Mahatma Ghandi, a Hero

Mahatma Gandhi For me, a hero is someone who tries to make the world a better place. Christopher Paolini said, â€Å"Without fear there cannot be courage. † I agree there has to be fear before there is courage. Gandhi turned his fear into courage and decided to try to make the world a better place and as a result India gained its independence. It took conquering his fears and being a courageous hero in a peaceful way to be the leader of Indian nationalism during British rule. Gandhi fought for Indian rights. Click any fact to locate it on the web.Click Wrong? to report a problem. Cancel Mohandas Karamchand Gandhi was given the holy name Mahatma which means Great Soul. He was born on October 2, 1869 in Porbandar, India. In 1888, he sailed to England to study at the University College London and then the University of London where he studied Law. In 1893, he accepted a job in South Africa and in 1903 Gandhi opened a law firm in Johannesburg, South Africa. In 1906, Gandhi had his first protest in South Africa against anti-Indian laws and two years later he was imprisoned.In 1914, he returned to India where he became leader of the Indian National Congress (INC) supporting a plan using nonviolence to get independence. He was jailed from 1922 until 1924 for conspiracy. He was jailed again in 1930 for breaking India’s Salt Laws. In 1932, Gandhi started his famous â€Å"fast unto death† to protest British support of a new Indian constitution which gave India’s lowest classes, the â€Å"untouchables†, their separate political representation. Gandhi believed this would unfairly divide India's social classes and he believed in equality.In 1942, Gandhi began the nationwide â€Å"Quit India† movement. Five years later, India became independent from the British. Gandhi was assassinated by a Hindu fanatic on January 30, 1948 in Birla House in Delhi while at a prayer meeting. Early in his life, after seeing the misery of millions of hi s countrymen, thousands of them dying from starvation, Gandhi gave up all his money and spent his life helping the poor and the oppressed. He was the leader of the Indian nationalist group against the British rule and is commonly known as the father of his country.His strategy of a non-violent protest to get political and social progress has influenced many people. His program of peaceful non-cooperation with the British included boycotts of their goods and institutions which lead to arrests of thousands. In 1945, the British government began negotiations which ended with the formation of the two new independent states of India and Pakistan divided along religious lines. Gandhi was opposed to partition and fasted to try to bring harmony in Calcutta and Delhi. Ghandi once said, â€Å"In a gentle way, you can shake the world. This is exactly what he did. He made positive changes around him using peaceful ways. He also said, â€Å"I do not want to foresee the future. I am concerned w ith taking care of the present. God has given me no control over the moment following. † He did change his present; he changed what was happening during his life. He devoted his life to helping his countrymen gain independence and be treated as equals. This is why I believe Gandhi is a hero; he made the world a better place by being courageous, brave, a leader and a believer in being able to make a difference.

A Child Called It Essays

A Child Called It Essays A Child Called It Essay A Child Called It Essay A Child Called It is a first-person narrative of a severely abused child, Dave Pelzer, who has survived to tell his tale. This book is a brief, horrifying account of the bizarre tortures Daves mother inflicted on him, told from his point of view as a young boy. Among the cruel games Daves maniac, alcoholic mother played were smashing him face-first into mirrors, forcing him to eat the contents of his baby brothers diaper, drinking ammonia, and burning him over a gas stove. Daves story has two objectives: the first is to inform the reader how a loving, caring parent can change to a cold, abusive monster venting frustrations on a helpless child; the second is the eventual survival and triumph of the human spirit over seemingly insurmountable odds (164). Dave describes his earlier years as idyllic: In the years before I was abused, my family was the Brady Brunch of the 1960s. My two brothers and I were blessed with the perfect parents. Our every whim was fulfilled with love and care (17). His mothers behavior began to change drastically and Dave and his brothers had become afraid of her. Eventually, Dave was singled out for such vicious treatment. His mother made sure he knew that theres nothing he can do to impress her. She told him, you are a nobody! An It! You are nonexistent! You are a bastard child! I hate you and I wish you were dead! Dead! (140) School held no appeal to Dave either: At school I was a total outcast. I had no one to talk to or play with. I felt all alone (58). Since his mother rarely gave him the luxury of eating food, Dave resorted to stealing from his classmates lunch pails. The teachers and principal knew and carefully watched him. Oddly, his father never intervened. His attempts to talk to his wife about Dave failed, and only worsened the abuse. This caused Dave to hate his father: he was fully aware of the hell I lived in, but he lacked the courage to rescue me as he had promised so many times in the past (134). As the beatings and the torture continued, Dave began to give up: With no dreams, I found that words like hope and faith were only letters, randomly put together into something meaningless-words only for fairy tales (132). Inside, my soul became so cold I hated everything (133). Whats your single greatest accomplishment and why? Im so alive (155). My life as a child was extremely turbulent, being pushed and pulled in every direction. I tried as hard as I could to reach the light at the end of the dark tunnel, but it always seemed out of reach. Until suddenly, without warning, I broke free (156). What was your biggest obstacle? How did you overcome it? My mothers abusing me was no doubt my biggest obstacle. I hated Mother most and wished that she were dead. But before she died, I wanted her to feel the magnitude of my pain and my loneliness for all these years (134). As the years passed by and the beatings became more intense, I wished shed returned with a knife and ended it all.. My morale had become so low that in some self-destructive way I hoped she would kill me (141). But I made a promise to myself that kept me going. I wanted to show The Bitch that she could beat me only if I died, and I was determined not to give in, even to death (91). What one trait or characteristic would you most like to be remembered for? Why? I would definitely most like to be remembered for my resilience. Perhaps my faith and the security of my early years helped me develop enough resilience to survive the abuse and grow up to be an emotionally healthy adult with a child of my own. The challenges of my past have made me immensely strong inside. I adapted quickly, learning how to survive from a bad situation. I learned the secret of internal motivation. My experience gave me a different outlook on life, that others may never know. I have a vast appreciation for things that others may take for granted.. I hope that my story will help instill resilience in others. What was the single, most important thing youve learned? Why do you consider this so? The single, most important thing Ive learned from my past hardships was that even in its darkest passages, the heart is unconquerable. It is important that the body survives, but it is more meaningful that the human spirit prevails (165). I believe that no matter what happens in your past, you can overcome the dark side and press on to a brighter world. It is perhaps a paradox that without the abuse of my past, I might not be what I am today (166). My Reaction: I read A Child Called It in one day. Its one of those books you cant put down because you want to know whats going to happen next. I was always in constant suspense as to what Daves emotionally unstable mother was going to do to him and how he was going to survive the abuse. This book really sunk into my heart and the imagery used in the book helped put a clear picture of the dysfunctional household Dave lived in. The fact that this is a true story and millions of children suffer from the same ordeal saddens me. Also, the fact that he remembers all those horrible things that he went through in the past, in detail, is very sad. Im glad that Dave triumphed not only in finding a better, loving family, but also within himself. If I was in his shoes, I dont think Id be able to make it where he is today. His story truly changed my perspective on life. I realized how lucky I am to belong to a nice, tight-knit family and that I have it good compared to most people.

ROLE OF ABU DHABI POLICE IN REDUCING SERIOUS OF ROAD TRAFFIC ACCIDENTS Dissertation - 1

ROLE OF ABU DHABI POLICE IN REDUCING SERIOUS OF ROAD TRAFFIC ACCIDENTS TO IMPROVE THE TRAFFIC SAFETY IN EMIRATE OF ABU DHABI - Dissertation Example The study discussed that urban traffic calming schemes are often implemented in residential areas in town as a means of decreasing the environmental and safety issues prompted by road traffic. A hierarchical road system was created and through traffic was eliminated from residential streets via street closures or one-way road systems. Speed-slowing devices were often put up in residential areas. The main roads were managed in order to ensure larger traffic volume without necessarily causing delays or accidents. The meta-analysis indicates how traffic calming techniques generally decrease accidents by about 15%, with the most reduction in accidents observed in the residential areas. A similar decrease in accidents is also seen in main roads. Reductions are also observed in terms of property damage only incidents. General results in evaluation studies are rich in terms of study design and no evidence of publication issues in the evaluation studies was observed. The results also have a significant degree of external validity. In relation to road safety engineering, the management of horizontal curves was also considered in the New Zealand study by Charlton (2007). The study indicates how driver errors related to horizontal curves was caused by three-related issues – failure in driver attention, miscalculation on speed and curves, and improper lane positioning. The study indicated how advance warning signs on their own are not effective in decreasing speeds, as when they are used in combination with chevron sight boards and/or repeater arrows. Among the road marking treatments used, only the rumble strips indicated any major decrease in speed. Herringbones road marking was seen to create major improvements in driver’s lane positions, allowing the flattening of drivers’ pathways within the curves. The combined use of herringbones and chevron with the repeater arrow signs indicated a significant decrease in speed including improvements in lane po sitioning. These results indicate evidence that treatments which support perceptual signs are the most valuable remedies in managing the curve speeds for drivers. A similar study by Afukaar (2010) sought to assess road safety engineering measures, specifically for developing countries. This study indicated how vehicle speed was a factor in vehicle crashes, with Ghana used as an example. The study revealed how main driver errors mostly referred to vehicle speeds. Rumble strips and speed humps proved to be effective measures in Ghana’s roads. The rumble strips indicated on the primary Accra-Kumasi highway decreased the incidents of crashes to about 35% and deaths to 55%. Decreasing speeds may be an effective remedy in decreasing traffic crashes for low income states; however the decreased speed limits are not effective interventions without the traffic law enforcement tools needed to guarantee that limits are observed. Developing states must consider the lack of other speed con trol measures, including rumble strips and speed bumps, as well as lanes which separate slow and high-speed users, and other solutions like speed governors, and improved awareness of the issue Abu Dhabi road safety practices In general, there are few studies which have specifically covered the road safety practices in Abu Dhabi. Majority of the studies on road safety practice have covered the entire United Arab Emirates. Some of these studies shall be included in this review. Bener and Alwash (2002) discussed how

