bluuebunny/crossref_metadata_2025_split huggingface dataset:
Okul Müdürlerinin Liderlik Stilleri İle Okulların Örgütsel Çekicilikleri Arasındaki İlişkinin İncelenmesi
Authors: SEVER Necla , ATİK Servet 
Published: May 2021

Bu araştırmada okul müdürlerinin benimsediği liderlik stilleri ile okulların örgütsel çekicilik düzeylerini incelemek, okul müdürlerinin kullanmış olduğu liderlik stilleri ile okulların örgütsel çekicilik düzeylerini bağımsız değişkenler açısından incelemek ve okul müdürlerinin benimsemiş olduğu liderlik stillerinin okulların örgütsel çekiciliğinin anlamlı yordayıcıları olup olmadığını incelemek amaçlanmıştır. Araştırmanın evrenini, Malatya ilinde yer alan kamu okullarında görev yapan Battalgazi ilçesinde 4600 ve Yeşilyurt ilçesinde 6024 olmak üzere 10624 öğretmen oluşturmaktadır. Araştırmanın örneklemini ise Malatya iline bağlı Battalgazi ve Yeşilyurt merkez ilçelerinde 2019-2020 Eğitim-Öğretim yılında, MEB’e bağlı kamu okullarında (ilkokul, ortaokul ve lise düzeyinde) görev yapan, evrende yer alan okullardan araştırmaya gönüllü olarak katılan 452 öğretmen oluşturmaktadır.
Araştırmanın verileri; Kişisel bilgiler formu, Örgütsel Çekicilik Ölçeği ve Liderlik Stilleri Ölçeği ile toplanmıştır. Araştırmanın sonuçlarına göre; dönüşümcü liderlik, öğretimsel liderlik, kültürel liderlik, vizyoner liderlik boyutları ve okulların örgütsel çekiciliklerinin “katılıyorum” düzeyinde olduğu; etik liderliğin ise “tamamen katılıyorum” düzeyinde olduğu belirlenmiştir. Okulların örgütsel çekiciliklerinde, öğretmenlerin müdürle çalışma süresine göre anlamlı farklılığa rastlanmıştır. Dönüşümcü liderlik, öğretimsel liderlik ve etik liderlik boyutlarında okuldaki öğrenci sayısına göre anlamlı farklılığa rastlanmıştır. Etik liderlik boyutunda mesleki kıdem değişkenine göre anlamlı farklılığa rastlanmıştır. Dönüşümcü liderlik ve kültürel liderlik değişkenlerinin ise okulların örgütsel çekiciliğinin anlamlı yordayıcıları olduğu belirlenmiştir.
Preliminary report on the Long Beach earthquake
Authors: Wood Harry O. 
Published: May 2021

Summary
The “Long Beach Earthquake” occurred on March 10, 1933, at 5:54:08 p.m., P.S.T., very nearly. Its origin was very near to 33° 34′.5 north latitude, 117° 59′ west longitude, at a depth of about ten kilometers (6 miles).
Previous shocks, emanating from sources not far distant, were not definitely recognizable as “fore-shocks” in advance, notwithstanding discovery in recent years of small changes in level in the neighboring region.
Many aftershocks followed. The sources of some were very near the chief epicenter; others originated at some distance. The distribution, and its significance, must await thorough study.
Hard shaking probably continued for ten to fifteen seconds. The duration of perceptible vibration varied from place to place, and with local conditions.
Doubtfully, on account of ground conditions, “apparent” intensity of grade IX, 1931 scale, may have been developed in a few small places. Grade VIII was manifested in numerous places, and is the characteristic maximum intensity of this shock. Serious damage to bad construction resulted in many places inside an area of about 1,200 square kilometers (say 450 square miles), with the greatest concentration in and near Compton, and in and near Long Beach.
No fault displacement was found at the surface anywhere.
To a small extent minor disturbances to ground water, secondary cracks in the ground, and similar minor geological effects were observed in the meizoseismal area.
As usual miscellaneous effects—sounds, movement of liquids, visible surface waves (?), luminous phenomena (?), etc.—were reported from the area of vigorous shaking.
All the evidence indicates a fairly strong, moderately large shock in the local earthquake class, manifesting about the same intensity over an area of about the same size as the shock in Santa Barbara in 1925.
The disastrous consequences of the shock were due chiefly to poor construction on bad natural ground in a rather densely populated district.
A second study of blasting recorded in Southern California
Authors: Wood Harry O. , Richter Charles F. 
Published: May 2021

