AMUSE News: BBQ Thursday! Welcome to our New Executive!
AMUSE News: Group 2 Important Announcement! Race and Work event! Film Screening!
Salut union friend! Welcome to this week's jam-packed listserv! Please take a minute to read through some very important information for Group 2s, and other upcoming AMUSE funtimes!
[AMUSE NEWS] BBQ Time! Free Life Insurance! Open Board Spot!
AMUSE Has a Board of Representatives Spot Open!


Viewing topic "Does the Motif 7 Classic got a ADAT out?"
I got the AIEB2 expension board but not quite sure what Optical out means. Is that what they also call ADAT out? I check in the specs on motifator.com but i dont see the word adat anywhere. I wanna get a ADA converter so i just wanna be sure before purchasing. Thanks for answering.
Re: Does the Motif 7 Classic got a ADAT out?
The stock Motif 7 has an optical digital output. Adding the AIEB2 provides you an additional optical and an electrical digital output as well as optical and electrical digital inputs. In all cases the outputs are digital duplicates of the analog Main outputs. All of these digital I/O utilize the S/PDIF format.
There is no support for ADAT digital interfaces for the Motif Classic.
So there's no other output on the entire Motif 7 Classic(AIEB2 included) that can be plugged to an ADA converter for me to get 16 tracks/outs running at the same time?
And is it true that i cannot use the ''RCA'' s/pdif out with the optical out(or vice versa) at the same time?
You are correct that there is no way to record 16 separate outputs (either analog or digital) from the Motif Classic at one time. With the AIEB2 the maximum would be 10 channels (the Main L&R and Assignable L&R from the stock Motif and then additional assignable outputs on the AIEB2).
One very last question Brad, Where do i go in my motif to assign my s/pdif out to a channel? I usually go to Edit/track 1/F3(outsel) when i use my analogs but i dont see any options for s/pdif. Is there somewhere i can enable the s/pdif out?
As I've stated in my earlier posts, the S/PDIF outputs are always duplicates of the Main Mix. Any part that is not routed to one of the assignable outputs will by definition be present on both the Main L&R analog outputs and (all of) the S/PDIF (digital) outputs.


text:
Jane Daly's writing career began at eight years old when a newspaper published one of her short stories. Over the years she has been featured in many publications and has matured into writing novels, including the award winning Because of Grace. Jane and her husband currently volunteer their time as counselors in a wide variety of subjects in Northern California.
Follow Jane on her website and Facebook.
Look for Because of Grace: A Mothers Journey from Grief to Hope in early 2015.
Every mother fears losing her child. When that horror became a devastating reality for author Jane Daly, everything she believed in became distorted. As she tried to come to grips with a life that would never be normal again, Jane found God's presence leading her from the pain of loss to the peace that passes all understanding. Take a walk with Jane Daly through this story of sorrow and healing, and experience the touch of God that ultimately carried her from grief to hope.
This book offers an honest and unfiltered glimpse into a mother's grieving process. Women who have experienced the loss of a child will find it helpful and repayable. I'm proud of Jane for opening up her heart with such honesty and vulnerability.
—Jim Daly, President, Focus on the Family
"Losing a child is the most heart-wrenching trauma a human being can ever experience. Jane Daly knows—she lost her beloved son, Bobby, to cancer when he was too young to die. Many who face such loss would be lost themselves, never to speak of it, never to come to grips with the awful reality, never to share with someone who had faced the same struggle. Not Jane. Instead she has given us Because of Grace, a headfirst dive into the dark pool of pain, agony, anger, fear, and despair that confronted her. But she doesn't drown in it. Instead, with beautifully crafted words and an open heart, she takes us sailing on an unforgettable journey that ends where it began—in the loving arms of a God who was with her every step of the way. Beautifully done, a must read."
—Patrick E. Craig, author of The Apple Creek Dreams series
"When grief comes our way, we feel alone . . . lost. It's then that we can appreciate comforting words from someone who has already walked the path leading from grief to grace. Jane has made that journey. Her experience bolsters us during the hardest days."
—Nick Harrison, author of Magnificent Prayer and Power in the Promises
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This is what the LORD says: "Cursed is the one who trusts in man, who draws strength from mere flesh and whose heart turns away from the LORD. — Jeremiah 17:5 (NIV)
Of David. The LORD is my light and my salvation— whom shall I fear? The LORD is the stronghold of my life— of whom shall I be afraid? — Psalm 27:1 (NIV)


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