Personal Statement Example | Topics and Well Written Essays - 1000 words - 2

Personal Statement Example Until now, I can still recall the exact time I fell in love with numbers and its analysis. I was in middle school, and an excellent teacher had been showing us how to tackle numerical problems. Imagine my delight with the adeptness I possess in following problem-solving techniques; after that memorable moment, I am hooked for life. The obsession I had helped me go through high school and college experience. As I passed entrance exam in secondary level with flying colors, I had been bombarded with different mathematical concepts, from geometry, trigonometry, algebra and calculus. Yet, another event marked my interest towards a specific course. When I took the class in Computer Science, we were introduced to C++ and FoxPro, deviating my interest towards analytical systems involved in computer processes. At 12th grade level, I had the honor of passing the course, with a Certificate to prove it. My interest in analytical mathematics led me to computer science programming, and the fascina tion had come to stay. In pursuance with numerical passion, it became the basis for my course selection Babes-Bolyai University, an excellent university in Cluj-Napoca. I took a program involving the combination of mathematics analysis and computer programming, Mathematics and Computer Science course, where I pored over a variety of concepts: Numerical analysis, Differential equations and Dynamic systems, Affine geometry, and Numerical solving of equations, Object oriented programming, Applications for mobile, Analysis and administration of complex computers systems, and Evolved programming methods. It may sound intimidating for others, but in my case, it had been like enjoying a favorite pastime. To top it all, I could get to share my enthusiasm with younger minds; I volunteered as tutor to students from grade 5-12. Giving my students a part of my analytical fixations with numbers is indeed a pleasurable episode for all of us. As much as I love my country, it seems that I am destin ed to go on a global scale. As I approached my fourth year in university, I was able to visit my relatives in Portland, Oregon for the summer. Unbeknown to me, I would meet the guy for me, Dan, who had been based in Seattle, Washington. We got on well together, as we both share an abundant love for life and adventure. Even though I went back to finish my course, we maintained constant contact. However, our love for each other had been adamant, and Dan proposed when he came to see me during my winter break--we got hitched summer that year. Forced to halt my studies in Romania, I relocated to follow my husband in Seattle, Washington. My need for mathematical challenges hunted me, and after thorough search for an outstanding university, I know what I am meant to do. I have to apply for degree on Applied Computational Mathematical Sciences in your top-rate institution, University of Washington. Only you have the competency to nurture my creative talent with numbers. Career Goals A few m onths after my marriage, I got pregnant, delaying my academic aspirations for a while, but was able to proceed years after. Unfortunately, my first attempt in the University of Washington had been denied. Thus, I channeled my energy towards another course in Bellevue College on Relational Database Developer, and this summer, I will have my certificate for the 45 units that I might accomplish. I am optimistic that this time, I will be given the chance

Science Meets Real Life Essay Example | Topics and Well Written Essays - 500 words - 1

Science Meets Real Life - Essay Example This essay stresses that people can become sick when they are exposed to virus and also by consuming contaminated food. An inspection of the restaurant has brought to fore the fact that it is not only unhygienic, but also lacks in the basic facilities. The kitchens of most of the restaurants do not have any ceilings and the shelves of the freezers are dirty. Besides, the cloths that the cooks use for wiping food contact surfaces are not cleaned in sanitizing solutions. Another major aspect that has come to notice is the fact that â€Å"Food thermometers were not being used by employees†. A comparison of the school calendars of the institutions indicates that the students from both schools have met and interacted on the occasion of the May Day Parade. They have also met on 15th May for planning meeting for the battle of the bands, which has been scheduled for 19th May. This paper makes a conclusion that more students may have become exposed to virus due to their interaction on the occasion of the functions related to band parade. The following testable questions can be offered for further investigation: what specific reasons can be attributed to the absence of students in both schools? what may be the causes for the common disease among the students? how are the students from both the schools affected at the same time? if the students from both the schools are suffering from the same problem when have they been exposed to the virus? how are they exposed to the same disease causing agents? what measures can be taken to prevent food contamination in restaurants?

Leadership Development Report Essay Example for Free

Leadership Development Report Essay Leadership has a paramount importance in the business world. It is not about a position, but how a person can influence others in creating and working towards that common organisation’s goal, and to create meaning in the works that we do. This report begins with the servant leadership framework that covers what I value in leadership. Also included in this report are the self-assessments that measure my leadership potential and competencies. This report also covers the issues associated to the industry I have chosen to work in and address my person-specific issues. II. LEADERSHIP DEVELOPMENT MODEL (175) Definition servant leadership Servant leadership is a type of leadership where the leader does order to be served; but focus on serving their followers in order to assist and guide them into more useful and satisfied people. This theory emphasize on the creation of moral purpose for leaders. It focuses on the impact that they leave on other people’s life to measure their greatness. Characteristics of servant leadership The servant leadership theory consists of ten key characteristics. These characteristics are; listening intently, empathy, healing, awareness, persuasion, conceptualization, foresight, stewardship, commitment to the growth of people, and building community. (Miller, Skringar, Dalglish Stevens, 2012) Why servant leadership? My concept of leadership is someone who is able to influence their followers through inspiration, empower them to realize their undiscovered true potential, and bring meaning to their life. In addition, I believe that a leader needs to be able to listen to their follower’s need in order to put the will of the group above their own will on the group. I strongly uphold the need for empathy in my leadership concept, because I believe that a leader must be able to put themselves in their follower’s shoes and perceive things through the eyes of their followers in order to gain understanding from different perspectives and to empower the followers to bring out their passion and thus bring forward their fullest potential in making a meaningful work. As mentioned by a successful leader – Fred A. Mansk Jr, â€Å" The ultimate leader is one who is willing to develop people to the point that they eventually surpass him or her in knowledge and ability.† Therefore, I find Servant Leadership as the most suitable framework for my leadership plan. III. Diagnosis of Strength and Weaknesses To support the diagnostic process and to provide the information on my leadership strengths and weaknesses I am using the information from two personality tests; Carl Jung’s and Issabel Briggs Myer’s Typology Test and a standardized emotional intelligent (EI) test. Self Assessments Carl Jung’s and Issabel Briggs Myer’s Typology Test Carl Jung’s and Issabel Briggs Myer’s Typology Test is a psychometric assessment designed to measure the preferences in how people perceive the world and make decisions based on their psychological preference. The aim of this test is to help people to have a better understanding of themselves, by understanding their strengths, weaknesses, possible career preferences and their preferred approach when interacting with others. This test puts one into four letter categories, where each letter stands for a specific personality type. (Briggs, Myers, 1998) After undertaking this typology test, I was classified under INFJ (Introvert, iNtuitive, Feeling, Judging) typology. Firstly, introversion displays a characteristic that is reserved and highly private. This goes in line with my personal characteristic as I look within for meaning and understanding. Secondly, intuition indicates an emphasis on abstract ideas and focusing on the meaning of the bigger picture rather than solid details. Feeling focuses mainly on personal concerns and emotional perception rather than the logical and objective facts. Judging describes about the need to have control by planning, organizing and making decisions as soon as possible because of INFJs’ deep attention on the future. INFJ type is described as having the strengths of being determined and passionate, altruistic, decisive, insightful, creative, inspiring and convincing. Dr. Dranitsaris stated that INFJ leadership style is quiet and influencing. INFJ leaders often lead by inspiring and motivating people with their ideals, working hard to gain the cooperation of others rather than demanding it. In a business context, INFJ leaders also tend to genuinely care about the people and how happy they are with their job. (Dranitsaris, 2009). This describes the traits considered as strengths of the INFJ type: that of being warm, altruistic and passionate. The main motive for every work done is not focused centrally on gaining personal benefit but for the greater good of the broader society; to find value and purpose for every tasks. Also, INFJs are described to be deeply concerned about their relations with people and how it links to humanity. (Heiss, Butt, 1996) These are the strengths I believe I possess in myself and these characteristics go in line with the framework of servant leadership as explained previously. However, the very strong need to have a cause for every work done can serve as a weakness for INFJ. This is because it can become difficult to maintain the drive and energy to complete works when I am not able to derive any deeper purpose or relate the objective of the work to a worthy goal. The complexity INFJ is further seen with the tendency to be idealistic. When objectives are not in line with a meaningful goal, INFJ will incline to grow restless and demotivated overtime. This will affect the effort and end result. The result may deviate from the targeted aim which becomes a conflict with the need for perfection. These weaknesses are worsen with the reserved nature of INFJ which may trigger unexpressed internal conflicts. Emotional Intelligent Test (EI) Emotional Intelligent test, on the other hand is a psychological test which allow an individual to identify their social skills that facilitate their interpersonal behavior. It identifies one’s capacity