Summary
Investigation of several blasts subsequent to those considered in our previous study, and in particular a major blast set off near Victorville, California, on September 12, 1931, has yielded results as follows.
1. In two cases the time of detonation was determined (a) very accurately in the case of the blast near Victorville by a precise method, and (b) probably with substantially equal accuracy in the case of the blast in the Arroyo Seco, though the method employed was inherently less precise.
2. Phases, or definite changes in registered motion, have been recognized and measured which appear to correspond to successive arrivals of waves traveling, apparently, along direct paths with different apparent velocities, as follows: 6.0− 5.9+, 5.55, 5.4−, 5.0+, 4.1, 3.5−, 3.4−, 3.25, 3.15, 3.0−, 2.7± kilometers per second.
3. In the present study no positive evidence has been found to indicate reflected waves, or waves refracted along deeper layers. Phases considered in the previous study to indicate such waves are now found to be susceptible of alternative explanations.
Difficulties have been encountered, as discussed in the body of the paper, in the interpretation and satisfactory explanation of certain of the very numerous apparent phases, particularly those which appear to indicate waves with apparent velocities of 6.0− to 5.9+, and 4.1 kilometers per second.
From this it is again clear that further opportunities for similar investigations are of great importance. For this reason, and also in order that blasts of moderate, or larger, magnitude may not be included in lists of small local earthquakes, it is suggested that all such blasts set off in the region of Southern California should be reported to the Seismological Laboratory at Pasadena—and, whenever practicable, sufficiently in advance to permit preparations for thorough study.
Surface-reflected waves of shallow-focus earthquakes*
Authors: Hodgson Ernest A. 
Published: May 2021

Abstract.—In the case of the seismological tables developed by seismologists during the first decade of the present century, it was always assumed that the focus lay in the surface. Under such circumstances, the so-called PR1-wave, the wave once reflected at the surface at a point midway between the focus and the point of observation, would be expected to have a travel-time double that for the compressional or P-wave to the mid-point. Observation failed to support the earlier PR1-tables, which were constructed from the P-tables on this assumption. It was later found that earthquake foci do not always, nor even generally, lie in the surface. Furthermore, the P-curves for earthquakes known to have shallow foci are now found to differ considerably from the earlier curves based on group data. It became desirable to study the travel-times for the reflected waves from the data of a single well-defined earthquake. The seismometric study of the Tango earthquake, Japan, March 7, 1927, recently completed by the writer, furnished the opportunity for such a study, the results of which are presented in this paper.
Motion of the surface of the earth in the compressional phase of a deep-focus earthquake, and the effects of a layered crust
Authors: Sharpe J. A. 
Published: May 2021

Summary and Conclusions
In this paper the difficulties which attend any attempt to obtain the ground displacement which occurs during the passage of an earthquake wave have been illustrated. Reliable curves of ground displacement are difficult to obtain because the majority of seismographs, as operated, are poorly adapted for any purpose but the indication of the time of arrival of earthquake phases. This study has demonstrated, however, the practicability of an attempt to obtain ground displacement from seismograms, and has illustrated some of the uses which may be made of curves of ground displacement, when obtained.
The use of the dynamic magnification to obtain the amplitude of ground displacement corresponding to an impulse on a seismogram was shown to give highly erroneous results. For long-period seismographs, calculation of displacement by methods in which the effect of transients was retained appeared to give fairly accurate results.
The results of the study of the effects of a layered crust on the surface motion are to be considered only as preliminary, and indicative of the usefulness of a technique which hitherto has seldom been applied to seismic problems. Displacements were indicated in the horizontal components of ground displacement that were absent in the vertical, suggesting effects of crustal discontinuities. If the use of composite curves of surface displacement is valid, and the agreement between the observed and predicted curves of horizontal component of displacement is significant, the following are possible conclusions: oscillation in seismograms is a result of reflections and transformations of primary waves within the crust; the average thickness of the crust beneath the stations whose records were studied is 32 km.; the velocity change at the base of the crust takes place in a distance which is small compared to the wave length.
An appropriate research for individual stations possessing good seismographs in three components would be a study of the thickness of the crust underlying each station. For this purpose the wave velocities as determined from local earthquakes or explosions, and the arrival time of P[S*S¯] for a few deep-focus earthquakes of simple initial form, would suffice.
A knowledge of the curves of ground displacement would facilitate the solution of the following problems, among others: the effects of crustal discontinuities on the ground motion in the S phase; and the azimuthal variation of the form of the P wave, in relation to the process at the focus.
The writer wishes to thank Professor L. B. Slichter, who suggested the problem, and the directors of the many seismological stations whose coöperation in providing seismograms made the investigation possible.
Earthquakes off the coast of northern California*
Authors: Byerly Perry 
Published: May 2021

