To examine the changes in pain, the severity of the neck disorder, craniovertebral angle, and muscle activity in young adults with forward head posture. 37 “N” University students in their 20s with forward head posture, including both male and female participants. Measurement of pain, NDI (neck disorder index) craniovertebral angle, and muscle activity were taken before and after the 6 week intervention period. The pain was measured using the visual analog scale. The severity of the neck disorder was measured using the NDI The craniovertebral angle was measured by taking a photo. The muscle activity was measured using surface electromyography. Neck posture correction exercises paired with proprioceptive training is the most effective intervention for reducing pain. Both neck posture correction exercises paired with Kinesio taping or proprioceptive training are effective interventions for addressing neck disability, craniocervical angle, and muscle activity. Neck posture correction exercises paired with Kinesio taping or proprioceptive training are more effective at addressing pain, neck disorder, craniocervical angle, and muscle activity than performing the neck posture correction exercises alone.

The aim of the study was to investigate the effects of incentive spirometry and Ujjayi breathing technique on the pulmonary function of smokers. Subjects were individuals who had a smoking habit of at least a year. Subjects were randomly divided into 3 groups: the incentive spirometry group (n=8), Ujjayi breathing technique (n=9), and a group applying both incentive spirometry as well as Ujjayi breathing technique (n=8). Each intervention was performed twice a day, 5 times a week, for a total of 8 weeks whereupon the change in pulmonary function was evaluated. A spirometer was used to measure FVC, FEV1, and FEV1/FVC. The survey used for this study included the Fagerström Test of Nicotine Dependence (FTND) and the Shortness of Breath Questionnaire (SOBQ). Study results for the comparison within groups showed that in the group that performed both the incentive spirometry and Ujjayi breathing technique, FEV1 improved with statistical significance (p<.05). Furthermore, within this comparison the FEV1/FVC improved with statistical significance. Comparison amongst the groups showed no statistically significant differences in all areas. Following, to effectively increase pulmonary function in young adult smokers, both incentive spirometry and Ujjayi breathing technique should be employed together.

황사발생 전과 후인 2003년 10월 26일 00시부터 29일 18시까지 한국의 동쪽 연안에 있는 강릉시에서 PM10, PM2.5와 PM1 매 시각별 분포를 조사하였다. 황사가 고비사막으로부터 유입되기 전까지는 매 시각 PM10 농도가 20μg/m3 내외, PM2.5가 10μg/m3 내외, PM1가 5μg/m3 내외로 매우 낮은 농도를 나타내지만 황사가 유입된 10월 27일 09시부터 28일 05시까지는 PM10의 농도의 범위가 48.20~154.57μg/m3이며, 평상시 비해PM10의 농도가 3.8배로 높았다. 유사하게 PM2.5의 농도는 26.92~93.19μg/m3의 변화폭을 나타내며, 최대 3.4배로 높게 나타났고, PM1의 농도는 19.63~76.05μg/m3의 변화폭을 갖고, 최대 14.1배가 되었다. 황사가 나타나는 동안에는 수송된 황사먼지의 집중적인 유입과 동시에 도로 위의 차량의 밀집과 일몰 후 주거지역에서의 보일러 가동으로 출근시각인 09시와 퇴근시각인 17시에 PM의 고농도가 나타났다. 황사가 관측되기 전에는 미세입자와 극미세입자의 비율을 나타내는 (PM10-PM2.5)/PM2.5는 0.75~7.12, 극미세입자와 초극미세입자의 비율을 나타내는 (PM2.5-PM1)/PM1는 0.23~1.90로 나타났으며, 황사가 관측되는 기간에는 0.60~1.25와 0.21~0.37을 각각 나타내었다. 강릉시에 황사가 나타나기 전에는 2.5μm 큰 입자들이 2.5μm 이하의 극미세입자보다 PM10의 농도에 큰 영향을 주었으나, 황사가 관측되는 기간에는 2.5μm 이하의 극미세입자들이 PM10의 고농도 출현에 크게 기여하였다. 황사가 관측되는 기간에는 지역의 PM고농도에 2.5μm 이상의 큰 입자가 기여하는 일반적인 양상과 반대였다.