for goal-oriented adaptive behavior. It focuses on the aspects of intelligence that govern self-knowledge and social adaptation. Below are the results that I have attained from this self-assessment: Strengths Potential Strength Weaknesses doing well in the area of emotional understanding chose good forms of resolution for others conflict situations on the test empathetic socially insightful driven towards self-development healthy approach in resolving conflict situations doing reasonably well in the area of emotional identification, perception, and expression act in accordance with your values lacking in self-motivation not very assertive need to strengthen self-esteem further development needed in personal resilience/hardiness. These strengths indicate that I possess some of the traits that are needed to display the characteristics of a good servant-leader. IV. Industry-Specific Issues Looking into the Hospitality industry, specifically Airlines, I will use Singapore Airlines as a basis of my evaluation. The extent of superior service is paramount for it to establish itself. In order to deliver the standard of service the company has set for itself, it requires highly passionate and motivated employees. One of the elements that contribute to the success of Singapore Airlines is its human resource that highly regards contribution of creative ideas in which rewards are later given. (Singh, 1984) To be passionate, to inspire and to encourage innovation are strengths found in INFJs that match with the traits of Servant Leaders who encourages and motivates the followers to making a meaningful and effective work efforts. V. Person-Specific Issues Gender, age and culture are important aspects to be considered in shaping one’s leadership development. Being someone coming from Asia, the idea of women becoming a leader will face cultural constraints. In the context of organization, becoming a female leader will be more challenging than the male counterpart because there is a strong notion whereby men are born to lead and women to follow or serve and men hold the leadership positions. (Carly, Eagly, 1999). This is still present in the traditional Asian culture. Even to the eyes of the followers, the figure that is seen to be capable of leading goes to male gender. The masculinity possessed becomes a symbol of strength and competency. (Schein, 2001) Instructions led by female leaders are more likely to be followed because of the idea of obedience to authority rather than being influenced through inspiration. The gender-bias corporate culture becomes a huge obstacle in making use of servant-leadership framework as a female. This gender bias is still evident in many office settings of Japanese corporations whereby higher ranking positions are given mostly to male; and in fact Japan seeing a near zero resemblance between women and managers. (Schein, Mueller, 1992) Besides that, age also becomes an issue in determining the level of experience of a professional. Younger age typically indicates limited exposure to the various real-life experiences and this may affect the extent of wisdom in making judgments. VI. Timeframe and Evaluation Plan The weaknesses based on the self-assessments are used to develop my leadership goals and the Michigan Leadership Competency Model serves as a tool to categorize the goals set and the timeframe for the plan. Time Frame Self-Developmental Goals Self-Management Conceptualization Servant leaders seek to nurture their abilities to dream great dreams; not just consumed by achieving operational goals. To develop characteristic and thinking process encompass broader-based conceptual thinking require discipline and practice. Leading Others Influencing/Persuasion Servant leaders seek to persuade and convince others through inspiration rather than coerce compliance. This requires a level of confidence, personal drive and energy to be emulated to the followers. As represented in one of my weaknesses from the self-assessment, I lack in self-motivation, self-esteem and assertiveness. These characteristics need to be developed in order to gain enough personal power to lead and guide others. Innovation Creativity Creativity is one of the key characteristics of servant leaders. Also, the hospitality industry takes great importance in areas of innovation to stay competitive and relevant. This is a characteristic that continually needs to be fostered and developed. Social Responsibility Ethically Social Servant Leadership highlights the importance of leading for the greater good for a deeper moral purpose. This emphasizes the need for moral awareness and ethical conducts when leading. This can be done by participating more in charitable or environmental causes which aim in improving social welfare of the broader society. Such participation allow exposure and knowledge-gaining. Evaluation by Multi-Step Action Plan 1 year Completing Bachelor of Business Degree 3 years Employment in Airline as Flight Attendant to gain exposure to new experiences, ethical conducts and ideas and insight knowledge on providing service in hospitality industry (Innovation Social Responsibility) 2 years Further study on Master of Hospitality Management to broaden conceptual thinking process. This also help to gain self-esteem and improve on the ability to influence (Conceptualization Influencing) Working in Management VII. Industry Leader Input Previously I focused my goals only on the trait developments. This was difficult measure because characteristics can only be proven once I’ve been put on the position to be a leader in a group. There was no tangible achievement to evaluate the success of my goal planning. Therefore, through his suggestion, I modified my goal timeframe by adding a multi-step action plan that cover the length of time to achieve each target. For example, the employment in an Airline industry will help me garner new experiences, perspective and practice discipline in work ethics. Feedback on my work performance from supervisors can serve as a form of evaluation. Also, the attainment of higher qualification will allow me to gain broader and deeper knowledge on the industry through research. The exposure and experience may help me to develop a stronger leadership characteristic and further evaluation can be done through taking re-test for EI. Wordcount: 1,509 words (Excluding References, Appedices, Headings Tables) VIII. Appendices 1. Michigan Leadership Competency Model Leadership Assessment Report Scores range from 1 to 6, with 1 indicating that you rated yourself low on that competency and 6 indicating that you rated yourself high. Introverted iNtuition Introverted intuitives, INFJs enjoy a greater clarity of perception of inner, unconscious processes than all but their INTJ cousins. Just as SP types commune with the object and live in the here and now of the physical world, INFJs readily grasp the hidden psychological stimuli behind the more observable dynamics of behavior and affect. Their amazing ability to deduce the inner workings of the mind, will and emotions of others gives INFJs their reputation as prophets and seers. Unlike the confining, routinizing nature of introverted sensing, introverted intuition frees this type to act insightfully and spontaneously as unique solutions arise on an event by event basis. Extraverted Feeling Extraverted feeling, the auxiliary deciding function, expresses a range of emotion and opinions of, for and about people. INFJs, like many other FJ types, find themselves caught between the desire to express their wealth of feelings and moral conclusions about the actions and attitudes of others, and the awareness of the consequences of unbridled candor. Some vent the attending emotions in private, to trusted allies. Such confidants are chosen with care, for INFJs are well aware of the treachery that can reside in the hearts of mortals. This particular combination of introverted intuition and extraverted feeling provides INFJs with the raw material from which perceptive counselors are shaped. Introverted Thinking The INFJs thinking is introverted, turned toward the subject. Perhaps it is when the INFJs thinking function is operative that he is most aloof. A comrade might surmise that such detachment signals a disillusionment, that she has also been found lacking by the sardonic eye of this one who plumbs the depths of the human spirit. Experience suggests that such distancing is merely an indication that the seer is hard at work and focusing energy into this less efficient tertiary function. Extraverted Sensing INFJs are twice blessed with clarity of vision, both internal and external. Just as they possess inner vision which is drawn to the forms of the unconscious, they also have external sensing perception which readily takes hold of worldly objects. Sensing, however, is the weakest of the INFJs arsenal and the most vulnerable. INFJs, like their fellow intuitives, may be so absorbed in intuitive perceiving that they become oblivious to physical reality. The INFJ under stress may fall prey to various forms of immediate gratification. Awareness of extraverted sensing is probably the source of the SP wannabe side of INFJs. Many yearn to live spontaneously; its not uncommon for INFJ actors to take on an SP (often ESTP) role. References Briggs, K. C., Myers, I. B. (1998). Myers-Briggs Type Indicator. Palo Alto, CA. Greenleaf, R. K. (1977). The Servant as Leader. Business Leadership: A Jossey-Bass Reader. San Francisco: Jossey-Bass. Miller, Skringar, Dalglish Stevens, (2012) Leadership and Change Management. 1st ed. Prahran VIC Australia: Tilde University Press. Maxwell, J. C., Dorvan, J. (1997). Becoming a Person of Influence: How to Positively Impact the Lives of Others. Nashville: Thomas Nelson Schein, V.E. (2001) A global look at psychological barriers to women’s progress in management. Journal of Social Issues. 57, pp. 675-688. Schein, V.E., Mueller, R. (1992). Sex role stereotyping and requisite management characteristics: A cross cultural look. Journal of Organizational Behavior. 13, pp. 439-447. Carli L.L., Eagly A.H. (1999). Gender effects on influence and emergent leadership Powell G.N. (Ed.), Handbook of gender and work, Sage, Thousand Oaks, CA, pp. 203–222 Soo Min Toh, Geoffrey J. Leonardelli (2012) Cultural constraints on the emergence of women as leaders. Journal of World Business, Vol. 47, Issue 4, pp. 604-611 Karmjit Singh (1984). Successful strategies—The story of Singapore Airlines (SIA) Long Range Planning, Vol.17, Issue 5, pp. 17-22 Dranitsaris, A., (ed.) 2009, Personality Type and Leadership Behaviour: Jung’s Typology for the Workplace, e-book, accessed 25 April 2013, Central Michigan University, 2004, Leadership Competency Model, accessed 20 April 2013, http://www.chsbs.cmich.edu/leader_model/CompModel/EDUMAIN.htm Heiss, M.M, Butt, J.,1999, INFJ, Typelogic, accessed 25 April 2013, HumanMetrics Jung’s Typology Test INFJ, 2012, accessed 25 April 2013,

Soil Analysis of the Himalayan Mountain System