SummaryThe epicenters as located for the earthquakes of July 6, 1934, January 2, 1935, and June 3, 1936, indicate that earthquakes centering off the coast of Humboldt County do not originate on a linear extension of the San Andreas fault in Mendocino County. Figure 1 shows the epicenters of these shocks as located by two methods, and also the epicenter of the earthquake of January 31, 1922, as located by Professor Macelwane.On the basis of least square residuals alone, the epicenters located by assuming a straight-line travel-time curve for Pn to Δ=18° are better than those located by the Jeffreys-Bullen curves. But for the shock of June 3, 1935, the epicenter located by the first method is inconsistent with the S-P interval at Ferndale, whereas that obtained by the second method is consistent. For the other two shocks the epicenters located by the two methods are little different in position.Whereas the July 6 shock shows a definite Sn travel-time curve with an intercept approximately equal to that of the Pn curve, the other two earthquakes show a marked wave preceding Sn and almost masking it at the coastal stations south of the epicenter. The travel-time curve of this wave has an intercept about 15 seconds below that of Pn. This wave is longitudinal and has a period of 4.35 km/sec. It is suggested that it is P in the sedimentary layer, although objections to such an interpretation are cited.The travel-time curve of P for the July 6 shock between 26° and 40° indicates that it is composed of two nearly straight branches rather than the more smooth curve of Jeffreys and Bullen.
On supposed regional variations in travel times*
Authors: Gutenberg B. 
Published: May 2021

SummaryAn investigation of the Tango earthquake of March 7, 1927, shows that travel times for P observed in that shock agree within the limits of error of one or two seconds with the travel times found for other earthquakes and that thus far there is no indication of differences beyond the limits of observational errors between the travel-time curves of earthquakes in different regions. This statement, however, does not include the travel times to short epicentral distances of a few degrees found in various regions which are influenced by the local structures in those regions, and especially not to the travel times found from waves which have traversed only the uppermost parts under the Pacific Ocean.
The earthquake of July 6, 1934: Amplitudes and First Motion.*
Authors: Byerly Perry 
Published: May 2021

Summary
The distribution of the first motion of the P waves for the earthquake of July 6, 1934, combined with knowledge of the general faulting trends of the region, leads to the conclusion that the earthquake was caused by movement on a Fig. 6.Berkeley Wood-Anderson seismograms of the earthquake of July 6, 1934. fault bearing about N 40° W, and dipping about 84° northeasterly. The displacement vectors dipped about 26° northwesterly. The displacement consisted of a motion of the Pacific side northerly and of the continental side southerly, as in 1906. This suggests an extension of the fault which broke in 1906 in Humboldt County. A second interpolation would give a fault bearing N 46° W.
Travel times for shear waves in a granitic layer*
Authors: Birch Francis 
Published: May 2021