In order to investigate the variations and corelation among PM10, PM2.5 and PM1 concentrations, the hourly concentrations of each particle sizes of 300 ηm to 20 μm at a city, Gangneung in the eastern mountainous coast of Korean peninsula have been measured by GRIMM aerosol sampler-1107 from March 7 to 17, 2004. Before the influence of the Yellow Dust event from China toward the city, PM10, PM2.5 and PM1 concentrations near the ground of the city were very low less than 35.97 μg/m3, 22.33 μg/m3 and 16.77 μg/m3, with little variations. Under the partial influence of the dust transport from the China on March 9, they increased to 87.08 μg/m3, 56.55 μg/m3 and 51.62 μg/m3. PM10 concentration was 1.5 times higher than PM2.5 and 1.85 times higher than PM1. Ratio of (PM10-PM2.5)/PM2.5 had a maximum value of 1.49 with an averaged 0.5 and one of (PM2.5-PM1)/PM1 had a maximum value of 0.4 with an averaged 0.25. PM10 and PM2.5 concentrations were largely influenced by particles smaller than 2.5 μm and 1 μm particle sizes, respectively. During the dust event from the afternoon of March 10 until 1200 LST, March 14, PM10, PM2.5 and PM1 concentrations reached 343.53 μg/m3, 105 μg/m3 and 60 μg/m3, indicating the PM10 concentration being 3.3 times higher than PM2.5 and 5.97 times higher than PM1. Ratio of (PM10-PM2.5)/PM2.5 had a maximum value of 7.82 with an averaged 3.5 and one of (PM2.5-PM1)/PM1 had a maximum value of 2.8 with an averaged 1.5, showing PM10 and PM2.5 concentrations largely influenced by particles greater than 2.5 μm and 1 μm particle sizes, respectively. After the dust event, the most of PM concentrations became below 100 μg/m3, except of 0900LST, March 15, showing the gradual decrease of their concentrations. Ratio of (PM10-PM2.5)/PM2.5 had a maximum value of 3.75 with an averaged 1.6 and one of (PM2.5-PM1)/PM1 had a maximum value of 1.5 with an averaged 0.8, showing the PM10 concentration largely influenced by corse particles than 2.5 μm and the PM2.5 by fine particles smaller than 1 μm, respectively. Before the dust event, correlation coefficients between PM10, PM2.5 and PM1 were 0.89, 0.99 and 0.82, respectively, and during the dust event, the coefficients were 0.71, 0.94 and 0.44. After the dust event, the coefficients were 0.90, 0.99 and 0.85. For whole period, the coefficients were 0.54, 0.95 and 0.28, respectively.

Using three-dimensional non-hydrostatical numerical model with one way double nesting technique, atmospheric circulation in the mountainous coastal region in summer was investigated from August 13 through 15, 1995. During the day, synoptic westerly wind blows over Mt. Mishrung in the west of a coastal city, Sokcho toward the East Sea, while simultaneously, easterly upslope wind combined with both valley wind from plain (coast) toward mountain and sea-breeze from sea toward inland coast blows toward the top of the mountain. Two different directional wind systems confront each other in the mid of eastern slope of the mountain and the upslope wind goes up to the height over 2 km, becoming an easterly return flow in the upper level over the sea and making sea-breeze front with two kinds of sea-breeze circulations of a small one in the coast and a large one in the open sea. Convective boundary layer is developed with a thickness of about 1km over the ground in the upwind side of the mountain in the west and a thickness of thermal internal boundary layer from the coast along the eastern slope of the mountain is only confined to less than 200 m. On the other hand, after sunset, no prohibition of upslope wind generated during the day and downward wind combined with mountain wind from mountain towardplain and land-breeze from land toward under nocturnal radiative cooling of the ground surfaces should intensify westerly downslope wind, resulting in the formation of wind storm. As the wind storm moving down along the eastern slop causes the development of internal gravity waves with hydraulic jump motion in the coast, bounding up toward the upper level of the coastal sea, atmospheric circulation with both onshore and offshore winds like sea-breeze circulation forms in the coastal sea within 70 km until midnight and after that, westerly wind prevails in the coast and open seas.

As prevailing synoptic scale westerly wind blowing over high steep Mt. Taegulyang in the west of Kangnung coastal city toward the Sea of Japan became downslope wind and easterly upslope wind combined with both valley wind and sea breeze(valley-sea breeze) also blew from the sea toward the top of the mountain, two different kinds of wind regimes confronted each other in the mid of eastern slope of the mountain and further downward motion of downlsope wind along the eastern slope of the mountain should be prohibited by the upslope wind. Then, the upslope wind away from the eastern slope of the mountain went up to 1700m height over the ground, becoming an easterly return flow in the upper level of the sea. Two kinds of circulations were detected with a small one in the coastal sea and a large one from the coast toward the open sea. Convective boundary layer was developed with a thickness of about 1km over the ground in the upwind side of the mountain in the west, while a thickness of thermal internal boundary layer(TIBL) from the coast along the eastern slope of the mountain was only confined to less than 200m. After sunset, under no prohibition of upslope wind, westerly downslope wind blew from the top of the mountain toward the coastal basin and the downslope wind should be intensified by both mountain wind and land breeze(mountain-land breeze) induced by nighttime radiative cooling of the ground surfaces, resulting in the formation of downslope wind storm. The wind storm caused the development of internal gravity waves with hydraulic jump motion bounding up toward the upper level of the sea in the coastal plain and relatively moderate wind on the sea.