Soil Analysis of the Himalayan Mountain System Chapter- 4 ABIOTIC ENVIRONMENTAL VARIABLES OF MORAINIC AND ALPINE ECOSYSTEMS Global warming/ enhanced greenhouse effect and the loss of biodiversity are the major environmental issues around the world. The greatest part of the worlds population lives in the tropical regions. Mountainous regions in many cases provide favourable conditions for water supply due to orographically enhanced convective precipitation. Earth scientists are examining ancient periods of extreme warmth, such as the Miocene climatic optimum of about 14.5-17 million years ago. Fossil floral and faunal evidences indicate that this was the warmest time of the past 35 million years; a mid-latitude temperature was as much as 60C higher than the present one. Many workers believe that high carbon dioxide levels, in combination with oceanographic changes, caused Miocene global warming by the green house effect. Pagani et al. (1999) present evidence for surprisingly low carbon dioxide levels of about 180-290ppm by volume throughout the early to late Miocene (9-25 million years). They concluded tha t green house warming by carbon dioxide couldnt explain Miocene warmth and other mechanism must have had a greater influence. Carbon dioxide is a trace gas in the Earths atmosphere, which exchanges between carbon reservoirs in particularly the oceans and the biosphere. Consequently atmospheric concentration shows temporal, local and regional fluctuations. Since the beginning of industrialization, its atmospheric concentration has increased. The 1974 mean concentration of atmospheric CO2 was about 330 ÃŽ ¼mol mol-1 (Baes et. al., 1976), which is equivalent to 2574 x 1015 g CO2 702.4 x 1015 C assuming 5.14 x 1021 g as the mass of the atmosphere. This value is significantly higher than the amount of atmospheric CO2 in 1860 that was about 290 ÃŽ ¼mol mol-1 (617.2 x 1015 g). Precise measurements of the atmospheric CO2 concentration started in 1957 at the South Pole, Antarctica (Brown and Keeling, 1965) and in 1958 at Mauna Loa, Hawaii (Pales and Keeling, 1965). Records from Mauna Loa show that the concentration of CO2 in the atmosphere has risen since 1958, from 315 mmol mol-1 to approximately 360 315 mmol mol-1 in 1963 (Boden et al., 1994). From these records and other measurements that began more recently, it is clear that the present rate of CO2 increase ranges between 1.5 and 2.5 mmol mol-1 per annum. In the context of the Indian Himalayan region, the effect of warming is apparent on the recession of glaciers (Valdiya, 1988), which is one of the climatic sensitive environmental indicators, and serves as a measure of the natural variability of climate of mountains over long time scales (Beniston et al., 1997). However no comprehensive long-term data on CO2 levels are available. The consumption of CO2 by photosynthesis on land is about 120 x 1015 g dry organic matter/year, which is equivalent to about 54 x 1015gC/yr (Leith and Whittaker, 1975). Variations in the atmospheric CO2 content on land are mainly due to the exchange of CO2 between vegetation and the atmosphere (Leith, 1963; Baumgartner, 1969). The process in this exchange is photosynthesis and respiration. The consumption of CO2 by the living plant material is balanced by a corresponding production of CO2 during respiration of the plants themselves and from decay of organic material, which occurs mainly in the soil through the activity of bacteria (soil respiration). The release of CO2 from the soil depends on the type, structure, moisture and temperature of the soil. The CO2 concentration in soil can be 1000 times higher than in air (Enoch and Dasberg, 1971). Due to these processes, diurnal variations in the atmospheric CO2 contents on ground level are resulted. High mountain ecosystems are considered vulnerable to climate change (Beniston, 1994; Grabherr et al., 1995; Theurillat and Guisan, 2001). The European Alps experienced a 20 C increase in annual minimum temperatures during the twentieth century, with a marked rise since the early 1980s (Beniston et al., 1997). Upward moving of alpine plants has been noticed (Grabherr et al., 1994; Pauli et al., 2001), community composition has changed at high alpine sites (Keller et al., 2000), and treeline species have responded to climate warming by invasion of the alpine zone or increased growth rates during the last decades (Paulsen et al., 2000). Vegetation at glaciers fronts is commonly affected by glacial fluctuations (Coe, 1967; Spence, 1989; Mizumo, 1998). Coe (1967) described vegetation zonation, plant colonization and the distribution of individual plant species on the slopes below the Tyndall and Lewis glaciers. Spence (1989) analyzed the advance of plant communities in response to the re treat of the Tyndall and Lewis glaciers for the period 1958- 1984. Mizumo (1998) addressed plant communities in response to more recent glacial retreat by conducting field research in 1992, 1994, 1996 and 1997. The studies illustrated the link between ice retreat and colonization near the Tyndall and Lewis glaciers. The concern about the future global climate warming and its geoecological consequences strongly urges development and analysis of climate sensitive biomonitoring systems. The natural elevational tree limit is often assumed to represent an ideal early warming line predicted to respond positionally, structurally and compositionally even to quite modest climate fluctuations. Several field studies in different parts of the world present that climate warming earlier in the 20th century (up to the 1950s 1960s) has caused tree limit advances (Kullman, 1998). Purohit (1991) also reported upward shifting of species in Garhwal Himalaya. The Himalayan mountain system is a conspicuous landmass characterised by its unique crescent shape, high orography, varied lithology and complex structure. The mountain system is rather of young geological age through the rock material it contains has a long history of sedimentation, metamorphism and magmatism from Proterozoic to Quaternary in age. Geologically, it occupies a vast terrain covering the northern boundary of India, entire Nepal, Bhutan and parts of China and Pakistan stretching from almost 720 E to 960 E meridians for about 2500 km in length. In terms of orography, the geographers have conceived four zones in the Himalaya across its long axis. From south to north, these are (i) the sub-Himalaya, comprising low hill ranges of Siwalik, not rising above 1,000 m in altitude; (ii) the Lesser Himalaya, comprising a series of mountain ranges not rising above 4000 m in altitude; (iii) the Great Himalaya, comprising very high mountain ranges with glaciers, rising above 6,000 m i n altitude and (iv) the Trans-Himalaya, Comprising very high mountain ranges with glaciers. The four orographic zones of the Himalaya are not strictly broad morpho-tectonic units though tectonism must have played a key role in varied orographic attainments of different zones. Their conceived boundaries do not also coincide with those of litho-stratigraphic or tectono-stratigraphic units. Because of the involvement of a large number of parameters of variable nature, the geomorphic units are expected to be diverse but cause specific, having close links with mechanism and crustal movements (Ghosh, et al., 1989). Soil is essential for the continued existence of life on the planet. Soil takes thousands of years to form and only few years to destroy their productivity as a result of erosion and other types of improper management. It is a three dimensional body consisting of solid, liquid and gaseous phase. It includes any part of earths crust, which through the process of weathering and incorporation of organic matter has become capable in securing and supporting plants. Living organisms and the transformation they perform have a profound effect on the ability of soils to provide food and fiber for expanding world population. Soils are used to produce crops, range and timber. Soil is basic to our survival and it is natures waste disposal medium and it serves as habitats for varied kinds of plants, birds, animals, and microorganisms. As a source of stores and transformers of plant nutrients, soil has a major influence on terrestrial ecosystems. Soil continuously recycles plant and animal remains , and they are major support systems for human life, determining the agricultural production capacity of the land (Anthwal, 2004). Soil is a natural product of the environment. Native soil forms from the parent material by action of climate (temperature, wind, and water), native vegetation and microbes. The shape of the land surface affects soil formation. It is also affected by the time it took for climate, vegetation, and microbes to create the soil. Soil varies greatly in time and space. Over time-scales relevant to geo-indicators, they have both stable characteristics (e.g. mineralogical composition and relative proportions of sand, silt and clay) and those that respond rapidly to changing environmental conditions (e.g. ground freezing). The latter characteristics include soil moisture and soil microbiota (e.g. nematodes, microbes), which are essential to fluxes of plant nutrients and greenhouse gases (Peirce, and Larson, 1996.). Most soils resist short-term climate change, but some may undergo irreversible change such as lateritic hardening and densification, podsolization, or large-scale erosion. Chemical degradation takes place because of depletion of soluble elements through rainwater leaching, over cropping and over grazing, or because of the accumulation of salts precipitated from rising ground water or irrigation schemes. It may also be caused by sewage containing toxic metals, precipitation of acidic and other airborne contaminants, as well as by persistent use of fertilizers and pesticides (Page et al., 1986). Physical degradation results from land clearing, erosion and compaction by machinery (Klute, 1986). The key soil indicators are texture (especially clay content), bulk density, aggregate stability and size distribution, and water-holding capacity (Anthwal, 2004). Soil consists of 45% mineral, 25% water, 25% air and 5% organic matter (both living and dead organisms). There are thousands of different soils throughout the world. Soil are classified on the basis of their parent material, texture, structure, and profile There are five key factors in soil formation: i) type of parent material; ii) climate; iii) overlying vegetation; iv) topography or slope; and v) time. Climate controls the distribution of vegetation or soil organisms. Together climate and vegetation/soil organisms often are called the active factors of soil formation (genesis). This is because, on gently undulating topography within a certain climatic and vegetative zone a characteristic or typical soil will develop unless parent material differences are very great (Anthwal, 2004). Thus, the tall and mid-grass prairie soils have developed across a variety of parent materials. Soil structure comprises the physical constitution of soil material as expressed by size, shape, and arrangement of solid particles and voids (Jongmans et al., 2001). Soil structure is an important soil property in many clayey, agricultural soils. Physical and chemical properties and also the nutrient status of the soil vary spatially due to the changing nature of the climate, parent material, physiographic position and vegetation (Behari et al., 2004). Soil brings together many ecosystem processes, integrating mineral and organic processes; and biological, physical and chemical processes (Arnold et al., 1990, Yaalon 1990). Soil may respond slowly to environmental changes than other elements of the ecosystem such as, the plants and animal do. Changes in soil organic matter can also indicate vegetation change, which can occur quickly because of climatic change (Almendinger, 1990). In high altitudes, soils are formed by the process of solifluction. Soils on the slopes above 300 are generally shallow due to erosion and mass wasting processes and usually have very thin surface horizons. Such skeletal soils have median to coarse texture depending on the type of material from which they have been derived. Glacial plants require water, mineral resources and support from substrate, which differ from alpine and lower altitude in many aspects. The plant life gets support by deeply weathered profile in moraine soils, which develops thin and mosaic type of vegetation. Most of the parent material is derived by mechanical weathering and the soils are rather coarse textured and stony. Permafrost occurs in many of the high mountains and the soils are typically cold and wet. The soils of the moraine region remain moist during the summer because drainage is impeded by permafrost (Gaur, 2002). In general, the north facing slopes support deep, moist and fertile soils. The south facing slopes, on the other hand, are precipitous and well exposed to denudation. These soils are shallow, dry and poor and are often devoid of any kind of regolith (Pandey, 1997). Based on various samples, Nand et al., (1989) finds negative correlation between soil pH and altitude and argues that decrease in pH with the increase in elevation is possibly accounted by high rainfall which facilitated leaching out of Calcium and Magnesium from surface soils. The soils are invariably rich in Potash, medium in Phosphorus and poor in Nitrogen contents. However, information on geo-morphological aspects, soil composition and mineral contents of alpine and moraine in Garhwal Himalaya are still lacking. Present investigation was aimed to carry out detail observations on soil composition of the alpine and moraine region of Garhwal Himalaya. 