Abstract
Travel times for shear waves in a layer of granite have been computed on the basis of recent laboratory work which permits an approximate evaluation of the variation of velocity with depth. The results are found to agree very closely with those of Leet, found by the method of timed blasts, for New England. The mean surface velocity of shear waves in granite having their focus at the surface is computed to be 3.52 km/sec. at 568 km., decreasing to 3.26 at 25 km.; the curvature is shown to be too small to be easily recognized from records of near earthquakes. A depth of 15 km. for the granitic layer is shown to be consistent with Leet's observations of pulses through a second layer.
The determination of the extent of faulting with application to the Long Beach earthquake*
Authors: Benioff Hugo 
Published: May 2021

SummaryAn instrumental method is described for the determination of the extent of faulting in a given earthquake which depends upon the early arrival of S. If the faulting velocity is known, the exact extent is determined; otherwise, only upper and lower limits are given. Conversely, if the extent of faulting is known from field or other evidence, the faulting velocity is determined.The development given refers to a vertical fault exhibiting horizontal displacement, or, more generally, to a fault in which the displacement is parallel to the direction of extension. When the displacement is perpendicular to the direction of extension, as in a simple vertical fault, the faulting impulse is propagated by shear waves. For this condition the shear waves from the end point can never arrive earlier than the wave from the focus. On the basis of these considerations an observed early arrival of S indicates that the source is a fault movement in which the displacement is parallel to the direction of extension. In general this would refer to a horizontal extension of fault slip, although for observers in the vicinity of the epicenter it could refer to a vertical fault movement originating in the depths and propagating upward.In applying this method to the Long Beach earthquake, the available evidence indicates that faulting extended from the focus approximately to Signal Hill, a distance of 27 km., with a faulting speed of approximately 4.2 km/sec.
Note on the Eureka earthquake of June 6, 1932†
Authors: Stoneley Robert 
Published: May 2021

Summary
A rediscussion of the observations of the Eureka earthquake of June 6, 1932, gives for the waves P7.0 and P7.4 the velocities 7.15±0.065 and 7.53±0.073 km/sec., respectively. The errors quoted are standard errors, not probable errors. On the assumptions of Sparks's paper the thicknesses of the upper (granitic) and second layers come out as 12.6±2.5 km. and 12.2±1.9 km., in fairly good agreement with the values 16 km. and 14 km. given in the paper. The uncertainties arise mainly from the uncertainties in the constant terms in the linear formulae for the travel times T7.8, T′7.8, T″7.8. In one respect the assumptions made in the previous discussion lead to an inconsistency among the data, and the need for and the value of further studies along the lines of Sparks's examination of the Eureka earthquake are stressed.
The Love waves of the South Atlantic earthquake of August 28, 1933*
Authors: Wilson James T. 
Published: May 2021

Summary
The epicenter of the South Atlantic earthquake of August 28, 1933, was located at 58° 56′ S, 24° 54′ W, and the time of occurrence fixed as 22h 19m 38s U.T.
A study was made of the first motion of P. On the assumption that the earthquake was caused by a fault movement, the strike of the fault was determined as between N 33° W and N 1° E, and the dip as between 63° E and 76° E.
By integration of the seismograms the earth motion during the G phase was determined at 17 stations. This wave was found to agree with the theoretical surface wave of Love.
A study of the dispersion of G yielded the following conclusions. The crustal structure of the Atlantic Ocean region is very similar to that of the Indian and Pacific regions, and is characterized by having material with a high velocity for shear waves much nearer the surface than is observed in the continental regions. The thickness of the crustal structure in continental regions is about 30 to 40 km.
Velocity of elastic waves and structure of the crust in the vicinity of Ottawa, Canada*
Authors: Hodgson Ernest A. 
Published: May 2021