4.1. OBSERVATIONS As far as the recordings of abiotic environmental variables of morainic and alpine ecosystems of Dokriani Bamak are concerned, the atmospheric carbon dioxide and the physical and chemical characteristics of the soil were recorded under the present study. As these are important for the present study. 4.1.1. Atmospheric Carbon Dioxide Diurnal variations in the atmospheric CO2 were recorded at Dokriani Bamak from May 2005- October 2005. Generally the concentration of CO2 was higher during night and early morning hours (0600-0800) and lower during daytime. However, there were fluctuations in the patterns of diurnal changes in CO2 concentration on daily basis. In the month of May 2005, carbon dioxide concentration ranged from a minimum of 375Â µmol mol-1 to a maximum of 395Â µmol mol-1. When the values were averaged for the measurement days the maximum and minimum values ranged from 378Â µmol mol-1 to 388Â µmol mol-1. A difference of 20Â µmol mol-1 was found between the maximum and minimum values recorded for the measurement days. When the values were averaged, a difference of 10Â µmol mol-1 was observed between maximum and minimum values. During the measurement period, CO2 concentrations varied from a minimum of 377ÃŽ ¼mol mol-1 at 12 noon to a maximum of 400ÃŽ ¼mol mol-1 at 0800 hrs in the month of June, 2005. When the CO2 values were averaged for 6 days, the difference between the minimum and maximum values was about 23ÃŽ ¼mol mol-1. In the month of July, levels of carbon dioxide concentrations ranged from a minimum of 369ÃŽ ¼mol mol-1 to a maximum of 390ÃŽ ¼mol mol-1. When the values of the carbon dioxide concentrations for the measuring period were averaged, the difference between the minimum and maximum values was about 21ÃŽ ¼mol mol-1. Carbon dioxide concentration ranged from a minimum of 367ÃŽ ¼mol mol-1 to a maximum of 409ÃŽ ¼mol mol-1 during the month of August. When the values of carbon dioxide were averaged for the measurement days, the difference in the minimum and maximum values was about 42ÃŽ ¼mol mol-1. During the measurement period (September), CO2 concentrations varied from a minimum of 371ÃŽ ¼mol mol-1 at 12 noon to a maximum of 389ÃŽ ¼mol mol-1 at 0600 hrs indicating a difference of 18ÃŽ ¼mol mol-1 between the maximum and minimum values. When the values of the measurement days were averaged the minimum and maximum values ranged from 375ÃŽ ¼mol mol-1 to 387ÃŽ ¼mol mol-1 and a difference of 12ÃŽ ¼mol mol-1 was recorded. During the month of October, carbon dioxide levels ranged from a minimum of 372ÃŽ ¼mol mol-1 at 1400 hrs to a maximum of 403ÃŽ ¼mol mol-1 at 2000 hrs indicating a difference of 31ÃŽ ¼mol mol-1. When the values were averaged, the carbon dioxide levels ranged from a minimum of 376ÃŽ ¼mol mol-1 to a maximum of 415ÃŽ ¼mol mol-1.A difference in the minimum and maximum values was found to be 39Â µmol mol-1 when the values were averaged for the measurements days. In the growing season (May-October) overall carbon dioxide concentration was recorded to be highest in the month of June and seasonally it was recorded highest during the month of October 4.1.2. A. Soil Physical Characteristics of Soil Soil Colour and Texture Soils of the study area tend to have distinct variations in colour both horizontally and vertically (Table 4.1). The colour of the soil varied with soil depth. It was dark yellowish brown at the depth of 10-20cm, 30-40cm of AS1 and AS2, brown at the depth of 0-10cm of AS1 and AS2 and yellowish brown at the depths of 20-30cm, 40-50cm, 50-60cm of AS1 and AS2). Whereas the soil colour was grayish brown at the depths of 0-10cm, 30-40cm, 50-60cm of MS1 and MS2, dark grayish brown at the depths of 10-20cm, 20-30cm of MS1 and MS2 and brown at the depth of 40-50cm of both the moraine sites (MS1 and MS2). Soil texture is the relative volume of sand, silt and clay particles in a soil. Soils of the study area had high proportion of silt followed by sand and clay (Table 4.2). Soil of the alpine sites was identified as silty loam category, whereas, the soil of the moraine was of silty clayey loam category. Soil Temperature The soil temperature depends on the amount of heat reaching the soil surface and dissipation of heat in soil. Figure 4.2 depicts soil temperature at all the sites in the active growth period. A maximum (13.440C) soil temperature was recorded during the month of July and minimum (4.770C) during the month of October at AS1. The soil temperature varied between 5.10C being the lowest during the month of October to 12.710C as maximum during the month of August at AS2. Soil temperature ranged from 3.240C (October) to 11.210C (July) at MS1. However, the soil temperature ranged from 3.40C (October) to 12.330C (July) at MS2. Soil Moisture (%) Moisture has a big influence on soils ability to compact. Some soils wont compact well until moisture is 7-8%. Â  Likewise, wet soil also doesnt compact well. The mean soil water percentage (Fig. 4.3) in study area fluctuated between a maximum of 83% (AS1) to a minimum of 15% (AS2). The values of soil water percentage ranged from a minimum of 8% (MS2) to a maximum of 80% (MS1). Soil water percentage was higher in the month of July at AS1 and during August at MS1 (. During the month of June, soil water percentage was recorded minimum in the lower depth (50-60cm) at both the sites. Water Holding Capacity (WHC) The mean water holding capacity of the soil varied from alpine sites to moraine sites (Table 4.4). It ranged from a maximum of 89.66% (August) to a minimum of 79.15% (May) at AS1. The minimum and maximum values at AS2 were 78.88% (May) to 89.66% (August), respectively. The maximum WHC was recorded to be 84.61 % during the month of September on upper layer (0-10 cm) at MS1 and minimum 60.36% during the month of May in the lower layer (50-60cm) at MS1. At MS2, WHC ranged from 60.66% (May) to 84.61% (September). However, maximum WHC was recorded in upper layers at both the sites of alpine and moraine. Soil pH The soil pH varied from site to site during the course of the present study (Table 4.5). Mean pH values of all the sites are presented in Figure 4.4 The soil of the study area was acidic. Soil of the moraine sites was more acidic than that of the alpine sites. Soil pH ranged from 4.4 to 5.3 (AS1), 4.5 to 5.2 (AS2), 4.9 to 6.1 (MS1) and 4.8 to 5.7 (MS2). 4.1.2 B. Chemical Characteristics of Soil Organic Carbon (%): Soil organic carbon (SOC) varied with depths and months at both the alpine and moraine sites (Table 4.6). High percentage of organic carbon was observed in the upper layer of all sites during the entire period of study. Soil organic C decreased with depth and it was lowest in lower layers at all the sites. Soil organic carbon was maximum (5.1%) during July at AS1 because of high decomposition of litter, while it was minimum (4.2%) during October due to high uptake by plants in the uppermost layer (0-10 cm). A maximum (5.0%) SOC was found during the month of July and minimum (4.1%) during October at AS2. At the moraine sites, maximum (3.58%, 3.73%) SOC was found during June and minimum (1.5% and 1.9%) during August at MS1 and MS2 respectively. Phosphorus (%): A low amount of phosphorus was observed from May to August which increased during September and October. The mean phosphorus percentage ranged from 0.02 Â ± 0.01 to 0.07 Â ± 0.03 at AS1 and AS2. It was 0.03Â ±0.01 to 0.03Â ±0.02 at MS1 and MS2. Maximum percentage of phosphorus was estimated to be 0.09 in the uppermost layer (0-10 cm) during October at AS1. The lower layer (40-50 cm) of soil horizon contained a minimum of 0.01% phosphorus during September at AS1 and AS2. In the moraine sites (MS1 and MS2), maximum phosphorus percentage of 0.03 Â ±0.01 was estimated in the upper layers (0-10, 10-20, 20-30 cm) while it was found to be minimum (0.02Â ±0.01) in the lower layers (30-40 cm). Overall, a decreasing trend in amount of phosphorus was found with depth in alpine as well as moraine sites Potassium (%): A decline in potassium contents was also observed with declining depth during the active growing season. Maximum value of potassium was found in the uppermost layer (0-10 cm) at all the sites. The mean values ranged from 0.71Â ±0.02 to 46Â ±0.06 at AS1 while it was 0.71Â ±0.02 to 0.47Â ±0.05 at AS2. In the moraine sites the values ranged from a minimum of 0.33 Â ±0.06 to a maximum of 0.59Â ±0.05 in the MS1 and from 0.59Â ±0.05 to 0.32Â ±0.06 at MS2. In the upper layer of soil horizon (0-10 cm), maximum value of 0.74 %, 0.75% of potassium was observed during the month of July at AS1 and AS2. While the values were maximum in the month of October at moraine sites MS1 and MS2 having 0.66% and 0.65% respectively Nitrogen (%): Highest percentage of nitrogen was found in the upper layers at all the sites. Maximum percentage of nitrogen were found during the month of July-August (0.25%, 0.25 and 0.26%, 0.25%) at AS1 and AS2, respectively. Maximum values of 0.18% and 0.15% respectively were found during the month of June at the moraine sites MS1 and MS2. The nitrogen percentage ranged from 0.23Â ±0.02 to 0.04Â ±0.01% at AS1. However, it ranged from a minimum of 0.05Â ±0.01 to 0.24Â ±0.02% at AS2. The nitrogen percentage ranged from a minimum of 0.03Â ±0.01, 0.02Â ±0.04% to a maximum of 12Â ±0.03, 13Â ±0.01%, respectively at MS1 and MS2 Overall, a decreasing trend was noticed in the nitrogen percentage with depth at both the alpine and moraine sites. 4.2. DISCUSSION Soil has a close relationship with geomorphology and vegetation type of the area (Gaur, 2002). Any change in the geomorphological process and vegetational pattern influences the pedogenic processes. However, variability in soil is a characteristic even within same geomorphic position (Gaur, 2002). Jenney (1941) in his discussion on organisms as a soil forming factors treated vegetation both as an independent and as dependent variable. In order to examine the role of vegetation as an independent variable, it would be possible to study the properties of soil as influenced by vegetation while all other soil forming factors such as climate, parent material, topography and time are maintaining at a particular constellation. Many soil properties may be related to a climatic situation revealing thousand years ago (e.g. humid period during late glacial or the Holocene in the Alps and Andes (Korner, 1999). The soil forming processes are reflected in the colour of the surface soil (Pandey, 1997). The combination of iron oxides and organic content gives many soil types a brown colour (Anthwal, 2004). Many darker soils are not warmer than adjacent lighter coloured soils because of the temperature modifying effect of the moisture, in fact they may be cooler (Pandey, 1997). The alpine sites of the resent study has soil colour varying from dark yellowish brown/yellowish brown to brown at different depths. Likewise, at the moraine sites, the soil colour was dark grayish brown/grayish brown to brown. The dark coloured soils of the moraine and alpine sites having high humus contents absorb more heat than light coloured soils. Therefore, the dark soils hold more water. Water requires relatively large amount of heat than the soil minerals to raise its temperature and it also absorbs considerable heat for evaporation. At all sites, dark colour of soil was found due to high organic contents by the addition of litter. Soil texture is an important modifying factor in relation to the proportion of precipitation that enters the soil and is available to plants (Pandey, 1997). Texture refers to the proportion of sand, silt, and clay in the soil. Sandy soil is light or coarse-textured, whereas, the clay soils are heavy or fine-textured. Sand holds less moisture per unit volume, but permits more rapid percolation of precipitated water than silt and clay. Clay tends to increase the water-holding capacity of the soil. Loamy soils have a balanced sand, silt, and clay composition and are thus superior for plant growth (Pidwirny, 2004). Soil of the alpine zone of Dokriani Bamak was silty predominated by clay and loam, whereas the soil of moraine zone was silty predominated by sand and clay. There is a close relationship between atmospheric temperature and soil temperature. The high organic matter (humus) help in retaining more soil water. During summers, high radiations with greater insulation period enhance the atmospheric temperature resulted in the greater evaporation of soil water. In the monsoon months (July-August) the high rainfall increased soil moisture under relative atmospheric and soil temperature due to cloud-filter radiations (Pandey, 1997). Owing to September rainfall, atmospheric and soil temperatures decreased. The soil moisture is controlled by atmospheric temperature coupled with absorption of water by plants. During October, occasional rainfall and strong cold winds lower down the atmospheric temperature further. The soil temperature remains more or less intact from the outer influence due to a slight frost layer as well as vegetation cover. Soil temperature was recorded low at the moraine sites than the alpine sites. During May, insulation period in creases with increase in the atmospheric and soil temperature and it decreases during rainfall. The increasing temperature influences soil moisture adversely and an equilibrium is attained only after the first monsoon showers in the month of June which continued till August. Donahue et al. (1987) stated that no levelled land with a slope at right angle to the Sun would receive more heat per soil area and will warm faster than the flat surface. The soil layer impermeable to moisture have been cited as the reason for treelessness in part of the tropics, wherein its absence savanna develops (Beard, 1953). The resulting water logging of soil during the rainy season creates conditions not suitable for the growth of trees capable of surviving the dry season. The water holding capacity of the soil is determined by several factors. Most important among these are soil texture or size of particles, porosity and the amount of expansible organic matter and colloidal clay (Pandey, 1997). Water is held as thin film upon the surface of the particles and runs together forming drops in saturated soils, the amount necessarily increases with an increase in the water holding surface. Organic matter affects water contents directly by retaining water in large amount on the extensive surfaces of its colloidal constituents and also by holding it like a sponge in its less decayed portion. It also had an indirect effect through soil structure. Sand particles loosely cemented together by it, hence, percolation is decreased and water-holding capacity increased. Although fine textured soil can hold more water and thus more total water holding capacity but maximum available water is held in moderate textured soil. Porosity in soil consists of that portion of the soil volume not occupied by solids, either mineral or organic material. Under natural conditions, the pore spaces are occupied at all times by air and water. Pore spaces are irregular in shape in sand than the clay. The most rapid water and air movement is observed in sands than strongly aggregated soils. The pH of alpine sites ranged from 4.4 to 5.3 and it ranged from 4.8 to 6.1 in moraine sites of Dokriani Bamak. It indicated the acidic nature of the soil. The moraine sites were more acidic than the alpine sites. Acidity of soil is exhibited due to the presence of different acids. The organic matter and nitrogen contents inhibit the acidity of soil. The present observations pertaining to the soil pH (4.4 to 5.3 and 4.8 to 6.1) were more or less in the same range as reported for other meadows and moraine zones. Ram (1988) reported pH from 4.0-6.0 in Rudranath and Gaur (2002) on Chorabari. These pH ranges are lower than the oak and pine forests of lower altitudes of Himalayan region as observed by Singh and Singh, 1987 (pH:6.0-6.3). Furthermore, pH increased with depth. Bliss (1963) analyzed that in all types of soil, pH was low in upper layers (4.0-4.30) and it increased (4.6-4.9) in lower layer at New Hampshire due to reduction in organic matter. Das et al. (1988) reported the simil ar results in the sub alpine areas of Eastern Himalayas. All these reports support the present findings on Dokriani Bamak strongly. A potent acidic soil is intensively eroded and it has lower exchangeable cation, and possesses least microbial activity (Donahue et al., 1987). Misra et al., 1970 also observed higher acidity in the soil in the region where high precipitation results leaching. Koslowska (1934) demonstrated that when plants were grown under conditions of known pH, they make the culture medium either more acidic or alkaline and that this property differed according to the species. Soil properties may ch Soil Analysis of the Himalayan Mountain System Soil Analysis of the Himalayan Mountain System Chapter- 4 ABIOTIC ENVIRONMENTAL VARIABLES OF MORAINIC AND ALPINE ECOSYSTEMS Global warming/ enhanced greenhouse effect and the loss of biodiversity are the major environmental issues around the world. The greatest part of the worlds population lives in the tropical regions. Mountainous regions in many cases provide favourable conditions for water supply due to orographically enhanced convective precipitation. Earth scientists are examining ancient periods of extreme warmth, such as the Miocene climatic optimum of about 14.5-17 million years ago. Fossil floral and faunal evidences indicate that this was the warmest time of the past 35 million years; a mid-latitude temperature was as much as 60C higher than the present one. Many workers believe that high carbon dioxide levels, in combination with oceanographic changes, caused Miocene global warming by the green house effect. Pagani et al. (1999) present evidence for surprisingly low carbon dioxide levels of about 180-290ppm by volume throughout the early to late Miocene (9-25 million years). They concluded tha t green house warming by carbon dioxide couldnt explain Miocene warmth and other mechanism must have had a greater influence. Carbon dioxide is a trace gas in the Earths atmosphere, which exchanges between carbon reservoirs in particularly the oceans and the biosphere. Consequently atmospheric concentration shows temporal, local and regional fluctuations. Since the beginning of industrialization, its atmospheric concentration has increased. The 1974 mean concentration of atmospheric CO2 was about 330 ÃŽ ¼mol mol-1 (Baes et. al., 1976), which is equivalent to 2574 x 1015 g CO2 702.4 x 1015 C assuming 5.14 x 1021 g as the mass of the atmosphere. This value is significantly higher than the amount of atmospheric CO2 in 1860 that was about 290 ÃŽ ¼mol mol-1 (617.2 x 1015 g). Precise measurements of the atmospheric CO2 concentration started in 1957 at the South Pole, Antarctica (Brown and Keeling, 1965) and in 1958 at Mauna Loa, Hawaii (Pales and Keeling, 1965). Records from Mauna Loa show that the concentration of CO2 in the atmosphere has risen since 1958, from 315 mmol mol-1 to approximately 360 315 mmol mol-1 in 1963 (Boden et al., 1994). From these records and other measurements that began more recently, it is clear that the present rate of CO2 increase ranges between 1.5 and 2.5 mmol mol-1 per annum. In the context of the Indian Himalayan region, the effect of warming is apparent on the recession of glaciers (Valdiya, 1988), which is one of the climatic sensitive environmental indicators, and serves as a measure of the natural variability of climate of mountains over long time scales (Beniston et al., 1997). However no comprehensive long-term data on CO2 levels are available. The consumption of CO2 by photosynthesis on land is about 120 x 1015 g dry organic matter/year, which is equivalent to about 54 x 1015gC/yr (Leith and Whittaker, 1975). Variations in the atmospheric CO2 content on land are mainly due to the exchange of CO2 between vegetation and the atmosphere (Leith, 1963; Baumgartner, 1969). The process in this exchange is photosynthesis and respiration. The consumption of CO2 by the living plant material is balanced by a corresponding production of CO2 during respiration of the plants themselves and from decay of organic material, which occurs mainly in the soil through the activity of bacteria (soil respiration). The release of CO2 from the soil depends on the type, structure, moisture and temperature of the soil. The CO2 concentration in soil can be 1000 times higher than in air (Enoch and Dasberg, 1971). Due to these processes, diurnal variations in the atmospheric CO2 contents on ground level are resulted. High mountain ecosystems are considered vulnerable to climate change (Beniston, 1994; Grabherr et al., 1995; Theurillat and Guisan, 2001). The European Alps experienced a 20 C increase in annual minimum temperatures during the twentieth century, with a marked rise since the early 1980s (Beniston et al., 1997). Upward moving of alpine plants has been noticed (Grabherr et al., 1994; Pauli et al., 2001), community composition has changed at high alpine sites (Keller et al., 2000), and treeline species have responded to climate warming by invasion of the alpine zone or increased growth rates during the last decades (Paulsen et al., 2000). Vegetation at glaciers fronts is commonly affected by glacial fluctuations (Coe, 1967; Spence, 1989; Mizumo, 1998). Coe (1967) described vegetation zonation, plant colonization and the distribution of individual plant species on the slopes below the Tyndall and Lewis glaciers. Spence (1989) analyzed the advance of plant communities in response to the re treat of the Tyndall and Lewis glaciers for the period 1958- 1984. Mizumo (1998) addressed plant communities in response to more recent glacial retreat by conducting field research in 1992, 1994, 1996 and 1997. The studies illustrated the link between ice retreat and colonization near the Tyndall and Lewis glaciers. The concern about the future global climate warming and its geoecological consequences strongly urges development and analysis of climate sensitive biomonitoring systems. The natural elevational tree limit is often assumed to represent an ideal early warming line predicted to respond positionally, structurally and compositionally even to quite modest climate fluctuations. Several field studies in different parts of the world present that climate warming earlier in the 20th century (up to the 1950s 1960s) has caused tree limit advances (Kullman, 1998). Purohit (1991) also reported upward shifting of species in Garhwal Himalaya. The Himalayan mountain system is a conspicuous landmass characterised by its unique crescent shape, high orography, varied lithology and complex structure. The mountain system is rather of young geological age through the rock material it contains has a long history of sedimentation, metamorphism and magmatism from Proterozoic to Quaternary in age. Geologically, it occupies a vast terrain covering the northern boundary of India, entire Nepal, Bhutan and parts of China and Pakistan stretching from almost 720 E to 960 E meridians for about 2500 km in length. In terms of orography, the geographers have conceived four zones in the Himalaya across its long axis. From south to north, these are (i) the sub-Himalaya, comprising low hill ranges of Siwalik, not rising above 1,000 m in