Summary
Ten seismograms, due to rockbursts at Lake Shore Mines, Kirkland Lake, Ontario, were recorded on a Benioff seismograph at Ottawa at a distance of 450 km. (279 mi.). The center of each burst was located within a few feet; but, for the purpose of preparing travel-time tables, they may all be considered to have occurred at a single point at the surface. Two of the bursts were accurately timed on the seismograph at the mine.
Six phases were registered on each seismogram, being more sharply marked on some records than on others. Five of these are well defined on nearly all the records. It is thus possible to deduce a set of arrival times at a distance of 450 km. for a burst (or earthquake) occurring at the surface; and this set of times is known with fair precision, since all the readings may be combined. The distance is determined within one part in 7000, the depth within 2000 ft. and the travel times with an error of ±.5 sec.
These travel times have been compared with those obtained by Joliat in computing his Tables for Near Earthquakes, based on the velocities deduced by Jeffreys for northern Europe and arbitrarily assuming an earth structure with two layers above the Mohorovičić discontinuity. The differences are minor and are to be explained as chiefly owing to the fact that Joliat assumed the focus to lie at the bottom instead of the top of the upper layer.
On the strength of the comparisons afforded by the ten seismograms, the focal time of each burst may be considered as known within ±.5 sec. One of the bursts was so severe that it was registered also at Shawinigan Falls, Quebec (Δ = 576 km., 358 mi.) and at Weston, Massachusetts (Δ = 935 km., 581 mi.). These records will afford a means of deducing the earth structure and velocities in the vicinity of Ottawa, and will permit the construction of tables for rock-bursts and blasts in that area up to 10° (1110 km., 690 mi.). These will be prepared and issued, together with corrections permitting their being used for local earthquakes with finite focal depth.
Should other bursts occur later at Kirkland Lake, timed by the mine seismograph and registered at Ottawa or the other stations, the data so made available may be directly used to check and add precision to the deductions made from the seismograms already in hand. Such further data would be most valuable.
Cytotoxic lesion of the corpus callosum in a patient with aphasic status epilepticus
Authors: Castiglione Juan Ignacio , Ricciardi Mario Emiliano , Bensi Catalina 
Published: May 2021

A 47-year-old man with a history of aphasic seizures presented to the emergency room with a 12-hour global aphasia. Upon admission, brain MRI did not reveal acute lesions, and EEG showed sharp waves in the left frontal-temporal region. An Aphasic Status Epilepticus was diagnosed and antiepileptic treatment was initiated with adequate response. A week after the episode, a new brain MRI showed a high-signal ovoid lesion on T2-weighted and FLAIR sequences in the central part of the splenium of the corpus callosum. On diffusion-weighted images (DWI) the lesion was hyperintense with decreased apparent diffusion coefficient (ADC) values, indicating restricted diffusion consistent with a cytotoxic lesion of the corpus callosum (CLOCC). Follow-up MRI one month later showed complete image resolution. CLOCCs are secondary lesions associated with various entities in which high levels of cytokines and extracellular glutamate cause intracellular edema and reduced diffusion, a condition called cytotoxic edema, which affects vulnerable brain regions such as the splenium of the corpus callosum. In epileptic patients, CLOCCs may be due to the effect of seizures, especially prolonged ones, as well as antiepileptic treatment itself. CLOCCs are rare radiological findings and must be recognized to avoid misdiagnosis.
Self-awareness, depression and neurocognitive functions in patients with moderate and severe traumatic brain injury
Authors: Vales Lisandro Heber , Brussain Silveira , Roman Fabian 
Published: May 2021

Introduction: Traumatic Brain Injury (TBI) is the most common cause of disability in youngpatients. In the self-awareness deficits that can arise after TBI, patients experience difficulties in understanding the disabilities resulting from their injury. This is an important problem that affects the rehabilitation processes. Materials and methods: Self-awareness, neurocognitive functions and depressive symptoms were observed in 31 outpatients with a diagnosis of moderate or severe TBI, aged between 16 and 45 years. Instruments: Patient Competency Rating Scale (PCRS), Neurocognitive Assessment and Hamilton Depression Rating Scale (HDRS). Results: Correlations were found between self-awareness and its dimensions with visuospatial skills, executive functions (double task and cognitive inhibition), episodic memory (Rey Auditory-Verbal Learning Test and Montevideo short story) and depressive symptoms. Conclusions: Patients who have suffered a moderate or severe TBI may have impaired self-awareness. Self-awareness is the ability to objectively perceive (perceive our own self), while maintaining a sense of subjectivity, It is a complex function that needs to use executive functions and episodic memory. The relationship found between interpersonal self-awareness and depressive symptoms does not seem to be conclusive, since this association is probably more complex, and involves other variables not considered in this study.