altitude; (ii) the Lesser Himalaya, comprising a series of mountain ranges not rising above 4000 m in altitude; (iii) the Great Himalaya, comprising very high mountain ranges with glaciers, rising above 6,000 m i n altitude and (iv) the Trans-Himalaya, Comprising very high mountain ranges with glaciers. The four orographic zones of the Himalaya are not strictly broad morpho-tectonic units though tectonism must have played a key role in varied orographic attainments of different zones. Their conceived boundaries do not also coincide with those of litho-stratigraphic or tectono-stratigraphic units. Because of the involvement of a large number of parameters of variable nature, the geomorphic units are expected to be diverse but cause specific, having close links with mechanism and crustal movements (Ghosh, et al., 1989). Soil is essential for the continued existence of life on the planet. Soil takes thousands of years to form and only few years to destroy their productivity as a result of erosion and other types of improper management. It is a three dimensional body consisting of solid, liquid and gaseous phase. It includes any part of earths crust, which through the process of weathering and incorporation of organic matter has become capable in securing and supporting plants. Living organisms and the transformation they perform have a profound effect on the ability of soils to provide food and fiber for expanding world population. Soils are used to produce crops, range and timber. Soil is basic to our survival and it is natures waste disposal medium and it serves as habitats for varied kinds of plants, birds, animals, and microorganisms. As a source of stores and transformers of plant nutrients, soil has a major influence on terrestrial ecosystems. Soil continuously recycles plant and animal remains , and they are major support systems for human life, determining the agricultural production capacity of the land (Anthwal, 2004). Soil is a natural product of the environment. Native soil forms from the parent material by action of climate (temperature, wind, and water), native vegetation and microbes. The shape of the land surface affects soil formation. It is also affected by the time it took for climate, vegetation, and microbes to create the soil. Soil varies greatly in time and space. Over time-scales relevant to geo-indicators, they have both stable characteristics (e.g. mineralogical composition and relative proportions of sand, silt and clay) and those that respond rapidly to changing environmental conditions (e.g. ground freezing). The latter characteristics include soil moisture and soil microbiota (e.g. nematodes, microbes), which are essential to fluxes of plant nutrients and greenhouse gases (Peirce, and Larson, 1996.). Most soils resist short-term climate change, but some may undergo irreversible change such as lateritic hardening and densification, podsolization, or large-scale erosion. Chemical degradation takes place because of depletion of soluble elements through rainwater leaching, over cropping and over grazing, or because of the accumulation of salts precipitated from rising ground water or irrigation schemes. It may also be caused by sewage containing toxic metals, precipitation of acidic and other airborne contaminants, as well as by persistent use of fertilizers and pesticides (Page et al., 1986). Physical degradation results from land clearing, erosion and compaction by machinery (Klute, 1986). The key soil indicators are texture (especially clay content), bulk density, aggregate stability and size distribution, and water-holding capacity (Anthwal, 2004). Soil consists of 45% mineral, 25% water, 25% air and 5% organic matter (both living and dead organisms). There are thousands of different soils throughout the world. Soil are classified on the basis of their parent material, texture, structure, and profile There are five key factors in soil formation: i) type of parent material; ii) climate; iii) overlying vegetation; iv) topography or slope; and v) time. Climate controls the distribution of vegetation or soil organisms. Together climate and vegetation/soil organisms often are called the active factors of soil formation (genesis). This is because, on gently undulating topography within a certain climatic and vegetative zone a characteristic or typical soil will develop unless parent material differences are very great (Anthwal, 2004). Thus, the tall and mid-grass prairie soils have developed across a variety of parent materials. Soil structure comprises the physical constitution of soil material as expressed by size, shape, and arrangement of solid particles and voids (Jongmans et al., 2001). Soil structure is an important soil property in many clayey, agricultural soils. Physical and chemical properties and also the nutrient status of the soil vary spatially due to the changing nature of the climate, parent material, physiographic position and vegetation (Behari et al., 2004). Soil brings together many ecosystem processes, integrating mineral and organic processes; and biological, physical and chemical processes (Arnold et al., 1990, Yaalon 1990). Soil may respond slowly to environmental changes than other elements of the ecosystem such as, the plants and animal do. Changes in soil organic matter can also indicate vegetation change, which can occur quickly because of climatic change (Almendinger, 1990). In high altitudes, soils are formed by the process of solifluction. Soils on the slopes above 300 are generally shallow due to erosion and mass wasting processes and usually have very thin surface horizons. Such skeletal soils have median to coarse texture depending on the type of material from which they have been derived. Glacial plants require water, mineral resources and support from substrate, which differ from alpine and lower altitude in many aspects. The plant life gets support by deeply weathered profile in moraine soils, which develops thin and mosaic type of vegetation. Most of the parent material is derived by mechanical weathering and the soils are rather coarse textured and stony. Permafrost occurs in many of the high mountains and the soils are typically cold and wet. The soils of the moraine region remain moist during the summer because drainage is impeded by permafrost (Gaur, 2002). In general, the north facing slopes support deep, moist and fertile soils. The south facing slopes, on the other hand, are precipitous and well exposed to denudation. These soils are shallow, dry and poor and are often devoid of any kind of regolith (Pandey, 1997). Based on various samples, Nand et al., (1989) finds negative correlation between soil pH and altitude and argues that decrease in pH with the increase in elevation is possibly accounted by high rainfall which facilitated leaching out of Calcium and Magnesium from surface soils. The soils are invariably rich in Potash, medium in Phosphorus and poor in Nitrogen contents. However, information on geo-morphological aspects, soil composition and mineral contents of alpine and moraine in Garhwal Himalaya are still lacking. Present investigation was aimed to carry out detail observations on soil composition of the alpine and moraine region of Garhwal Himalaya. 4.1. OBSERVATIONS As far as the recordings of abiotic environmental variables of morainic and alpine ecosystems of Dokriani Bamak are concerned, the atmospheric carbon dioxide and the physical and chemical characteristics of the soil were recorded under the present study. As these are important for the present study. 4.1.1. Atmospheric Carbon Dioxide Diurnal variations in the atmospheric CO2 were recorded at Dokriani Bamak from May 2005- October 2005. Generally the concentration of CO2 was higher during night and early morning hours (0600-0800) and lower during daytime. However, there were fluctuations in the patterns of diurnal changes in CO2 concentration on daily basis. In the month of May 2005, carbon dioxide concentration ranged from a minimum of 375Â µmol mol-1 to a maximum of 395Â µmol mol-1. When the values were averaged for the measurement days the maximum and minimum values ranged from 378Â µmol mol-1 to 388Â µmol mol-1. A difference of 20Â µmol mol-1 was found between the maximum and minimum values recorded for the measurement days. When the values were averaged, a difference of 10Â µmol mol-1 was observed between maximum and minimum values. During the measurement period, CO2 concentrations varied from a minimum of 377ÃŽ ¼mol mol-1 at 12 noon to a maximum of 400ÃŽ ¼mol mol-1 at 0800 hrs in the month of June, 2005. When the CO2 values were averaged for 6 days, the difference between the minimum and maximum values was about 23ÃŽ ¼mol mol-1. In the month of July, levels of carbon dioxide concentrations ranged from a minimum of 369ÃŽ ¼mol mol-1 to a maximum of 390ÃŽ ¼mol mol-1. When the values of the carbon dioxide concentrations for the measuring period were averaged, the difference between the minimum and maximum values was about 21ÃŽ ¼mol mol-1. Carbon dioxide concentration ranged from a minimum of 367ÃŽ ¼mol mol-1 to a maximum of 409ÃŽ ¼mol mol-1 during the month of August. When the values of carbon dioxide were averaged for the measurement days, the difference in the minimum and maximum values was about 42ÃŽ ¼mol mol-1. During the measurement period (September), CO2 concentrations varied from a minimum of 371ÃŽ ¼mol mol-1 at 12 noon to a maximum of 389ÃŽ ¼mol mol-1 at 0600 hrs indicating a difference of 18ÃŽ ¼mol mol-1 between the maximum and minimum values. When the values of the measurement days were averaged the minimum and maximum values ranged from 375ÃŽ ¼mol mol-1 to 387ÃŽ ¼mol mol-1 and a difference of 12ÃŽ ¼mol mol-1 was recorded. During the month of October, carbon dioxide levels ranged from a minimum of 372ÃŽ ¼mol mol-1 at 1400 hrs to a maximum of 403ÃŽ ¼mol mol-1 at 2000 hrs indicating a difference of 31ÃŽ ¼mol mol-1. When the values were averaged, the carbon dioxide levels ranged from a minimum of 376ÃŽ ¼mol mol-1 to a maximum of 415ÃŽ ¼mol mol-1.A difference in the minimum and maximum values was found to be 39Â µmol mol-1 when the values were averaged for the measurements days. In the growing season (May-October) overall carbon dioxide concentration was recorded to be highest in the month of June and seasonally it was recorded highest during the month of October 4.1.2. A. Soil Physical Characteristics of Soil Soil Colour and Texture Soils of the study area tend to have distinct variations in colour both horizontally and vertically (Table 4.1). The colour of the soil varied with soil depth. It was dark yellowish brown at the depth of 10-20cm, 30-40cm of AS1 and AS2, brown at the depth of 0-10cm of AS1 and AS2 and yellowish brown at the depths of 20-30cm, 40-50cm, 50-60cm of AS1 and AS2). Whereas the soil colour was grayish brown at the depths of 0-10cm, 30-40cm, 50-60cm of MS1 and MS2, dark grayish brown at the depths of 10-20cm, 20-30cm of MS1 and MS2 and brown at the depth of 40-50cm of both the moraine sites (MS1 and MS2). Soil texture is the relative volume of sand, silt and clay particles in a soil. Soils of the study area had high proportion of silt followed by sand and clay (Table 4.2). Soil of the alpine sites was identified as silty loam category, whereas, the soil of the moraine was of silty clayey loam category. Soil Temperature The soil temperature depends on the amount of heat reaching the soil surface and dissipation of heat in soil. Figure 4.2 depicts soil temperature at all the sites in the active growth period. A maximum (13.440C) soil temperature was recorded during the month of July and minimum (4.770C) during the month of October at AS1. The soil temperature varied between 5.10C being the lowest during the month of October to 12.710C as maximum during the month of August at AS2. Soil temperature ranged from 3.240C (October) to 11.210C (July) at MS1. However, the soil temperature ranged from 3.40C (October) to 12.330C (July) at MS2. Soil Moisture (%) Moisture has a big influence on soils ability to compact. Some soils wont compact well until moisture is 7-8%. Â  Likewise, wet soil also doesnt compact well. The mean soil water percentage (Fig. 4.3) in study area fluctuated between a maximum of 83% (AS1) to a minimum of 15% (AS2). The values of soil water percentage ranged from a minimum of 8% (MS2) to a maximum of 80% (MS1). Soil water percentage was higher in the month of July at AS1 and during August at MS1 (. During the month of June, soil water percentage was recorded minimum in the lower depth (50-60cm) at both the sites. Water Holding Capacity (WHC) The mean water holding capacity of the soil varied from alpine sites to moraine sites (Table 4.4). It ranged from a maximum of 89.66% (August) to a minimum of 79.15% (May) at AS1. The minimum and maximum values at AS2 were 78.88% (May) to 89.66% (August), respectively. The maximum WHC was recorded to be 84.61 % during the month of September on upper layer (0-10 cm) at MS1 and minimum 60.36% during the month of May in the lower layer (50-60cm) at MS1. At MS2, WHC ranged from 60.66% (May) to 84.61% (September). However, maximum WHC was recorded in upper layers at both the sites of alpine and moraine. Soil pH The soil pH varied from site to site during the course of the present study (Table 4.5). Mean pH values of all the sites are presented in Figure 4.4 The soil of the study area was acidic. Soil of the moraine sites was more acidic than that of the alpine sites. Soil pH ranged from 4.4 to 5.3 (AS1), 4.5 to 5.2 (AS2), 4.9 to 6.1 (MS1) and 4.8 to 5.7 (MS2). 4.1.2 B. Chemical Characteristics of Soil Organic Carbon (%): Soil organic carbon (SOC) varied with depths and months at both the alpine and moraine sites (Table 4.6). High percentage of organic carbon was observed in the upper layer of all sites during the entire period of study. Soil organic C decreased with depth and it was lowest in lower layers at all the sites. Soil organic carbon was maximum (5.1%) during July at AS1 because of high decomposition of litter, while it was minimum (4.2%) during October due to high uptake by plants in the uppermost layer (0-10 cm). A maximum (5.0%) SOC was found during the month of July and minimum (4.1%) during October at AS2. At the moraine sites, maximum (3.58%, 3.73%) SOC was found during June and minimum (1.5% and 1.9%) during August at MS1 and MS2 respectively. Phosphorus (%): A low amount of phosphorus was observed from May to August which increased during September and October. The mean phosphorus percentage ranged from 0.02 Â ± 0.01 to 0.07 Â ± 0.03 at AS1 and AS2. It was 0.03Â ±0.01 to 0.03Â ±0.02 at MS1 and MS2. Maximum percentage of phosphorus was estimated to be 0.09 in the uppermost layer (0-10 cm) during October at AS1. The lower layer (40-50 cm) of soil horizon contained a minimum of 0.01% phosphorus during September at AS1 and AS2. In the moraine sites (MS1 and MS2), maximum phosphorus percentage of 0.03 Â ±0.01 was estimated in the upper layers (0-10, 10-20, 20-30 cm) while it was found to be minimum (0.02Â ±0.01) in the lower layers (30-40 cm). Overall, a decreasing trend in amount of phosphorus was found with depth in alpine as well as moraine sites Potassium (%): A decline in potassium contents was also observed with declining depth during the active growing season. Maximum value of potassium was found in the uppermost layer (0-10 cm) at all the sites. The mean values ranged from 0.71Â ±0.02 to 46Â ±0.06 at AS1 while it was 0.71Â ±0.02 to 0.47Â ±0.05 at AS2. In the moraine sites the values ranged from a minimum of 0.33 Â ±0.06 to a maximum of 0.59Â ±0.05 in the MS1 and from 0.59Â ±0.05 to 0.32Â ±0.06 at MS2. In the upper layer of soil horizon (0-10 cm), maximum value of 0.74 %, 0.75% of potassium was observed during the month of July at AS1 and AS2. While the values were maximum in the month of October at moraine sites MS1 and MS2 having 0.66% and 0.65% respectively Nitrogen (%): Highest percentage of nitrogen was found in the upper layers at all the sites. Maximum percentage of nitrogen were found during the month of July-August (0.25%, 0.25 and 0.26%, 0.25%) at AS1 and AS2, respectively. Maximum values of 0.18% and 0.15% respectively were found during the month of June at the moraine sites MS1 and MS2. The nitrogen percentage ranged from 0.23Â ±0.02 to 0.04Â ±0.01% at AS1. However, it ranged from a minimum of 0.05Â ±0.01 to 0.24Â ±0.02% at AS2. The nitrogen percentage ranged from a minimum of 0.03Â ±0.01, 0.02Â ±0.04% to a maximum of 12Â ±0.03, 13Â ±0.01%, respectively at MS1 and MS2 Overall, a decreasing trend was noticed in the nitrogen percentage with depth at both the alpine and moraine sites. 4.2. DISCUSSION Soil has a close relationship with geomorphology and vegetation type of the area (Gaur, 2002). Any change in the geomorphological process and vegetational pattern influences the pedogenic processes. However, variability in soil is a characteristic even within same geomorphic position (Gaur, 2002). Jenney (1941) in his discussion on organisms as a soil forming factors treated vegetation both as an independent and as dependent variable. In order to examine the role of vegetation as an independent variable, it would be possible to study the properties of soil as influenced by vegetation while all other soil forming factors such as climate, parent material, topography and time are maintaining at a particular constellation. Many soil properties may be related to a climatic situation revealing thousand years ago (e.g. humid period during late glacial or the Holocene in the Alps and Andes (Korner, 1999). The soil forming processes are reflected in the colour of the surface soil (Pandey, 1997). The combination of iron oxides and organic content gives many soil types a brown colour (Anthwal, 2004). Many darker soils are not warmer than adjacent lighter coloured soils because of the temperature modifying effect of the moisture, in fact they may be cooler (Pandey, 1997). The alpine sites of the resent study has soil colour varying from dark yellowish brown/yellowish brown to brown at different depths. Likewise, at the moraine sites, the soil colour was dark grayish brown/grayish brown to brown. The dark coloured soils of the moraine and alpine sites having high humus contents absorb more heat than light coloured soils. Therefore, the dark soils hold more water. Water requires relatively large amount of heat than the soil minerals to raise its temperature and it also absorbs considerable heat for evaporation. At all sites, dark colour of soil was found due to high organic contents by the addition of litter. Soil texture is an important modifying factor in relation to the proportion of precipitation that enters the soil and is available to plants (Pandey, 1997). Texture refers to the proportion of sand, silt, and clay in the soil. Sandy soil is light or coarse-textured, whereas, the clay soils are heavy or fine-textured. Sand holds less moisture per unit volume, but permits more rapid percolation of precipitated water than silt and clay. Clay tends to increase the water-holding capacity of the soil. Loamy soils have a balanced sand, silt, and clay composition and are thus superior for plant growth (Pidwirny, 2004). Soil of the alpine zone of Dokriani Bamak was silty predominated by clay and loam, whereas the soil of moraine zone was silty predominated by sand and clay. There is a close relationship between atmospheric temperature and soil temperature. The high organic matter (humus) help in retaining more soil water. During summers, high radiations with greater insulation period enhance the atmospheric temperature resulted in the greater evaporation of soil water. In the monsoon months (July-August) the high rainfall increased soil moisture under relative atmospheric and soil temperature due to cloud-filter radiations (Pandey, 1997). Owing to September rainfall, atmospheric and soil temperatures decreased. The soil moisture is controlled by atmospheric temperature coupled with absorption of water by plants. During October, occasional rainfall and strong cold winds lower down the atmospheric temperature further. The soil temperature remains more or less intact from the outer influence due to a slight frost layer as well as vegetation cover. Soil temperature was recorded low at the moraine sites than the alpine sites. During May, insulation period in creases with increase in the atmospheric and soil temperature and it decreases during rainfall. The increasing temperature influences soil moisture adversely and an equilibrium is attained only after the first monsoon showers in the month of June which continued till August. Donahue et al. (1987) stated that no levelled land with a slope at right angle to the Sun would receive more heat per soil area and will warm faster than the flat surface. The soil layer impermeable to moisture have been cited as the reason for treelessness in part of the tropics, wherein its absence savanna develops (Beard, 1953). The resulting water logging of soil during the rainy season creates conditions not suitable for the growth of trees capable of surviving the dry season. The water holding capacity of the soil is determined by several factors. Most important among these are soil texture or size of particles, porosity and the amount of expansible organic matter and colloidal clay (Pandey, 1997). Water is held as thin film upon the surface of the particles and runs together forming drops in saturated soils, the amount necessarily increases with an increase in the water holding surface. Organic matter affects water contents directly by retaining water in large amount on the extensive surfaces of its colloidal constituents and also by holding it like a sponge in its less decayed portion. It also had an indirect effect through soil structure. Sand particles loosely cemented together by it, hence, percolation is decreased and water-holding capacity increased. Although fine textured soil can hold more water and thus more total water holding capacity but maximum available water is held in moderate textured soil. Porosity in soil consists of that portion of the soil volume not occupied by solids, either mineral or organic material. Under natural conditions, the pore spaces are occupied at all times by air and water. Pore spaces are irregular in shape in sand than the clay. The most rapid water and air movement is observed in sands than strongly aggregated soils. The pH of alpine sites ranged from 4.4 to 5.3 and it ranged from 4.8 to 6.1 in moraine sites of Dokriani Bamak. It indicated the acidic nature of the soil. The moraine sites were more acidic than the alpine sites. Acidity of soil is exhibited due to the presence of different acids. The organic matter and nitrogen contents inhibit the acidity of soil. The present observations pertaining to the soil pH (4.4 to 5.3 and 4.8 to 6.1) were more or less in the same range as reported for other meadows and moraine zones. Ram (1988) reported pH from 4.0-6.0 in Rudranath and Gaur (2002) on Chorabari. These pH ranges are lower than the oak and pine forests of lower altitudes of Himalayan region as observed by Singh and Singh, 1987 (pH:6.0-6.3). Furthermore, pH increased with depth. Bliss (1963) analyzed that in all types of soil, pH was low in upper layers (4.0-4.30) and it increased (4.6-4.9) in lower layer at New Hampshire due to reduction in organic matter. Das et al. (1988) reported the simil ar results in the sub alpine areas of Eastern Himalayas. All these reports support the present findings on Dokriani Bamak strongly. A potent acidic soil is intensively eroded and it has lower exchangeable cation, and possesses least microbial activity (Donahue et al., 1987). Misra et al., 1970 also observed higher acidity in the soil in the region where high precipitation results leaching. Koslowska (1934) demonstrated that when plants were grown under conditions of known pH, they make the culture medium either more acidic or alkaline and that this property differed according to the species. Soil properties may ch